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ratigraphic Lexicon of S and recommendations for nomencla

Upper Palaeozoic to Quaternary Bedrock

Stratigrafisk Komitk for Svalbard (SKS) Committee on the Stratigraphy of Svalbard

Edited by W. K. Dallmann (Norwegian Polar Institute, Polar Environmental Centre,

9296 Tromsra, Norway)

valbard .ture use

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Editorial committee: Knysztof Birkenmajer (Polish Academy of Sciences, Krakbw, Poland) Henning Dypvik (University of Oslo, Norway) John G. Gjelberg (Norsk Hydro ASA, Bergen, Norway) W. Brian Harland (University of Cambridge, United Kingdom) Hilde B. Keilen (Saga Petroleum ASA, Sandvika, Norviray) Atle W k (MU Petroleum Research, Trondheirn, Norway) Jew Nagy (University of Oslo, Norway) Arvid NBttvedt (Norsk Hydro ASA, Bergen, Norway) Tatjana M. PEelina (VNIIOkeangeologija, St. Petersburg, Russia) Ron J. Steel (University of Bergen, Norway; presently: University of Wyoming, USA) David Worsley (Saga Petroleum ASA, Sandvika, Norway)

List of authors:

Winfried K. Dallmann (Norwegian Polar Institute, Tromss, Norway) Henning Dypvik (University of Oslo, Norway) John G. Gjelberg (Norsk Hydro as, Bergen, Norway) W. Brian Harland (University of Cambridge, United Kingdom) Erik P. Johannessen (Statoil, Stavanger, Norway) Hilde B. Keilen (Saga Petroleum ASA, Sandvika, Norway) Geir Birger Larssen (Norwegian Petroleum Directorate 1 Saga Petroleum ASA, Harstad, Norway) Arve LDWY (Norsk Hydro as, Bergen, Norway) Peter S. Midbse (Norsk Hydro as, Oslo, Norway) Atle Mmk (IKU Petroleum Research, Trondheirn, Norway) Jew Nagy (University of Oslo, Norway) Inger Nilsson (Saga Petroleum ASA, Harstad, Norway) Arvid NBttvedt (Norsk Hydro as, Bergen, Norway) Snorre Olaussen (Saga Petroleum ASA, Sandvika, Norway) Tatjana M. PEelina (VNIIOkeangeologija, St. Petersburg, Russia) Ron J. Steel (University of Bergen, Norway; presently: University of Wyoming, USA) David Worsley (Saga Petroleum ASA, Sandvika, Norway)

This publicatin is sponsered by:

Amerada Hess Norge AS Conoco Norway Inc. Elf Petroleum Norge AS Mobil Exploration Norway Inc. Norske Shell A/S Norsk Hydro ASA Saga Petroleum ASA Statoil Total Norge A.S.

8 Norsk Polarinstitutt Technical Editor: Annemor Brekke Design and production: Grimshei -ske, Lmenskog Printed December 1999 by Gjsvik Trykkeri As ISBN 82-7666-166-1

Cwer photo: WK. Dallmann: The mountain Pyramiden, Central Spitsbegen,

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1. INTRODU~ON

1.1 About this book 1.2 Committee on the Stratigraphy of Svalbard: Organisation and purpose 1.3 How to use this book - important user information

1.3.1 Main objectives of this book 1.3.2 Organisation of the book 1.3.3 Use of ID numbers and quotation marks 1.3.4 Stratigraphic tables and applied ages 1.3.5 Type localities and type sections 1.3.6 Maps 1.3.7 Correlations with the geology of the Barents Sea Shelf 1.3.8 Change of place-name segments 1.3.9 Lower boundary definitions and descriptions of geological units 1.3.10 Notes on references 1.3.1 1 Explanations of place names 1.3.12 Transliteration of Russian names and references

1.4 Outline of the geological history of Svalbard 1.4.1 Tectonic setting 1.4.2 Pre-Old Red 1.4.3 Old Red (Devonian) 1.4.4 Late Palaeozoic 1.4.5 Mesozoic 1.4.6 Tertiary 1.4.7 Tertiary and Quaternary volcanic activity

2. UPPER PALAEOZOIC LITHOSTRATIGRAPHY

2.1 General subdivision 2.2 Previous stratigraphic schemes 2.3 Major revisions

2.3.1 Revised nomenclature for the Lower Carboniferous of the Billefjorden Trough 2.3.2 Revised nomenclature of the Nordenskioldbreen Formation

2.4 Correlation with the Barents Sea Shelf 2.5 Regional description

2.5.1 Lowerlmiddle Carboniferous of Bj~rwya 2.5.2 Lowerlmiddle Carboniferous of the Smkapp-Homsund High 2.5.3 Lowerlmiddle Carboniferous of the Inner Homund Trough and adjacent areas 2.5.4 Lowerlmiddle Carboniferous of the St. Jonsfjorden Trough and adjacent areas 2.5.5 Lowerlmiddle Carboniferous of the Billefjorden Trough and Nordfjorden High 2.5.6 Lowerlmiddle Carboniferous of northeastern Svalbard 2.5.7 Upper Carboniferous and Permian platform of Svalbard

2.6 Lexicon of lithostratigraphic units 2.6.1 Billefjorden Group 2.6.2 Gipsdalen Group 2.6.3 Bjanneland Group 2.6.4 Tempelfjorden Group

2.7 Abandoned lithostratigraphic unit names 2.7.1 Names with a place name segment 2.7.2 Names without a place name segment

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CONTENTS

MESOZOIC LITHOSTRATIGRAPHY

3. l Stratigraphic development of Svalbard and the Barents Sea Shelf 3.2 General subdivision 3.3 Previous stratigraphic schemes 3.4 Regional descriptions and major revisions

3.4.1 Sassendalen Group 3.4.2 Kapp Toscana Group 3.4.3 Adventdalen Group 3.4.4 Nygrunnen Group 3.4.5 Intrusive rocks

3.5 Lexicon of lithostratigraphic units 3.5.1 Sassendalen Group 3.5.2 Kapp Toscana Group 3.5.3 Adventdalen Group 3.5.4 Nygrunnen Group 3.5.5 Intrusive rocks


4. T E R ~ LITHOSTRA~GRAPHY

4.1 General subdivision 4.2 Previous stratigraphic schemes 4.3 Regional descriptions and major revisions

4.3.1 Central Tertiary Basin 4.3.2 Kongsfjorden area 4.3.3 Forlandsundet Graben 4.3.4 Renardodden area 4.3.5 Plateau basalts

4.4 Lexicon of lithostratigraphic units 4.4.1 Van Mijenfjorden Group 4.4.2 Buchananisen Group 4.4.3 Calypsostranda Group 4.4.4 Other units


5. QUATERNARY VOLCANIC AND SUBVOLCANIC ROCKS

5.1 General remarks 5.2 Lexicon of lithostratigraphic units

6. TABLES 6.1 Recommended stratigraphic unit names 6.2 Type sections and type localities

7. BIBLIOGRAPHY (complete, as far as possible, grouped according to topic, with published articles, theses, reports and maps listed separately)

INDEX LIST (all stratigraphic names listed alphabetically with page references)

APPENDIX 1: Biostratigraphic tables APPENDIX 2: Extract from 'Rules and recommendations for naming geological units in Norway'

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STRATIGRAPHIC OVERVIEW SCHEMES: Fig. 2-01: Group and subgroup subdivision of Upper Palaeozoic

rocks Fig. 2-04: Proposed lithostratigraphic scheme for the Upper

Palaeozoic Fig. 3-01: Group and subgroup subdivision of Mesozoic rocks Fig. 3-05: Proposed lithostratigraphic scheme for the Mesozoic Fig. 4-01: Group and subgroup subdivision of the Tertiary rocks Fig. 4-03: Proposed lithostratigraphic scheme for the Tertiary

MAPS: Fig. 1-02: Svalbard in relation to major tectonic units Fig. 1-04: Geological overview map of Svalbard Fig. 1-05: Structural overview map of Svalbard Fig. 1-06: Names of major geographical features, index of detailed

maps Fig. 2-02: Sketch and map of Middle Carboniferous troughs and

highs Fig. 2-05: Distribution map CP-I: Upper Palaeozoic of Bjmmya

(incl. Triassic) Fig. 2-06: Distribution map CP-11: Upper Palaeozoic of the Ssrkapp-

Hornsund area (S Spitsbergen) Fig. 2-07: Distribution map CP-111: Upper Palaeozoic of the Torell

Land and Bellsund-Isfjorden areas (SW Spitsbergen) Fig. 2-08: Distribution map CP-IV Upper Palaeozoic of Oscar I1

Land (Central W Spitsbergen) Fig. 2-09: Distribution map CP-V: Upper Palaeozoic of Dickson Land

and Biinsow Land (Central Spitsbergen) Fig. 2-10: Distribution map CP-VI: Upper Palaeozoic of northeastern

Svalbard Fig. 3-06: Distribution map M-I: Mesozoic of the Smkapp-Hornsund

area (S Spitsbergen) Fig. 3-07: Distribution map M-11: Mesozoic of Torell Land and

Bellsund-Isfjorden (SW Spitsbergen) Fig. 3-08: Distribution map M-III: Mesozoic of Storfjorden S (SE

Spitsbergen) Fig. 3-09: Distribution map M-TV: Mesozoic of Oscar I1 Land and

Dickson Land (Central W Spitsbergen) Fig. 3-10: Distribution map M-V: Mesozoic of Nordenskiold Land

NE and Sabine Land (Central E Spitsbergen) Fig. 3-11: Distribution map M-VI: Mesozoic of Kong Karls Land Fig. 3-12: Distribution map M-VII: Mesozoic of Barentseya,

Edgesya, Hopen and Olav V Land (E Svalbard) Fig. 4-04: Distribution map T-I: Tertiary of the Central Tertiary Basin,

southern part, and the Renardodden area Fig. 4-05: Distribution map T-11: Tertiary of the Central Tertiary

Basin, northern part Fig. 4-06: Dismbution map T-III: Tertiary of the Forlandsundet and

Kongsfjorden areas Fig. 4-07: Dismbution map T-TV: Tertiary and Quaternary volcanic

rocks

PREVIOUS STRATIGRAPHIC SCHEMES: Fi. 2-03: F'revious and proposed stratigraphic schemes for the Late

Palaeozoic

Fig. 3-02: Revision of Mesozoic group/subgroup subdivision of the Barents Sea Shelf

Fig. 3-03: Previous and proposed stratigraphic schemes for the Triassic

Fig. 3-04: Previous and proposed stratigraphic schemes for the Jurassic-Cretaceous

Fig. 4-02: Previous and proposed stratigraphic schemes for the Tertiary

BIOSTRATIGRAPHIC TABLES: Appendix Fig. A-l: Biostratigraphic correlation scheme of the late

Palaeowic of Svalbard. Appendix Fig.A-2: Biozones of the Mesozoic of Svalbard;

Sassendalen Group. Appendii Fig. A-3: Biozones of the Mesozoic of Svalbard; Kapp

Toscana Group. Appendix Fig.A-4: Biozones of the Mesozoic of Svalbard;

Adventdalen Group.

TYPE SECTIONS: Fig. 2-15: Stratigraphic section CP-02/04 - Hmbyebreen Fm. Fig. 2-18: Stratigraphic section CP-03 - Hrarbyebreen Fm. Fig. 2-19: Stratigraphic section CP-05/06/07 - Mumien Fm. Fig. 2-21: Stratigraphic section CP-08/09 - Orusfdalen Fm.,

Vegardflella Fm. Fig. 2-22: Stratigraphic section CP-10/13 - Adriabukta Fm. Fi. 2-25: Stratigraphic section CP-14 - Hornsundneset Fm. Fig. 2-26: Stratigraphic section CP-15 - Sergeijeflellet Fm. Fig. 2-28: Stratigraphic section CP-16 - Rsedvika Fm. Fig. 2-29: Stratigraphic section CP-17 - Rsedvika Fm. Fi. 2-30: Stratigraphic section CP-18 - Rsedvika Fm. Fig. 2-31: Stratigraphic section CP-19 - Rsedvika Fm. Fig. 2-32: Stratigraphic section CP-20a/21/22a - Nordkapp Fm. Fig. 2-33: Stratigraphic section CP-20b/22b - Nordkapp Fm. Fig. 2-38: Stratigraphic section CP-25a - Hultberget Fm. Fig. 2-39: Stratigraphic section CP-25b - Hultberget Fm. Fig. 2-41: Stratigraphic section CP-26a129 - Ebbadalen Fm. Fig. 242: Stratigraphic section CP-26b/28a - Ebbadalen Fm. Fig. 2-44: Stratigraphic section CP-27 - Ebbadalen Fm. Fig. 2-46: Stratigraphic section CP-28b - Ebbadalen Fm. Fig. 2-49: Stratigraphic section CP-30131a - Minkinfjellet Fm. Fig. 2-50: Stratigraphic section CP-3 lb - Minkinfjellet Fm. Fig. 2-54. Stratigraphic section CP-35 - Brraggertinden Fm. Fig. 2-56: Stratigraphic section CP-36 - Scheteligfjellet Fm. Fig. 2-57: Stratigraphic section CP-37 - Petrellskaret Fm. Fig. 2-58: Stratigraphic section CP-38 - Thkanten Fm. Fig. 2-60: ~ t r a t i ~ r a ~ ~ s e c t i o n CP-39 - Thkanten Fm. Fig. 2-63: Stratigraphic section CP-41143 - Hyrnefjellet Fm. Fig. 2-66: Stratigraphic section CP-44 - Hyrnefjellet Fm. Fig. 2-68: Stratigraphic section CP-45 - Treskelodden Fm. Fig. 2-70: Stratigraphic section CP-48158 - Wordiekammen Fm. Fig. 2-71: Stratigraphic section CP-49 - Wordiekammen Fm. Fig. 2-73: Stratigraphic section CP-5 1/52 - Wordiekammen Fm. Fig. 2-74: Stratigraphic section CP-55 - Wordiekammen Fm. Fig. 2-75: Stratigraphic section CP-56 - Wordiekammen Fm.

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ILLUSTRATIONS

Fig. 2-76: Stratigraphic section CP-57 - Wordiekammen Fm. Fig. 2-77: Stratigraphic section CP-59/68a - Wordiekammen

Fm./H&ardbreen Fm. Fig. 2-80: Stratigraphic section CP-60a - Gipshuken Fm. Fig. 2-81: Stratigraphic section CP-60b/64 - Gipshuken Fm. Fig. 2-83: Stratigraphic section CP-61- Gipshuken Fm. Fig. 2-84: Stratigraphic section CP-62 - Gipshuken Fm. Fig. 2-85: Stratigraphic section CP-65 - Gipshuken Fmr Fig. 2-86: Stratigraphic section CP-66 - Gipshuken F&' Fig. 2-88: Stratigraphic section CP-67 - Maite Brunfjellet Fm. Fig. 2-89: Stratigraphic section CP-68b - Hbbardbreen Fm. Fig. 2-91: Stratigraphic section CP-69a - Landnerdingsvika Fm. Fig. 2-92: Stratigraphic section CP-69b - Landnerdingsvika Fm. Fig. 2-94: Stratigraphic section CP-70171- Kapp Kilre Fm. Fig. 2-95: Stratigraphic section CP-72 - Kapp Kilre Fm. Fig. 2-96: Stratigraphic section CP-73 - Kapp Kilre Fm. Fig. 2-98: Stratigraphic section CP-74a - Kapp Hanna Fm. Fig. 2-99: Stratigraphic section CP-74b - Kapp Hanna Fm. Fig. 2-103: Stratigraphic section CP-75a - Kapp Dunk Fm. Fig. 2-104: Stratigraphic section CP-75b - Kapp Dun& Em. Fig. 2-105: Stratigraphic section CP-77a - Hambergfjellet Fm. Fig. 2-106: Stratigraphic section CP-7% - Hambergfjellet Fm. Fig. 2-110: Stratigraphic section CP-79180/81/82 -

Kapp Starostin Fm. Fig. 2-111: Stratigraphic section CP-83 - Kapp Starostin Fm. Fig. 2-112: Stratigraphic section CP-84 - Kapp Starostin Fm. Fig. 2-113: Stratigraphic section CP.85 - Kapp Starostin Fm. Fig. 2-114: Stratigraphic section CP-86a - Kapp Starostin Fm. Fig. 2-115: Stratigraphic section CP-86b - Kapp Starostin Fm. Fig. 2-116: Stratigraphic section CP-87 - Tokrosssya Fm. Fig. 2-117: Stratigraphc section CP-88 - Toluosssya Fm. Fig. 2-119: Stratigraphic section CP-89 - Miseryfjellet Fm. Fig. 3-18: Stratigraphic section M-02 -Vardebukta Fm. Fig. 3-21: Stratigraphic section M-09 - Tvillingodden Fm. Fig. 3-22: Stratigraphic section M-1011 1 -Tvillingodden Fm. Fig. 3-23: Stratigraphic section M-12 - Tvillingodden Fm. Fig. 3-25: Stratigraphic section M-13/14/15/16 -Vikinghogda Fm. Fig. 3-28: Stratigraphic section M-17/18/36 - Urd Fm./Skuld Fm. Fig. 3-31: Stratigraphic section M-19120bl22b - Bnwaisberget Fm. Fig. 3-32: Stratigraphic section M-20d22a - Bravaisberget Fm. Fig. 3-34: Stratigraphic section M-21 - Bravaisberget Fm. Fig. 3-35: Stratigraphic section M-23 - Bravaisberget Fm. Fig. 3-37: Stratigraphic section M-24 - Botueheia Fm. Fig. 3139: Stratigraphic section M-25 - Botneheia Fm. Fig. 3-42: Stratigraphic section M-33 - Tschennakfjellet Fm. Fig. 3-45: Stratigraphic section M-34d35 - Lk Geerdalen Fm. Fig. 3-46: Stratigraphic section M-Mb - Lk Geerdalen Fm. Fig. 3-47: Stratigraphic section M-38149bl53 - Wilhelnwya Subgp. Fig. 3-50: Stratigraphic section M-40 - Smalegga Fm. Fig. 3-53: Stratigraphic section M43 - Knomngfjellet Fm. Fig. 3-54: Stratigraphic section M-46a - Flatsalen Fm. Fig. 3-55: Stratigraphic section M-46b - Flatsalen Fm. Fig. 3-57: Stratigraphic section M47148150 - Svenskqa Fm. Fig. 3-61: Stratigraphic section M-51/52 - Kongsraya Fm. Fig. 3-63: Stratigraphic section M-54a - Brentskardhaugen Bed Fig. 3-64: Stratigraphic section M-54b - Brentskardhaugen Bed Fig. 3-66: Stratigraphic section M-55 - Marhegda Bed Fig. 3-70: Stratigraphic section M-65/66d76a - Agardhfjellet

Fm./Runkfjellet Fm. Fig. 3-71: Stratigraphic section M-66bl70172 - Agardhfjellet Fm.

Fig. 3-72: Stratigraphic section M-71 - Agardhfjellet Fm. Fig. 3-73: Stratigraphic section M-73 - AgardhSJellet Fm. Fig. 3-74: Stratigraphic section M-74/75 - Agardhfjellet Fm. Fig. 3-75: Stratigraphic section M-76bl77 - Rurikfjellet Fm. Fig. 3-78: Stratigraphic section M-79 - Rurikfjellet Fm. Fig. 3-82: Stratigraphic section M-89 - Helvetiafjellet Fm. Fig. 3-84: Stratigraphic section M-90 - Helvetiafjellet Fm. Fig. 3-87: Stratigraphic section M-91a - Helvetiafjellet Fm. Fig. 3-88: Stratigraphic section M-91b - Helvetiafjellet Fm. Fig. 3-89: Stratigraphic section M-91c - Helvetiafjellet Fm. Fig. 3-91: Stratigraphic section M-92 - Helvetiafjellet Fm. Fig. 3-93: Stratigraphic section M-93194195196 - Carolinefjellet Fm. Fig. 3-97: Stratigraphic section M-9%/98 - Caroliiefjellet Fm. Fig. 4-10: Stratigraphic section T-01 -Van Mijenfjorden Gp. Fig. 4-14: Stratigraphic section T-03a - Firkanten Fm. Fig. 4-15: Stratigraphic section T-03b - Firkanten Fm. Fig. 4-16: Stratigraphic section T-04 - Firkanten Fm.

'

Fig. 4-17: Stratigraphic section T-05 - Firkanten Fm. Fig. 4-19: Stratigraphic section T-06 - Firkanten Fm. Fig. 4-20: Stratigraphic section T-07 - Basilika Fm. Fig. 4-21: Stratigraphic section T-09/10b/11- Frysjaodden Fm. Fig. 4-22: Stratigraphic section T-lOdl3a - Frysjaodden

Fm./Hollendardalen Fm. Fig. 4-25: Stratigraphic section T-12 - Frysjaodden Fm. Fig. 4-26: Stratigraphic section T-13b - Hollendardalen Fm. Fig. 4-27: Stratigraphic section T-14 - Baqellet Fm. Fig. 4-29: Stratigraphic section T-15 -Aspelintoppen Fm. Fig. 4-32: Stratigraphic section T-18 - Kongsfjorden Fm. Fig. 4-34: Stratigraphic section T-19a - Kongsfjorden Fm. Fig. 4-35 : Stratigraphic section T-19b - Kongsfjorden Fm. Fig. 4-37: Stratigraphic section T-20 - Kongsfjorden Fm. Fig. 4-38: Stratigraphic section T-22 - Bwggerbreen Fm. Fig. 4-39: Stratiwphic section T-23 - Brsggerbreen Fm. Fig. 4-40: Stratigraphic section T-25 - Selvhgen Fm. Fig. 4-41: Stratigraphic section T-26 - Sesshegda Fm. Fig. 4-42: Stratigraphic section T-27 - Reinhardpynten Fm. Fig. 4-43: Stratigraphic section T-28 - Krokodillen Fm. Fig. 4-44: Stratigraphic section T-29 - Marchaislaguna Fm. Fig. 4 - 4 5 ~ Stratigraphic section T-30, T-30.1, T-30.2 -

Aberdeenflya Fm. Fig. 4-45b: Stratigraphic section T-30.3, T-30.4 - Aberdeenflya Fm. Fig. 4-45~: Stratigraphic section T-30.5 - Aberdeenflya Fm. Fig. 4-46: Stratigraphic section T-32 - Sarsbukta conglomerate Fig. 4-47: Stratigraphic section T-33 - Sarstangen conglomerate Fig. 4-49: Stratigraphic section T-34/35/36 - Skilvika

Fm./Renardodden Fm.

PHOTOGRAPHS: Fig. 2-11: Fault block with Devonian and Carboniferous strata on

Triungen (Dickson Land); Hmbyebreen, Mumien, Hultberget and Wordiekammen formations.

Fig. 2-12: Typical sediments of the Billefjorden Group at Billefjorden, representing delta plain and overbank deposits. Fig. 2-13: The Russian coal mining settlement Pyramiden with

transportation facilities to the mine in the mountain side. Fig. 2-14: Sigillaria stems, Billefjorden Group. Fig. 2-16: Gravelstones and crossbedded sandstones, Triungm h&mber

on Alen @ickson and). %' P

Fig. 2-17: Alluvial fan deposits with reworked, light sandstone,

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ILLUSTRATIONS

Triungen Member on Faraofjellet (Dickson Land). Fig. 2-20: Crossbedded, light grey sandstones with tidal bundles,

Orustdalen Formation at Bellsund. Fig. 2-23: Thick alluvial fan conglomerates of the Haitanna Member,

Haitanna (central Smkapp Land). Fig. 2-24: Sandstones of the Julhergda Member, Pinsetoppen

(northern Smkapp Land). Fig. 2-27: Fluvial channel in the lower part of the bedvika

Formation, kedvika ( B j q ) . Fig. 2-34: Carboniferous succession north of Ansewika

(Billefjorden); Hultberget, Wordiekammen, Gipshuken and Kapp Starostin formations.

Fig. 2-35: Terriexfjellet (northeastern Biinsow Land), showing Precambrian basement, Hultberget and Ebbadalen, Minkifjellet and Wordiekammen formations.

Fig. 2-36: Carnpbellryggen Subgroup of the Billefjorden Trough at Trikolorfjellet (western Dickson Land).

Fig. 2-37: Hultberget Formation and Ebbaelva Member at Odellfjellet (northwestern Dickson Land).

Fig. 2-40: Ebbadalen Formation at Wordiekammen, Ebbadalen (eastern Dickson Land).

Fig. 2-43: Ebbaelva Member at the northern slope of Odellfjellet (northwestern Dickson Land).

Fig. 2-45: Odellfjellet Member, Odellfjellet (northeastern Dickson Land).

Fig. 2-47: Trikoloxfjellet Member at Cadellfjellet (northern Bmow Land).

Fig. 2-48:, M i f j e l l e t Formation deformed into a major flexure at hehovden (eastern Dickson Land).

Fig. 2-51: Dolomite breccias of the Fortet member forming peculiar pinnacles and towers, Fortet (Billefjorden).

Fig. 2-52: Charlesbreen Subgroup of the St. Jonsfjorden Trough with Petrellskaret and Thkanten formations at Thkanten (St. Jonsfjorden).

Fig. 2-53: Fluvial conglomerate with inte~ening, crossbedded sandstones, Brnggertinden Formation, Braggerfjellet (Bmggerhalveya).

Fig. 2-55: Multithecopore limestone from the Scheteligtjellet Formation, Braggerhalveya.

Fig. 2-59: Jutulslottet Member at Jutulslottet (St. Jonsfjorden). Fig. 2-61: Hyrnefjellet at Hornsund, showing the folded Treskelen

Subgroup of the Inner Hornsund Trough. Fig. 2-62: Carboniferous succession at the mountain Hjelmen

(Sarkapp Land). Fig. 2-64: Hjelmen member on the mountain Hjelmen (Ssrkapp

Land). Fig. 2-65: Detail of the Brattberget member, Adriabukta (Hornsund). Fig. 2-67: Treskelodden Formation at Austjakultinden (Smkapp Land). Fig. 2-69: Cliff-forming shelf carbonates of the Wordiekammen

Formation at Langtma (Sabine Land). Fig. 2-72: Typical concretions of the Cadellfjellet Member (Malte

B e e l l e t , northern Sabine Land). Fig. 2-78: Gipshuken Formation (Templet and Skansdalen members)

at Sindballefjellet (Ternpelfjorden). Fig. 2-79: Carboniferous-Permian stratigraphy at Kolosseum

(Elananfjorden): Wordiekammen, Gipshuken and Kapp Starostin formations.

Fig. 2-82: Gypsum layers of the Vengeberget member at Palatidellet (James I Land).

Fig. 2-87: Upper parts of the Malte Brunfjellet Formation, Malte B d j e l l e t (northern Sabiie Land).

Fig. 2-90: Lanhdingsvika Formation (Bjerwya). Fig. 2-93: Bogevika Member, Kobbebukta (Bjernsya). Fig. 2-97: Kapp Hanna Formation, Kapp Hanna (Bjrmneya). Fig. 2-100: Kapp Dun& Formation with lenticular Palaeoaplysina

buildups, Kapp Dunk (Bjrmneya). Fig. 2-101: Vertically stacked Palaeoaplysina buildups at Amfiet

(Bjmeya) in the Kapp Dun& Formation. Fig. 2-102: Forereef facies in the Kapp Dun& Formation, Kapp

Dun& (Bjmwya). Fig. 2-107: Kapp Starostin Formation at Skansen (Billefjorden). Fig. 2-108: Kapp Starostin Formation at Skansbukta (Billefjorden). Fig. 2-109: Kapp Starostin Formation in western Nordenskiold Land

showing five depositional cycles. Fig. 2-118: Miseryfjellet on Bjnrmnrya, seen fmm the east (Rnedvlka,

Miseryfjellet, Urd and Skuld formations). Fig. 3-13: Sassendalen Group at Bravaisberget (Van Keulenfjorden),

typical development of the western areas. Fig. 3-14: Hyrnefjellet at Hornsund, showing the Sassendalen Group

as typical for the Hornsund area. Fig. 3-15: Sassendalen Group at Hagrinden (Barentseya), showing a

typical development of the eastern areas. Fig. 3-16: Sassendalen Group at Waveltoppen (Torell Land). Fig. 3-17: Myalina limestone in the Vardebukta Formation, Festningen

(outer Isfjorden). Fig. 3-19: Thin development of the Sassendalen Group on the

Serkapp-Homsund High at Kistefjellet. Fig. 3-20: Triassic unconformity with the conglomeratic

Brevassfjellet Bed above folded basement. Fig. 3-24: Sassendalen Group at Milne Edwardsfjellet (central

Spitsbergen). Fig. 3-26: The Permian-Triassic boundary in Lusitaniadalen. Fig. 3-27: The Triassic succession of B j m y a (Urd and Skuld

formations) overlying the Miseryfjellet Formation. Fig. 3-29: The Bravaisberget Formation at Bravaisberget

(Van Keulenfjorden). Fig. 3-30: Typical phosphate nodule horizons in the Bravaisberget

Formation at Festningen (outer Isfjorden). Fig. 3-33: Deltaic channel sediments typical for the Karentoppen

Member at Karentoppen (Smkapp Land). Fig. 3-36: Blanknuten Member at Blanknuten (Edgeeya). Fig. 3-38: Vertebrate remains in the Blanknuten Member, Blanknuten

(Edgeva). Fig. 3-40: The Kapp Toscana Group at Milne Edwardsfjellet (central

Spitsbergen). Fig. 3-41: Blanknuten Member, Tschermakfjellet and De Geerdalen

formations at Blanknuten (Edgeeya). Fig. 3-43: Large crossbeds in deltaic sandstones of the De Geerdalen

- Formation at Treskelen (Hornsund). q i g . 3-44: Deltaic sandstone lobes in the De Geerdalen Formation,

Kvalpynten (Edgeeya). Fig. 3-48: The equivalent of the Slottet Bed at Lyngefjellet (Hopen). Fig. 3-49: Cone-in-cone texture (siderite) in the Smalegga Formation,

Treskelen (Hornsund). Fig. 3-51: Knorringfjellet Formation at Festningen (outer Isfjorden). Fig. 3-52: Megaripples in the Knorringfjellet Formation, Tilasberget

(Wedel Jarlsberg Land). Fig. 3-56: Cliffs of the Svenskqa Formation on Svenskqa (Kong

Karls Land). Fig. 3-57: Kongseya, Agardhfjellet and Helvetiafjellet formations on

Hhfagrehaugen, Kongseya (Kong Karls Land).

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ILLUSTRATIONS

Fig. 3-58: Trough cross-beds in the Sjegrenfjellet Member, Hhfagrehaugen (Kongwya).

Fig. 3-59: Sandstone with tidal bundles and truncation surface, Mohnhegda Member at Hhfagrehaugen (Kongsarya).

Fig. 3-60: Magrehaugen (Kong Karls Land), showing Kongsarya, Agardhfjellet and Helvetiafjellet formations.

Fig. 3-62: Brentskardhaugen Bed deposited on crossbedded sandstones of the Knorringfjellet Formation at Drwbreen (central Spitsbergen).

Fig. 3-65: Brentskardhaugen and Marhngda beds at Marhngda (central Spitsbergen).

Fig. 3-67: Janusfjellet Subgroup at Janusfjellet (central Spitsbergen), overlain by the Helvetiafjellet and Carolinefjellet formations.

Fig. 3-68: Agardhfjellet Formation at Janusfjellet (central Spitsbergen).

Fig. 3-69: Agardhfjellet Formation with a huge carbonate concretion, Heimfjella (Wedel Jarlsberg Land).

Fig. 3-76: The MyklegardtjeIlet Bed at Janusfjellet (central Spitsbergen).

Fig. 3-77: Ullaberget Member of the Runkfjellet Formation at Keilhaufjellet (Serkapp Land).

Fig. 3-79: Helvetiafjellet Formation at Fotografryggen (Torell Land) with two sandstone lobes of the Festningen sandstone member.

Fig. 3-80: Delta front growth faults at the base of the Helvetiafjellet Formation, Kvalvdgen (Heer Land).

Fig. 3-81: Foot imprints of a carnivorous dinosaur in the Helvetiafjellet Formation at Kvalvdgen (Heer Land).

Fig. 3-83: Crossbedded sandstone, Festningen sandstone member, Kikutodden (Serkapp Land). Fig. 3-85: Dolerite dikes transsecting sandstones of the

Hhfagrehaugen Member, Kongsarya (Kong Karls Land). Fig. 3-86: A fossil tree trunk in the Hhfagrehaugen Member at

Tordenskjoldberget, Kongseya (Kong Karls Land). Fig. 3-90: Columnar basalt of the Kong Karls Land Flows at

Retziusfjellet, Kongsaya (Kong Karls Land). Fig. 3-92: Cretaceous succession at Zillerberget (Torell Land). Fig. 3-94: Prodelta facies of the Langstakken Member, Longyearbyen. Fig. 3-95: "Canon balls" in the Innkjegla Member of the

Carolinefjellet Formation at Utnibba, Kvalvdgen (Heer Land). Fig. 3-96: The upper members of the Carolinefjellet Formation at

Kostinsmellet (Torell Land). Fig. 4-08: Liljevalchfjellet and the coal mine Sveagruva. Fig. 4-09: Upper part of the Van Mijenfjorden Group at Krokryggen

(Van Mijenfjorden). Fig. 4-11: Cretaceous-Tertiary boundary at w o r d e n . Fig. 4-12: The abandoned coal mine "nye gruve 1" at Longyearbyen

(Firkanten Formation).

Fig. 4-13: Coal seam in the Todalen Member (Firkanten Formation), Longyearbyen.

Fig. 4-18: Sandstone of the Endden Member with typical convolute bedding at Kapp Hesselman (Van Keulenfjorden).

Fig. 4-23: Gilsonryggen shales (Frysjaodden Formation) near Sveagruva.

Fig. 4-24: Bentonite horizon in the Gilsonryggen Member, NordenskiBldfjellet (central Spitsbergen).

Fig. 4-28: Fossil leaves in the Aspelmtoppen Formation on Urdkollen, Van Mijenfjorden. Photo: W.K. Dallmann

Fig. 4-30: The former mining community (now research station) of Ny-Alesund, the coal field in the background.

+?!g. 4-31: During the drilling of borehole 24 at ~y-kesund; Scheteligtjellet with thrusted Carboniferous and Permian strata in the background.

Fig. 4-33: Tvillingvatnet Member, Agnes Field, Ny-Alesund. Fig. 4-36: Conglomerates of the Mmebekken Bed at Mnirebekken,

~y-kesund. Fig. 4-48: Sandstone and coal seam in the Skilvika Formation

(Wedel Jarlsberg Land). Fig 4-50: Basalt flows of the Seidfjellet Formation filling in a

palaeo-relief (Andr6e Land). Fig. 5-01: Sverrefjellet at Bockfjorden; preserved part of a

Quaternary volcano. Fig. 5-02: Halvdanpiggen at Woodfjorden; an eroded Quaternary

volcanic pipe.

OTHERS: Fig. 1-01: Conversion table for Russian Cyrillic leners Fig. 1-03: Table of post-Caledonian tectonic events and character of

sedimentation in Svalbard. Fig. 7-01: Bedrock map series of Svalbard, Norwegian Polar Institute:

Map index and publication status. Table of recommended stratigraphic names (status, rank, spelling in

EnglishNorwegian, superior unit): see Chapter 6.1 Table of type sections and type localities (with UTM positions):

see Chapter 6.2

INDEX MAPS: This book contains 90 index maps showing the geographical &stribution of groups, subgroups and formations, placed in the lexicon parts (Chapters 2.6,3.5,4.4, 5.2) with the respective key words. Units of member and bed rank have no index maps, because their geographical distribution is normally not mapped in detail, or their lateral boundary relations are not sufficiently defined.

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'Lithostratigraphic Lexicon of Svalbard' comprises the Upper Palaeozoic to Tertiary lithostratigraphy of Svalbard. The lexicon is the result of a very comprehensive compilation and evaluation of hundreds of formal and informal lithostratigraphic units carried out by the Committee on the Stratigraphy of Svalbard (SKS) during the period 1990-1998. The Stratigraphic Committee of Svalbard has been affiliated to the Norwegian Committee on Stratigraphy (NSK) which has supervised the work of SKS. According to the 'Rules and recommendations for naming geological units in Norway' (Nystuen 1989) NSK has approved the proposals from SKS of redefinition, revision and abandonment of all published as well as unpublished Upper Palaeozoic to Tertiary lithostratigraphic units of Svalbard.

The geological investigations of Svalbard started in the last part of the nineteenth century. Geological research groups from France, Germany, Great Britain, Norway, Poland, Russia, Sweden, USA and other countries have contributed to the present knowledge on stratigraphy and geological development of Svalbard. Principles on how to define lithostratigraphic units have changed a lot during more than one hundred years and have also varied through time between geologists working in Svalbard. Due to this long and mixed history of geological studies the resulted lithostratigraphy at the end of the 1980s happened to contain numerous inconsistencies in subdivision and naming of the rock record. The aim of the 'Lithostratigraphic Lexicon of Svalbard' has been to establish a lithostratigraphic scheme for Svalbard, harmonised as well as possible to the principles of lithostratigraphy recommended by the International Subcomrnission on Stratigraphic Classification of IUGS Commission on Stratigraphy (Hedberg 1976; Nystuen 1989).

The Svalbard archipelago forms the uplifted and emerged parts of the northwesternmost Eurasian lithospheric plate, now mostly flooded by the epeiric Barents Sea. Great scientific as well as economic interests are connected to this region. It is hoped that theLLithostratigraphic Lexicon of Svalbard', will give an improved overview of the lithostratigraphy of the region and act as a guide for future geological studies. The Norwegian Committee on Stratigraphy acknowledges the work of the Stratigraphic Committee of Svalbard, its subcommittees, the great number of individual contributors and the Editor of the Lexicon, Winfried K. Dallmann.

Oslo, June 29th 1999

Johan Petter Nystuen Chairman of Norwegian Committee on Stratigraphy (1986-1998)

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We appreciate especially the conn?'butions 08 m all committee members of SKS whose efforts made

this work possible; m other scientists who made valuable contributions,

especially: A. Dalland, C. Dons, PW. Grogan, T. Hellem, K. Kleinspehn, R. Knarud, G. B. Larssen, S. Olaussen, N. Pickard, K. Saalmann, M. Smelror;

m the then chairman of NSK, J.P. Nystuen, who supported the realisation of this project over many years and greatly improved the manuscript by his profound review;

m the reviewers K.-S. Lervik and N. Spjeldnaes, who contributed significantly to the improvement of the manuscript;

m F. Gustavson and I. Fossen, who redrew all type sections on the computer, standardising them from an extremely variegated original material.

We are grateful to the following institutions for allowing their employees to work on this project: m Norsk Polarinstitutt, Oslo and Tromss m IKU Petroleum Research, Trondheim m Norsk Hydro ASA, Oslo and Bergen m Norwegian Petroleum Directorate, Harstad m VNIIOkeangeologija, Lomonosov/St. Petersburg m Polish Academy of Sciences, Krakbw m Saga Petroleum ASA, Sandvika and Harstad m Statoil, Stavanger

University of Cambridge m University of Oslo m VNIIOkeangeologija, St. Petersburg

We are gmtefil to the following institutions for theirfinan- cial support to the present publication: m Amerada Hess Norge AS m Conoco Norway Inc. m Elf Petroleum Norge AS m Mobil Exploration Norway Inc.

m Norske Shell N S m NorskHydro ASA m Saga Petroleum ASA m Statoil m Total Norge A.S.

. . . for thefinancial support to the Secretariat for correlation of the stmtigmphy of Svalbard and the Barents Sea Shew m Conoco Norway Inc. e E l f Petroleum Norge AS m Mobil Exploration Norway Inc. m Norske Shell N S m Norsk Hydro ASA m Saga Petroleum ASA m Statoil m Total Norge A.S.

... and for the financial support given to the tmnslation of the "Stratigrafiieskij ~ l a t a r ' JPicbergena ''hm Russian to English (1991): m IKU Petroleum Research, Trondheim m Norsk Hydro ASA m Saga Petroleum ASA m Statoil

We also thank m the Commissioner of Mines at Svalbard for logistic

support; m S. Teigre, S. Holstad and A. Igesund for technical

support.

English review by David Worsley Tjpe sections drawn by Finn Gustavson and Ingrid Fossen Biostmtigraphic tables dmwn by Atle Mmk and Inger

Nilsson All o thermres and tables dmwn by Winfkied Dallmann -.

Technical editing by Amemor Brekke

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1. INTRODUCTION

WINFRIED K. DALLMANN

1.1 About this book

For the last 15 years or so, Norwegian geologists have been working on the registration and regulation of stratigraphic nomenclature for geological units in Norway. The need for registration and proper definition of stratigraphic names in a central database had long been obvious. With the increase of geological knowledge and literature, the amount of imprecise geological unit names was growing rapidly. Impre- cise names in this sense are understood as those not well- defined, or not used according to previously published definitions, or with definitions that are problematic in relation to more recent understanding of the regional geological framework.

A formalisation of the nomenclature was needed in order to distinguish between formally established unit names, informal working names, and traditional names that were not defined according to modern requirements. Especially with the onset of oil exploration on the Norwegian continental shelves, where insufficient geographical names are available, the variety of names grew dramatically, threatening to form a jungle impenetrable for the average, non-initiate scientist.

In 1982, the Norwegian Committee on Stratigraphy (Norsk Stmtigrefisk Komitd, NSK) was established by the Norwegian Council of Geology (Norsk Geologirdd). The committee consists of representatives of all major Norwe- gian geological institutions and oil companies, as well as a representative of the Norwegian Language Council (Norsk sprdkrdq. The committee's first main task consisted of es- tablishing rules and recommendations for naming geological units in Norway, based on international agreements, but specially aimed at Norwegian conditions. This project was successfully completed with the publication of "Rules and recommendations for naming geological units in Norway" in Norwegian (Nystuen 1986) and, subsequently, in English (Nystuen 1989).

The second main task was to establish a database at the Norwegian Geological Survey (Norges Geologiske Under- sakelse, NGU) in Trondheim, where all geological unit names are to be registered. The number of names registered and defined there ' considerable by now. Newly established names have to 1 ergo an approval procedure through NSK prior to their publication in Norwegian journals in order to ensure their accordance with the nomenclature rules, a measure not always appreciated, but generally accepted by individual authors.

In Svalbard, the history of geological names is unique, due to the pronouncedly international research carried out on the archipelago. Geologists from Norway and the Soviet Union, two of the main active nations, tried to communicate as much as possible for many years, but the political situation did not always permit sufficient and fast enough ex-

change of information. In places, different stratigraphic schemes developed in the respective countries. Geologists from other countries, especially the United Kingdom and Poland, also made significant contributions to the geological exploration of Svalbard, and also to the increasing numbers of unit names.

To avoid confusion without being able to offer immediate support, NSK initially considered names from Svalbard published prior to the publication of the "Rules and recommendations for naming geological units in Norway" (1986), as formal ones. Dissatisfaction with the situation, notably at the Norwegian Polar Institute which is responsible for the geological mapping programme in Svalbard, led to the establishment of the Committee on the Stratigraphy of Sval- bard (Stmtigrafiskfimitk for Svalbard, SKS) in 1990. SKS gathered representative stratigraphers fram the major research environments with interest in the subject and placed itself under the umbrella of NSK. The aim of SKS was (a) to collect and define all names ever given to rocks in Sval- bard and to register them in the NSK database, and (b) to work out and recommend a formalised lithostratigraphic nomenclature for Svalbard's bedrock, where superfluous names are rejected and, where considered necessary, new names are added.

A helpful step on the way was the lexicon "Stratigrafice- skij Slovar Spicbergena7' edited by Gramberg, Krasil'Eikov and Semevskij and published in Russian in 1990, which covers the major part of previously published unit names with short explanations. SKS edited an English translation (Dallmann & Mark, eh., 1991).

Compilation of the material presented in the present volume was eventually finished in 1997, and the resulting recommendations approved by NSK in 1995-1998. It is the first of two planned volumes covering the entire bedrock stratigraphy of Svalbard's land areas. The present volume starts with the Carboniferous system, or in places, where sedimentary troughs of mainly Carboniferous age started to develop earlier, with the latest Devonian (Famennian). The second volume is intended to cover the Devonian (more precise: Old Red) and Pre-Old Red basement stratigraphy. The reason for this subdivision is twofold: First, the presentation of the Devonian is more similar to that of the older rocks, with many informal unit names and the general lack of logged type sections, in contrast to the Upper Palaeozoic and younger strata. Second, ongoing mapping projects in the Devonian of Svalbard indicate that many changes of the present nomenclature will be necessary in the near future. Postponing the Devonian to a joint publication with the older stratigraphy in a few years' time will probably result in a significantly better and more up-to-date presentation.

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1. INTRODUCTION

1.2 Committee on the Stratigraphy of Svalbard: Organisation and purpose

The Committee on the Stratigraphy of Svalbard (Stmti- grafisk Komitb for Svalbard, SKS) was established by the Norwegian Council of Geology (Norsk Geologirdd) through the Norwegian Committee on Stratigraphy (Norsk Stmti- p f i s k Komitb, NSK). Its aim was primarily defined to elaborate a unified, formal lithostratigraphic nomenclature for the pre-Quaternary bedrock succession of the land areas of Svalbard. The committee's proposals are to be approved by the Norwegian Committee on Stratigraphy prior to their publication.

SKS is composed of working groups (subcommittees) or individuals each being responsible for one lithostratigraphic section or an area. These working groups are consultative to the main committee which is in charge of submitting the proposals to the Norwegian Committee on Stratigraphy.

The member composition hopefully reflects the variety of research groups and exploration companies doing stratigraphic work in Svalbard. Nevertheless, members do not participate on behalf of their affiliation, but on the basis of their own scientific competence.

SKS is obliged to follow the Rules and recommendations for naming geological units in Norway published in Norsk Geologisk Tidsskrift, Vol. 66, supplem. 1, 1986 (in Norwe- gian) and Vol. 69, supplem. 2, 1989 (in English).

Composition of the main committee during compilation of the present work:

Winfried Dallmann, chairman (Norwegian Polar Institute, Norway)

Krzysztof Birkenmajer (Polish Academy of Sciences, Poland)

Henning Dypvik (University of Oslo, Norway) David Gee* (University of Uppsala, Sweden) John Gjelberg (Norsk Hydro ASA, Norway) W. Brian Harland (University of Cambridge, United

Kingdom) Natascha Heintz* (University of Oslo, Norway) Audun Hjelle* (Norwegian Polar Institute, Norway) Hilde Keilen (Saga Petroleum ASA, Norway) Aleksandr A. Krasil'lEikov* (Polar Marine Geological

Expedition, P M G ~ , Russia) Atle Mark (MU Petroleum Research, Nonuay) Jew Nagy (University of Oslo, Norway) Arvid Nnttvedt (Norsk Hydro ASA , Norway) Yoshihide Ohta* (Norwegian Polar Institute, N t Norway) Tatjana M. PEelina ( WIIOkeangeologija, Russia) Ron Steel (University of Bergen, Norway; now University

of warning, USA) David Worsley (Saga Petroleum ASA, Norway)

* These members participate in work related to the Pre-Old Red or Old Red (mainly Devonian) not treated in this book.

1.3 How to use this book - important user information

1.3.1 Main objectives of this book

m Svalbard is the Norwegian administrative name for the Arctic archipelago situated between 74" and 81" North, and 10" and 34" East. The lexicon deals in particular with the land areas of Svalbard, including Bjnrrnraya (Bear Island). See Section 1.3.7 for remarks on the inclusion of offshore areas.

(r9 m The first purpose of this book is to present a complete

overview of the lithostratigraphic units of Svalbard (Late Palaeozoic and younger), with their geographical distributions, definitions, descriptions, type sections, literature references and other related information.

m All stratigraphic names ever published are intended to be contained in this book. Those names not recommended for future use are only provided with concise explanations and references to the recommended alternative names.

m The other purpose of this book is to "tidy up" the equivocal, and sometimes imprecise, use of names and nomenclature schemes in the geological literature of Svalbard. The book recommends a revised lithostratigraphic nomenclature which will hopefully guide the future use of stratigraphic names in the area.

m The recommendations of nomenclature suggested herein are based on several years' committee work and have passed a process of approval by the Norwegian Committee on Stratigraphy. This approval widely en- sures the proper use of the recommended names according to international nomenclature rules. Nevertheless, there are diverging opinions among scientist - in parts even among the authors - about several parts of the presented stratigraphic schemes. This divergence is discussed in the individual chapters of the book. The resulting recommendations reflect the opinion of the majority of scientists involved, but must certainly not be misunderstood as a directive. ;rwi W#.

c , L m

m The authors are fully aware that future research will lead to adjustments, and possibly major changes, of the stratigraphic nomenclature. The present r m e n d a - tion is thought to be a guide line for those using nomenclature as a tool, and an up-to-date starting point for stratigraphers working on the further development of the stratigraphic framework of the Arctic archipelago of Svalbard and the Barents Sea.

1.3.2 Organhation of the book

m The introductory part (Chapter 1) gives technical information about the present book, and an averview of the geological development of Svalbard. Overview maps

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1. INTRODUCTION

showing the distribution of stratigraphic groups and major tectonic elements, as well as major geographical names, are included.

m The main part of the book is subdivided into three chapters: Chapter 2 for the Upper Palaeozoic, Chapter 3 for the Mesozoic, and Chapter 4 for the Tertiary strata. Each of these chapters starts with general texts on the lithostratigraphic subdivision, previously used schemes, and regional descriptions of the geological development. These general texts are followed by lexicon parts, where each stratigraphic unit is defined and described, mostly including a log diagram of the type section(s). The defitions include synonyms, previously used names, origin of names, age detenninations, structural setting, thickness, boundary definitions, lithological descriptions and literature references. Short explanations of names which are not recommended for future use are listed separately. Each chapter also contains a stratigraphic overview table and maps showing the outcrop areas of all formations and superior units as well as the localities of type sections.

m A short chapter (5) deals with the Quaternary volcanic rocks.

m Chapter 6 shows tables, where technical information such as status, rank, spelling (English and Norwegian), superior unit, localities of type sections and type localities can be found. This information is essential for the correct use of unit names in scientific writing.

m A comprehensive bibliography (Chapter 7) should provide relevant literature for most questions concerning the Late Palaeozoic and younger bedrock stratigraphy of Svalbard.

m The index contains all stratigraphic names used in the book with ID numbers and page references to the definitions in the lexicon parts.

1.3.3 Use of ID numbers and quotation marks

m All recommended stratigraphic units are contained in the lexicon parts of chapters 2 to 5. These units have ID numbers witb&fiies indicating the related era (CP for Late Palaeozoic or Carboniferous/Permian, M for Meso- zoic, T for Tertiary, Q for Quaternary). The ID numbers are used throughout the book and can be used to quickly find and identify a respective unit on tables, lists, log di- agrams, type localities, etc.

m Previous names that are not recommended for future use by SKS are written in quotation marks throughout the book. These have short explanations and are listed at the end of each chapter.

1.3.4 Stratigraphic tables and applied ages

m Stratigraphic overview tables are schematic. They are meant to show the subdivision, geographic extension and approximate chronological correlations of units.

m Age indications on the stratigraphic overview tables are rough and should be used with care. In cases where diverging age interpretations exist, only one interpretation is shown in the tables. See age sections in the lexicon parts for more comprehensive information.

m The ages and age boundaries of the units are indicated in accordance with existing data, but are admittedly schematic. Possible diachronous boundaries are drawn straight unless there are reliable data that document the diachronism.

m The appendix contains biostratigraphic tables applied to Svalbard's Late Palaeozoic and Mesozoic successions (Chapters 2 and 3). The biostratigraphic zonation of the Tertiary succession (Chapter 4) is not known precisely enough. See remarks in the age sections of the lexicon part (Chapter 4.4).

2.3.5 w e localities and type sections

m All type sections in this book are redrawn from the ori- ginals according to a technical standard established for this purpose at Norsk Polarinstitutt.

m A fold-out legend for all type sections is contained at the inside of the back cover.

m The extremely varying standards, quality and scientific foci of the original sections made it impossible to redraw them according to a scientifically uniform standard. This means that differentiation made in some sections (e.g. sandstone, silty sandstone, siltstone, sandy shale, shale) may not be made in others (e.g. sandstone, siltstone, shale). In most cases, the original quality of information is maintained, although generalisation was undertaken where the purpose of technical standardisa- tion required this.

m As a result of this, for instance, some original sections show a very rough grain sue classification, different ways of particle classification (e.g. for carbonate rocks), or none at all which would satisfy the presently accepted standard grain size scale. These sections are adapted to the standard scale, with the note "grain size approximate".

m Almost all redrawn sections have been checked and accepted by the authors of the orig-mals or by a research partner or supervisor. For a few older sections, this was, , of course, not possible.

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1. INTRODUCTION

m Where newer and more informative logs of a previously defined type section existed, these new sections are used here. The reference to the original defintion is only shown in the text.

m Different kinds of type localities and sections used in this book: Stmtotype: The main type locality and section which

presently define the unit. Due to the often poor documentation of other previously defined type localities, the term neostmtotype is not applied, but previously defined stratotypes are mentioned in the text.

Hypostmtotype: The second or third type locality of a unit that documents major regional variations. Hy- postratotypes for some units in Svalbard are defined herein for the first time.

Boundary stmtotype and Unit stmtotype: If a unit does not have a documented locality where both its base and its main body are sufficiently represented, type localities for the lower boundary and the main unit body are defined separately. The use of boundary and unit stratotypes is here introduced to Svalbard stratigraphy.

m The name-giving localities of stratigraphic units in Sval- bard rarely coincide with their type localities. The reason for this is that unit names mostly have not been changed since their first appearance or definition in the geological literature, when type localities were not sufficiently documented. Later, better type localities were often found and documented in different places. Another reason may be. th6 lack of geographical names in the area of the type locality, or the use of the same type locality for several units.

Availability of cores from type wells: For most Meso- zoic type wells, apply to the Norwegian Petroleum Directorate (NF'D). For cores from wells containing the letter U in the well number, apply to SINTEF Petroleum Research. For cores from Tertiary type wells, apply to Kings Bay A/S in ~y-&esund, Svalbard.

1.3.6 Maps

m Maps in the introductory chapter: The overview maps in Chapter 1 show the distribution of stratigraphic groups (Fig. 1-04), major structural elements (Fig. 1-05), and the position of all detailed maps and the names of major geographical areas frequently mentioned in the text (Fig. 1-06).

m The other maps show the geographical distributions of formations. Sets of maps belonging to each of chapters 2 to 4, show the respective formations of Late Palaeo- zoic, Mesozoic and Tertiary age, while rocks of other ages are only subdivided into major complexes.

For the geographical distribution of units with a lower stratigraphic rank (members, beds) the reader is referred

to the text. The exact distribution of many of these units is still poorly known.

Ages indicated roughly in the legend of these maps are meant for general orientation. See age sections in the lexicon parts for more comprehensive information.

The maps are not tectonic maps. To keep the map information clear, only faults that have influenced either the deposition of the respective stratigraphic interval or its present outcrop pattern, are shown. For instance, faults bounding Carboniferous troughs are not shown on the maps belonging to the chapters on Mes ic or Tertiary stratigraphy, while faults displacing o 8' Mesozoic and Tertiary rocks at the surface do not occur on the maps in the Late Palaeozoic stratigraphy chapter. For fault symbols used on the detailed maps, see legend on the ouer- view maps (Figs. 1-04, 1-05).

The positions of all type localities are indicated by the ID number of the respective unit (section 1.3.3). Q-pe localities which are not provided with a stratigraphic log are also shown in this way.

m Most geographical names used in the text, including name-giving or type locality names, are shown on the maps.

m References to sources of map data are too abundant to be indicated on the maps. Most information is referred to on the bedrock maps published by Norsk Polarinsti- tutt, including preliminary editions.

1.3.7 Correlations with the geology of the Barents Sea Shev

During the committee's work on the lithostratigraphic nomenclature, correlations with the stratigraphy of the western Barents Sea Shelf were considered important. Hydrocarbon prospecting in the western Barents Sea has been going on since 1980, and with the expected future developments there, the amount of stratigraphic names will increase. Svalbard is often used as a reference and training area by offshore geologists working in the Barents Sea. It is the committee's opinion that the lithostratigraphic nomenclature systems should clearly show the relationship between the onshore and offs$ore development and that the framework of stratigraphic groups should reflect this relationship.

m The Late Palaeozoic stratigraphic nomenclature of the offshore areas is presently being worked on by another committee in close co-operation with NSK l@ m& is not yet concluded, but there is a general consem that the h e w o r k at group l m l will be applied from M- bard, while an additional group is defmed in the wmkm Barents Sea, with only one formation represented txwbme on the i s l d of Bjsmarya Available data points on the Upper Palaeozoic of the Bmnts Sea Shelf am still sparse.

' .-

l . . F$

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INTRODUCTION

m The nomenclature of the Mesozoic stratigraphy in the western Barents Sea has preliminarily been established in connection with the present work. Abundant data are available, although published data are mainly restricted to the Hammerfest Basin. The overall group framework proposed here will probably be applicable for a long time ahead, while adjustments or additions at lower levels are expected. Work on the offshore Mesozoic nomenclature has made significant progress and Meso- zoic offshore formations are included in the present volume.

m The stratigraphy of the Tertiary offshore basins is not yet well enough known. Tertiary offshore basins probably developed separately from those exposed onshore.

1.3.8 Change of place-name segments

m Place names in Svalbard have changed significantly throughout history. One reason is the international use of Svalbard through the last centuries. Norway did not start to execute her sovereignty earlier than 1925 (according to the Svalbard Treaty of 1920), when names fiom other languages gradually started to be translated into Norwegian. Even later, Norway started to pursue the policy of naming - and renaming -places according to spelling in the less wide-spread of the two Norwegian languages, Nynorsk. Many modern, revised spellings did not occur on maps or publications previous to the 1990s. For these reasons, many place-name segments of stratigraphic units do not coincide with the spelling of the respective place names on modern maps, which is disadvantageous.

m SKS has adopted the new spellings for those place names where changes were minor, and where the original name is easily recognised (e.g.: Petrelskardet Forma- tion - Petrellskaret Formation).

m SKS has changed incomplete place names into complete ones in order to avoid formation names with a first segment reflecting, for instance, a person rather than a mountain F.: Vegard Formation - Vegardfjella Forma- tion). '

SKS has not adopted translations of names from, for instance, ori@ English place names (ex.: Wood Bay - Woodfjorden, for a Devonian formation), or other major changes where the original place name would then not be easily recognised.

1.3.9 Lower boundary definitions and descriptions of geological units

m This lexicon is attempting to standardise descriptive data fiom a huge variety of original sources and authors. The varioGs geological units have been investigated and described for different purposes and with a varying quality in the geological literature. It was therefore not always

possible, on the basis of existing data, to achieve a consistent way of description. So, for instance, while some units may lack a reference to an interpretation of the depositional environment, others may lack sufficient data on lateral facies variations, etc.

m To avoid much repetition, some features may be described for a superior rank unit (e.g. formation), without being repeated in the description of the inferior rank units (members), or .vice versa, depending on what ap- peared to be most appropriate. The user of the lexicon is therefore asked always to check superior and inferior rank units in order to find the requested information.

m A good definition of its lower boundary is an important property of any geological unit. The great variety of authors of different nations defining these units in Sval- bard may result in an inconsistent @ty of lower boundary definitions. In many cases, geological units were defined without a proper defition of their lower boundary. These units may still have survived history and be accepted by present geologists as "good" units, simply because they designate characteristic rock successions. Many lower boundary definitions, a demand of modern lithostratigraphy, have therefore been added by the authors of this lexicon as precisely as possible from the existing data. For a number of units, especially for those with interfirngering contacts or transitional boundary features, these definitions may appear rather arbitrary.

1.3.10 Notes on references

m The literature references cited in this book are preferen- tially confined to work fiom the 1920s onward. The reason is that earlier authors often did not subdivide the stratigraphic succession in a way that makes their work relevant for the nomenclatorial issues treated in this book. It must still not be forgotten that the geological description of Svalbard started more or less in the 1860s, and the first two generations of Svalbard geologists provided simcant pioneer work. To find references to this, the reader is referred to the bibliography (Chapter 7).

m A relatively high amount of units have been defined andtor described on the basis of previously unpublished data. The reason for this is the enormous amount of data collected by petroleum geologists and only contained in internal reports of their companies, and a large amount of unpublished theses. For future reference to these units, the present lexicon is to be considered as the original publication, although reference to the unpublished source always should be provided in addition. The use of unpublished data in this case should not be problematic; the respective unit definitions have been extensively re- viewed by the entire subcommittee (authorship of the respective lexicon chapter), prior to the reviews by SKS, NSK (Norwegian Committee on Stratigraphy), and final referees.

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1. INTRODUCTION

1.3.11 Explanation of place names

Place names in Svalbard which have been used for stratigraphic unit names, have either a descriptive meaning, or are fiom persons, vessels, etc. Descriptive meanings are translated in the lexicon part of the book, because these names may have geological implications.

For other place names, and for more information about the names, the reader is referred to 'Place names in Sval- bard', Norges Svalbard- og Ishavsunderserkelser (1 942) and Orvin (1958), both reprinted by Norsk Polarinstitutt (1991).

Explanation of common place-name endings: -bekken Creek -berget: Mountain -breen: Glacier -bukta: Bay -byen: Town -dalen: Valley -egga: Crest -elva: River, Creek -fjella: Mountains -gellet: Mountain -fjorden: Fiord, Inlet, Firth -flya: Plateau -fonna: Ice Cap -halvwa: Peninsula -hamna: Harbour -haugen: . Hill -hatten: Hat -heia: Hill -heim: Home, Hut -hornet: Horn, Peak -hsgda: Hill -huken: Point -isen: Ice, Glacier -kammen: Crest, Ridge -kampen: TOP -kanten: Edge Kapp -: Cape

-kjegla: -1aguna: - Land: -neset: -nuten: -odden: -wa: -passet: -pynten: -ryggen: -salen: -S&:

-skaret: -sletta: -strands: -sun& -tangen: -tind(en): -toppen: -v&gen: -vatnet: -vika:

Cone Lagoon Land Point, Cape Summit Point, Cape Island Pass Point; Cape Ridge Saddle Haystack (cone-shaped mountain) Notch, Pass Plain Beach Sound Point, Cape Peak Summit Bay Lake BayICove

1.3.12 Transliteration of Russian names and references

Russian names and references correspond to the IS0 (Inter- national Standard Organisation) transliteration, which - with a very minor deviation - is also used in the Inter- national Bibliographic System. The advantage of this transliteration compared with national transcriptions, such as the English transcription, is its reversibility. Russian names transcribed in English or other languages cannot unequivo- cally be transcribed back into the Cyrillic alphabet; this may cause problems when inquiring for authors, or when looking for place names on Russian maps. Unfortunately, various electronic databases and international journals have adopted the English transcription. For this reason, a conversion table is added below (Fig. 1-01).

Fig. 1-01: Conversion table for Russian Cyrillic letters, IS0 transliteration and English transcription. Be aware that conversion is only valid from Cyrillic or IS0 to English, but not vice versa.

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1. INTRODUCTION

1.4 Outline of the geological history of Svalbard

1.4.1 Tectonic setting

The archipelago of Svalbard is the emergent northwestern corner of the Barents Sea Shelf, which was uplifted by late- Mesozoic and Cainozoic crustal movements. The area provides a splendid insight into the varied geological structure and geo-historical development of the northwestern Barents Sea since the Palaeoproterozoic. The geological record ranges from possible Archean to Recent and shows a multi- orogenic development with prominent tectonic events of Grenvillian (late-Mesoproterozoic), Caledonian (Ordovi- cian-Silurian), Ellesmerian or Svalbardian (Late-Devonian), Variscan (Mid-Carboniferous) and Alpidic (Early-Tertiary) age.

North of Svalbard, 50-100 km from the shore, a steep passive continental margin with slopes up to 10° (average 4") forms the boundary with the Eurasian Basin of the Arctic Ocean. Offshore to the west of Svalbard, a 40-80 km wide shelf separates the coast of the main island, Spitsbergen, from a structurally complex oceanic area, the Knipovich Ridge (Talwani & Eldholm 1977). The central part of this ridge is a spreading axis which is segmented by a transform fault system, the Spitsbergen Fracture Zone in the north, and the Greenland Fracture Zone in the south (Fig. 1-02).

The northwestern shelf corner borders the Yermak Plateau, the northern part of which may be the remainder of an Early-Tertiary hot spot (Feden et al. 1979). Late-Creta- ceous thermal uplift, Early-Tertiary shoulder uplift along the rifted margin of the developing Arctic Ocean, and subsequent transform movements in a periodically trampres- sive regime along the western margin may all have their share in explaining the uplift of the archipelago and especially of its western and northern reaches.

1.4.2 Pre-Old Red t

The term Pre-Old Red is here applied for the rocks already present under the main Caledonian orogenic phase in the Middle Silurian. The literature on the geology of Svalbard often applies the term 'Hecla Hoek' to this basement. There has been confusion about this name due to its original definition (Nordenskiold 1863) and the later elaborated com- plexity of the Pre-Old Red strata causing several redefinitions (Orvin 1940; Harland & Wilson 1956; Krasil'BEikov 1970,1973).

The Pre-Old Red succession is exposed in the west and north of the archipelago. It has long been considered to be mainly the product of the Caledonian orogeny, though distinctive unconformities have been reported fiom southern Spitsbergen (e.g. Birkenmajer 1975, 1991; Bjornemd 1990) and Nordaustlandet (e.g. Flood et al. 1969; Ohta 1982). Since the late 1980s, U-Pb zircon isotopic age determination has revealed several Precambrian events (e.g. Ohta 1994; Gee et al. 1994). The Pre-Old Red thus has a poly- orogenic development: Baikalian movements (600-650 Ma), the Grenvillian tectonothermal event (950-1000 Ma), and indications of earlier events recognised in several areas (ca. 1400 Ma, 1700-1800 Ma, and two or three older ones;

Ohta 1992) are followed by two distinct Caledonian fold- thrust events, including evidence for an oceanic suture zone in the Western province.

The Pre-Old Red is subdivided into three different tectonostratigraphic "basement provinces", whose structure, sedimentary record and tectonothermal evolution differ from each other. Their juxtaposition occurred probably during the Caledonian period, though no consensus about the involved mechanisms yet exists (Harland 1969, 197 1 ; Birkenmajer 1981; Ohta et al. 1989; Ohta 1994). After the Middle Silurian, however, Svalbard formed part of the 'Old Red Continent'.

1.4.3 Old Red (Devonian)

During the Devonian Period, Svalbard experienced the deposition of a vast thickness of Old Red molasse sediments which are mainly preserved in a down-faulted crustal block in northern Svalbard, bounded by the northwestern and eastern basement provinces. The main tectonic overprint and tectonic style of this graben system is related to a Late- Devonian culmination of tectonism, the 'Svalbardian Phase', which resulted in contractional movements predominant in northern Svalbard (Orvin 1940). The Svalbardian Phase is normally considered to be a late, post-molasse- stage phase of the Caledonian orogeny and may be related to the Ellesmerian-North Greenland Foldbelt deformation in the Canadian Arctic and northern Greenland.

1.4.4 Late Palaeozoic

During the Carboniferous Period, Svalbard developed from a site of fault block tectonism with differential sedimentation to a stable shelf that experienced overall subsidence (except for southern Spitsbergen). A local (?) phase of folding and thrusting, only locally recorded on southern Spits- bergen, occurred possibly in the Visean ('Adriabukta event': Birkenmajer 1964; Dallrnann 1992). The main fault block movements occurred in the Bashkirian and Moscovian, resulting in a new constellation of troughs, mainly half- grabens, with a syntectonic sedimentary record, developed along older tectonic lines (Gjelberg & Steel 1981). With waning tectonic movements in the later Carboniferous, most of Svalbard developed into a carbonate platform with episodes of evaporite formation. These conditions lasted through the Early Permian, while the later part of the Per- mian experienced renewed clastic influx and a subsequent hiatus at the era boundary (Steel & Worsley 1984).

Late-Palaeozoic sedimentation in the SvaIbard/Barents Sea area was continuous with that in the Wandel Sea Basin in northeastern Greenland ( H b s o n & stemme& 1984), a site at that time situated not farther than maybe 100 km from what is now the western coast of Svalbard.

1.4.5 Mesozoic

The Mesozoic stratigraphic record consists of repeated clastic sedimentary successions, mainly delta-related coastal and shallow shelf sediments (Triassic-Early Jurassic), deeper shelf sediments Wddle Jurassic to earliest Creta-

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1. INTRODUCTION

ceous) and again shallow shelfldelta deposits (later part of Early Cretaceous). The source area of the sediments was mainly situated in the west, and later also in the north, while the basin opened towards the present Barents Sea (Steel & Worsley 1984). This view is consistent with the less complete Mesozoic sections in the Wandel Sea Basin of NE Greenland (Hhnsson et al. 1991). Early Jurassic block faulting and development of sedimentary basins during the Cretaceous in the Wandel Sea Basin are explained by the Mesozoic onset of transform faulting between Greenland and the Barents Sea (Birkelund & Haansson 1983; H b s o n et al. 1991). In Svalbard, no such tectonics are seen, and the entire Upper Cretaceous is lacking due to an overall uplift, with highest uplift rates in the northwest.

The first sign of break-up between Greenland and Europe and the opening of the Arctic and North Atlantic oceans recorded in Svalbard is the intrusion of dolerites from the latest Jurassic through the Early Cretaceous (Burov et al. 1977). They occur most commonly as sills in Carboniferous through to Jurassic strata (progressively younger to the east). On Kong Karls Land, in eastern Svalbard, basaltic lavas were extruded during the later part of the Early Creta- ceous. They belong to a larger volcanic province which also includes large parts of the Barents Sea and Franz Joseph Land.

1.4.6 Tertiary

The opening of the Arctic and North Atlantic oceans caused a tectonic overprint with convergent structures in the Pale- ocene and Eocene. Structures that developed were related to a transform fault system, the Spitsbergen Fracture Zone, or "De Geer Fault", situated offshore to the west of Svalbard (Fig. 1-02). Convergent movements during part of the transform movement caused the reverse uplift of the western basement province, thrusting the basement rocks and overlying cover strata onto the simultaneously developing foreland basin, the Central Tertiary Basin (Steel et al. 1985). Though associated with a major, dextral plate transform setting between the Greenland and Barents shelves and previously described as a typical transpressive orogen (Harland 1969; &land & Horsfield 1974; Lowell 1972), the Tertiary fold-thrust belt consists mainly of convergent structures (e.g. Maher et al. 1986; Nnrttvedt et al. 1988; Dallmann & Maher 1989; Haremo et al. 1990; Bergh & Andresen 1990). This led to a decoupling model (Nnrttvedt et al. 1988; Maher & Craddock 1988), meaning that strike-slip and convergent movements may be localised in different deformation zones. Recent work revealed the local existence of additional strike-slip-related structures along several N-S oriented fault zones (Dallmann 1992; McCann & Dallmann 1996; Maher et al. 1997).

ENE-WSW shortening was transferred east ahead of the fold belt along high level detachments within the cover sediment~, and interfered with renewed, reverse faulting along basement-involved structures farther east (Billefjorden and Lomfjorden faultzones; Haremo et al. 1990; Haremo & Andresen 1992; Haremo et al. 1993; Miloslavskij et al. 1993).

During later stages of foldbelt development (Eocene- Oligocene), minor sedimentary basins (especially the For- landsundet Basin) developed in westernmost areas. Their structural record is complex and difficult to relate to the deformation phases of the main foldbelt (Gabrielsen et al. 1992, Kleinspehn & Teyssier 1992). The latest tectonic overprint was an overall E-W extension that affected more or less all favourably oriented earlier faults and generated new faults in the foldbelt area. These fault movements must be seen in the context of the post-Eocene development of a passive continental margin to the west, when Svalbard, drift- ing along the transform fault system, had separated from the continental shelf of Greenland.

1.4.7 Tertiary and Quaternary volcanic activiiy

Volcanic activity of both Tertiary and Quatenmry age occurred in NW Spitsbergen, overlying Devonian and Pre- cambrian rocks. The Tertiary volcanites are plateau basalts (transitional olivine basalts) of mainly Miocene to Pliocene age (Burov & Zagruzina 1976; Prestvik 1978), while the Quaternary volcanites are volcanic centres (off-ridge alkali basalts) situated on faults that date back& least to the De- vonian; their age is probably between 100,000 and 250,000 years (SkjelhvAle et al. 1989). Hot springs in several places in northwestern and southern Spitsbergen witness to continuously high geothermal gradients along the Tertiary fold- thrust belt.

Fig. 1-02: Geological ove~iew map of Svalbard and the western Bar- ents Sea Shelf, showing the positions of major tectonic elements. Offshore &ta are mainly from Sigmond (1992); faults north of the Bjarmeland platform are added fiom unpublished data (Norwegian Petroleum Directorate, 1998) and refer to the top Permian level. The indicated type wells refer to Mesozoic offshore formatio~~s defiied in Chapter 4. 4 -vi*;~!t*

. 8 8 dt!. - . , - .- 7'

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' . INTRODUCTION

PUocene and younger sedlments 1 on contln. slope and Yermak Plateau T e r m sedhnents In rltl-related basins close to continental margln ,

T- sedlments on Barents Shelf

Sedlments of unknown age

~dventdalen Group (M.Jur. - Cret SBssendalen and Kapp Toscana mm lTrlassk - Middle Jurasslc

with salt dlaplrs (age of San Carbonlf. - Early P m Carbonif. and Pemlan sedlments

Devonkrn sedlments

Pre-Old Red b m e n t E

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I . INTRODUCTION

Fig. 1-03

regional uplm

l' I eontinwous S"kapp-

Homund - High remains

I C \I/

development of stable shelf

extensional block faulting W d o m of several de- positioneil tm!igh

&

Adliabukta Phase ? local idcling in S' Svalbwd

blmk faulting Svalbardkzn Phase foldl~hhrusting in N' Svalb.

si~lcicimtic influx prevding splcufitle rocks;

Caledon~an Orogeny -m Tectonothermal events I cmor . I Ulholmv

onglomerate

sandstone

limestone

dolomite

Fig. 1-03: Table of post-Caledonian tectonic events and character of sedimentation in Svalbard. The absolute age scale refers to Haq & van Eysinga (1987).

Fig. 1-04 (p. 22): Geological overview map of Svalbard showing lithostratigraphic groups. Legend for symbols used on all maps. Fig. 1-05 (p. 23): Overview map of Svalbard showing major structural elements. Legend for symbols used on all maps. --. S . Fig. 1-06 (p. 24): Map of Svalbard showing names of major geographical features and an index of detailed maps.

. a y

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pp

Leaend for maD svmbols used in thls book1

I Settlement or abandoned place '

i Coal mine (ln operation /abandoned)

$ 0 - Fault, undifferentlated ,, Normal fault

barbs towards dowwfaulted b W ,, Reverse tauit or thrust

teeth towards upllfted block ,, Fault with multiple moveme& . teeth towards uplltted block I

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2.1 General subdivision

During the last three decades, geologists concerned with Svalbard have mostly applied the stratigraphic scheme of Cutbill & Challinor (1965) for the Upper Palaeozoic of Svalbard. Revisions of the scheme concerning individual stratigraphic units, however, have occurred with increasing frequency, especially since the early 1980s when a more detailed understanding of the late Palaeozoic tectonic framework of the archipelago developed. Today, we are in a situation where minor revisions have become numerous and a major nomenclatorial review will facilitate a more mean- ingful use of stratigraphic names.

The general stratigraphic subdivision of the Upper Palaeozoic strata into three groups, as proposed by Cutbill & Challinor (1965), is well-established and generally accepted in the geological literature; these groups are recommended for continued use.

The oldest Billejorden Group is of latest Devonian to Early Carboniferous age and consists of clastic sedimentary rocks. Deposition started in the Famennian in separate, possibly isolated troughs, but deposition became widespread through the Early Carboniferous (Steel & Worsley 1984). Most significant exposures are preserved in the Inner Horn- sund, St. Jonsfjorden, Billefjorden and West Bjsrnsya troughs (Figs. 2-02,2-03).

The overlying Gipsdalen Group comprises Bashkirian through to Lower Permian strata. Lowermost clastic units of a predominantly redbed facies are found in the same troughs as the underlying Billefjorden Group (Steel & Worsley 1984). Deposition started in the Serpukhovian and most of the troughs show an increasing marine influence, with both evaporites and carbonates replacing the clastics through the Bashkirian and into the Moscovian. Intermediate platform

and structurally high areas (Wedel Jarlsberg Land High, Smkapp-Hornsund High [Steel & Worsley 19841, Nord- fjorden High [Cutbill & Challinor 19651) were progressively transgressed through the Moscovian leading to the widespread development of platform carbonates. An important exception is the Inner Hornsund Trough, where clastic deposition prevailed to the latest Carboniferous.

The complex stratigraphic development of the Gipsdalen Group justifies a stratigraphic subdivision at a higher than formation rank. Such a grouping enables us to address to the sedimentary fill of an individual trough or basin with related depositional environments. Such subdivisions had been proposed prior to the stratigraphic scheme of Cutbill & Challinor (1965). These units had group rank, but should now be considered as subgroups of the Gipsdalen Group.

The Charlesbreen Subgroup (according to Dineley 1958), originally used for the Bashkirian-Moscovian clastic deposits of the St. Jonsfjorden area, can reasonably be extended to comprise the sedimentary fill of the entire St. Jonsfjorden Trough, so that the more or less coeval sediment~ of Brflggerhalvraya (NW Oscar 11 Land) should be included in this unit.

The Campbelliyggen Subgroup (according to Gee et al. 1952) designates the Bashkirian-Moscovian fill of the Bille- fjorden Trough with transitional clastic, carbonate and evaporite facies, with uppermost units onlapping areas to the east of the trough.

The Bashkirian to Lower Permian clastic fill of the third, well-defined trough, the Inner Hornsund Trough, is here collectively called the lFesRelen Subgroup.

Coeval deposits on Bjnrmsya and in the Eastern Ny Fries- land/Lomfjorden/Nordaustlandet area are not assigned to

Fig. 2-01: Group and subgroup subdivision of Upper Palaeozoic rocks

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and , ligh St. Jons~,", rlen

Trough

B. Bellsund - outer lsfjorden

Nordflorden High

C. Snrrkapp - Hornsund NNE W Inner ~omsund E

wedel Jarlsberg Land High

L'."",,~I,V, W, I Trough

Legehdforool~onprofiles Ternpe ordenGrwp ( rna~nbLe ~ e n i a n ) Glpsdalen Gmup undlffersntlated (Late ~arboniferdus - Eerly Permlan)

~ ~ c k s o n Land Subgroup

Carnpbellryggen Subgroup

Chariesbreen Subgroup

Treskelen Subgroup

m Bllleljorden Group (Early Carbonifemus)

Pre-Old Red Basement and Old Red rnolasse

Legend for colours on map:

m Areas where Bashklrhn-Mosoovlan L . trough strata are exposed

BT - Bllle~orden T m @ ? /HT - Inner Homwnd Tmugh NFH - Ny F-d High NH - N w ~ ~ High SHH - S&@p-Hom~~nd Hlgh a '4

L

ig. 2-02: Sketch profiles and map oftlie middle Eatbrrnifm troughs -, ~ighs. The Lower to the troughs, but preferably preserved within them. The mainly Bashkirian-Moscovian strata is confined to the troughs, with one sub - L ' signed to each of them, while the Dickson Land Subgroup overties troughs and highs.

2 .

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""PER PALAEOZOIC LITHOSTRATIGRAPHY

any subgroup, because regional distribution and affiliation with defined troughs are too poorly known.

The overlying, extensively deposited platform carbonates and evaporites that were deposited over most of Svalbard are here called the Dickson Land Subgroup.

The Upper Artinskian to Kazanian Tempeljorden Group consists of siliceous, spiculitic platform sediments, locally interbedded with carbonates or sandstones. They have been deposited all over Svalbard, except on the Smkapp-Horn- sund High. West of the Smkapp-Hornsund High, another basinal area - the extent of which into present offshore areas is still unknown - existed in the late Permian.

One additional group recently recognised on the southern Barents Sea Shelf, the Bjarmeland Group, has only one thin representative formation on Bjsmsya, stratigraphically below the Tempelfjorden Group.

2.2 Previous stratigraphic schemes

The generally applied stratigraphic scheme for the Upper Palaeozoic of Svalbard is that of Cutbill & Challinor (1 965), who - for the first time - constructed their nomenclature on a stratigraphic synthesis of data from the entire Svalbard archipelago (Fig. 2-03). A variety of local formation and group names were replaced by the new correlation scheme. Since 1965, a number of minor revisions of the scheme of Cutbill & Challinor have been proposed. These are - with the exception of the two remote islands Nordaustlandet and Bjsrnnrya - not shown here, but are discussed in the subsequent sections of this Chapter.

2.3 Major revisions

A few revisions of the established nomenclature proposed herein have regional significance. The two main items are discussed below, while minor revisions are argued for in the subsequent sections andtor in the definitions of individual stratigraphic units.

2.3.1 Revised nomenclature for the Lower Carboniferous of the Billefiorden h u g h

The hitherto accepted subdivision of the Billefjorden Group in the Billefjorden area (Hmbyebreen and "Svenbreen" formations of Cutbill & Challinor 1965; Fig. 2-03b) is problematic. A major sedimentary break has been demonstrated in the upper of the two, the "Svenbreen Formation", between its lower, light-coloured members and the overlying red-coloured Hultberget Member (Gjelberg & Steel 1981; Gjelberg 1984, unpubl.). Also, the colour change from coal- bearing, grey sandstones and shales of the major part of the succession to non-coal-bearing redbeds of the Hultberget Member defines a more distinct formation boundary. Even more important, the Hultberget redbeds show a transitional contact towards the overlying clastics of the Ebbadalen For- mation. It is therefore proposed to raise the Hultberget redbeds to formation rank (Hultberget Formation) and as-

sign them to the Gipsdalen Group (Campbellryggen Sub- group).

The Hultberget redbeds should not be regarded as a member of the Ebbadalen Formation as proposed by Johannessen (1980, unpubl.) and applied in several newer articles (referred to as "Anservika Member"). This would involve moving the base of the Ebbadalen Formation 200 m downward, significantly changing the meaning of the well-established name 'Ebbadalen Formation'. Unlike the Ebbadalen Forma- tion, the Hultberget redbeds occur also far to the west of the Billefjorden Fault Zone in the Triungen-Citadellet area, and probably far to the north-east, in the Lomtjorden area.

A more radical nomenclatorial revision would probably not define several formations at all in the Billefjorden Group of the Billefjorden area, because existing formational boundaries are neither easy to map nor constitute any major change of lithofacies or depositional environment. However, in order to avoid too much confusion, the name H0rbye- breen Formation is recommended to be used unchanged, while the overlying non-redbed part of the former "Sven- breen Formation" (Sporehsgda and Birger Johnsonfjellet members; Fig. 2-03b) is proposed to be called Mumien For- mation, after a mountain in the vicinity of those giving names to its members (Sporehsgda and Birger Johnson- fjellet). All use of the nyne "Sypbreen Formation" should be discontinued.

2.3.2 Revised nomenclature of the 66Nordenskioldbreen Formation"

The name "Nordenskioldbreen Formation" was given by Cutbill & Challinor (1965) to a thick, heterogeneous, though carbonate-dominated succession that was deposited across most of Svalbard except in the southernmost areas. It originally contained six members (mellfjellet, Cadell- fjellet, Kapitol, M i e l l e t , Marrebreen, Scheteligfjellet members). Later authors added the Idunfjellet and HArbard- breen members (Lauritzen 198 1) and the Jutulslottet Mem- ber (Johannessen et al. 1984, unpubl. report, Statoil).

This complex unit contains Moscovian clastic sediments, evaporites and/or carbonates that were deposited in separate troughs (Jutulslottet, HArbardbreen, Scheteligfjellet and Minkinfjellet members) and transitional, transgressive facies to extensive platform carbonates that overlie the former troughs. The "Nordenskioldbreen Formation" defined in this way appears too complex to be one formation. It contains several subunits that deserve formational rank due to their distinctive lithological successions and genetic con- finement to certain troughs or sub-basins.

Formational rank should be applied to those of the former members that are completely or mainly confined to separate troughs, viz. the HArbardbreen, Scheteligfjellet and Minkin- fjellet members. The clastic Jutulslottet Member is advan- tageously grouped with the TAmkanten Formation of the Charlesbreen Subgroup.

The remaining platform carbonate part of the "Norden- skioldbreen Formation" (consisting of the Wellfjellet, Cadellfjellet, Kapitol, Mmebreen and Idunfjellet members) will belong to a new formation that - in order to avoid con-

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2. UPPER PALAEOZOIC LiTHOSTRATlGRAPHY

pp

3jorneya iNDERSSOL IYUU

IORN & ORVlN 19

ILL & C 198s I WORSLEY & EDWARDS 1976 SKS, present volume

RBedvi Formation RBedvika Formation

IW' and S' Serka and ~IEDLECK11960.1964 CUTBILL ICHALLINOR 7; SKa "d.

Tnkr r a

rjenrral aer~app Lana, nornsuna - -

BIRKENMAJER & BIRKENMAJER 1964 CUTBILL &

CZARNIECH

h., x

U& p,,.,., 4:p

H d n d e n Mb.

Formation

Hcvthldm mb.

Formation

Formation

Wordiekammeh Formetton

Nordenskiijldbreen Formation

I I Tamkanten Tllmkanm Thkantw I J u h r / s w mb.

I Biandstone Sandstone Forination Formation I I

Petrelskardet Petml&ardet $hale Shale Formation Petdskaret Formation

I 1

Vegard Formation Vegprdfjella Formation

gg$z I Orustdaien Formation Orustdalen Formatin -

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Nordflotden - Mckoon Land

m

Billefjort OEE et al. l9

tlnden Mb. HankKfsn Mb. Z L t i n m- F o r

Vadngcn Mb.

Formation Lower Oypars Zone

Formatkm -mm - - U ," ,?a% -. L-

Norden- fpm skibldbreen g,",:

TyrrellfJelkt Member Caddnylia Member

Mlnklnflsllet Member

Lh- l ski6ldbnan 1 Formation - m.

Tabqella b. TrlkoWj. Mb. Qettelva Mb. Ebbaelva Mb. Hultberget Member

Ebbadalen Member Formatton TkolorfleUet

Member I EbbaelmMb.

Huitberget Formation B1 rJohnsoi

Mumien f@K ember Formation S o n h m a

drnber Hoelbrwn

H~rbyebreen Member

Farmation Verlngen Mh. Vwlilg.n Mb. *

" 1 :%E!'" I MaIte Brunfjeliet Formation

Fig. 2-03: Previous and proposed stratigraphic schemes for the Late Palaeozoic showing the formation and member levels. The tables are sorted according to area and present the general development af the lithostratigraphic nomenclature. The references do not necessarily indicate that the author@) introduced the individual namts. In each table, the column to the right shows the presently recommended scheme.

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fusion with overlapping definitions - must be renamed. Clear priority is given to the name 'Wordiekammen Forma- tion' (Gee et al. 1952: "Wordiekammen limestones"), used for the Cadellfjellet and Tyrrellfjellet members in the Bille- fjorden Trough and the Kapitol and T3mellfjellet members on the Nordtjorden High - exactly the range of strata referred to herein. All use of the name "Nordenskioldbreen Formation" should be discontinued.

2.4 Correlation with the Barents Sea Shelf

The Upper Palaeozoic stratigraphy of the Barents Sea Shelf is presently being elaborated by a committee under the umbrella of the Norwegian Committee on Stratigraphy (NSK). There is a general understanding that the overall stratigraphic development of the Barents Sea Sbelf reflects a similar palaeobasin development and is correlative to that of Svalbard. The lithological succession known from the wells of the southern Barents Sea Shelf admits the application of the lithostratigraphic group names fiom Svalbard, with Bjrrrmnrya in an intermediate position.

However, the thick development of late Sakmarian - Artin- skian strata with cold-water carbonate facies associations on the southern Barents Sea Shelf contrasts with Svalbard. This is why a new group, the Bjarmeland Group, is established there, coMprising three formations. A relatively thin, ?late Artinskian wedge of this group is recognised on Bjsrnarya and assigned to it as an individual formation, lateral equivalent to the upper part of the Bjarmeland Group on the southern Barents .Sea Shelf (see Chapter 2.5.1).

2.5 Regional description

2.5.1 LowerJmiddle Carboniferous of Bjerneya pig. 2-05)

Bjsrnarya (Bear Island), situated half-way between Svalbard and the mainland of Norway, provides a local exposure of the Famennian to Triassic stratigraphy of the Barents Sea Shelf margin. Early Permian faulting and westward tilting of the West Bjsrmya Trough (Fig. 2-02) resulted in westward younging exposures of Fame& to earliest Permian formations, while the two youngest formations of Artin- skian to Ufimian age unconformably overlie the tilted older ones (Horn & OrYin 1928).

Although most of the individual formations of Bjrrrmnrya can be correlated with contemporaneous units on Spits- bergen, the nomenclature has developed independently (Andersson 1900; Horn & k i n 1928; Cutbill & Challinor 1965; Krasil' SEikov & LivSic 1974; Worsley & Edwards 1976). Considering the distance from Spitsbergen, the poorly known stratigraphy between the two islands, and distinct lithological differences in parts of the succession, there are sufficient reasons to keep separate formation names for Bjrrrmnrya, but apply group names from Spitsbergen as proposed by Cutbill & Challinor (1965). No subgroup names are applied to Bjmnaya because of insufficient knowledge of lateral extent and possible correlations of trough and platform facies regimes.

The original subdivisions of Andersson (1900), adopted by Horn & Orvin (1928), have essentially been maintained by all subsequent authors. Names for the lowermost two formations were proposed by Cutbill & Challinor (1965), and for the other formations by Krasil'SEikov & L s i c (1974). Worsley & Edwards (1976) defined these formations formally, though using different names for three of them (Fig. 2-03).

The difficult communication between Russian and West- ern geologists at that time resulted in a situation where both name sets have to be regarded as contemporaneously developed, and no priority principle can be applied, in spite of apparently different years of publication. Both name sets are well-established in the geological literature of the respective countries. %o of the formations (Kapp KArer'Kobbebukta" and Miseryfjel1etP"'aksvatnet" formations) are undoubtedly better exposed at the localities indicated by Worsley & Edward's names, while the third formation (Hamberg- fjellet~Alfiedtjellet" Formation) is well exposed in both name-giving localities. It is recommended to use the nomenclature of Worsley & Edwards (1976) in order to keep one frequently used set of names together rather than constructing an artificial compromise.

The nomenclature recommended herein consists of the clastic R0edvika and Nordkapp formations (Cutbill & Challinor 1965) in the Billefjorden Group, while the following formations are assigned to the Gipsdalen Group: Landnsrdingsvika (Krasil'bEikov & LivSic; Worsley & Edwards), Kapp Krfre (Worsley & Edwards), Kapp Hanna (Krasil7SCikov & LivSic; Worsley & Edwards) and Kapp Dun& (KrasilYbEikov & Livbic; Worsley & Edwards). The Bjarmeland Group is represented by its only onshore unit, the Hambedellet Formation (Worsley & Edwards 1976). The Tempelfjorden Group is represented by the Misery- fjellet Formation (Worsley & Edwards).

2.5.2 Lower/middle Carboniferous of the Surkapp-Horn- sund High pig. 2-06)

The Sorkapp-Homund High (Steel & Worsley 1984) occu- pies most of the western and southern parts of Sarrkapp Land on southern Spitsbergen (Figs. 1-05,2-02). The Lower Carboniferous Billefjorden Group was probably deposited across large parts of the area, then removed by subsequent uplift in central and eastern parts (Gjelberg 1987; Dalhnann 1992), and is now preserved in its northwestern areas. It consists of the Hornsundneset Formation and the overlying Sergeijevfjellet Formation (Siedlecki 1960).

The Smkapp-Hornsund High acted as a topographical high and a sediment source for the adjacent troughs fiom the Bashkirian through the Permkm into the early Triassic. To our present knowledge, neither Gipsdalen nor TempeJ- fjorden Group sediments were ever deposited on the high itself.

In the basinal area to the southwest of the high, thick deposits of the Artinskian to Upper Pennian Tempelfjorden Group, the Tokross0yu Formation (Siedlecki 1964), occur on the islands of Smkapparya and Tokrossarya and on the peninsula 0yrlandsodden. Underlying rocks are poorly exposed and possibly constitute an extension of the Bille-

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fjorden Group sediments from the Smkapp-Hornsund High (Dallmann et al. 1993).

2.5.3 Lowedmiddle Carboniferous of the Inner Hornsund Trough and adjacent areas (Figs. 2-06,2-07)

The Inner Hornsund Trough (Gjelberg & Steel 1981; Steel & Worsley 1984) stretches from eastern Smhpp Land across the inner part of Homuqd northwestward into Wedel Jarlsberg Land (Figs. 1-05,2-02). Its northwestward contin- uation is unknown, because Late-Cretaceous and Tertiary basement uplift removed the record. Its northeastern limit is buried below Mesozoic and Tertiary strata. The trough is bound by the Smkapp-Hornsund High (Steel & Worsley 1984) to the southwest.

Carboniferous sediments were deposited aver an erosional unconformity on Caledonian basement, and, in western parts of the trough, on Devonian rocks preserved within the Samarinbreen Syncline (Dallmann 1992).

Billefjorden Group strata occur both in the Inner Horn- sund Trough and in western parts of the SIsrkapp-Hornsund High. The lower formation, the Adriabukta Formation (Birkenmajer & Turnau 1962) is confined to the trough. The overlying Hornsundneset Formation (Siedlecki 1960) may have been deposited continuously across the Smkapp-Horn- sund High and the Inner Hornsund Trough. Thin remnants of the Sergeijevjellet Formation have also been reported from the trough (Gjelberg 1984).

A problem related to the Adriabukta Formation is its pos- tulated Tournaisian to Visban age that totally depends on the correctness of palynomorph age determination of only two samples (Birkenmajer & %mau 1962). This dating also has critical tectonic implications, as the local Adriabukta folding event thus cannot be correlated with the Svalbardian foldmg. The grouping of the Adriabukta Formation within the Billefjorden Group must remain tentative until further biostratigraphic results are obtained.

Gipsdalen Group strata are confined to the Inner Horn- sund Trough and are exposed along a segment of the Ter- tiary fold-and-thrust belt. They are subdivided into the lower HymeJellet Formation and the upper Treskelodden Formation (Birkenmajer 1959,1964); these probably extend from the Bashkirian to the Asselian or Sakmarian and thus overlap in time with the other subgroups of the Gipsdalen Group. These two formations constitute the Treskelen Sub- group.

The above formations have not been redefined since their first description, though some of them have been extended into the Bellsund area after regional mapping (Dallmann et al. 1993; Ohta & Dallmann 1994). Units previously defined in areas north of Homund ("Reinodden Formation", Orvin 1940; "Drevbreen beds", Nysaether 1977) are correlated with the Treskelodden Formation and these names are recommended to be dropped in favour of the established and well-described stratigraphic nomenclature system which was established in the Homund area.

Thin fossiliferous limestone horizons overlying the Treskelodden Formation may be correlatives of the Wordie- kammen Formation and, on Kopernikusfjellet, the Gips- huken Formation.

The Kapp Stamstin Formation of the Tempelfjorden Group forms a few metres thin horizon in the Inner Horn- sund Trough, probably wedging out against the Serrkapp- Homund High.

2.5.4 Lower/middle Carboniferous of the St. Jonsflorden Trough and adjacent areas (Fig. 2-08)

The Early Carboniferous predecessor to the St. Jonsfjorden Trough was situated in north-central Spitsbergen, to the west of the line Kongsfjorden-Nordfjorden, the approximate onlap area of trough sediments on the western side of the Nordfjorden Block (Figs. 1-05, 2-02). To the south, the Early Carboniferous basin reached the Bellsund area (Steel & Worsley 1984).

The Billefjorden Group rests unconformabiy on folded and eroded Caledonian basement, though remains of De- vonian sediments occur locally and may underlie the Car- boniferous. Billefjorden Group strata of this basin have been referred to the monotonous, sandstone-dominated Orustdalen Formation (Cutbill & Challinor 1965) and the overlying, more heterogeneous, clastic "Vegard Formation" (Dineley 1958). The latter should be changed into the complete name Vegardjella Formation. The "Trygghamna For- mation" (Dineley 1958), a local name from the northern coast of Isfjorden, is equivalent to the Orustdalen h m a - tion. It has not been established in the geolugical literature for the benefit of the name Orustdalen Formation. In spite of the priority rule, we recommend use of the much better established name in order to avoid unnecessiry confusion.

Bashkirian-Moscovian sedimentation was confined to a narrow trough to the southwest of the Nordfjorden High, now exposed mainly in the inner part of St. Jonsfjorden and on Broggerhalverya. The conglomerate facies of the trough sediments that occur on Brrggerhalvoya are assigned to the Breggertinden Formation (Orvin 1934) of Bashkirian to ?Moscovian age. The shale-dominated Petrellskaret Forma- tion and the red sandstone-dominated Tdrnkanten Forma- tion (Dineley 1958) probably form, at least in part, the age equivalents of the Bmggertinden Formation in the St. Jons- fjorden area. The upper, transitional part of the trough sediments on Brerggerhalvoya, the Schetelidellet Fmation (Gobbett 1963: Scheteligfjellet beds) of Moscovian age was previously defined as a member of the "Nordenskioldbreen Formation" (Cutbill & Challinor 1965) and is here raised to formation rank in accordance with similar strata in the Billefjorden Trough. Upper parts of the Thkanten Forma- tion (Juhlslottet member) may be laterally equivalent to the Scheteligfjellet Formation. The Tihkanten and Schetelig- fjellet formations conclude the trough sedimentation to the west of the Nordfjorden Block. Together with the underlying Bashkirian and Moscovian clastic formations, they constitute the Charlesbreen Subgroup, defining the sedimentary fill of the St. Jonsfjorden Trough.

The platform deposits of the Dickson Land Subgroup (Wordiekammen and Gipshuken formations) and the Tempelfjorden Group (Kapp Starostn Formation) overlie the fill of the St. Jonsfjorden Trough (see section 2.5.7).

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- - .. - . - - . - . -- - - - - - - .- -

Palanded~ukta member i

-- -i D -i 3

7 . . . . . . . " . - . 3ickson Land Subgroup 7 . - ' - -. . V

X ' . carisdalen ftIc3mber Templet mem - - - - - - -- . , - - - - - - - -

Vengeoe gel rnemoer Ze pe wden member - - - --

hnlqqnlet sods

reliable data can documant the diachronism. The indicated major hiati are also h whematically and do not olaim any preciai.011 coaeernjag their age range. Minot hiati are omitted. Vertical lines between formations may represent interfiierhg mlationshijm

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2.5.5 Lawer/middle Carboniferous of the Billeflorden lhugh and Nordflorden High (Fig. 2-09)

The Billefjorden Trough, situated to the east of the Nordfjor- den High, trends in a north-south direction along Wijdefjor- den, Austfjorden and Billefjorden, and subcrops below younger cover strata in the inner Isfjorden area (Figs. 1-05,2- 02). It formed a syndepositional trough Erom the Famennian to the Moscovian (Steel & Worsley 1984). V i s h strata overlap the western trough margin (at least in the south) and the eastem margin. Sedimentation was largely confined to axial areas of the half-graben during the Bashkirian, but the eastern basin margin was progressively onlapped during the Moscovian.

On the Nordfjorden High, Carboniferous sediments were deposited on Devonian rocks, while the Devonian had been completely eroded in the trough, exposing Caledonian folded basement prior to the onset of Carboniferous sedimentation. Consequently, both the Nordfjorden High and the Billefjorden Trough are inverted structures, due to tectonic movements along the Billefjorden Fault Zone during the Latest Devonian Svalbardian tectonic phase. The eastern crest of the Nordfjorden High formed the uplifted footwall of the Billefjorden Fault Zone during the Carboniferous movements; this crestal area was the longest emergent, at least until the latest Moscovian.

The Billefjorden Group within the Billefjorden Trough comprises the Hmbyebreen Formation and the Mumien For- mation (see section 2.3.1).

Bashkirian to Moscovian trough sediments of the Gips- dalen Group (Campbellryggen Subgroup) comprise the clastic redbeds -of the Hultberget Formation (see section 2.2), the mixed clastic, carbonate and evaporitic Ebbadalen Formation (Cutbill & Challinor 1965) and Minkinjellet Formation (Cutbill & Challinor 1965), the latter being ex- cluded from the platform-type 'Wordenskioldbreen Forma- tion" and raised to formation rank due to its association with the Billefjorden Trough (see section 2.3.2).

The platform deposits of the Dickson Land Subgroup (Wordiekammen and Gipshuken formations) and the Tempelfjorden Group (Kapp Stamstin Formation) overlie both the Billefjorden Trough and the Nordfjorden High (see section 2.5.7).

2.5.6 Lowedmiddle Carbonifrous of northeastern Svalbard (Fig. 2-1 0)

On eastern Spitsbergen and Nordaustlandet, the Upper Palaeozoic succession is less investigated than in other areas and several correlations must remain highly tentative.

Billefjorden Group sediments are only reported from the Lomfjorden area and have been assigned to the redbeds of the "Svenbreen Formation" (Cutbill 1968; see section 2.2). Recent investigations might restrict this occurrence to the west of the Lomfjorden Fault (S.G. Bergh, pers. comm. 1994). No formation name should be applied to this occurrence until more stratigraphic work is done. Correlations with the Hultberget Formation (Billefjorden Trough), Malte Brunfjellet Formation or Hilrbardbreen Formation (Nord- austlandet) may turn out to be possible.

Clastic redbed deposits assigned to the Gipsdalen Group are found in several isolated places on the Ny Friesland High in Olav V Land (Olaussen et al. 1986, unpubl. report, Statoil; Miloslavskij et al. 1998). Due to the lack of reliable correlations, the independent name Malte Brunjellet For- mation is proposed here.

On Nordaustlandet, the probably Bashkirian andor Moscovian clastic Hdrbardbreen Formation (previous member of the Gipshuken Formation [Cutbill & Challinor 19651 and Nordenskiildbreen Formation [Lauritzen 19811) is proposed for formational rank on a level with the coeval clastic and transitional trough successions of Spitsbergen.

Occurrences of a similar redbed unit in the Hinlopen- stretetLomfjorden area have been described by Cutbill (1968) and Skarpnes (1984, unpubl.). Farther documentation is needed to verifjl a possible correlation with the Malte Brunfjellet a d o r Hkbardbreen Formation. .

Because of the lack of sufficient lcnowledge of the depositional regimes in north-eastern Svalbard, no subgroups should be assigned to these clastic deposits of the Gipsdalen Group east of the Billefjorden Trough.

Overlying platform deposits of the Wordiekammen and Gipshuken formations (Dickson Land Subgroup of Gips- dalen Group) and the Kapp Starostin Formation (Tempel- fjorden Group) are present over the whole area (Burov et al. 1965; Cutbill 1968; Lowell 1968; Lauritzen 1981; Keilh 1992).

2.5.7 Upper Carboniferous and Permian plrrtform of Svalbard (Figs. 2-06,Z-Oz2-08,2-09,2-10)

By the latest Moscovidearliest Kasimovian, most of Sval- bard (apart from the Inner Hornsund Trough and Smkapp- Homsund High) formed a carbonate shelf with little differentiation between earlier troughs and intermediate platform areas. These deposits comprise the Wordiekemmen Forma- tion (Late Moscovian to Sakmarian; see section 2.3.2) and the Gipshuken Formation (Mid to Late Sakmarian, ?earliest Artinskian; Cutbill & Challinor 1965). These shelf deposits are gathered in the Dickson Land Subgroup.

After an Artinskian hiatus, shelf sedimentation was dominated by the bioclastic limestones and siliceous to carbonate, spiculitic lithologies of the Tempelfjorden Group, the Kapp Stamstin Formation (Cutbill & Challinor 1965). Tempelfjorden Group strata are thought to have been deposited across all of Svalbard except for the Smkapp-Horn- sund High.

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Ng. 2-05

1 type sectton - CP-18 (ID-No.)

Fig. 2-05 DktrWion map GP-I: Upper Palaeozoic of E4j-a (incl. Triassic) Fig. 2 4 6 (p. 3): DiPMbution map GP-E[: Upper Pabomic of the Sdapp-Hommmd area (Southern Spitsbergen) R& 247 @37): DkWutim map CP-EL Upper P&e~z~ic ofthe T o d bud and BellsMd-Isij&h areas (southwestem Spitdmgen). R& 248 (p. 38): Ihtrhtion map GP-IW Upper PWzoic of 0- II Land (Central western Spits-). Fig. 209 (p. 39): D i m map CP-V Upper Paiaeozoic of W c h Land and B i b a v Land (Central Spitsben). Fig. 2-18 (p. 40): DbtdWanmsp CP-VI: Upper P h z o i c of northeastem SvaibPrd

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'ertlary cover rocks

Mesozoic cover rocks

a Glpshuken Fm.

B Wordiekammen Fm.

Treskelodden Fm.

Hyrnefjellet Formation

Group

Dre-Old Red basement

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Kapp Starostin Frn.

GUpshuken Formation

/ Pre-Old Red basement

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;i

SCALE 1:4W O W

5 10 15 kn

- C 0 " type section - CP-27 (ID-NO.)

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2. UPPER PACAEOZOIC LITHOSTRATIGRAPHY

Fig. 2-10

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2.6 Lexicon of lithostratigraphic units

2.6.1 Billefiorden Group

BILLEFJORDEN GROUP (GP-01)

Billefjorden

Fig. 2-12: Typical sediments of the Billefjorden Group at Billefjorden, representing delta plain and overbank deposits. Photo: E.P. Johan- 4 nesen

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): "Culm sandstones": ~at6orst 19 10 ORIGIN OF NAME: Billefjorden: A fiord in central Spits- bergen, a bifurcation of Isfjorden TYPE AREA: Area between Billefjorden and Austfjorden, Dickson Land, central Spitsbergen STRUCTURAL SETTING: Late Palaeozoic platform of Sval- bard and the Barents Sea Shelf; in Svalbard widely preserved in middle Carboniferous troughs DEPOSITIONAL AGE: Famennian - Vis6an OVERLYING m ( s ) : Gipsdalen Group; locally on Smkapp- Hornsund High: Sassendalen Group UNDERLYING UNIT@): AndrBe Land Group (Devonian), Pre-

THICKNESS: Up to 2500 m (cumulative) MAm LITHOLOGIES: Sandstone, shale, conglomerate DESCRIPTION: Clastic sediments with local coal seams, bound to a number of tectonic depressions developed subsequent to the deposition of Old Red sediments. The group comprises the Hmbyebreen and Mumien formations of the Billefjorden-Ny Friesland area, the Orustdalen and Vegard- fjella formations of western Spitsbergen, the Adriabukta, Hornsundneset and Sergeijevfjellet formations of the S0rkappHomund area, the Rnredvika and Nordkapp formations of Bj-a and timelfacies equivalents of the Barents Sea Shelf.

, , ' ' , > I I ,

Old Red SUPERIOR UNIT: None OTHER USE OF NAME: Billefjorden Fault Zone (Harland et I al. 1974) Billefjorden Trough (Gjelberg & Steel 1981)

DISTRIBUTION SHOWN ON RIG@).: 2-09 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill et al. 1976 SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Hsrbyebreen: A glacier tongue endmg in the inner part of Billefjorden, central Spitsbergen TYPE SECTION (FIG. 2-15): Stratotype: Ferdinandbreen, Dickson Land . . _ . C ,

Fig. 2-11: A fault Mock with Devonian and unconformably werfying STRUCTURAL SETTING: Early Carboniferous basin h central Carboniferous strata (left) displaced against Devonian (right) at Tri- and northern Spitsbergen, plunging southward below ungen (northwe&m Dickson Land). Carboniferous strata include younger strata; mainly preserved in the middle Cfubon,ifer- Hnrrbyebreen and Mumien formations (light and grey), Hultberget O ~ S Billefjorden Trough cm.; . J ;

I "

Formation (upper red band) and Wordiekarnmen Formation (upper- DEPOSITIONAL AGE: Famennian - Vis6an . - most cliff), Photo: W.K. Dahann DATING METHOD: Palyll010gy

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Fig. 2-13: The Russian coal mining settlement Pyramiden (recently abandoned) with transportation facilities to the mine in the mountain side. The coal seams occur in the kbyebreen and Mumien formations in a fault block displaced against the strata in the mountain Pyrarniden (background). The mountain side shows the Ebbadalen Formation with the red-coloured conglomerates of the Odellfjellet Member, overlying sandstones of the M-ellet Formation, and limestones of the Wordiekammen Formation (uppermost cliff). Photo: J. Nagy

REFERENCE(S) FOR AGE: Playford 1962, 1963; Nsttvedt et al. 1992; Vigran 1994 (unpubl.) OVERLMNG -S): Mumien Formation UNDERLYING m(sj: An&& Land Group, Pre-Old Red SUPERIOR m: Billefjorden Group OTHER USE OF NAME: None THICKNESS: Up $0 200 m, >l40 m in stratotype M.m LITHOLOGIES: Sandstone, conglomerate, coal LOWER B O ~ A R Y D E ~ I O N : Angular unconfonnity, with greyish sandstones or conglomerates overlying folded basement strata or folded or tilted sediments of the Devonian Wood Bay or Mimerdalen formations DESCRIPTION: The Hmbyebreen Formation occurs between Dicksonfjorden and Nordenskiiildbreen, with good expo- m e s in the Billefjorden Trough between Billefjorden and

Fig. 2-14: Sigillaria stem# are common in the deposits of the Billeijorden Group; here at Ix,msWmfjellet (southwestern Ny Friesland). Photo: W.K. Dallmann

grain size approximate

v m - clslvf f mcvcg pcbb

Fig. 2-15: Stratigraphic section CP-02/04 Shatotype for: kbyebreen Formation, Hoelbreen Member Locality: Ferdinandbreen (Mumien NE) Refmnce: Gjelborg, XG. (unpubl.)

Ausaorden. The formation is also present in Ny Friesland fonning a few down-faulted (wtlitxs along &a gin of the Ny Friesbd Black.

~ h e l o t v e r p a r t o f t h e f b n m t t h ~

the east. It consists of can&tmm and conglmerates of fluvial origin, with in- h t r i n e and flaod-basbj shales. <

The upper part ofthe ( H o e l b m- sists mainly af MacWgrey shales and mudstones, htefbed- ded with thin sandstones, coaIsl) coaly shales and hoeons of clay irmtones, q m e n t h g flood plain to flood basin deposits (Fig. 2 12). Sigilhm &ems accur Ereqwntly @g. 2-14). I

Palynological studies indicate that there is a stratigraphic break between the Trimgen and the Hoelbreea Member (I? van Veen, pm. comm. 1989; Nsttvedt et al. 1992). Ac- cording to Playford (1962, 1963) two different assemblages

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2. UPPER ,PACAEOZQlt LITHQSTRATIGRAPHY p - p p

- p p

Fig. 2-16: Gravel- stones and cross- bedded sandstones in the basal part of the Triungen Member on h e n (Dickson Land). Photo: W.K. Dallmann

Triungen Fault (McCann & Dallmann 1996) THICKNESS: 130 m in stratotype lMAIN LITHOLOGIES: Sandstone, conglomerate, shale -R BOUNDARY DEFINITION: See Hsrbyebreen Forma- tion DESCRIPTION: The Triungen Member consists mainly of grey sandstones and conglomerates (Figs. 2-16, 2-17). There are, however, some thick units of greylgreyish purple shale, interbedded with thin sandstones, in the type section at Triungen. It is also reported that fine-grained sediments

of palynomorphs are present within the formation. The transition between the two assemblages occurs within the Hoel- breen Mb. and is not marked by lithological changes (Cut- bill et al. 1976).

Triungen Member (CP-03)

STATUS OF UNIT: F0IVld FIRST USE OF NAME: CutbilI & Challinor 1965 CURRENT DEFINITION: Cutbill et d. 1976 SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Triungen (Norw. from "Mt. Triplex"): A mountain in NW Dickson Land TYPE SECTION (FIG. 2-18): Stratotype: Triungen West, Dickson Land DEPOSITIONAL AGE: Famennian DATING METHOD: PdyIl010g~ REFERENCE(S) FORAGE: Playford 1962,1963; Kaiser 1970, 197 1; Vigran 1994 (unpubl.); Veen, P. van (unpubl. data) OVERLY~G UNIT(S): Hoelbreen Member UNDERLYING UNIT(S): AndrBe Land Group, Pre-Old Red SUPERIOR UNIT: Hsrbyebreen Formation OTHER USE OF NAME: Triungen-Grmhorgdalen Fault Zone

1111- l Pm- Old Red

AS- ih IS- R\

I Basement-

units

1 l vm - cls~vf f mcvcg pcbb Fig. 2-17: A U M fa &posits with reworked, light sandstone in the

Triungen Member on FmfjeIlet (Dickson Land). Photo: E.F! Fig. 2-18: Stratigraphic section CP-03 Stratotype for: Triungen

Johannessen Itember Locality: Triungen W Reference: Gjelberg, J.G. (G~ubl.)

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are relatively common at other localities, though poorly exposed. The member probably represents fluvial and lacustrine depositional environments.

Palynological material studied by Playford (1962, 1963), and reinterpreted by P. van Veen (unpubl.) and Vigran 1994 (unpubl.), suggests an upper Devonian (Farnennian) age of the member, corresponding in age with the Rnredvika Fm. on Bjnrmsya (based on comparisons with studies by Kaiser 1970, 1971 on Bjlmaaya). There may be a stratigraphic break between the Trimgen Member and the overlying Hoelbreen Member of Tournaisian age (P. van Veen, pers. comm. 1996; Vigran, 1994, unpubl.).

Hoelbreen Member (CP-04)

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill et al. 1976 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Hoelbreen: A glacier in Dickson Land, NW of Billefjorden TYPE SECTION (FIG. 2-15): Stratotype: Ferdinandbreen, Dickson Land The stratotype was originally defined at the northwestern slope of Birger Johnsonfjellet (Cutbill & Challinor 1965), but no documentation is available. DEPOSITIONAL AGE: Tournaisian - Vi~6an DATING METHOD: Palynology REFERENCE(S) FOR AGE: Playford 1962, 1963; Nsttvedt et al. 1992; Vigran -1994 (unpubl.) OVERLYING UNIT@): Mumien Formation UNDERLYING =(S): Triungen Member SUPERIOR UNIT: Hnrbyebreen Formation O T ~ R USE OF NAME: None THICKNESS: Up to 150 m, 110 m in stratotype MAIN LITHOLOGIES: Shale, sandstone, coal LOWER BOUNDARY DEFINITION: The lower boundary is defined at the onset of a shale-dominated succession above the sandstones of the Triungen Member. DESCRIPTION: The Hoelbreen Member consists generally of black to grey shales and mudstones with thinly interbedded ripple-laminated sandstones, coals and clay ironstones (siderite). Interbedded thin sandstones (2-50 cm) and thin mudstones are common lithological associations and may form up to several metre thick units. Only a few prominent sandstone units (3-5m thick) occur within the member. These sandstones represent fluvial channels. Coal seams occur at several levels; the thickest seams are located in the uppermost part of the member in the Pyramiden area. The member reflects deposition on flood plains and in flood basins with associated meandering and ribbon channels.

Coal from the Hoelbreen Member is mined at the Russian mining community of Pyramiden (Fig. 2-13). The mine is situated in a narrow tectonic block between two strands of the Billefjorden Fault Zone, in the mountains Pyramiden and Mumien.

DISTRIBUTION SHOWN ON FIG@).: 2-09 STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): The Mumien Formation comprises most of the "Svenbreen Formation" (Cutbill & Challinor 1965), though excluding the "Hultberget Mem- ber". ORIGIN OF NAME: Mumien (transl. "The Mummy"): A mountain in northeastern Dickson Land TYPE SECTION (FIG. 2-19): Stratotype: Northern slope of Birger Johnsonfjellet, Dick- son Land STRUCTURAL SETTING: Early Carboniferous basin in central and northern Spitsbergen, plunging southward below younger strata; mainly preserved in the middle Carbonifer- ous Billefjorden Trough DEPOSITIONAL AGE: VisBan DATING METHOD: Palynology REFERENCE(S) FOR AGE: Nllttvedt et al. 1992; Vigran 1994 (unpubl.); Veen, P. van (unpubl.) OVERLYING UNIT@): Hultberget Formation; locally in the Billefjorden Fault Zone: Ebbadalen Formation, Wordie- kammen Formation UNDERLYING UNIT@): Hmbyebreen Formation; Pre-Old Red SUPERIOR UNIT: Billefjorden Group OTHER USE OF NAME: None THICKNESS: Up to 100 m, 95 m in stratotype MAIN LITHOLOGIES: Sandstone, shale, coal LOWER BOUNDARY DEFINITION: The base of the formation is defined at the base of the prominent sandstones of the Sporebgda Member (see below), which overlie various lithologies of the Hoelbreen Member. The boundary is easy to recognise within the Billefjorden Fault Zone. It is less distinct on the eastern side of Austfjorden and in central Dickson Land, where the sandstones of the Sporebgda Mb. are less prominent and frequently interbedded with shales.

Cutbill and Challinor (1965) discussed the boundary between the Herrbyebreen Formation and the overlying Spore- bgda Member and suggested that it represents a slight angular unconformity. Palaeocurrent studies indicate a possible change at this boundary from a northern to a southern drainage direction (Aakvik 198 1; Gjelberg 1984), sup- porting the assumption of an unconformity between the HBIbyebreen and Mumien formations. There is, however, no palaeontological or palynological evidence for an unconfor-

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red

- 8 '7 m u n b ddvf f mcvcg pcbb

Fig. 2-19: Stratigraphic section CP-05/06/07 Smtotype for: Mumien Fonnation, Sporebgda and Birger Johnson-

fjellet members Locality: Birger Johnsonfjellet N Reference: Gjelberg 1984 (unpubl.)

mity that might involve a detectable period of non-deposition or erosion (Playford 1962,1963; Vigran 1994, unpubl.). Available palaeocurrent data consist of very few measurements and may be statistically insigmficant. DESCRIPTION: The Mumien Formation consists of a lower, relatively thick sandstone interval and alternating black and grey shales and coals in the upper part. It is divided into two members, the Sporebgda Member and the Birger Johnson- fjellet Member.

The Sporebgda Member comprises the sandstone-dominated lower part of the formation. The overlying prominent coal-bearing shales are defined as the Birger Johnsonfjellet Member. The formation onlaps Pre-Old Red eastwards on the Ny Friesland Block. The sandstones of the Sporebgda Member represent fluvial channel deposits with braided or meandering streams (Aakvik 1981, unpubl.; Gjelberg 1984, unpubl.). The Birger Johnsonfjellet Member reflects a lacustrine/flood basin depositional environment.

Most of the coal seams are cannel coals rich in Botry- ococcus algae. The coals are derived from a sapropelic lacustrine environment (Abdullah et al. 1988). Coals are mined at the Russian mining community of -den (see Harbyebreen Formation).

Sporehagda Member (CP-06)

STATUS OF UNIT: Formal FIRST USE OF NAME: CUtba & chdh01: 1965 CURRENT DEFINITION: Cutbill et al. 1976 SYNONYM(S) AND REFERENCE(5): None ORIGIN m NAME: Spodmgda (transl. "The Spur Hill"): A mountain in northem Biinsm Land TYPE SECTION (FIG. 2-19): Stratotype: Ferdinandbreen, Dickson Land DEPOSIT~ONAL AGE: ~ s ~ U

DATING METHOD: Palynology REFERENCE(S) FOR AGE: Nsttvedt et al. 1992; Vigran 1994 (unpubl.); Veen, F! van (unpubl.) OVERLYING UNIT@): Birger Johnsonfjellet Mb. UNDERLYING UNIT@): Hoelbreen Member; Pre-Old Red SUPERIOR UNIT: Mumien Formation OTHER USE OF NAME: None THICKNESS: Up to 90 m, 45 m in stratotype MAIN LITHOLOGIES: Sandstone, shale LOWER BOUNDARY DEFINITION: See Mumien Formation DESCRIPTION: The Sporebgda Member contains several superimposed, metre- to ten-metre-scale, trdugh cross-stratified sandstone units. Individual units show slight grada- tion, and are often bounded by curved erosion surfaces. Several metres thick units of fine-grained material are preserved between sandstone sequences, especially in the northern part of the area. Plant fossils, mainly preserved as carbonaceous films and trunk casts or trunk impressions are common.

The member represents mainly braided stream deposits (Gjelberg & Steel 198 1; Aakvik 198 1, unpubl.).

The member is 30-40 m thick along the Billefjorden Fault Zone west of Petuniabukta, but increases to more than 90 m northwards to Lemstrrmfjellet. It pinches out eastwards above Pre-Old Red rocks on the Ny Friesland Platform.

Birger Johnsonfjellet Member (CP-07)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here; after Gjelberg 1984 (unpubl.) CURRENT DEFINITION: Here; after Gjelberg 1984 (unpubl.) SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Birger Johnsonfjellet: A mountain in NE Dickson Land TYPE SECTION (FIG. 2-19): Stratotype: Birger Johnsonfjellet, Dickson Land DEPOSITIONAL AGE: Vi~kan DATING METHOD: Pdp0lgy REFERENCE(S) FOR AGE: Playford 1962, 1963; Nsttvedt et al. 1992; Vigran 1994 (unpubl.); Veen, F! van (unpubl.) OVERLYING UNIT(S): Hultberget Formation; in easternmost

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exposures: Mmkinfjellet Formation; locally in the Bille- fjorden Fault Zone: Ebbadalen Formation, Wordiekammen Formation UNDERLYING UNIT(S): Sporebgda Member SUPERIOR UNIT: Mumien Formation OTHER USE OF NAME: None THICKNESS: Up to 55 m, 51 m in stratotype MAIN L ~ O L O G I E S : Shale, siltstone, coal LOWER BOUNDARY DEFINITION: The lower boundary is defined where a shale-dominated succession overlies the sandstones of the Sporebgda Member. DESCRIPTION: The Birger Johnsonfjellet Member consists mainly of blackfgrey shales, coaly shales and dark grey claystones, interbedded with thin siltstones (siderite bands) and coal. Plant root horizons are common, especially in the lower part of the member. Most of the coal seams are made up of algal material (Botryococcus) and may represent good source rocks for oil and gas (Abdullah et al. 1988). The member represents mainly flood-basin and lake deposits and becomes more flood-plain dominated eastwards.

The member is 50 m thick on Birger Johnsonfjellet and 55 m at the west side of Elsabreen. It seems to be restricted to the area around the Billefjorden Fault Zone in the Dickson Land area.

ORUSTDALEN FORMATION (CP-OS)

DISTRIBUTION SHOWN ON FIG(s).: 2-07,2-08 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Orustdalen: A valley in western Norden- skiold Land, Western Spitsbergen TYPE SECTION (FIG. 2-21): The base of the section is not exposed. The previously defined stratotype at Orustdalen (Cutbill & Challinor 1965) is not logged. Hypostratotype: Diabasbukta, Bellsund Both sections are tectonically disturbed (Braathen & Bergh 1995). STRUCTURAL SETTING: Early Carboniferous basin in western Spitsbergen; connection with other coeval basins not documented DEPOSITIONAL AGE: ?Tournaisian - Viskan (?Serpukhovian) DATING METHOD: Palynology REFERENCE(S) FOR AGE: Cutbill & Challinor 1965; Fair- child 1982 OVERLYING UNIT(S): Braggertinden Formation, Vegardfjella

Formation, Treskelodden Formation UNDERLYING UNIT(S): Pre-Old Red SUPERIOR UNIT: Billefjorden Group OTHER USE OF NAME: None THICKNESS: Up to >700 m MAIN LITHOLOGIES: Sandstone, shale LOWER BOUNDARY DEFINITION: The lower boundary is an angular unconformity, with greyish sandstones, shales or conglomerates overlying folded Pre-Old Red basement. DESCRIPTION: The Orustdalen Formation is exposed in western Spitsbergen from Brsggerhalvnrya in the north to Hornsund in the south. The formation is mainly composed of a complex stack of fining-upward units of Merent scale and thickness (Gjelberg 1984, qubl .) . These units often start with cross-stratified Oplanar and trough) pebbly sandstones and conglomerates and terminate in relatively thin shales. The facies associations indicate a braided stream and flood-plain fines origin.

Gjelberg (1984, unpubl.) concluded that the Orustdalen Formation consists only of continental deposits in the central and southern parts of Spitsbergen. Marginal marine influence in the formation has been suggested by Fairchild (1982), who identified some tidal influence in sediments assigned to the Orustdalen Formation on Brsggerhalvnrya, and by Dallmann et al. (1990), who locally observed tidal bundles south of Bellsund (Fig. 2-20).

Fig. 2-20: Cross-bedded, light grey sandstones with tidal bundles occur frequently in the Orustdalen Formation, here at Bellsund. Photo: W.K. Dallmann

DISTRIBUTION SHOWN ON RG(s).: 2-07,2-08 STATUS OF UNIT: Formal FIRST USE OF NAME: Dineley 1958

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coaly shale

coaly shale

poorly exposed

coaly shale

coaly shale

clslvf f mcvog pcbb

Fig. 2-21: Stratigraphic section CP-08/09 Hypostmtotype for: Orustdalen and Vegardtjella formation? Localiv: Diabasbukta Reference: GjeIberg 1984 (unpubl.)

CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): "Vegard Sandstone For- mation", "Vegard Formation": The above mentioned authors did not use the complete place name. ORIGIN OF NAME: Vegardfjella: A mountain complex at St. Jonsfjorden, Oscar I1 Land, Western Spitsbergen TYPE SECTION (FIG. 2-21): The base of the section is not exposed. The suggested stratotype at Vegardfjella (Dineley 1958) is not logged. Cutbill & Challinor's (1965) revised type locality at Orustdalen is

Petrellskaret Formation

U)

0 W C

Ir,

LL m p:

Z " W

coaly shale

unrts clsivf f mcvcg pcbb

exposed

not documented. Until further documentation is provided, SKS does not decide which stratotype should be valid. Hypostratotype: Diabasbukta, Bellsund STRUCTURAL SETTING: Early Carbonifer~u~ basin h West- ern Spitsbergen; connection with other coeval basins not documented DEPOSITIONAL AGE: VisBan DATING METHOD: Palynology in adjacent units REFERENCE(S) FOR AGE: see Orustdalen Formation OVERLYING UNIT(S): Braggertinden Formation, Petrell- skaret Formation, Wordiekammen Formation UNDERLYING -(S): OTuStdalen Formation SUPERIOR UNIT: Billefjorden Group OTHER USE OF NAME: None THICKNESS: Up to >l50 m. The suggested type section of Dineley (1958) in Orustdalen was reported to be 358 m

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thick. This interval also includes the redbeds of the overlying Petrellskaret Formation (Cutbill & Challinor 1965). MAIN LITHOLOGIES: Mudstone, sandstone, coaly shale LOWER BOUNDARY DEFINITION: The base of the formation is defined where the thick sandstones of the Orustdalen For- mation transitionally grade upwards into the heterolithic, finer-grained sediments which dominate the Vegardfjella Formation. DESCRIPTION: The Vegardfjella Formation ("Vegard Sand- stone Formation") was first named by Dineley (1958), who described "thinly bedded, pinkish, quartzose sandstones and thin shales". It was redefined by Cutbill & Challinor (1965).

The formation consists mainly of greyldark grey shales, interstratified with grey sandstones. Some of the sandstone intervals are relatively thick, particularly in the St. Jons- fjorden area, where both fining- and coarsening-upward trends are present. In the Bellsund area (here defined as the type area), the formation consists mainly of rhythrmc alternations of thin sandstones and thin shales, representing thinly bedded turbidites (Gjelberg 1984, unpubl.). The uppermost part of the formation at Bellsund consists of a thick coarsening upward sandstone unit.

The formation represents mainly flood plain and lacustrine deposits in the St. Jonsfjorden area, and mainly lacustrine turbidites in the Bellsund area (Gjelberg 1984, unpubl.).

DISTIUBUTION SHOWN ON FIG(s).: 2-06 STATUS OF UNIT: Formal FIRST USE OF NAME: Birkenmajer & Turnau 1962; rank revised to 'formation' by Cutbill & Challinor (1 965) CURRENT DEFINITION: DaUmaDLl et al. 1993 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Adriabukta: A bay in the Hornsund fiord, southern Spitsbergen TYPE SECTION (FIG. 2-22): Stratotype: Adriabukta (coastal section), Hornsund STRUCTURAL SETTING: Early ~~tboniferous (?) basin in southern Spitsbergen, p-ed in Samarinbreen Syncline DEPOSITIONAL AGE: Vis& mdlor possibly older: The Early Carboniferous age is b a d on only two samplis with spore specimens of doubtful age-indicative value; a late Devonian age cannot be totally ruled out as yet. DATING METHOD: Palynology &FERENCE(S) FOR AGE: Birkenmajer & lhmau 1962

OVERLYING UNIT@): Hyrnefjellet Formation, Homund- neset Formation UNDERLYING UNIT(S): Marietoppen Formation, Pre-Old Red SUPERIOR UNIT: Billefjorden Group OTHER USE OF NAME: None THICKNESS: Up to 1750 m cumulative MAIN LITHOLOGIES: Shale, sandstone, conglomerate LOWER BOUNDARY DEFINITION: The lower boundary of the Adriabukta Formation in Smkapp Land is placed at a distinct erosional unconformity over Caledonian folded base-

l ? .

strongly deformed section

strongly deformed sectkn

l 1 1 1 1 1 1 1 1 1 1 d sivf f m cvo g pcbb

Fig. 2-22: Stratigraphic section CP-10/13 Stmtolype for: A&iab&a Formation, Merantjellet Member Locality: Adriabukta Reference: UjeIberg 1984 (mpubl.)

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ment. Its boundary with Devonian deposits is only exposed north of Hornsund, (Adriabukta) where it is apparently conformable. In the type section, the base is defined by an organic-rlch black shale which overlies multicoloured Devon- ian shales and sandstones. DESCRIPTION: The basal black shale (see above) is overlain by grey sandstones and conglomerates (Julbgda Member). Exceptionally, at the mountain Haitanna, thick conglomerates (Hrutama Member) form the base of the formation above crystalline basement. The upper part of the formation consists of a dark, shale-dominated succession (Meran- fjelld Member). The upper boundary is defined by the unconformity t m d s the overlying red conglomerates of the middle Carboniferous Hyrnefjellet Formation north of Homsund a . south of the fiord, by the tectonised boundary towards massive sandstones of the Homsundneset For- mation.

The formation occurs from the type area north of Horn- sund to Guilbaudtoppen in the south, mostly on the eastern flank of the Samasinbreen Syncline. Steel & Worsley (1984) mention an isolated exposure of possible Adriabukta For- mation lithologies at Van Keulenfjorden, south of Rein- odden, but there are no biostratigraphic data that would be needed to confirm this possible correlation.

The local appearance of the thick and very proximal deltaic or alluvial fan facies of the Haitama Member suggests that the assumed boundary fault of the sedimentary basin of the Adrhbukta Formation (Steel & Worsley 19&4) was active during sedimentation and is sifnabd close to Hai- tanna. TEme upward development fkom alluvial through deltaic to an increasisgly restricted basin facies, as well as the apparent gradual onlap towards the northwest suggest that the Adriabukta Formation represents the infii of a narrow graben or half-graben which was initiated by Svalbar- dian block tectonics. The Adriabukta Formation was folded prior to the middle Carboniferous (YAdriabukta event").

Haitanna Member (CP-11)

S ~ T U S OF UNIT: Formal FIRST USE OF NAME: Da&TWU 1992 CURRENT DEFINITION: Da&TWU et al. 1993 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Haitanna (transl. "The Shark Tooth"): A mountain in central Smkapp Land, southern Spitsbergen TYPE LOCALITY: Haitanna, Smkapp Land DEPOSITIONAL AGE: Viskan or older (see Adriabukta For- mation) DATING METHOD: Palynology in adjacent units REFERENCE@) FOR AGE: Birkenmajer & Turnau 1962 OVERLYING UNIT(S): Julhsgda Member U N D E R L ~ G m(s) : Pre-Old Red SUPERIOR UNIT: Adriabukta Formation OTHER USE OF NAME: None THICKNESS: ca. 450 m MAIN LITHOLOOIES: Conglomerate LOWER BOUNDARY DEFINITION: See Adriabukta Formation DESCRIPTION: The Haitanna Member forms the lower, conglomeratic part of the Adriabukta Formation, occurring only

Fig. 233: The o c m m m of thick alluvial fan congl-s of the H a i U Member is restricted to the mountain Haitmm ("The Shark Tooth"), central Smkapp Land Photo: W.K. Dallmann

l d y on the mountain Haitanna, where it constitutes the middle part of the massif and the summit (Fig. 2-23). It can be traced laterally for 2.3 km. It unconformably overlies ?Mid-Proterozoic garnet mica schists.

The conglomerates are texturally and compositionally immature and clast-supported, with up to metre-sized clasts derived from the underlymg basement. The member can be subdivided into several thick lobes of probable alluvial fan origin. I Y , , , # ,

- , L '

Jnlhugda Member (CP-12)

STATUS OF UNIT: Fo& FIRST USE OF m Dallmasln et al. 1993 CURRENT DEFINITION: Ddhl'WW et d. 1993 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: JuIhsgda (transl. "Christmas Peak"): A mountain at the Hornsund fiord in northern Smkapp Land, southern Spitsbergen TYPE LOCALITY: JulhergdaHaitanna, Ssrkapp Land DEPOSITIONAL AGE: Vis6an or older (see Adriabukta For- mation) DATING METHOD: Palynology REFERENCE(S) FOR AGE: Birkenmajer & TWMU 1962 OVERLYING UNIT(S): Meranfjellet Member UNDERLYING UNIT(S): Haitanna Member, Pre-Old Red SUPERIOR UNIT: Adriabukta Formation C ~ H E R USE OF NAME: None THICKNESS: Up to 700 m MAIN LITHOLOGIES: Sandstone, conglomerate LOWER BOUNDARY DEFINITION: Where situated above basement, see Adriabukta Formation. Where the Haitam M m - ber is present, the base of the Julhergda Member is defmed by the first dominance of sandstones above the Haitanna conglomerates. DESCRIPTION: The Julhergda Member forms the middle part of the Adriabukta Formation. It consbts mainly of sandstones with subordinate conglomemtes and shales.

Approx. 700 m thickness are exposed at Haitanna and Guilbaudtoppen, where it conformably overlies the Hai-

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Fig. 2-24: Sandstones of the Julhragda Member unconformably overlie Precambrian basement at Pinsetoppen (northern Ssrkapp Land). The sandstones occur in the lower part of the slope and dip slightly steeper than the slope towards the observer. Photo: W.K. Dallmann

tanna Member. At Julhprgda and Pinsetoppen it unconformably overlies folded, ?Middle Proterozoic basement and is still more than 100 m thick (Fig. 2-24), while only 40-50 m are preserved in Adriabukta (N of Hornsund). The composition of the sandstones is macroscopically identical with the matrix of the conglomerates of the other members.

The sandstones are characteristically light to dark grey weathering, dark grey, tight, medium- to fine-grained and often current or trough cross-stratified. They are texturally and compositionally immature with angular grains and abundant detrital micas. The conglomerate intercalations show a texture and composition similar to the Haitanna Member, but are only observed to be max. 1 m thick, polymict, and contain pebbles and boulders of basement lithologies, mostly quartzites, mica schists and marbles of the underlying basement. The matrix is coarse sand to grit. Plant imprints are common.

Meranfjellet Member (CP-13)

STATUS OF UNIT: Formal FIRST USE OF NAME: Dallmann et al. 1993 CURRENT DEFINITION: Dallmann et d . 1993 SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Merantjellet: A mountain near the Horn- sund fiord in northern Smkapp Land, southern Spitsbergen TYPE SECTION (FIG. 2-22): Stratotype: Adriabukta (coastal section), Hornsund DEPOSITIONAL AGE: VisBan or older (see Adriabukta For- mation) DATING METHOD: Palyn010gy REFERENCE(S) FOR AGE: Birkenmajer & Turnau 1962 OVERLYING UNIT@): Hyrnefjellet Formation, Hornsund- neset Formation UNDERLYING UNIT@): Julhragda Member SUPERIOR UNIT: Adriabukta Formation OTHER USE OF NAME: None THICKNESS: 300-600 m MAIN LITHOLOGIES: Shale, siltstone, sandstone

LOWER BOUNDARY DEFINITION: The lower boundary of the Meranfjellet Member is defined where a dark siltstone- and shale-dominated succession overlies dark, but light weathering quartzitic sandstones and coarse conglomerates of the Julhragda Member. DESCRIPTION: The Merantjellet Member consists of dark or silty shales and siltstones with subordinate sandstones and conglomerates, similar to those of the Julhsgda Member. The thickness is ca. 300 m in the type section at Adriabukta, but a more complete development (ca. 600 m) with a higher amount of sandstone intercalations has been observed at Meranfjellet. Due to intense folding and thrusting of the Meranfjellet exposures, the internal stratigraphic succession is uncertain, and the indicated thickness values are very rough.

The succession starts above dark, light weathering, quartzitic sandstone and coarse conglomerates or breccias of the Julhprgda Member in Adventpasset: 1. black shale (a few metres); 2. alternating silty shales, dark grey sandstones and thin, dark conglomerate and breccia (150-200 m); 3. dark to medium grey, platy sandstones alternating with subordinate silty shales (100-150 m); 4. dark silty shales (250-300 m). Plant imprints are common.

DISTRIBUTION SHOWN ON FIG@).: 2-06 STATUS OF UNIT: Formal FIRST USE OF NAME: Siedlecki 1960; rank revised to 'formation' by Cutbill & Challinor (1965) CURRENT DEFINITION: Birkenmajer 1979 SYNONYM(S) AND REFERENCE(S) "Homsundneset Beds": Siedlecki 1960 ORIGIN OF NAME: Hornsundneset (tran~l. "Horn Sound Point": The coastal plain forming the NW tip of Snrkapp Land (type area) TYPE SECTION (FIG. 2-25): Stratotype: Hohenlohefjellet, east of Hornsundneset, Snr- kapp -Land

The base of the formation is not exposed in this section, but in Andvika a little further to the NNE. STRUCTURAL SETTING: Early Carboniferous basin in southern Spitsbergen; connection with other coeval basins not documented DEPOS~T~ONAL AGE: Viskan DATING METHOD: Palp010gy REFERENCE(S) FOR AGE: Siedlecki & k a u 1964 OVERLYING UNIT@): Sergeijevfjellet Formation, Hyme- fjellet Formation. Vardebukta Formation

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UNDERLYING UNIT(S): Adriabukta Formation, Pre-Old Red SUPERIOR UNIT: Billefjorden Group O~IER USE OF NAME: None THICKNESS: 700-1 100 m, 370 m in stratotype MAIN LITHOLOGIES: Sandstone LOWER BOUNDARY DEFINITION: Angular unconformity either above folded rocks of the Pre-Old Red or above the dark shales of the Adriabukta Formation (?"Adriabukta event"). The base of the Hornsundneset formation in the Hornsundneset area is commonly defined by a thin quartz conglomerate. DESCRIPTION: The Hornsundneset Formation occurs in two different areas and structural regimes in Ssrkapp Land: (1) gently inclined, overlying the Caledonian basement in the Hornsundneset area, and (2) steeply inclined to overturned within the foldbelt between Bladegga and Gratinden. Other, minor occurrences are suggested underlying folded Permian strata at Oyrlandsodden and Smkappnya. The Hornsund- neset Formation of the Hornsundneset area has been described by De Geer (in Nathorst 1910), O ~ i n (1940), Siedlecki 1960, Birkenmajer (1964, 1979a), Haczewski (1984), Liparski & ~ m i e l (1984) and WendorfT (1985).

homogenised NV\

black n. black

A

A

h

age 1 ~ith. strat. m IIIIIIIIII] l units dsivf f mcvcg pcbb

Fig. 2-25: Stratigraphic section CP-14 Stmtofype for: Homsundneset Formation Locality: Hohenlohefjellet Refrence: Wendarff 1985

Detailed stratigraphic investigations were published by Siedlecki (1960) and Wendor@ (1985).

The base of the formation in the Hornsundneset area is commonly defined by a thin quartz conglomerate. The prevailing rocks are medium- to fine-grained, light grey sandstones with darker (or even black) siltstone intercalations. The sandstones locally contain pebble or gravel horizons with quartz clasts. Large-scale, tabular cross-bedding is common, while trough cross-bedding is observed at several stratigraphic levels. Erosional channels up to 1.5 m in depth have been reported. In the lower part of the formation, plant detritus and occasionally rootlets occur, usually in fine- grained (silty) beds. The succession shows an overall, though irregular, fining-upward trend.

Knowledge of the formation in the foldbelt area is restricted to rough surveying. There are prevailing massive, light sandstones, occasionally with minor siltstone horizons. Plant remains are very common, and large tree trunks have been observed. A major, coarse quartz or quartzite conglomerate strikes along the north-eastern ridge of Auster- nebba, 300-350 m above the formation base, where it is ca. 50 m thick, southward to Gratinden, where it is much closer to the base of the formation. Thin coaly shales occasionally occur within the light grey sandstones, for instance in the summit area at Stuptinden.

Thickness values vary significantly and probably reach 700-750 m at Hornsundneset and 1100 m at Austernebba and Knattberget in the foldbelt.

The depositional environment of the Hornsundneset For- mation is interpreted as braided, quickly mig'rating channels and sand bars, though with an unexpected lack of overbank fmes and in situ vegetation (Birkenmajer 1979a; Haczewski 1984; WendorB 1985).

The Hornsundneset Formation is a possible equivalent to the Orustdalen Formation in Western Spitsbergen.

DISTRIBUTION SHOWN ON FIG(s).: 2-06 STATUS OF UNIT: Formal F'IR~T USE OF NAME: Siedlecki 1960; rank revised to 'formation' by Cutbill & Challinor (1965) CURRENT DEFINITION: Siedlecki 1960 SYNONYM(S) AND REFERENCE(S): "Sergeijevfjellet Beds": Siedlecki 1960 ORIGIN OF NAME: Sergeijevfjellet: A mountain to the east of Hornsundneset, NW Ssrkapp Land (type locality)

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TYPE SECTION (FIG. 2-26): Stratotype: Sergeijevfjellet, E of Hornsundneset, S Spits- bergen. STRUCTURAL SETTING: Early Carboniferous basin in southern Spitsbergen; connection with other coeval basins not documented DEPOSITIONAL AGE: ViS6an DATING METHOD: Palyll010gy REFERENCE(S) FOR AGE: Siedlecki & %rIlau 1964 OVERLYING UNIT@): Vardebukta Formation, locally ?Hymefjellet Fm.

KiefpUet Formation

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Fig. 2-26: Stratigraphic section CP-l5 Stratotype for: Sergeijevfjellet Formation Locality: Sergeijevfjellet Reference: Gjelberg 1984 (unpubl.)

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UNDERLYING UMT(S): Hornsundneset Formation SUPERIOR UNIT: Billefjorden Group OTHER USE OF NAME: None THICKNESS: Up to 260 m, 160 m in stratotype MAIN LITHOLOGIES: Sandstone, shale LOWER BOUNDARY DEFINITION: The base of the formation is defined above the tick sandstones of the Homsundneset Formation, at the base of the first fining-upward sandstone unit that ends up with a distinct shale interval. On Hohen- lohefjellet, the base is situated above a thick coal seam. DESCRIPTION: The Sergeijevfjellet Formation forms the upper, shale-rich part of the Billefjorden Group in the Horn- sund area. The formation occurs exclusively in the Horn- sundneset area (Hohenlohefjellet, Sergeijevfjellet, Lisbet- dalen) and is cut by the sub-Triassic unconformity. Thin developments through basal parts of the unit are possibly preserved in the Austjerkulen-Kronglebreen area within the Tertiary foldbelt segment of Smkapp Land. The formation has been described by Siedlecki (1960), Birkenmajer (1964), Liparski & ~miel(1984) and Wendorff(1985).

The Sergeijevfjellet Formation consists of medium- to fine-grained, light grey, cross-bedded sandstones, interbed ded with a high portion of shales and siltstones. Wavy and lenticular laminations occur frequently. Two thin levels of coal and coaly shale occur. Carbonised plant detritus, leaves and tree ?trunks, as well as trails and burrows, are common within the fine-grained deposits. The maximum observed thickness is 260m.

The sedimentary environment is interpreted to be braided rivers and floodplains (Wendorff 1985).

The Sergeijevfjellet Formation is a possible equivalent to the Vegardfjella Formation in Western Spitsbergen.

(Induan:

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DISTRIBUTION SHOWN ON FIG@).: 2-05 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE@): "Ursa Sandstone", lower part: Holtedahl 1920 ORIGIN OF NAME: Raedvika: A bay on the E coast of B jm- oya (type area) TYPE SECTION (FIG. 2-28): Composite section from localities along the E coast of Bjmerya; see individual members (C-1 7,18,19) STRUCTURAL SETTING: Early Carboniferous basin of the Western Barents Sea Shelf DEPOSITIONAL AGE: Famennian - Tournaisian

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2. UPPER PALAEOZOlC LITHOSTRATIGRAPHY

DATING METHOD: Paly'n010gJJ REFERENCE(S) FOR AGE: Kaiser 1970; Worsley & Edwards 1976; Vigran 1994 (unpubl.) OVERLYING UNIT(S): Nordkapp Formation, locally Kapp Hanna or Hambergfjellet formations. UNDERLMVG m ( s ) : Pre-Old Red SUPERIOR UNIT: BiUefjorden Group OTHER USE OF NAME: None THICKNESS: 120-360 m MAIN LITHOLOGIES: Sandstone, shale, coal LOWER BOUNDARY DEFINITION: The base of the formation is defined by the onset of clastic sedirnents, normally sandstones, above the main Caledonian angular unconformity and the erosive boundary with underlying folded or tilted rocks of the Pre-Old Red. DESCRIPTION: The Rsedvika Formation represents the lower part of the Ursa Sandstone of earlier investigators. A detailed description was published by Horn & Orvin (1928). Worsley & Edwards (1976) subdivided the formation into the Vesalstranda, Kapp Levin and W e i m members.

The Vesalstranda Member consists of alternating fining- and coarsening-upward units composed of sandstones, siltstones, mudstones, coaly shales and coals. The fining-upward units represent mainly fluvial channel deposits (Fig. 2-27) with a dominating palamcurrent direction towards the northwest, whereas the coarsening upward units probably represent lacustrine deltaic sequences (Gjelbq 1978,1981, 1987).

The Kapp Levin Member consists mainly of fluvial braided and meandering sandstones and conglomerates dmning eastwards.

The lbheim Member consists of fluvial sandstones interbedded with fine-grained flood-plain deposits and coal.

The RPredvika Formation thins westward on Bjermnrya and it is only 120 m thick at SW Alfiedfjellet (Horn & Orvin 1928; Gjelberg 1981). The thinning may be caused by angular unconformities within the Carboniferous succession. At Alfredfjellet, the Kapp Hanna and Hambergfjellet formations unconformably overlie the Rsedvika Formation.

Fig. 24% Elwisd dmmei in rhe l m r part of the RBedvika Formation, Rmdvika, Bjernarya. Photo: D. Womley

Pre- Old Red Basement

-1 I m -

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Fig. 23%: Stratigraphic section CP-16 Composite stmtotype for: RBedvika Formation Locality: VesaIstranda - Kapp Levin - M e i m Reference: Gjelberg 1981 (unpubl.)

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UPPER PALAEOZOIC LITHOSTRATIGRAPHY

Vesalstranda Member (CP-17)

STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley & Edwards 1976 CURRENT DEFINITION: Worsley & Edwards 1976 SYNONYM(S) m REFERENCE(S): None. The unit is represented by the "Skrekk" and "Misery subfonnations" (Russ.: podsvity) of Pavlov et al. (1983). ORIGIN OF NAME: Vesalstranda: The coastal strip at the foot of Miseryfjellet, E coast of Bjsrnraya (type locality) TYPE S E C ~ N (FIG. 2-29): Stratotype: Vesalstranda, eastern Bjsrnraya DEPOSITIONAL AGE: Famennian DATING METHOD: Palfl010gJ' REFERENCE(S) FOR AGE: Kaiser 1971; WorSley & Edwards 1976 OVERLYING UNIT@): Kapp Levin Member UNDERLYING UNIT(S): Pre-Old Red SUPERIOR UNIT: Rciedvika Formation OTHER USE OF NAME: None THICKNESS: ca. 200 m, >l55 m in stratotype MAIN LITHOLOGIES: Sandstone, shale, coal LOWER BOUNDARY DEFINITION: See Rciedvika Formation DESCRIPTION: The Vesalstranda Member consists of coarsening- and fining-upward units of sandstone, siltstone and shale. Coal seams and coaly shale are interbedded with these units. Siderite bands and concretions are often associated with the coals. Plant fossils are common, both within the shales and the sandstones.

The fining-upward units represent flood-plain environments constructed mainly from northwestward flowing streams of high sinuosity and ribbon channel systems. The coarsening-upward units represent a lacustrine deltaic environment constructed mainly from prograding delta lobes into standing water bodies (lakes). The Vesalstranda Mem- ber contains approximately 20 coal seams and coaly shales. Most of these are thin, however, but may locally be up to one meter thick (Horn & Orvin 1928).

Kapp Levin Member (CP-18)

STATUS OF UNIT: Formal FIRST USE OF NAME: W0r~ley & Edwards 1976 CURRENT DEFINITION: Worsley & Edwards 1976 SYNONYM(S) m REFERENCE(S): None. The rank 'subfor- rnation' (Russ.: podsvita) was used by Pavlov et al. (1983). ORIGIN OF NAME: Kapp Levin: A cape on the eastern coast of Bjarmnrya (type locality) TYPE SECTION (FIG. 2-30): Stratotype: Kapp Levin, eastern Bjermya DEPOSITIONAL AGE: Late Famennian - Early Tournaisian DATING METHOD: Palynology in over- and underlying units REFERENCE(S) FOR AGE: Vigfan 1994 (unpubl.); Worsley & Edwards 1976 OVERLYING UNIT(S): Tunheim Member UNDERLYING UNIT@): Vesalstranda Member SUPERIOR UNIT: Rciedvika Formation OTHER USE OF NAME: None THICKNESS: 7 1 m in stratotype

Tunheim Member

(Famenniad

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Fig. 2-30: Stratipphie mtion CP-18 Stmtotype for: &pp Levin Member Localily: &pp Levin Refirence: Gjelberg 198 1

MAIN LITBOLOGIES: Sandstone, shale LOWER BOUM)ARY DEFINITION: The lower boundary is defined at the base of the thick sandstone succession which dominates most of the unit. Conformably underlying lithologies are shales. DESCRIPTION: The lower part of the Kapp Levin Member consists of relatively thick, f i - u p w a r d sandstone units with lateral accretion surfaces. The overlying sandstones and pebbly sandstones reflect a more complex vertical development of alternating sandstones, pebbly sandstones, thin cong1omerates and thin shales, probably representing braided stream deposits (Gjelberg 1981). The uppermost part of the member consists of a relatively thick mudstone interval coarsening upwards into conglomerates which constitute the lower part of the Tunheim Member.

The sediments of the Kapp Levin Member are virtually barren of organic material (Vigran 1994, unpubl.), though imprints of lepidodendrid stems are relatively common (Gjelberg 1981).

http://jurassic.ru

2 . UPPER PALAEOZOIC LITHOSTRATIGRAPHY

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Big. 2-31: Stratigraphic section CP-19 Composite stmtotype for: Tunbeim Member Locality: Tunheim (upper part) / Rifleodden (lower part) Reference: Gjelberg 1981 (unpubi.)

Tnnheim Member (CP-19)

STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley & Edwards 1976 CURRENT DEFINITION: Worsley & Edwards 1976 SYNONYM(S) AND REFERENCE(S): None. The unit is represented by the "Tunheim" and "Fugle subformations" @us.: podsvity) of Pavlov et al. (1983) ORIGIN OF NAME: Tunheim: An abandoned coal mining settlement, NE Bjmwya (type locality) TYPE SECTION (FIG. 2-31): Composite section: Rifleodden (lower part) and 'hnheim (upper part), NE Bjmwya DEPO~~TI~NAL AGE: Late Famennian - Early Tournaisian DATING METHOD: Palynology in adjacent units REFERENCE(S) FOR AGE: see Ebedvika Formation OVERLYING UNIT@): Nordkapp Formation UNDERLYING UNIT@): Kapp Levin Member SUPERIOR UNIT: Ebedvika Formation OTHER USE OF NAME: "Tunheim series" (Horn & Orvin 1928): lower, coal-bearing part of Tunheim Member; "Tunheim subformation" (Russ.: podsvita; Pavlov et al. 1983): lower part of W e i m Member. The present definition of the lbhe im Member is well- established in the literature and has priority. THICKNESS: ca. 80 m MAIN LITHOLOGIES: Sandstone, shale, conglomerate, coal LOWER BOUNDARY DEFINITION: The lower boundary is defined at the conglomeratic base of the lowennost of the stacked fining-upward sequences that build up the member. The conformably underlying lithology is nonnaly sandstone. DESCRIPTION: The Tunheim Member starts with several metres thick conglomerate and pebbly sandstones defined as the "Rifleodden Conglomerate Bed" by Worsley & Ed- wards (1976), followed by a 20-30 m thick sandstone unit. The member is composed of 3-4 stacked, poorly defined, fining upward sequences, probably representing meandering streams (Gjelberg 1981). The internal organisation of the member is very complex, with several erosional surfaces and mudstone lenses.

The coals of the Tunheim member were mined at the rnin- ing settlement of Tunheim from 19 16 to 1925.

Nord kapp I Formation

DISTRIBUTION SHOWN ON FIG@).: 2-05 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965

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2. UPPER PALAEOZOlC LITHOSTRATIGRAPHY

CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): "Ursa Sandstone", upper part: Holtedahl 1920 Owcm OF NAME: Nordkapp (transl. 'Worth Cape"): A cape at the N coast of Bjsrnsya TYPE SECTION (FIGS. 232,233): Unit stratotype: Landnsrdingsvika , SW Bjsrnsya Hypostratotype (upper part of formation): Nordhamna, N Bjnrmqa

The base of the formation is not exposed at the type locality itself, but is found at several localities along the NE coast north of Tunheim (Worsley & Edwards 1976; Gjelberg 1981). STRUCTURAL SETTING: Early Carboniferous basin of the Western Barents Sea Shelf DEPOSITIONAL AGE: Tournaisian - Vis6an DATING METHOD: Palynology REFERENCE(S) FOR AGE: Vigrall1994 (unpubl.); W0IXley & Edwards 1976 OVERLYING UNIT(S): Landnsrdingsvika -ation, locally Hambergfjellet Formation UNDERLYING UNIT(,%): Raedvika Formation SUPERIOR UNIT: Billefjorden Group OTHER USE OF NAME: Nordkapp Basin (southern Barents Sea), from a different locality on mainland Norway THICKNESS: Up to 230 m 1MAm LITHOLOGIES: Sandstone, conglomerate LOWER BOUNDARY DEFINITION: The base is defined at the onset of rapidly alternating clastic litbologies including conglomerates above the Raredvika Formation. Horn & Orvin (1928) describe. a slight angular unconfonnity due to regional tilting of the underlying substratum. DESCRIPTION: The formation is divided into the Kapp Harry Member (below) and the Nordhamna Member (above).

The Kapp Harry Member consists mainly of grey cross- stratified sandstones, representing eastward draining braided streams (Gjelberg 1981; Gjelberg & Steel 1981). The Nordhamna Member consists of alternating grey conglomerates, sandstones, pebbly sandstones and greylreddish shale, representing braided- stream and debris-flow deposits (Gjelberg 1981; Gjelberg & Steel 1981).

The formation thins west- and southwestward and is less than 100 m thick on the southeastern coast (Horn & Orvin 1928). On Alfredfjellet, the Hambergfjellet Formation unconformably overlies tilted and truncated beds of the Nord- kapp Formation.

Kapp Harry Member (CP-21)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here; after Gjelbe~g 1984 (unpubl.) CURRENT DEFINITION: Gjelberg 198 1 SYNONYM(S) AND REFERENCE(S): None O R I G ~ OF NAME: Kapp Harry: A cape on the SW coast of Bjmllya (type locality) TYPE SECTION (FIG. 2-32): Unit stratotype: Kapp Harry at Landnsrdingsvika, SW Bjsrnraya DEPOSITIONAL AGE: Tournaisian - ?Vistan

DATING METHOD: Palynology REE'ERENCE(S) FOR AGE: Vigran 1994 (unpubl.) OVERLYING UNIT(S): Nordhamna Member UNDERLYING UNIT(S): Rsedvika Formation SUPERIOR UNIT: Nordkapp Formation OTHER USE OF NAME: None THICKNESS: >50 m in stratotype MAIN LITHOLOGIES: Sandstone, conglomerate LOWER BOUNDARY D E ~ T I O N : See Nordkapp Formation DESCRIPTION: The Kapp Harry Member consists mainly of medium-grained sandstone, dominated by planar and trough cross-stratification, with occasional beds of pebbly sandstone and thin conglomerates. Beds of mudstones (shales) and siltstones are scarce (1.6 %). Beds are usually distinctly lenticular. Soft-sediment deformation structures occur fiequently.

The unit represents braided stream deposits. Palaeocur- rent indicators suggest an easterly drainage direction.

In addition to the area north of Kapp Harry, the member is well exposed around Nordkapp at the north coast.

Nordhamna Member (CP-22)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here; after Gjelberg 1984 (unpubl.) CURRENT D E F ~ O N : Gjelberg 198 1 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Nordhamna (transl. 'Worth Harbour": A bay on the northern coast of Bjsrnraya (locality of reference stratotype) TYPE SECTION (FIGS. 232,233): Unit stratotype: Landnsrdingsvika , SW Bjsrnsya Hypostratotype: Nordhamna, N Bjnnnraya DEPOSITIONAL AGE: VisBan DAWG METHOD: Palynology in adjacent units REFERENCE(S) FOR AGE: See Nordkapp Formation OVERLYING UNIT(S): Landnsrdingsvika Formation UNDERLYING UNIT(S): Kapp Harry Member SUPERIOR UNIT: Nordkapp Formation -R USE OF NAME: None THICKNESS: %5 m in stratotype MAIN LITHOLOGIES: Sandstone, conglomerate, shale LOWER BOUNDARY DEFINITION: The lower boundary of the member at the type locality is defined at the base of a prominent interval of alternating siltstone and shale (> 10 m thick), with conformably underlying sandstones of the Kapp Harry Member. DESCRIPTION:. The Nordhamna Member consists of alternating cross stratified grey sandstones, pebbly sandstones, grey conglomerates (composed of quartzitic and chert pebbles) and grey or greyish-red siltstone and shale with thin coaly shale interbeds (Gjelberg 1981; Gjelberg & Steel 1981).

The sharp environmental change from the Kapp Harry Member to the Nordhamna Member may reflect the early onset of a climatic andlor tectonic change whose main effect was felt in Bashkirian times (Gjelberg & Steel 1981, 1983; Steel & Worsley 1984; Gjelberg 1987). The sediments of the Nordhamna Member represent mainly braided stream de-

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2. UPPER PALAEOZOIC LlTHOSTRATlGRAPHY

red

posits, probably closely associated with an alluvial fan system. The thick units of fiie-grained sediment5 may represent flood-plain or lacustrine deposits.

In addition to the type IoettlitJT, the Notdhma Member is also well exposed in Nor- and KO- on the northern coast. The member is not coqbtaly exposed at these localities, and it is difficult b make a reWle tbiok- ness estimate there. However, &data &from borebole 1 (at Laksevatnet) and borehole 7 (S end of Hauswhet) tentatively suggest that the east (Horn & Orvin 1928,

2.6.2 Gipsdalen Group

GIPSDALEN GROUP (CP-23)

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Rg. 2-33: Stratigraphic section CP-20bl22b Hypostmtolype for: Nordkapp Formation, Nordhamna Member Locality: Nordhamna Refemnce: Gjelberg 1981

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Gipsdalen (transl. "Gypsum Valley": A broad glacier v$ley in Biinsow Land, central Spitsbergen TYPE AREA: Gipsdalen and adjacent mountains in Biinsow Land, central Spitsbergen STRUCTURAL SETTING: Late Palaeozoic platform of Sval- bard and the Barents Sea Shelf

G ipsdalen Group

Fig. 2-34: The Carboniferous succession north of Ansenika (L.,,- fjorden), showing redbeds of the Hultberget Formation (hypostratotype) in a fault slice at sea level, and the Wordiekamtnen (yellowish- grey carbonate rocks), Gipshuken (white gypsum and grey dolomite rocks) and Kapp Starostin formations (upper yellowish and grey spiculitic rocks and limestones). The Cowantoppen Fault (a strand of the Billefjorden Fault Zone) cuts the right part of the photo sub- parallel to the slope. Photo: H.B. Keilen

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CAMPBELLRYGGEN SUBGROUP (CP-24)

Ng. 2-35: Terrierfjellet (northeastern Biinsow Land), showing Pre- cambrian basement (dark colour) eastward-thinning wedges of Hult- berget Formation sandstones (red) and gypsiferous parts of the Ebbadalen Formation (mostly covered) below cliff-forming carbonate rocks of the Minkmfjellet (Terrierfjellet member) and Wordie- kammen formations. Photo: E.P. Johannessen

DEPOSITIONAL AGE: Serpukhovian - Artinskian OVERLYING UNIT(S): Tempelfjorden Group; locally on Smkapp-Homsund High: Sassendalen Group UNDERLYING UNIT(S): Billefjorden Group, Pre-Old Red SUPERIOR UNIT: None OTHER USE OF NAME: None TIUCKNESS: Up to 1800 m MAIN LITHOLOGIES: Various carbonate and clastic rocks, evaporites DESCRIPTION: The Gipsdalen Group shows the stratigraphic development from middle Carboniferous clitstic graben- related sediments to Late CarboniferousIEarly Permian marine shelf carbonates with evaporite intercalations (Figs. 2-34, 2-35). The group is separated from the underlying Billefjorden Group by a hiatus starting in the early Ser- pukhovian. The duration of the period of non-deposition varies sigmficantly and is distinctly shorter in the middle

L . . a b h

STATUS OF UNIT: Formal FIRST USE OF NAME: Gee et al. 1952 CURRENT DEFINITION: Here. Rank revised to 'subgroup'. The name was introduced by Gee et al. (1952) as a group name. SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Campbellryggen: A mountain in NW Biinsow Land, central Spitsbergen TYPE AREA: NE Dickson Land, central Spitsbergen STRUCTURAL SETTING: Billefjorden Trough DEPOSITIONAL AGE: Serpukhovian - early Kasimovian OVERLYING UNIT(S): Dickson Land Subgroup UNDERLYING UNIT(S): Billefjorden Group, locally Pre-Old Red SUPERIOR UNIT: Gipsdalen Group OTHER USE OF NAME: None THICKNESS: Up to 1400 m MAIN LITHOLOGIES: Various carbonate and clastic rocks, evaporites DESCRIPTION: CampbeUryggen Subgroup is a collective name for the thee formations (Hultberget, Ebbadalen and Mbbfjellet formations) assigned to the roughly Bash- kirian to early Kasimovian sedimentary fill of the Bille- fjorden Trough (Fig. 2-36). For detailed descriptions see the individual formations.

carboniferous troughs than on the intermediate highs (Fig. 2-04). The Gipsdalen Group comprises the Treskelen, Charlesbreen and Campbellryggen subgroups (each related to an individual graben structure), the Dickson Land Sub- group (overlapping shelf carbonates and evaporites) and a number of formations of uncertain subgroup affiliation, especially in Eastern Spitsbergen and on~j&a. I

Fig. 2-36: The succession of the Campbellryggen Subgroup of the Billefjorden Trough at Trikolorfjellet (western Dickson Land). The stratigraphy from below is represented by the Hultberget Formation (lowermost redbeds), the Ebbadalen Formation with the multicoloured Ebbaelva Member, the redbeds of the Odellfiellet Member and the light, gypsum-dominated Trikolorfjellet Member. The latter two are interfingering. The mountain is capped by sandy carbonate and carbonate rocks of the Mududjellet Formation (upper grey beds). Photo: E.P. Johannessen

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Formation '-l

Ebbadalen Formation

DISTRIBUTION SHOWN ON FIG(s).: 2-09 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Here

. kank revised to 'formation' SYNONYM(S) AND REFERENCE@): "Hultberget Member": Cutbill & ChalIinor 1965; "Anservika Member": Gjelberg 1984 (unpubl.) ORIGLN OF NAME: Hultberget: A mountain in NE Dickson Land, central Spitsbergen TYPE SECTION (FIGS. 238,239): Unit stratoty-pe: Odellfjellet, NE Dickson Land

C m

V) .c Boundary stratotype: Anservika, SW Biinsow Land 3 .- The thickest and most complete section at Odellfjellet is o g

defined as the type section of the Hultberget Formation, CC

though it lacks the basal part of the formation. The Anser- E m vika section is therefore used as the boundary stratotype. ; .! Because of easier access it q y also be used as a reference 0 stratotype. m c STRUCTURAL SETTING: Billefjorden Trough CC

a DEPOSITIONAL AGE: Late Serpukhovian DATING METHOD: Palyn010gy

: V)

REFERENCE(S) FOR AGE: Playford 1962 OVERLYING UNIT(S): Ebbadalen Formation; locally in easternmost exposures: Minkinfjellet Formation UNDERLYING UNIT(S): Mumien Formation SUPERIOR UNIT: GipSdalen Group OTHER USE OF NAME: None THICKNESS: Up to 120 m MAIN LITHOLOGIES: Red shale, sandstone, conglomerate

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Fig. 2-38: Stratigraphic section CP-25a Unit shatotype for: Hultberget Formation

Fig. 2-37: Redbeds of the Hultberget Formation at Odellfjellet (north- Locality: Odellfjellet western Dickson Land), overlain by multi-coloured debris of the Reference: Gjelberg 1984 (unpubl.) Ebbaelva Member. Photo: W.K. Dallmann

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LOWER BOUNDARY DEFIMTION: The lower boundary (only exposed in Anservika) is sharp and marks a prominent lithological change from coal-bearing, grey sandstones and shales of the Mumien Formation to the non-coal-bearing redbeds of the Hultberget Formation. DESCRIPTION: The "Hultberget Member", origudly part of the "Svenbreen Formation", Billefjorden Group (Cutbill and Challinor 1965), was redefined by Johannessen (1980, unpubl.) to include only the upper red-bed, mainly coal- barren part of the unit. It was placed within the Ebbadalen Formation. These Hultberget redbeds are here raised to formation rank (Hultberget Formation), and assigned to the Campbellryggen Subgroup, Gipsdalen Group (Fig. 2-37).

The Hultberget Formation consists of alternating red (subordinately grey) shale, sandstone and conglomerate. These are interpreted as ephemeral stream and overbank deposits, partly on alluvial fans which built out from the. Billefjorden Fault Zone, interfingering eastwards into alluvial floodplains, lagoons and shoreline deposits. Marine transgressions probably came from the north.

A possibly significant age break between the Hultberget Formation and the underlying Billefjorden Group has recently been suggested (Nmedt et al. 1992). The boundary would thus be a stratigraphic unconformity. The upper boundary with the Ebbadalen Formation is a transitional or sharp contact with overlying grey sandstones.

DISTRIBUTION SHOWN ON FIG@).: 2-09 STATUS OF UNIT: Fonnal FIRST USE OF NAME: Cutbill & Chdinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM@) AND REFERENCE(S): "Untere Gipsstufe": Nathorst 1910; "Lower Gypsiferous Series": Gee et al. 1952 ORIGIN OF NALME: Ebbadalen: A glacier valley in NE Dick- son Land

Fig. 2-39: Stratigraphic section CP-25b TYPE SECTION (FIGS. 2-41,2-42): . ,

Boundaly stmtotype for: Hultberget Formation Stratotype: Wordiekammen, NE Dickson Land (Fig. 2-40) Locahy: A n ~ e ~ i k a Hypostratotype: Odellfjellet, NE Dickson Land Reference: Gjelberg 1984a (unpubl.), redrawn from Aakvik (unpubl.) STRUCTURAL SETTING: Billefjorden Trough

D E P ~ ~ I T I ~ N A L AGE: Bashkirian (roughly). Based on brachiopods, Holliday & Cutbill (1972) raised the possibility that the lower part of the Ebbadalen Formation might be of Early Carboniferous (Namurian) age, rather than Bash- kirian, as previously supposed (Orvin 1940; Gee et al. 1952; Forbes et al. 1958; Forbes 1960; Cutbill & Challinor 1965). The upper part of the Ebbadalen Formation on Odellfjellet may have a Moscovian age (Johannessen 1980, unpubl.).

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Fig. 2-40: Type section of the Ebbadalen Formation at Wordiekammen,

I Ebbadalen (eastem Dickson Land). The light- coloured bands are gypsum layers of the Trikolorfjellet

Member. Photo: E.P. Johannessen

DATING METHOD: Invertebrate fossils, (foraminifera, brachiopods) REFERENCE@) FOR AGE: Holliday & Cutbill 1972 OVERLYING UNIT@): Minkinfjellet Formation; locally ?Wordiekammen Formation UNDERLYING UNIT@): Hultberget Formation SUPERIOR UNIT: Campbellryggen Subgroup OTHER USE OF NAME: None THICKNESS: 0 to >55O m, 282 m in stratotype MAW LITHOLOGIES: Wide range of clastics, carbonate rocks and evaporites LOWER BOUNDARY D E ~ T I O N : Grey sandstones of the Ebbaelva Member mark the formational base and rest with a sometimes sharp contact, sometimes with a transitional contact zone on red sandstones and shales of the Hultberget Formation. DESCRIPTION: The Ebbadalen Formation lies in an asymmetric, elongate basin (approx. 18 km wide) on the down- throw side of the Billefjorden Fault Zone, the Billefjorden Trough. The unit thins from more than 550 m along the western edge of the trough at Odellfjellet to its pinchout on the eastern basin margin at Temerfjellet. The facies within the formation. are highly variable, both vertically and laterally, and are described in more detail for the individual members.

Several workers interpret the base of the Ebbadalen For- mation to be an unconformity (Tprell 1922; O ~ i n 1940; Holliday & Cutbill 1972), while others suggest continuous deposition from the underlying Hultberget Formation into the Ebbadalen Formation (Gee et al. 1952; McWhae 1953; Gobbett 1963; Johannessen 1980, unpubl.; Johannessen & Steel 1992). The grey sandstones of the Ebbaelva Member are interbedded with black and green shales.

Overlying the Ebbaelva Member occur gypsum, anhydrite and limestones (Trikolorfjellet Member), which pass westward into red shales and red coarse clastics (Odellfjellet Member).

The upper contact is transitional in the west, where both Ebbadalen Formation and the overlying Mmkmfjellet For-

Minkinfjellet Formation

(Mosco*

0

P

E 0

2 * Y

0 .m C z 3.

0 " H

V)

3 < .- 0 c 2 ; w a d

"J: 0 L .- lz,

X

o r W m m A K m $ a Q

0 m m W

-

CI

D

P

a 0

2

> 4

0 c8

P P

ul

Hultberget Formation

(Serpukhovian?)

age I 11th strat l units

green

dolomites: black

shales: - red and green

sandstones: multi-coloured

........... ................ grain size info not available m 11/)11(1111

clslvf f mcvcg pcbb

Fig. 2-41: Stratigraphic section CP-26a129 Stratotype for: Ebbadalen Formation, Trikolorfjellet Member Locality: Wordiekammen, Ebbadalen Reference: Holliday & Cutbill 1972

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2. UPPER PALAEOZOIC LITHOSTRATIGRAPHY P

Fig. 2-42: Stratigraphic section CP-26bI28a H ~ o s t m t o ~ e for: Ebbadalen Formation Srmrotype for: Odellfjellet Member Locality: Odellfjellet Reference: Johannessen & Steel 1992, from Johannessen 1980 (unpubl.)

11111111111 dmvt f mcvcg pcbb

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mation consist of clastic lithologies (Johannessen & Steel 1992). In the central part of the basin, the contact is easily recognised by a sudden change from the gypsiferous Trikolorfjellet Member to clastic sediments in the lower part of the Minkinfjellet Formation (Holliday & Cutbill 1972). On the eastern basin margin, the boundary is again transitional, where evaporites and black carbonates of the Trikolorfjellet Member grade into evaporitic limestones and grey dolomites ("Umtonfjellet Limestone Beds", Holliday & Cutbill 1972) of the Minkinfjellet Formation ( L m q 1995):

Depositional environments are lakes, alluvial fans, braided streams, mouth bars, fan deltas, sabkhas, lagoons and shorefaces (Johannessen & Steel 1992).

Ebbaelva Member (CP-27)

STATUS OF UNIT: Formal FIRST USE OF NAME: Holliday & Cutbill 1972 CURRENT DEFINITION: Johannessen & Steel 1992 SYNONYM(S) AND RE~RENCE(S): None ORIGIN OF NAME: Ebbaelva: The main river in the valley Ebbadalen, NE Dickson Land, central Spitsbergen TYPE SECTION (FIG. 2-44): Stratotype: Hultberget, north-eastern Dickson Land DEPOSITIONAL AGE: Bashkirian or slightly older DATING METHOD: Fusulinids REFERENCE(S) FOR AGE: Holliday & Cutbill 1972 OVE~LYING UNIT(S): Trikolorfjellet Member, Odellfjellet Member UNDERLYING UNIT(S): Hultberget Formation SUPERIOR UNIT: Ebbadalen Formation OTHER USE OF NAME: None THICKNESS: 0-220 m, 70 m in stratotype MAIN LITHOLOGIES: Sandstone, shale LOWER BOUNDARY DEFINITION: See Ebbadalen Formation DESCRIPTION: The thickness of the Ebbaelva Member varies around 220 m along the western margin of the Bille- fjorden Trough and the member pinches out on the eastern basin margin at Terrierfjellet.

m III[IIIIIII dsivf f m cvcg pcbb

Ftg. 2-44: Stratigraphic section CP-27 Stmtotypefor: Ebbaelva Member

L

Locality: Hultberget Refence: Johannessen & Steel 1992, fiom Johannessen

The lower boundary corresponds to the base of the Ebbadalen Formation. The upper boundary is taken at the base of dominant evaporitelcarbonate beds. The "Ebbabreen sandstone beds", "Ebbabreen shale beds" and "Gerritelva

Fig. 2-43: Outcrops of the Ebbaelva Member at the northern slope of sandstone member" (Holliday & Cutbill 1972) describe Odellfjellet. The multi-coloured succession contains greenish-grey only local facies within the Ebbaelva Member and are not shales, white or pink gypsum, red mark, yellowish silt- and sand- correlated basin-wide (Johannessen 1980, unpubl.). stones. Photo: W.K. Dallmann The facies variations within the Ebbaelva Member are

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L Fig. 2-45: Alluvial channel and overbank deposits in the Odellfjellet

Member, Odellfjellet (northeastern Dickson Land). Photo: E.P. Johannessen

highly variable,. both vertically and laterally, and are described in detail by Johannessen (198Q, unpubl.). The member comprises grey and yellow sandstones interbedded with grey-green shales and minor interbeds of carbonates, evaporites, conglomerates and red sandstones (Fig. 2-43). Depo- sitional environments include lakes, lagoons, sabkhas, braided streams, mouth bars, fan deltas and shorefaces.

Locally on the southeastern side of the Billefjorden Trough, at the top of the Ebbaelva Member, the "Margaret- breen conglomerate facies" is developed (Holliday & Cut- bill 1972; Johannessen 1980, unpubl.). This unit has a thickness variation from 2.5 m to 20 m and comprises yellow sandstones, conglomerates and sandy dolomites with echin- oderm hgments.

Odellfjellet Member (CP-28)

STATUS OF UNIT: Formal FIRST USE OF NAME: Johannessen & Steel 1992 CURRENT DEFJNITION: Johannessen & Steel 1992 SYNONYM(S) AND REFERF,NCE(S): ' 'P~~;lr~lden Formation": Ljutkevic 193%; "Low./Up. redbed facies": Holliday & Cutbill 1972 ORIGIN OF NAME: Odellfjellet: A mountain in NE Dickson Land, central Spitsbergen TYPE SECTION (FIGS. 242,244): Stratotype: Odellfjellet, NE Dickson Land Hypostratotype: Pyramiden, NE Dickson Land DEPOSITIONAL ACE: Bashkirian. The upper part of the

l HuRberget Format~on

(Bashkirian) - d sivf f m cvcg pcbb

eolian sediment

eolian sediment

F@ 2-46: Stratigmphic section GP-28b Hyposhutotypefbr: Odellfjellet Member Locality: -den Refemce: Johannessen t Steel 1992. Brmn Johmmasen

publ.)

Odellfjellet Member on Odellljellet may have a Moscoyiitn age ( J o ~ ~ s e n 1980, lmpubl.). DATING METHOD: Fossils itl adjiwent units RERERENCE(S) r n ~ m: HoErlsy Bt Cutbill 1972 OVERLYING WNIT(S): MhkidjeIlet Formation; locally ?Wordiekammen Formdon UNDERLYING UNIT(S): Ebbaelva Member, Trikolorfjellet Member LATERALLY ADJACENT UNIT(S): Trikolorfjellet Member SUPERIOR UNIT: Ebbadalen Formation OTHER USE OF NAME: None

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2. UPPER PALAEOZOIC LITH'OSTRATIGRAPHY

THICKNESS: Up to 400 m MAIN LITHOLOGIES: Multicoloured conglomerate, sandstone and dolomite LOWER BOUNDARY DEFINITION: The lower part of the member interfingers with the carbonate-evaporite-dominated lithologies of the underlying Trikolorfjellet Member. The bouadary is defined at the onset of multicoloured, coarse clastic racks above carbonates and evaporites. DESCRIPTION: The Odellfjellet Member onlaps the faulted basin margin of the Billefjorden Trough in the west (Pyra- miden section) and consists of red, grey and yellow conglomerates and sandstones, red shales (locally with gypsum nodules), yellow dolomites and sandy dolomites.

The member consists of a series of clastic wedges built out from the Billefjorden Fault Zone and has been interpreted largely in terms of alluvial fan (Fig. 2-45), fan delta, shoreline and aeolian deposits. The sediments are arranged in 15-30 m thick coarsening-upward sequences consisting of red alluvial fan sandstones and conglomerates, capped by white q d t i c sandstones and yellow dolomites and limestones.

Trikolorfjellet Member (CP-29)

STATUS OF UNIT: Formal FIRST USE OF NAME: Holliday & Cutbill 1972 CURRENT DEFINITION: Johannessen & Steel 1992 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Trikolorfjellet: A mountain in NE Dick- son Land, central Spitsbergen TYPE SECTION (FIG. 2-41): Stratotype: Wordiekammen, NE Dickson Land DEPOSITIONAL AGE: Bashkirian DATING METHOD: Fusulinids REFERENCE(S) FOR AGE: Holliday & Cutbill 1972 OVERLYING UNIT(S): Odellfjellet Member, -ellet Formation UNDERLYING UNIT@): Ebbaelva Member LATERALLY ADJACENT UNIT(S): Odellfjellet Member SUPERIOR UNIT: Ebbadalen Formation W H E R USE OF NAME: None THICKNESS: Up to 240 m, 185 m in stratotype MAIN LITHOLOGIES: Carbonate rocks, evaporites LOWER BOUNDARY DEFINITION: The lower boundary is defined where evaporite-carbonate bed alternations start to dominate above the Ebbaelva Member or above interfingering clastic lobes of the Ebbaelva Member. DESCRIPTION: The Trikolorfjellet Member has its greatest thickness (240 m) in the central part of the Billefjorden Trough and thins towards the Billefjorden Fault Zone (5- 50 m at Odellfjellet and 0 m at Mamiden). It interfingers with the Odellfjellet Member (Johannessen 1980, unpubl.). On the eastern basin margin, the Trikolorfjellet Member pinches out at Terrierfjellet. Holliday & Cutbill (1972) reported an overall thickness variation from 150 m to over 400 m because they included both the "Redbed facies" (now Odellfjellet Member) and the "Urmstonfjellet Limestone Bed" (part of Minkinfjellet Formation) in their Trikolor- fjellet Member.

Fig. 2478 The gypsifemus Tl&&@&Wh- at Chdell@ellet (northern Biinsow Land). Photo: E.R Johamessen .*. , l,

., ' The Trikolorfjellet Member consists of gypsdanhydrite

(interpreted as sabkha deposits) in alternation with black and minor yellow limestones and dolomites (interpreted as open marine/lagoonal to intertidal deposits) (Fig. 2-47). Red mudstones and minor red sandstones (interpreted as distal alluvial fans), related to the interfingering Odellfjellet Member, occur in western and central areas.

Formation 1

DISTRIBUTION SHOWN ON FIG(s).: 2-09 STATUS OF UNIT: F 0 d FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor (1965) defined the unit as a member of the 'Wordenskioldbreen Forma- tion". Slightly redefined here. SYNONYM(S) AND REFERENCE(S): "Passage Beds": Gee et al. 1952; "Mnkinfjellet Member": Cutbill & Challinor 1965 ORIGIN OF NAME: M m e l l e t : A mountain in N Biinsow Land TYPE SECTION (FIG. 2-49): Stratotype: Urmstonfjellet W, N Dickson Land

The stratotype was originally defined at the northern face of Mududjellet (Cutbill & Challinor 1965), but no documentation is available. The two localities are situated close to each other. STRUCTURAL SETTING: Billefjorden Trough DEPOSITIONAL AGE: Moscovian - early Kasimovian DATING METHOD: Fossils (fisulinids) REFERENCE(S) FOR AGE: Pickard et al. 1996

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Fig. 248: Lmehov- den (eastern Dickson Land), showing strata of the Minkin- tjellet Formation deformed into a major Elm. To the bottom right, gypsum of the Ebbadalen For-

/ mation occurs. The yellowish rocks in the core of the flex- we are sandy lithologies of the Carron- e h member, while overlying grey dolomites of the Terrierfjellet member turn upwards into dolomite breccias of

the Fortet member. The uppermost cliff is formed by the Black Crag Beds of the Wordiekammen Formation. Photo: W.K. Dallmann

OVERLYING UNIT($): Wordiekammen Formation UNDERLYING UNIT(S): Ebbadalen Formation; locally Hult- berget Formation or Pre-Old Red LATERALLY ADJACENT -(S): Upper part of Ebbadalen Formation; lower part of Wordiekammen Formation (Pye- fjellet Beds) SUPERIOR mrr:.Campbellryggen Subgroup OTHER USE OF NAME: None THICKNESS: Up to 300 m, 246 m in stratotype MAIN LITHOLOGIES: Dolomite, sandstone, gypsum LOWER BOUNDARY DEFINITION: The formation's lower boundary is in most places easily recognisable by a sudden change from the underlying gypsiferous Trikolorfjellet Member of the Ebbadalen Formation into the alternating sediments (dolomites, limestones, sandstones, evaporites) of the Carronelva Member. In eastern areas, the dolomitic rocks of the Terrierfjellet Member overlie sandstones of the Billefjorden Group or folded Pre-Old Red. The boundary is an angular unconformity on a regional scale. DESCRIPTION: The m e l l e t Formation forms part of the sedimentary fill of the asymmetric Billefjorden Trough. The strata are exposed to the east of the N-S trending Bille- fjorden Fault Zone, between Isfjorden and Austfjorden. Thickness values range from 0 m to ca. 300 m, the thickest exposures occur 5-12 km east of the fault zone, north of Petuniabukta. I

Lithologies are cross-bedded sandstones, \ limestones, dolomites, carbonate breccias and, subordinate anhyclritel gypsum. Gypsum predominates only in the southern part of Campbellryggen. The Minkinfjellet Formation is characterised by lateral facies changes with interfingering lithologies. The member subdivision reflects specific lithological associations: Carronelva member (clastic and carbonate), Terrierfjellet member (mostly dolomite), Fortet member (mostly carbonate breccia) (Fig. 2-48). For details see these entries.

The upper boundary of the M i e l l e t Formation is always marked by the characteristic lithologies of the overlying Cadellfjellet Member of the Wordiekammen Formation. The eastern boundary is placed at the lateral transition into limestone-dominated carbonates of the open platform facies of the Wordiekammen Formation. A formational boundary is not obvious in this area, and the eastern limit is arbitrarily defined at the glacier Tunabreen. The relative continuity with the Wordiekammen Formation in these eastern reaches was probably the reason for the grouping of the Minkin- fjellet beds with the "Nordenskioldbreen Formation" (Cut- bill & Challinor 1965; see Section 2.3.2).

Depositional settings are dominated by restricted peritidal, including sabkha, to shallow subtidal environments. Pe- riodically, conditions were semi-restricted to open marine. Intermittent subaerial exposure with palaeokarst formation occurred. Solution collapse of peritidal deposits in the northwestern part of Biinsow Land caused by the influence of meteoric waters formed the breccias of the Fortet member (Lonsy 1995).

Carronelva member (CP-31)

STATUS OF UNIT: Informal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 Raised to 'member' rank here SYNONYM(S) AND REFERENCE(S): "Carronelva Beds": Cut- bill & Challinor 1965 ORIGIN OF NAME: Carronelva: A river between the mountains Teltfjellet and Urmstonfjellet (type sections) TYPE SECTION FIGS. 2-49,250): Stratotype: Urmstonfjellet W, northern Biinsow Land Hypostratotype: Teltfjellet, NW Biinsow Land DEPOSITIONAL AGE: Early Moscovian DATING METHOD: Fossils (not documented), stratigraphic relationships REFERENCE($) FOR AGE: Cutbill & Chahor 1965 OVERLYING UNIT(S): Terrierfjellet Member UNDERLYING UNIT($): Ebbadalen Formation SUPERIOR UNIT: M i e l l e t Formation OTHER USE OF NAME: None THICKNESS: 0 - >l00 m, 67 m in stratotype MAIN LITHOLOGIES: Carbonate rocks, sandstone, gypsum LOWER BOUNDARY DEFINJTION: See hfhkldjellet Forma- tion DESCRIPTION: The Carronelva member forms the lower part of the Minkrnfjellet Formation in the Billefjorden Trough. The base is defined at the transition from the evaporite- dominated Trikolorfjellet Member to a carbonate-dominated succession. Minor evaporitic sequences also occur within the Carronelva member in the southern part of Campbellryggen. The top is defined at the top of the uppermost massive sandstone. The member underlies the breccias of the Fortet member in northwestern parts of the exposure area (Petuniabukta), and the carbonate rocks of the Terrier- fjellet member elsewhere.

Lithologies are alternating dolomites, limestones, sandstones and evaporites. Limestones are most common in the

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Wordiekarnrnen Formation

(Kasimovian) -

2 0

V, .r, = 2

O & h

U "I', Z 4 H

0 h4 z 1:

-

pale green

*

pale red

red

black

black

black

Ebbadalen Formation

(Bash kirian) - M W P G B

cluvf f mcvcg pcbb

Fig. 249: Stratigraphic section CP-3013 1a

Stmtoppe far: w e l l e t Formation, Carronelva member Locality: UnnstonfJellet W Reference: Lwuey, A. (unpubl.)

m - M W P O B

clsivtf mcvcg pcbb

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- , -

unrts M W P G clstvf f movcg

Fig. 2-50: Stratigraphic section CP-3 l b Hypostmtotype for: Carronelva member Localify: Teltfjellet NW Reference: L m y , A. (unpubl.)

black

abundant ripple

lamination

yellow

mainly covered

abundant cmss

bedding

red

southeastern part of Biinsow Land. Dolomites are generally unfossiliferous and some have a characteristic yellow weathering surface. The gypsum content decreases upwards in the sequence and southeastwards in Biinsow Land. Sand- stones are red, green or yellow and are very fine- to coarse- grained.

At Ebbabreen and Ragnarbreen, the member starts with coarse clastic rocks at the base (polymict sedimentary breccias with a carbonate matrix, "Ragnarbreen Breccia", McWhae 1953). These basal beds pinch out westwards, where they are replaced by greenish to yellowish medium- grained sandstones (western half of Sfinksen, Lmehovden and Wordiekammen). The overlying succession consists of yellowish sandstones, partly with a distinct sulphurous smell. Shales, marls, limestones and sandy limestones with gypsum vugs are intercalated in the upper part, where lithologies of the Temerfjellet and Carronelva members interfinger.

The Carronelva member was deposited in peritidal to shallow subtidal environments. Restricted, periodically hypersaline marine settings in the northern part of Biinsow Land, grade southwards into mixed restricted and open marine settings. Intermittent subaerial exposure with karst formation occurred. The lower part of the member represents the eastward extension of the upper Trikolorfjellet Member, Ebbadalen Formation. It is equivalent to the "Lower" and "Middle" units of Lslllay (1995).

Terriertjellet member (CP-32)

STATUS OF UNIT: Informal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Temerfjellet: A nunatak close to the type section, in the middle of the glacier Nordenskioldbreen TYPE SECTION:

Stratotype: Urmstonfjellet E, northern Biinsow Land DEPOSITIONAL AGE: Moscovian - early Kasimovian DATING METHOD: Fossils (not documented), stratigraphic relationships REFERENCE(S) FOR AGE: Cutbill & Challinor 1965- OVERLYING UNIT(S): Wordiekammen Formation, locally Fortet member UNDERLYING UNIT(S): Carronelva member; locally Hult- berget Formation or Pre-Old Red LATERALLY ADJACENT WT(S): Wordiekammen Formation, Malte Brunfjellet Formation, Fortet member SUPERIOR UNIT: Mmkidjellet Formation OTHER USE OF NAME: None THICKNESS: Up to 300 m MAIN LITHOLOGIES: Carbonate rocks, gypsum LOWER BOUNDARY DEFINITION: The base of the Terrier- fjellet member is defined at the onset of an almost purely carbonate succession defining the member, overlying the uppermost massive sandstone bed of the underlying Carron- elva member. DESCRIPTION: The Temerfjellet member consists of dolomites and subordinate limestones, as well as fine-

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grained limestone conglomerates. It is dominated by mud- supported textures and is commonly unfossiliferous, although the minor fossil content increases northeastwards. Bituminous laminae are abundant in the southeastern part of Biinsow Land. The eastern limit is represented by the lateral transition towards limestone-dominated successions of the Wordiekarnmen Formation (see Minkinfjellet Formation).

In places, the member comprises most of the basin succession, e.g. on Minlunfjellet, Terrierfjellet and Fleming- fjellet, although thin clastic beds of the Carronelva member may underlie it.

In eastern areas, the carbonate rocks are interbedded with marls or marly limestones which o&n give the succession a distinctly stratified appearance. In western areas, they are more massive and rich in flint concretions or flintstone intercalations, as at Petuniabukta. A few gypsum beds are intercalated in their lower part at Petuniabukta, but these rapidly pinch out to the east. Foraminifera have been described by Sosipatrova (1967), while brachiopods, corals, bryozoans and molluscs have been reported by others (Gee et al. 1952; Gramberg et al. 1990, Dallmann & Mmk 1991). Beds with crinoid debris are found on Trikolorfjellet.

The Terrierfjellet member is equivalent to the "Upper unit" of Lnmary (1995), excluding the northwestern dolomite breccia (Fortet member), and to the "Anservika Member" of Dallmann (1993). Most of the member is generally scree- covered. Restricted marine deposits dominate in Biinsow Land, but become more open marine eastwards in Sabine Land ( L m y 1995).

Fortet member (CP-33)

STATUS OF UNIT: Informal FIRST USE OF NAME: McWhae 1953 CURRENT DEFINITION: Dallmann 1993 SYNONYIW(S) AND REFERENCE(S): "Cyathophyllum Lime- stones Breccia": Gee et al. (1952); "Fortet Breccia": McWhae 1953 ORIGJN OF NAME: Fortet (transl. "The Castle"): A mountain edge at the SW corner of the mountain Wordiekammen, NE Biinsow Land TYPE LOCALITY: Fortet, NE Dickson Land DEPOSITION.& AGE: Moscovian - early Kasimovian DATING METHOD: Fossils in adjacent units, stratigraphic relationships REFERENCE(S) FOR AGE: Cutbill & Challinor 1965 OVERLYING UNIT(S): Wordiekammen Formation UNDERLYING UNIT(S): Terrierfjellet member LATERALLY ADJACENT UNIT(S): Terrierfjellet member SUPERIOR UNIT: Minkinfjellet Formation OTHER USE OF NAME: None TAICKNESS: Up to 240 m MAIN LITHOLOGIES: Dolomite breccia LOWER BOUNDARY DEFINITION: First appearance of brecciated dolomites. The boundary is transitional; lithologies interfinger with those of the Temerfjellet member. DESCRIPTION: The Fortet member is characterised by a carbonate breccia occurring in the northwestern part of Biinsow Land. The breccias grade southwards into evapo-

Fig. 2-51: The dolomite breccias of the Fortet &ember form peculiar pinnacles and towers on the mountain sides at Petuniabukta, here at Fortet. Photo: W.K. Dallmann

rites and eastwards into dolomites, both assigned to the Temerfjellet member. Breccia clasts range in diameter from a few cm to more than a metre (occasionally) and form high breccia porosity. The member is extensively scree-covered.

The breccias may locally represent in-situ brecciated bedrock, but consist of distinctly transported clasts in other places. Both grain-supported and matrix-supported varieties occur, with a micritic carbonate matrix. The rocks show different degrees of cementation, so that well-cemented parts tend to form cli* and pinnacles, while the 'surrounding material is removed by erosion (Fig. 2-5 1). The exposures on the southern side of Fortet, near Rudmosepynten, are well suited as a type section for the Fortet member, though it has not been logged. In this locality the member is ca. 240 m thick, which is approximately its maximum observed thickness.

Different explanations have been indicated for the origin of the breccia, including solution collapse (McWhae 1953; Sundsbnr 1982, unpubl.; Llannry 1995), subsurface sliding associated with late Jurassic faulting (Cutbill & Challinor 1965), and synsedimentational earthquake activity (Dall- mann 1993). L,

CYMUESBREEN SUBGROUP (CP-34)

STATUS OF UNIT: Formal RRST USE OF NAME: Dineley 1958 CURRENT DEFINITION: Here; rank revised to 'subgroup'. The name was introduced by Dineley (1958) as a group name.

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SYNONYIW(S) AND R E F E ~ c E ~ s ) : None ORIGIN OF NAME: Char le~km: A in O%ar 11 h d , central western Spitsbmgen TYPE AREA: St. Jo~~QoLden WeSteZn Spits- bergen STRUCTURAL SETTING: St. J O I W ~ O T L ~ Trough DEPOSITIONAL AGE: - WfWWi'hl OVERLYING =(S): D~&SQU Lazld 8 m u p UNDERLYING UNIT(S): Bilit@orden Group, locally Pre-Old Red SUPERIOR UNIT: Gipddm C h a p OTHER USE OF NAME: W- THICKNESS: Up to ca. 650 m MAIN L~THOLOGIES: Ccmgbimrate, sandstone, shale DESCRIPTION: Charlesbrm Subgoup is a coUectiw name for the four formations (Erraggertinden, Scheteligfjellet, Petrellskaret and Thnkmten formations) assigmd to the (roughly) Basbkirian-Moa&an fiJl of the St. Jonsfjorden Trough. See the individual formations. The subgroup shows a stratigraphic development from redbed to carbonate environments (Fig. 2-52).

DISTRIBUTION SHOWN ON FIG(s).: 2-08 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Braggertinden: Highest peak of Brmger- fjellet, BrsggerhalvBya TYPE SECTION (FIG. 2-54): Stratotype: Braggerfjellet S, Broggerhalvaya STRUCTURAL SETTING: St. Jonsftorden Troueh . - W

DEPOS~IOML AGE: BasWan (upper part of formation). Earlier suggestions: Early Carboniferous (Holtedahl 1913); Devonian (Orvin 1934, based on poorly preserved fish fragments) DATING METHOD: Fossils, e.g. conodonts*

i &FE:RENCE(S) FOR AGE: Cutbill & Challinor 1965 (no ~ O C -

umentation); *Buggisch et al. (in press) OVERLYING UNIT(S): Scheteligfjellet Formation UNDERLYWG UNIT(S): Pre-Old Red, Orustdalen Formation SZTPERIOR mm Charlesbreen Subgroup ( ~ E E R USE OF NAME: None THICKNESS: 13-360 m, ca. 355 m in stratotype (?max. 290 m according to Ludwig 1991, mpubl.) MAIN LITHOLOGIES: Conglomerate, sandstone, shale

Fig. 2-52: The mountain Thkanten near St. Jonsfjorden, showing the LOWER BOUNDARY D E ~ T I O N : The Brraggertindm F o m - (hrlesbreen Subgroup of the St. Jonsfjorden Tmugh with the shale- tion rests unconfonnably on folded Precambrian basement, sandstone succession of the Petrellskaret Formation and the overly- locally on sandstows of the Formation. hg, sandstone-dominated Thkanten Formation. Photo: E.F! Johan- DESCRIPTION: The Br&hertjnden Fomtion comprises re4 nessen yellow and brown congl-tes, red (some white and

grey) micaceous sandstones and red sandy shales in h-

Fig. 2-53: A fluvial conglomerate with intern-, crossbedded send- stones fnnn the Braggertinden Formation. Type section at Bnagger- gellet. Photo: I? Ludwig

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Scheteligljellet Fmation

(Mosmvian)

l

z 2

; 2 0 !=4 Q.:: W '-

L .z 2 - x W Z X Q 0 : E m g m ; * W ::

Q p: m

- m clsivf f rncvcg p

Fig. 2-54: Stratigraphic section CP-35 StmtotVpe for: Bwggertinden Fonnation LocuIip: B&fgg,esSjellet S Reference: (sjeikg 1984 (unpubl.), redrawn from Orvin 1934

Scheteligfjelle~ Format ion

NORTHWESTERN C > SVALBARD

D I S T ~ U T I O N SHOWN ON FIG(s).: 2-08 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): Cutbill & Challinor (1965) defined the unit as a member of the 'Wordenskiold- breen Formation". ORIGIN OF NAME: Scheteligfjellet: A mountain on Brrgger- halvsya TYPE SECTION (FIG. 2-56): Stratotype: Traudalen, Brnrggerhalvlaya The stratotype was originally defined at northeastern Scheteligfjellet (Cutbill & Challinor 1965), but no documentation is available. STRUCTURAL SETTING: St. Jonsfjorden Trough DEPOSITIONAL AGE: Early - Middle Moscovian DATING METHOD: Fossils, e.g. fusulinids REFERENCE(S) FOR AGE: Holtedabl 19 1 1, 19 13; Cutbill & Challinor 1965 (no documentation); Buggisch et al. (in press) OVERLYING UNIT(S): Wordiekammen Formation UNDERLWG UNIT(S): Bmggertinden Formation SUPERIOR m: Charlesbreen Subgroup C ~ X W R USE OF NAME: None THICKNESS: 0-120 (?150) m, 105 m in stratotype MAIN LITHOLOGIES: Carbonate rocks, calcareous sandstone, conglomerate and sedimentary breccia LOWER BOUNDARY DEFINITION: The boundary of the carbonate-dominated Scheteligfjellet Formation with the un-

quent alternations. The upper part is less conglomeratic and thin limestones are interbedded with the clastic sediment~. The sediments probably represent arid alluvial fan systems which, according to Barbaroux (1967), built out Fig. 2-55: A multithecopore limestone typical for the Scheteligfjellet towards the west (Fig. 2-53). The upper boundary is de- Formation, here photographed in the basal part of the type section in fined by the transition into the thick limestones of the Traudalen. Similar multithecopore colonies have also been observed Scheteligfjellet Fomaion. in the Wordiekammen Formation. Photo: K. SaaIrnann

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Wnliekamrnen Formation

( M o s c o m

z 0 Y

e 4 2

o r 0 w r n h U

'-

I . : w - 2 0 4 0 " r l

'

m 0 5 W = h

0 0 Y

rl W H W

m U m

Breggertinden Formation x q y r

yellowish- brown

red

grey

black

grey grey red O-a*oX grey

Fig. 2-56: Stratigraphic section CP-36 Stmtotype for: Scheteligfjellet Formation Locality: Traudalen

Reference: Saalrnann, K. 1995 (unpubl.)

derlying red clastics of the Brnggertinden Formation is an interfingering surface. The boundary is defined at the onset of dominant carbonate lithologies in each place. On NW Br~ggerhalvoya, a 5- 10 m thick, polymict conglomerate with a yellowish, dolomitic matrix, infilling topographic relief in the Orustdalen Formation, constitutes the underlying Brnggertinden Formation. Where present, a bluish-grey Multithecopora (coral) limestone be4 which is lithologically distinctive, is defined as the basal layer of the Scheteligfjellet Formation (Ludwig 1991, unpubl.; Fig. 2- 55). It may locally be replaced by reef facies limestones (Kmrstranda). D E S C ~ O N : The main lithology consists of grey or dark grey micrites or biomicrites (interpreted as shelf carbonates), often interbedded with greenish-grey or reddish calcareous sandstone, siltstone and shale. Yellow-weathering dolomites occur, and occasionally conglomerates. A 2-3 m coral biostrome is locally observed above the basal conglomerate. Intraformational or solution breccias, up to 50 m thick, with fragments (MPS 10 cm) of grey and yellow dolomite and limestone, are also observed. The carbonate rocks contain white or yellow cherty nodules and calcite- or quartz-filled vugs. The formation contains abundant marine fauna, including brachiopods, fusulinids, corals, crinoids and bryozoans, less frequently gastropods, trilobites, ostracods and fish remains. Especially in the lower parts of the formation, many fossils are preserved in red chert; chert may also occur in nodules and thin layers.

The upper boundary is transitional to the pure carbonates of the Mmebreen Member. It is taken at the first appearance of massive, thick, grey limestones with a distinct content of silica/dolomite nodules typical for the Wordiekammen For- mation. Locally, e.g. at Strypbekken, the first massive beds containing abundant silica nodules are dolomites, which then define the formation boundary. Above the boundary, no more siliciclastic beds occur (Saalmann 1995, unpubl.; Sidow 1988, unpubl.).

DISTRIBUTION SHOWN ON E'IG(s).: 2-07,2-08 IIIIIII(III STATUS OF UNIT: Formal

M W P G B dsivf f mcvcg pcbb

FIRST USE OF NAME: D.L. Dineley in: Gobbett 1963 CURRENT DEFINITION: Cutbill & Challinor 1965

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strongly tectonised

black

I black

black

I5 a

calcrete

I5 calcrete A

calcrete

calcrete

Fi. 2-57: Stratigraphic section CP-37 Unit stratotype for: Petrellskaret Formation Locality: Petrellskaret, Vegardfjella Reference: Gjelberg 1 984

' TArnkanten Formation

2

o - = W

LL ,

Z

O m K

a 0

NORTHWESTERN n SVALBARD

TBrn

ii 3

C

.- L

.-

"2

m

SYNONYM(S) AND REFERENCE(S): "Petrelskardet Shale For- DISTRIBUTION SHOWN ON PIG(s).: 2-08 mation": Cutbill & Challinor (1965) STATUS OF UNIT: Formal ORIGIN OF NAME: Petrellskaret (transl. "Petrel Notch": A FIRST USE OF NAME: Dineley 1958 mountain saddle in the Vegardfjella massif, inner St. Jons- CURRENT DEFINITION: Cutbill & Challinor 1965

fjorden. Until 1991, the place name was only known from the geological literature. The Place Name Committee for Svalbard accepted the place name in 1991 to allow formal use of the formation name, but with the Nynorsk spelling (PetreEIsKaret) obligatory for place names in Svalbard. TYPE SECTION (FIG. 2-57): Unit stratotype: Petrellskaret, Vegardfjella STRUCTURAL SETTING: St. Jonsfjorden Trough DEPOSITIONAL AGE: ? B a ~ E a n DATING METHOD: I n h c t from fossil age of underlying and overlying formations REFERENCE(S) FOR AGE: Cutbill & Challinor 1965 OVERLYING UNIT(S): Thkanten Formation UNDERLYING UNIT(S): Vegardfjella Formation SUPERIOR UNIT: Charlesbreen Subgroup OTHER USE OF NAME: None THICKNESS: ca. 360 m in type area MAIN LITHOLOGIES: Interbedded shales and sandstones, predominantly red-coloured LOWER BOUNDARY DEFINITION: NO exposure of the lower boundary has been found, but there is suggested a conformable contact on thinly bedded sandstones and shales of the Vegardfjella Formation (Dineley 1958).

calcrete Tn-a

DESCRIPTION: The Petrellskaret Formation consists mainly caicrete offed and blacwgrey shales, interstratified with thin, red, cabrete grey and white sandstone beds and red calcretes. The only

prominent sandstone horizon (7 to 20 m thick beds) occurs in the middle of the formation. The upper part of the formation shows a very thick accumulation of black shales.

Thin evaporite and limestone beds are present in the lower part of the red shale succession, while in the black shales at the top of the formation, a bone-bed horizon has been observed.

The boundary with the overlying Thkanten Formation is conformable, and no major timebreak appears between the two formations. The stratigraphic contact between the forma-

calcrete tions is, however, not exposed at the type locality because of

~$ca~orete small thrust faults. The boundary is placed at the base of cliff-

%%? forming thick sandstones of the Thkanten Formation.

calcrete The various lithofacies are interpreted as fluvial channel sandstones, red fine-grained floodplain and coastal plain deposits. Black shales and fine-grained sandstones were deposited in lagoons, bays or lakes (?).

l/llllllr/l clslvf f mcvcg pcbb

kanten Formation (bloswvian)

z 0 CI

W

d

2 g o

'-'a

b

W

~4

* cl

cl

F4 W

W

P,

unlts Ym

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Fig. 2-58: Stratigraphic section CP-38 Stmtotypefor: Thkanten Formation Locality: Thkanten Vegardfjella Reference: Johannessen, Gjelberg and Olaussen,

in Johannessen et al. 1984 (unpubl.)

e black

Wordiekammen Formation

red --V, yellow red

red

8 W

III YW

Ill I I

yellow

red Isgreen II

v red v v red m

clsivf f mcvcg pcbb

clsivf f mcvcg pcbb

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SYNONYM@) AND REFERENCE(S): None ORIGIN OF NAME: TArnkanten (transl. "Tower Edge": A mountain edge in the Vegardfjella massif, inner St. Jons- fjorden. TYPE SECTION (FIG. 2-58): Stratotype: TArnkanten, Vegardfjella STRUCTURAL SETTING: St. Jo~lsfjorden Trough DEPOSITIONAL AGE: Early - Middle Moscovian DATING METHOD: Fossils, fnainly brachiopod~. %O marine bands comprising black shales with grey argdlaceous and fossil rich limestones are interbedded with the TArnkanten sandstones. The fauna consists of abundant spiriferid and stropheodontid brachiopods, but other brachiopods, small pelecypods, corals and a single trilobite have also been found. The brachiopods correlate closely with those of the Scheteligfjellet Formation, suggesting that the TAmkanten Formation probably is of Early and Middle Moscovian age (Gobbett 1963). REFERENCE(S~P'OR AGE: Gobbett 1963 OVERLYING UNIT@): Wordiekammen Formation UNDERLYING UNIT@): Petrellskaret Formation SUPERIOR UNIT: Charlesbreen Subgroup OTHER USE OF NAME: None THICKNESS: 247 m in stratotype MAIN LITHOLOGIES: Multicoloured sandstone succession with interbedded shales, intercalated carbonate beds in upper Part LOWER BOUNDARY DEFINITION: The stratigraphic contact between the Petrellskaret and TArnkanten formations is normally not exposed because of small thrust faults, but seems to be conformable. The boundary is placed at the base of cliff-forming thick sandstones of the Thkanten Formation over the shale-dominated underlying succession. DESCRIPTION: Lithologies are multicoloured (red, grey, green, yellow, white) sandstones and minor conglomerates, interbedded with red shales containing calcareous nodules and black shales with thin limestone beds. These black bands are fossil-rich marker beds and separate the formation into at least three sections. The special development of the Jutulslottet member (upper part of the formation) comprises yellow dolomitic sandstones and dolomite-limestone beds.

The boundary with the overlying Wordiekammen Forma- tion is a sharp lithological break. The contact at the type locality in Vegxdfjella is a thrust fault plane. The upper part of the formation, the Jutulslottet member, is apparently much thinner here than at its type locality at Jutulslottet.

The depositional environments were intertidal to deltaic, comprising braided stream channels, mouth bars, lagoons, tidal flats, beaches, marine sands (?tidal) and open marine black shales and carbonates. Increasing marine influence is suggested in upper parts of the formation.

Jutulslottet member (CP-39)

STATUS OF UNIT: Informal FIRST USE OF NAME: Here, after Johannessen et al. 1984 (unpubl.) CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Jutulslottet (transl. "The Giant Castle"): A nunatak in Oscar I1 Land, south of St. Jonsfjorden TYPE SECTION (FIG. 2-60): Stratotype: Jutulslottet, Inner St. Jonsfjorden, Oscar I1 Land DEPOSITIONAL AGE: Early - Middle Moscovian DATING METHOD: Fossils, mainly brachiopods. See TArn- kanten Formation REFERENCE(S) FOR AGE: Gobbett 1963 OVERLYING UNIT@): Wordiekammen Formation UNDERLYING UNIT(S): TAmkanten Fm., lower part SUPERIOR UNIT: TArnkanten Formation OTHER USE OF NAME: None THICKNESS: Up to 100 m MAIN LITHOLOGIES: Multicoloured sandstones and subordinate shales, intercalated carbonate beds LOWER BOUNDARY DEFINITION: The lower boundary is transitional, from the thickly bedded sandstones in the lower part of the TArnkanten Formation to the thinner sandstone beds, interbedded with carbonates and thin shale beds of the Jutulslottet member. The boundary is placed at about 150 m level in the type section at Jutulslottet. DESCRIPTION: The Jutulslottet member comprises multicoloured (red, grey, yellow, white) sandstones and dolomitic sandstones, interbedded with red and black shales as well as grey, black and yellow limestones and dolomites (Fig. 2- 59).

The upper boundary is not exposed in the type locality at Jutulslottet. At Vegardfjella, the boundary is a thrust contact.

The depositional environment reflects rapidly interchang- ing shallow marine carbonates, (?tidal) sandstones, lagoons and shoreface sections with delta plain to distal alluvial fan deposits, including paleosols.

Fig. 2-59: The mountain Jutulslottet near St. Jomtjotden, showing the carbonate-bearing upper part of the sandstone-dominated Ti.Lmkan- ten Formation, the Jutulslottet Member, reflecting the initial marine iduence in this part of the St. Jonsfjorden Trough. Photo: E.P. Jo- hannessen

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The lower half of the nunatak Jutulslottet (lower part of low angle fauns TAmlcanten Fm.) has not yet been logged, and a correlation red between the Tiirnkanten and Jutulslottet sections is ques-

tionable. Different levels of thrusting complicate a possible low angle fauWs correlation. The member therefore has informal status. 15s red -0 A TRESKELEN SUBGROUP (CP-40)

redlgreen mottled

yellow

---red fossils

red mottled yellow red mottled yellow red mottled

white

grey and redish

black

units -

dsivf f mcvcg pcbb

Fig. 2-60: Stratigraphic section CP-39 Shultotype for: Jutulslottet member Locality: Jutulslottet

Reference: Johannessen et al. 1984 (unpubl.)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Treskelen (transl. "The Threshold"): A peninsula in the inner part of Hornsund TYPE AREA: Inner Hornsund, southern Spitsbergen STRUCTURAL SETTING: Inner Homund Trough DEPOSITIONAL AGE: Bashkirian - Early Permian OVERLYING UNIT@): Dickson Land Subgroup, Tempel- fjorden Group; locally on Serrkapp-Hornsund High: Sassen- dalen Group UNDERLYING UNIT@): Billefjorden Group, locally Pre-Old Red SUPERIOR UNIT: Gipsdalen Group OTHER USE OF NAME: None THICKNESS: Up to 750 m MAIN LITHOLOGIES: Conglomerate, sandstone, subordinate shale DESCRIPTION: Treskelen Subgroup is a collective name for the two formations (Hyrnefjellet and Treskelen fms.) assigned to the Bashkirian-Early Permian fill of the Inner Hornsund Trough (Fig. 2-61). See the individual formations.

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DISTRIBUTION s m ON FIG@).: 2-06,2-07 STATUS OF UNIT: Formal FIRST USE OF NAME: Birkenmajer 1959 CURRENT DFFINITION: Birkenmajer 1964 SYNONYM(S) AND REFERENCE(S): Hyrnefjellet "beds": Birkenmajer 1959, 1964. The unit was first ranked as a formation by Cutbill & Challinor (1965). ORIGIN OF NAME: Hyrnefjellet (transl. "Corner Mountain"): A mountain at the northern side of the inner part of Horn- sund, southern Spitsbergen TYPE SECTION (FIG. 2-63): Stratotype: Hyrnefjellet South, Adriabukta STRUCTURAL SETTING: Inner Hornsund Trough DEPOSITIONAL AGE: Bashkirian - Moscovian (?Kasimovian) DATING METHOD: Indirect. The age is interpreted by correlation with synsedimentational tectonism suggested from facies development. The overlying Treskelodden Formation contains latest Carboniferous and Early Permian fossils. REFERENCE(S) FOR AGE: Gjelberg & Steel 1981 OVERLYING UNIT@): Treskelodden Formation; locally on Smkapp-Homund High: Vardebukta Formation UNDERLYING UNIT@): Adriabukta Formation, Hornsund- neset Formation, ?Sergeijevfjellet Formation, Pre-Old Red SUPERIOR UNIT: Treskelen Subgroup OTHER USE OF NAME: "Hyrnefjellet Formation" (PEelina 1983): Part of the Triassic Bravaisberget Formation (M-19) THICKNESS: Up to 600 m, ca. 235 m in stratotype

MAIN LITHOLOGIES: Conglomtes and sandstones, predominantly red LOWER BOUNDARY DEFINITION: South of Hornsund, the base is marked by the prominent change from grey quartzites and dark grey shales of the Billefjorden Group to red and multicoloured clastics of the Hymefiellet Formation. North of Hornsund, similar multicoloured clastics of the Hyrnefjellet Formation overlie grey shales and smdstones of the folded Adriabukta Formation with an a n p h unconfonnity. DESCRIPTION: The Hyrnefjellet Formation occurs along the West Spitsbergen Foldbelt from north of Hornsund to Msnslsen on Ssrkappfonna. Stratigraphic and lithological descriptions have been published previously only from north of Hornsund, where the formation is ca. 270 m thick, and where only the upper member is present. The thickness reaches more than 600 m at Knattberget and Hjelmen, where a preliminary subdivision into three members, the Hjelmen, Brattberget and Bladegga members, is made. North of Hornsund, exposures of the Hyrnefjellet Formation (270 m) seem to belong entirely to the Brattberget member.

The predominant lithologies in the type area (Hymefjellet and Treskelen) are red, frequently graded gravel- to boulder- size conglomerates. They may form channel fills and laterally interfinger with sandstones. The matrix is sandy with detrital micas. Light, fairly well-sorted, medium-grained quartzitic sandstones occur in places. South of Hornsund, a grey, unstructured conglomerate with angular to subangular quartz, quartzite and subordinate chert boulders occurs (Bladegga member). At the lowermost stratigraphic level, also south of Hornsund, multicoloured sandstones with occasional shales or conglomerates (Hjelmen member) occur (Fig. 2-62).

The facies of the Hymefjellet Formation - at least the Brattberget member - reflect alluvial, distributary channel and interdistributary bay (overbank deposits) environments (Birkenmajer 1984a). Climatic conditions were warm and arid. All detrital material is derived fiom nearby source

Fig. 2-61: The mountain Hyrnefjellet at Homsund, showing the folded Treskelen Subgroup of the Inner Homsund Trough with the redbeds of the Hyrnefjellet Formation and the calcareous clastics of the

eskelodden Formation. Photo: W.K. Dallmann

X

ta I ... Fig. 2-62: Carboniferous succession at the mountain Hjelmeg

Helmet") Smkapp Land. Grey sandstones of the Hornsundneset For- mation build up the lower half of the exposed strata, while the higher levels show the Hjelmen member (multi-coloured clastic rocks below the large snow field) and the conglomeratic Brattberget member (summit and right part of mountain) of the Hyrnefjellet Forma- tion. Photo: W.K. Dallmann

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Fig. 2-63: Stratigraphic section CP-41/43 Smtorype for: Hymefjellet Formation, Brattberget member

Locality: Hymefjellet S Reference: Gjelberg & Steel 1981

rocks (Siedlecka 1968), i.e. the Proterozoic basement, De- vonian and Early Carboniferous sedimentary rocks of the Samarinbreen area. The sudden upward coarsening at the base of the Brattberget and Bladegga members is thought to indicate synsedimentational fault activity along the Inner Hornsund Fault Zone (Gjelberg & Steel 1981).

MPS = g MPS = 6 MPS = 3 MPS = 5 MPS = 7 MPS = 3

MPS = 4 MPS = 2

MPS = 8 Hjelmen member (CP-42) MPS = 3 MPS = 4 MPS = l 5 STATUS OF UNIT: Informal MPS = 4 FIRST USE OF NAME: Dallmann et al. 1993 MPS = l 3 CURRENT DEFINITION: Dallrnann et al. 1993

SYNONYM(S) AM) REFERENCE(S): None ORIGIN OF NAME: Hjelmen (transl. "The Helmet"): A nunatak in Sarkapp Land TYPE LOCALITY: Hjelmen, Smkapp Land ,

MPS = 2 DEPOSITIONAL AGE: Bashkirian - Moscovian MPS = 3 DATING METHOD: Indirect, stratigraphic relationships.

See Hyrnefjellet Formation MPS = 3 REFERENCE(S) FOR AGE: Gjelberg & Steel 1981

OVERLYING UNIT(S): Brattberget member MPS=7 UNDERLYING UNIT(S): Hornsundneset Formation MPS = 3 SUPERIOR UNIT: Hyrnefjellet Formation MPS = 2 OTHER USE OF NAME: None

THICKNESS: ca. 100 m MA~N LITHOLOGIES: Multicoloured sandstones LOWER BOUNDARY DEFINITION: See Hyrnefjellet Formation,

MPS = 8 south of Hornsund

MPS = 3 DESCRIPTION: The Hjelmen member consists of multi- MPS = 3 coloured sandstones, with subordinate beds of pebble con-

glomerates and sedimentary breccias. The best accessible MPS = 3 section is at Hjelmen, where it is ca. 100 m thick (Fig. 2-64).

It thins northward and pinches out at Tsjernajafjellet, while the southernmost exposure has been observed on the southern ridge of Knattberget. Different sandstone varieties alter-

MPS = 5 MPS = l 7 nate: MPS = 7 1. Coarse- to medium-grained, red, texturally and compo- MPS = 11 sitionally immature sandstones with a hematite matrix, oc- MPS = 4 casionally with pebbles of sedimentary, probably Devonian, MPS = 9 MPS = 3

MPS = 7 MPS = 4 MPS = 2

I MPS = 7 MPS = 4

MPS = 8 MPS = 2 MPS = 14

I . - . . , - clsivf f mcvcg pcbb I

Fig. 2-64: The multicoloured clastic succession of the Hjelmen member on the western slope of the mountain Hjelmen (Serkapp Land), mainly composed of red and grey sandstones, light quartzites and pinkish sedimentary breccias. Photo: W.K. Dallmann

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2. medium- to fine-grained, light grey or white, impure quartzites with an irregular cross lamination, abundant zircon grains and, locally, a secondary lamination of hematite matrix or a spotted appearance by weathered aggregates of iron minerals; I

3. very fine-grained, grey, immature sandstones with cross-lamination and wave ripple marks;

4. sedimentary breccias with a pink, immature sandstone matrix and pbbles of sedimentary rocks (some are sandstones of the Adriabukta Formation);

5. fine-grained, red, immature, carbonate-cemented sandstones with scattered grains of fine quartz gravel (Knatt- berget). -,

Brattberget member (CP-43)

STATUS OF UNIT: Inf0rmal FLRST USE OF NAME: Dallmann et al. 1993 CURRENT DEFINITION: Dallmann et al. 1993 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Brattberget (transl. "Steep Rock"): A nunatak in S0rkapp Land TYPE SECTION (FIG. 2-63): Stratotype: Hyrnefjellet South, Adriabukta, Hornsund DEPOSITIONAL AGE: Bashkirian - Moscovian (?Kasimovian) DATING METHOD: Indirectly firom stratigraphic relations. See Hyrnefjellet Formation RE~RENCE(S) FOR AGE: Gjelberg & Steel 1981 OVERLYING UNIT(S): Treskelodden Formation UNDERLYING UNIT(S): Blgdegga or Hjelmen members, Adriabukta Formation, Hornsundneset Formation, Re-Old Red SUPERIOR UNIT: Hyrnefjellet Formation OTHER USE OF NAME: None THICKNESS: Up to 425 m, ca. 235 m in stratotype MAIN LITHOLOGIES: Red conglomerates and subordinate sandstones LOWER BOUNDARY DEFINITION: %X Hyrnefjellet Formation, north of Hornsund. South of Hornsund, there is a distinct onset of coarse, red conglomerates above the finer-grained lithologies of the other members of the Hyrnefjellet Forma- tion. DESCIUPTION:T~~ Brattberget member occurs along the entire outcrop of the Hyrnefjellet Formation, extending from north of Hornsund (northernmost exposure at Zittelberget, Dallmann et al. 1990), to Msnsilsen on Ssrkappfonna. Thickness values range from ca. 350 m at Brattberget, ca. 425 m at Knattberget to ca. 275 m at Steinhatten. The unit passes laterally into the Bladegga member (see below) in the Chomjakovbreen area.

Lithologies are mainly gravel- to boulder-size conglomerates, clast-supported, red (rarely grey or very light) and frequently graded (single or multiple). They may form channel fills and laterally interfinger with sandstones (Fig. 2-65). The matrix is sandy with detrital micas. The rocks are often silica-cemented. The boulders or pebbles are angular to subangular and consist of vein quartz and feldspar as well as metamorphic quartzites of many colours, cherts, red, grey and multicoloured sandstones (probably derived partly from

Fig. 2-65: A typical detail of the Brattberget member, consisting of red, coarse, alluvial fan conglomerates (upper cliffl, light and grey sandstones and red siltstones (overbank deposits). Adriabukta, Hornsund. Photo: W.K. Dallmann

the Hjelmen member and lower parts of the Brattberget member). Sandstone boulders are confined to coarse, red conglomerates, while fine-grained conglomerates and grit- stones have quartzitic pebbles.

Many of the sandstones are also texturally and compositionally immature, red or grey, with mixed silica, fermgi- nous, chlorite and, occasionally, carbonate cements. Scat- tered quartz gravel or pebbles occur. Light, fairly well-sorted, medium-grained quartzitic sandstones occur in places.

Bladegga member (CP-44)

STATUS OF UNIT: Informal FIRST USE OF NAME: Gjelberg & Steel 1981 CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): Bladegga "Formation": Gjelberg 1984 (unpubl.) ORIGIN OF NAME: Bladegga (transl. "The Blade Edge"): A nunatak in Sankapp Land TYPE SECTION (FIG. 2-66): Stratotype: Bladegga, Smkapp Land DEPOSITIONAL AGE: Bashkirian - Moscovian (exact age very uncertain) DATING METFIOD: Indirect, stratigraphic relationships. See Hyrnefjellet Formation REFERENCE(S) FOR AGE: Gjelberg & Steel 198 1 OVERLYING UNIT(S): Brattberget member, Vardebukta For- mation UNDERLYING UNIT@): Hornsundneset Formation, locally ?Sergeijevfjellet Formation SUPERIOR UNIT: Hyrnefjellet Formation &TIER USE OF NAME: None THICKNESS: Up to >350 m, ca. 260 m in stratotype MAIN LITHOLOGIES: Conglomerates LOWER BOUNDARY DEFINITION: See Hyrnefjellet Formation, south of Hornsund. At Bladegga (type section), the base of the Bladegga member is defined at the base of massive, light-coloured, quarkitic sandstones that are not typical for other members of the Hyrnefjellet Formation.

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.Vardebukta Formation (Induan)

l. P S

B D

8

2 ; 0 2 C I o

P

: < : .- X m

: H 0 0 V)

0 D.

= F -

W = J .: 4

3 .E W

0:;

= : m * w m z ;

w a - * P

z z a 0 10

DD

m M P

-0 10 a -

0 m

F-- 2 2 B 0 k

= F m W

MPS = 5 grey

MPS = 18 red and green

red MPS = 12

red

red MPS = 15

h % Y 5 MPS = 5

MPS = 2

white

MPS = 3

I

I I

/poorly exposed I I

I I

I

MPS = 4

MPS = 2 white

MPS = 4

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Hornsundneset

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Fig. 2-66: Stratigraphic section CP-44 Shrztotype for: Bladegga member Locality: Bladegga Reference: Gjelberg 1984 (unpubl.)

DESCRIPTION: Most of the Bladegga member is a grey, mostly unstructured conglomerate with angular to subangular quartz, quartzite and subordinate chert boulders of up to 30 cm size. It is at least 350 m thick at Mannsfeldkamrnen (Bautaen) where it laterally replaces the Brattberget member. The two members are observed to interfinger at Meran- pynten and Konglomeratodden (a peninsula east of Meran- pynten), which results in intercalated sandstones. The Bladegga member thins at Bladegga below the Brattberget member and pinches out farther south.

Both Bautaen and Bladegga form spectacular mountain crests that illustrate the weathering properties of this lithology.

DISTRIBUTION SHOWN ON FIG@).: 2-06,2-07 STATUS OF UNIT: Formal ~ R S T USE OF NAME: Birkenmajer 1959 CURRENT DEFINITION: Birkenmajer 1964 SYNONYM(S) AND REFERENCE(S): Treskelodden "beds": Birkenmajer 1959,1964. The unit was first ranked as a formation by Cutbill & Challinor (1965). ORIGIN OF NAME: Treskelodden (transl. "Threshold Point"): A cape at the southern end of the Treskelen peninsula, inner Hornsun4 southern Spitsbergen TYPE SECTION (FIG. 2-68): Stratotype: Treskelen, creek IV STRUCTURAL SETTING: Inner Homsund Trough DEPOSITIONAL AGE: Latest Carboniferous to Early Permian DATING METHOD: Fossils, mainly brachiopods and foraminifera REFERENCE(S) FOR AGE: Liszka 1964; Birkentmjer & Czarniecki 1960. OVERLYING UNIT@): Gipshuken Formation, Kapp Starostin Formation; locally on Smkapp-Hornsund High: Vardebukta Formation UNDERLYING UNIT(S): Hyrnefjellet Formation; locally Pre- Old Red SUPERIOR UNIT: Treskelen Subgroup OTHER USE OF NAME: None THICKNESS: Up to 185 m, 98 m in stratotype MAIN LITHOLOGIES: Carbonate-cemented pebble conglomerates and sandstones LOWER BOUNDARY DEFINITION: The lower boundary is defined at the distinct onset of carbonate-cemented, yellowish and grey coloured, clastic lithologies above the redbeds of the Hyrnefjellet Formation. DESCRIPTION: The Treskelodden Formation occurs'from Bellsund to Homund, is absent at Chomjakovbreen south

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Fig. 2-67: The Treskelodden Formation at Austj~kultinden ( S h p p Land): Calcite-cemented, yellowish sandstones and conglomerates interbedded with red shales. Hyrnefjellet Formation conglomerates in the foreground, Triassic deposits in the background. Photo: W.K. Dallmann

of Hornsund (Fig. 2-6 l), but can be traced through a few exposures from Tsjernajafjellet southward to Knattberget in Smkapp Land. The thickness is 185 m at Triasnuten, ca. 100 m at Hyrnefjellet and Treskelen, and 115 m at Aust- joMtinden (Fig. 2-67). Detailed descriptions of the formation are published from north of Homsund (Birkenmajer 1964, 1984b; Czarniecki 1966, 1969; Siedlecka 1968; Fedorowski 1982).

The sediment types are alternating quartz sandstones (mostly calcareous), gravelstones and pebble conglomerates (Fig. 2-67). Sandstones are usually sorted to well-sorted and are both texturally and compositionally more mature than those of the underlymg Hyrnefjellet Formation. Gravel- stones often show graded bedding, and multiply graded units may have either fining- or coarsening-upward trends. Conglomerates form irregularly shaped beds and are poorly sorted. Ripple marks, cross bedding, erosional unconformities and small channels are frequently observed, and mud cracks occur.

An interesting phenomenon is the presence of up to five coral horizons on Treskelen, partly within intercalated dolo-

Triassic Kapp Stamtin

Formation (Artinsian)k

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stones and limestones. The only investigated section south of Hornsund (Austjokultinden) shows only the uppermost of these. Both colonial and solitary rugose and tabulate corals occur, as well as sponges, foraminifera, brachiopods, crinoids, bryozoans, molluscs and trilobite fragments. The Fig. 268: Stratigraphic section CP-45 fauna has been studied by Birkenmajer & Czarniecki (1960) Stmtotypefor: Treskelodden Formation and Czarniecki (1966, Late Carboniferous brachiopods), Locality: Treskelen, "creek W' Liszka (1964, Early Permian foraminifera), Fedorowski Refrence: Birkenmajer 1984b (1964, 1965, 1967, rugose corals), Osmblska (1968, trilobites), Birkenmajer (1979b, rugose corals), Karczewski (1982, molluscs), and Nowinski (1982, tabulate corals).

Siedlecka (1968) and Birkenmajer (1984b) pointed out a distinct "cyclicity" (rhythmicity) of the succession. With the exception of the lower alluvial cycle, the facies passes repeatedly from shallow marine to lagoonal and alluvial envi- rowski (1982) discussed the distinctive redeposited nature ronments (Birkenmajer 1984b). Czarniecki (1966, 1969), of the coral clasts in terms of synsedimentational tectonism however, regarded the formation as entirely marine. Fedo- along basinal margins.

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2. UPPER PALAEOZOIC LITHOSTRATIGRAPH"

DICXSON LAND SUBGROUP (GP-46)

STATUS OF UNIT: Formal h R s ~ USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Dickson Land: The land area between Billefjorden and Dicksonfjorden, central Spitsbergen TVPE AREA: Dickson Land and Biinsow Land, central Spits- bergen STRUCTURAL SETTING: Late Palaeozoic platform of Svai- bard/Barents Sea Shelf DEPOSITIONAL AGE: E& Moscovian to k t h k i a n OVERLYING UNIT@): Tempelfjorden Group UNDERLYING UNIT@): Malte Brunfjellet or HMardbreen formations, Campbellryggen, Charlesbreen or Treskelen subgroups, Billefjorden or h d r & Land groups, Pre-Old Red SUPERIOR UNIT: Gipsdalen Group OTHER USE OF NAME: None THICKNESS: Up to 500 m MAIN LITHOLOGIES: Carbonate rocks and subordinate evaporites DESCRIPTION: Dickson Land Subgroup is a collective name for the two upper formations of the Gipsdalen Group, the Wordiekammen and Gipshuken formations, that are not deposited in individual troughs. The sediments of the subgroup show distinct overlap with the intertrough highs and progressively develop upwards into a laterally continuous shelf sequence.

DISTRIBUTION SHOWN ON FIG@).: 2-07,2-08,2-09,2-10 STATUS OF UNIT: Formal FIRST USE OF NAME: Gee et al. 1952 CURRENT DEFINITION: Here. The formation constitutes the upper and main part of the former "Nordenskioldbreen For- mation", which overlies and onlaps both troughs and highs

of mid-Carboniferous age. Lower, trough-bound members of the "Nordmkib1dbreen Formation" are rslised to formation status (Minkinfjellet and Scheteligfjeilet formations), while the remaining platfonn suacession is referred to the W o r d i e h e n Formation in the sense of Gee et al. (1952). SYNONYM(S) AND REFERENCE(S): - Wordiehmmen limestones: Gee et al. 1952 ORIGIN OF NAME: W o r d i e h e n : A mountain east of Billefjorden, central Spitsbergen TYPE AREA: DicksOn Land and Biinsow Land, central Spits-

STRUCTURAL SETTING: Late Palaeozoic platform of S d - bard/Barents Sea Shelf DEPOSITIONAL AGE: Early Moscovian - Sakmarian DATING METHOD: Fossils, mainly fusulinids REFERENCE(S) FOR AGE: Cutbill & Challinor 1965 (no doe- mentation); Nilsson 1988 (unpubl.) OVERLYING UNIT(S): Gipshuken Formation UNDERLYING UNIT@): Malte Brunfjellet, HMardbreen, Treskelodden, Thhn ten , Scheteligfjellet or Minkinfjellet formations, Billefjorden or An&e Land groups, Pre-Old Red SUPERIOR UNIT: Dickson Land Subgroup OTHER USE OF NAME: None THICKNE~S: Up to ca. 350 m MAIN LITHOLOGIES: Carbonate rocks LOWER BOUNDARY DEFINITION: In Biinsow Land, the base of the Wordiekammen Formation is def-ed at the change from a dolomite-dominated (Minkinfjellet Formation) to a limestonedominated succession. In the western part of the Billefjordm Trough this coincides with the base of the Black Crag Beds, a prominent, dark-coloured limestone unit (see there). Further east, in the Gipsdalen area, it marks the onset of stacked marine limestone intervals with phylloid algal build-ups (Pyefjellet Beds; Piekard et al. 1996), and this sequence is probably situated at a lower level than the Black Crag Beds. In Sabine Land and Ny Friesland, where the M i e l l e t Formation is absent, the base is defined at

Fig. 2-69: The cliff- forming shelf bestones and dolomites of the Wordiekammen Formation make up numerous steep mountain walls on central

<Spitsbergen, here at Langtuna ( k b r e e n , northwestern Sabiie Land). Photo: W.K. Dallrnann

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the onset of platform carbonates over Pre-Old Red or other Carboniferous, predominantly clastic lithologies (Malte Brunfjellet Formation and its probable equivalents).

For more exact local definitions of the formational base , see Mmebreen, Kapitol, Cadellfjellet and Idunfjellet mem-

bers. DESCRIPTION: The Wordiekammen Formation comprises a mainly marine limestone succession (Fig. 2-69). Lithologies are dominant limestones, especially in western areas alternating with dolomites. In western areas there are also subordinate, partly arenaceous or silicified, dolomitic sandstones and grey shales, defining the transitional lower part of the unit. The rocks are fossiliferous, with an abundant fusulinid microfauna and corals, crinoids, bryozoans, brachiopods, sponges, conodonts and ostracods. Bituminous matter, trace fossils and bioturbation are common. A wide range of carbonate build-ups is present, including bryozoan build-ups, phylloid algal build-ups and palaeoaplysinid build-ups.

The Wordiekammen Formation was mostly deposited in open to semi-restricted shallow subtidal marine and restricted intertidal to supratidal environments.

Merebreen Member (CP-48)

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Mmebreen: A glacier on Brraggerhalvarya, probably named after Mme, a coastal region in the middle part of Norway TYPE SECTION (FIG. 2-70): Stratotype: Strypbekken, Br~rggerhalvarya DEPOSITIONAL AGE: ?Moscovian - Gzhelian DATING METHOD: Indirect, stratigraphic relationships. REFERENCE(S) FOR AGE: Cutbill & Challinor 1965 OVERLYING UNIT@): 7)rrellfjellet Member UNDERLYING UNIT@): Scheteligfjellet Formation SUPERIOR UNIT: Wordiekammen Formation OTHER USE OF NAME: None THICKNESS: 159 m in stratotype MAIN LITHOLOGIES: Limestone, dolomite LOWER BOUNDARY DEFINITION: The member shows a transition with the underlying Scheteligfjellet Formation. Its base is arbitrarily defined at the first appearance of massive, thick, grey limestones with a distinct content of silica1 dolomite nodules typical of the Wordiekammen Formation, and above the uppermost, multicoloured sand- and siltstones of the Scheteligfjellet Formation. Locally, e.g. at Strypbekken, the first massive carbonate beds containing abundant nodules are dolomites, which then def ie the formational base. DESCRIPTION: The Mmebreen Member forms the lower part of the Wordiekammen Formation in the St. Jonsfjorden Trough area. The Marrebreen Member has only been described fiom Brraggerhalvwa; almost no data about the facies and subdivisions of the Wordiekarnmen Formation in the St. Jonsfjorden area are found in the geological literature.

The Mmebreen Member is an alternating succession of yellow-weathering dolomites and various limestone types (fossiliferous wackestones, packstones and grahstones). Fossil-rich horizons are almost confimed to wackestones and packstones in the lower to middle part. Concentric, sparitic dolomite and silica conaetions, white, yellow or black, occur abundantly in the dolomites. Limestones show varying degrees of silicification. Limestone breccias occur at a few levels within the middle and upper parts of the formation. Algal build-ups have been described from SE Scheteligfjellet (Sidow 1988, unpubl.; Saalrnann 1995, unpubl.).

The upper boundary with the 'Ijlrrelltjellet Member coincides with the base of the Brucebyen Beds (see there). Where the Brucebyen Beds are lacking or indistinctly developed (northern part of Brraggerhdv!aya), the boundary is poorly expressed, but it is defined by the base of a dark grey to black limestone with dolomite veins (possibly replacing the Brucebyen beds), stratigraphically situated above the upper of two limestone breccias in the type section. It is followed by a monotonous, alternating succession of limestones and dolomites, each a few metres thick (Sidow 1988, unpubl.; Saalrnann 1995, unpubl.).

Kapitol Member (CP-49)

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 'l 965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Kapitol: A mountain between Dickson- fjorden and Ekmantjorden (James I Land), central Spits- bergen TYPE SECTION (FIG. 2-71): Stratotype: Trollfuglfjella, Dicksonfjorden, James I Land The stratotype was originally defined at the northern ridge of the mountain 'Kapitol' (Cutbill & Challinor 1965), but no documentation is available. DEPOSITIONAL AGE: Early Moscovian - Gzhelian DATING METHOD: Fusulinids REFERENCE(S) FOR AGE: Cutbill & Challinor 1965 (no documentation); Nilsson 1988, 1993 (both unpubl.) OVERLYING UNIT@): Qrrellfjellet Member UNDERLYING UNIT@): Hultberget Formation, Billefjorden Group, AndrBe Land Group SUPERIOR UNIT: Wordiekammen Formation HER USE OF NAME: None THICKNESS: 20-125 m, 73 m in stratotype MAIN LITHOLOGIES: Limestone, subordinate dolomite LOWER BOUNDARY DEFINITION: The lower boundary of the Kapitol Member is defined by a distinct angular unconformity, where the member overlies folded Devonian clastic rocks. Where clastic rocks of the Billefjorden Group or the Hultberget Formation underlie the Kapitol Member, the lower boundary is defined by a distinct onset of carbonate rocks, which also form prominent cliffs in the mountain sides. DESCRIPTION: The Kapitol Member forms the lower part of the Wordiekammen Formation on the Nordfjorden High. It

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C A R B O N I F E R O U S M o s c o v i a n ? K a s i m o v i a n - G z h e l i a n

S C H E T E L I G F J E L L E T F O R M A T I O N W O R D I E K A M M E N F O R M A T I O N

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P E R M I A N h

A s s e l i a n - S a k m a r i a n

W O R D I E K A M M E N F O R M A T I O N MsrebreenMember I T y r r e l l f j e l l e t M e m b e r

d 1 K i a e r f j e l l e t b e d s I

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consists of dolomites and limestones, with a thin siliciclastic basal succession; this comprises some few cm to metres of mica-rich, red and green coloured, locally conglomeratic transgressive sandstones. Dominant limestone types are packstone and grainstone (Dons 1983, unpubl.).

The sediments were mainly deposited on a shallow, open marine, high-energy platform during the progressive transgression of the Nordfjorden High from the west-southwest (Dons 1983, unpubl.). The depositional area was periodically subaerially exposed.

Cadellfjellet Member (CP-50)

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Cadellfjellet: A mountain east of Bille- fjorden, central Spitsbergen TYPE SECTION:

Stratotype: Boltonbreen, Biinsow Land The stratotype was originally defined at the western ridge of Cadellfjellet (Cutbill & Challinor 1965), but no docurnenta- tion is available. DEPOSITIONAL AGE: Late Moscovian - late Gzhelian DATING METHOD: Fwulinids REFERENCE(S) FOR AGE: Nilsson 1993 (unpubl.) OVERLYING UNIT(S): T~ellfjellet Member UNDERLYING UNIT@): Minkinfjellet Fokmation, Malte Brunfjellet Formation SUPERIOR UNIT: Wordiekammen Formation OTHER USE OF NAME: None THICKNESS: 90-250 m MAIN LITHOLOGIES: Limestone, dolomite LOWER BOUNDARY DEFINITION: In Biinsow Land, the base of the Cadellfjellet Member is defined at the transition from a dolomite-dominated (Minkinfjellet Formation) to a limestone-dominated succession. In the western part of the Billefjorden Trough this coincides with the base of the Black Crag Beds, a prominent, dark-coloured limestone unit (see there). Further east, in the Gipsdalen area, it marks the onset of stacked marine limestone intervals with phylloid algal build-ups (Pyefjellet Beds; Pickard et al. 1996), and this succession is probably situated at a lower level than the Black Crag Beds. In Sabine Land and Ny Friesland, where the M i e l l e t Formation is absent, the base is defined at the onset of platform carbonates over the Hecla Hoek basement or predominantly clastic lithologies (Malte Brunfjellet Formation and its probable equivalents). DESCRIPTION: The Cadellfjellet Member forms the lowermost part of the Wordiekammen Formation in the Bille- fjorden Trough area and to the east of it, on eastern Spits- bergen. Its lower part is dominated by limestones (Black Crag, Pyefjellet and Gemtbreen beds), while the upper part

Fig. 2-71: Stratigraphic section CP49 consists of dolomites, limestones .and sandy carbonates. Stmtotype for: Kapitol Member Concentric, siliceous-dolomitic concretions are common Locality: Tmllfuglfjella (Fig. 2-72). Refemncnce Nilsson 1993 (uapubl.) based on Skaug 1982 (unpubl.) The top of the Cadellfjellet Member is defined by the base

and Dons 1983 (unpubl.) of the fusulinid limestones of the Brucebyen Beds.

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Fig. 2-72: Concentric siliceous concretions typically occur in limestones of the Cadellfiellet Member (here at Malte Brunfjellet, northern Sabine Land), but also in other members of the Wordiekammen Formation. Photo: W.K. Dallmann

The Cadellfjellet Member was mostly deposited in open to semi-restricted shallow subtidal and restricted, intertidal or supratidal environments (Sundsber 1982, unpubl.; Dons 1983, unpubl.; Pickard et al. 1996).

Pyefjellet beds (CP-51)

STATUS OF UNIT: Informal FIRST USE OF NAME: Pickard et al. 1996 CURRENT DEFINITION: Pickard et al. 1996 SYNONYM(S) AN^ REFERENCE(S): None ORIGIN OF NAME: Pyefjellet: A mountain in central Biinsow Land, central Spitsbergen TYPE SECTION (RG. 2-73): Stratotype: Pyefjellet North, Biinsow Land DEPOSITIONAL AGE: Late Moscovian - Early Kasimovian DATING METHOD: Fusulinids REFERENCE(S) FOR AGE: I. Nilsson in Pickard et al. 1996 OVERLYING UNIT(S): Black Crag Beds UNDERLYING UNIT(S): Minkl~lfjellet Formation (Temer- fjellet member) SUPERIOR UNIT: Cadellfjellet Member OTHER USE OF NAME: None THICKNESS: Up to ca. 45 m, 36 m in stratotype lMAIN LITAOLOGIES: Limestone LOWER BOUNDARY DEFLNITION: The base of the Pyefjellet beds defines the base of the Cadellfjellet Member (see there) in parts of Biinsow Land. DESCRIPTION: The Pyefjellet beds consist of stacked marine limestone units with phylloid algal build-ups. The base of the stacked units consists of bedded, bioclastic wackestones which are normally overlain by massive phylloid algal andlor palaeoaplysina wackestones. The latter form distinct rock units which possessed a topographical relief on the sea-floor (carbonate build-ups). Thin packstone or grainstone beds are commonly developed near the top of the units and may form interbeds in the build-up facies. Each unit is capped by a subaerial exposure surface. Six units (ranghg fiom ca. 3 m to 15 m in thickness) have been identified and correlated across central and eastern Biinsow Land.

*

P, ,psum moulds

* gypsum 4 moulds

gypsum moulds

unlts IIIIITIITI1

M W P G B

Fig. 2-73: Stratigraphic section CP-51/52 Stmtotype for: F'yefiellet beds, Black Crag Beds Localib: Pyefiellet N Reference: Pickard et al. 1996

The Pyefjellet beds grade transitionally westwards into the predominantly evaporite-dolomite cycles of the uppermost part of the Mududjellet Formation. The beds are interpreted to have been deposited on an open marine platform.

Black Crag Beds (CP-52)

STATUS OF UNIT: Formal. Although "Black Crag" is a typical informal unit name, a formal status should be applied to the unit because of its prominence and widespread use in the geological literature. FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965

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SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Black Crag: A descriptive name of the dark weathering cliff made up of this unit along the mountain sides in central Biinsow Land, central Spitsbergen TYPE SECTION (FIG. 2-73): Stratotype: Pyefjellet North, Biinsow Land The stratotype was originally defined at western ridge of Cadellfjellet (Cutbill & Challinor 1965), but no documentation is available. DEPOSITIONAL AGE: Early Kasimovian - earliest Gzhelian DATING METHOD: F d i n i d s REFERENCE(S) FOR AGE: I. Nilsson in Pickard et al. 1996 OVERLYING UNIT@): Gerritbreen beds UNDERLYING IJNIT(S): Pyefjellet beds, Minkidjellet Forma- tion SUPERIOR UNIT: Cadellfjellet Member OTHER USE OF NAME: None THICKNESS: Up to ca. 60 m, 25 m in stratotype MAIN LITHOLOGIES: Limestone LOWER BOUNDARY DEFINITION: The Black Crag Beds form the lowermost part of the Cadellfjellet Member in western Biinsaw Land, but seem to overlie the Pyeqellet Beds farther east. The lower boundary is defined by the bottom of a prominent, dark weathering, cliff-forming limestone interval. The cliff is easily seen along the mountain sides and forms a distinct marker unit. DESCRIPTION: The Black Crag Beds form a series of mainly massive or thickly bedded, black to dark grey lime mudstones. They are commonly sparsely fossiliferous or totally barren, although the lower parts of the individual beds may contain abundant fusulinids. Subaerial exposure surfaces marked by minor karst development and locally by in situ Micmcodium development are present in the tops of beds (Pickard et al. 1996). The thickness is >60 m in western Biinsow Land, but the unit thins towards the east.

The Black Crag Beds are probably diachronous and young eastwards across Biinsow Land. The beds represent stacked subtidal, open marine to restricted hypersaline depositional settings (Pickard et al. 1996).

Gerritbreen beds (CP-53)

STATUS OF UNIT: Informal. The transition from the Gerrit- breen to the overlying Mathewbreen beds is commonly poorly exposed and difficult to localise in the field. The status of the two units is therefore informal. RRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Gerritbreen: A glacier at Cadellfjellet in Biinsow Land, east of Billefjorden TYPE LOCALITY: Cadellfjellet, Biinsow Land DEPOSITIONAL AGE: Early Gzhelian DATING METHOD: Fusulinids REFERENcE(s) FOR AGE: I. Nilsson in Pickard et al. 1996 OVERLYING UNIT(S): Mathewbreen beds UNDERLYING UNIT@): Black Crag Beds SUPERIOR UNIT: Cadellfjellet Member HER USE OF NAME: None

TEUCKNESS: 70-180 m MAIN LITHOLOGIES: Limestone LOWER BOUNDARY DEFINITION: The base of the Gerritbreen Beds is defined by the top of the prominent, dark weathering, cliff-forming limestone interval of the Black Crag Beds. DESCRIPTION: The Gerritbreen beds display various carbonate lithologies including carbonate mudstones to packstones, and locally relatively thick (ca. 5 m) cross-bedded grainstone units. Grainstones dominate in coeval sedirnents on the Nordfjorden High @art of Kapitol Member) whereas mud-dominated textures are most common in the Gerrit- breen beds of the Billefjorden Trough (Sundsbs 1982, unpubl.). The sabkha environments in the southeastern part of Biinsow Land grade into more open marine lagoonal settings towards the northeast. On the Nordfjorden High open marine, shallow, subtidal and high energy shoals acted as barriers to the more low-energy depositional settings to the east (Sundsbs 1982, unpubl.).

Mathewbreen beds (CP-54)

STATUS OF UNIT: Informal. The transition from the Gerrit- breen to the overlying Mathewbreen beds is commonly poorly exposed and diffhdt to localise in the field. The status of the two units is therefore informal. FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Mathewbreen: A glacier at Cadellfjellet in Biinsow Land, east of Billefjorden TYPE LOCALITY: Cadellfjellet, Biinsow Land DEPOSITIONAL AGE: Middle Gzhelian DATING METHOD: Fusulinids REFERENCE(S) FOR AGE: I. Nilsson in Pickard et al. 1996 OVERLYING UNIT@): 'Qrrellfjellet Member, Brucebyen Beds UNDERLYING UNIT($): Gemtbreen beds SUPERIOR UNIT: Cadellfjellet Member OTHER USE OF NAME: None THICKNESS: 30-70 m MAIN LMWOLOGIES: Dolomite LOWER BOUNDARY DEFINITION: The base of the Mathew- breen beds is defined at a change in lithology from the limestone-dominated Gerritbreen beds to the dolomite-dominated Mathewbreen beds (Cutbill & Challinor 1965; Sundsbs 1982, unpubl.). Due to the lack of a better boundary definition, the Gerritbreen and Mathewbreen members are not considered to be formal units. DESCRIPTION: The Mathewbreen beds form a very poorly exposed succession of dolomites (often with gypsum moulds) and thin intercalated gypsum beds. Thin carbonate mudstone and packstone beds are also present (Sundsbs 1982, unpubl.). The unit is 30-45 m thick in Biinsow Land.

The depositional environments were restricted, periodically hypersaline, shallow subtidal to peritidal settings (Sundsbs 1982, unpubl.).

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Tyrrellfjellet Member (CP-55)

STATUS OF UNIT: F0fmd FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965; base redefined here

9 0

Fig. 2-74: Stratigraphic section CP-55 Stratotype for: Tyrrellfjellet Member Locality: Urmstonfjellet Reference: Lmay, A. (unpubl.)

Gipshuken Formation

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SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: rnellfjellet: A mountain east of Bille- fjorden, central Spitsbergen TYPE SECTION (FIG. 2-74): Stratotype: Urmstonfjellet, Biinsow Land The stratotype was originally defined at the northern slope

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of Wellfjellet (Cutbill & Challinor 1965), but no documentation is available. DEPOSITIONAL AGE: Late Gzhelian - Sakmarian DATING METHOD: Fusulinids REFERENCE(S) FOR AGE: Nilsson 1993 (unpubl.) OVERLYING UNIT(S): Gipshuken Formation UNDERLYING UNIT(S): Cadellfjellet, Kapitol and Mmebreen members SUPERIOR UNIT: Wordiekammen Formation OTHER USE OF NAME: None THICKNESS: 1 10- 180 m, 12 1 m in stratotype MAIN LITHOLOGIES: Dolomite, limestone LOWER BOUNDARY DEFINITION: The base is here redefined to coincide with the base of the Brucebyen Beds, a prominent, dark hulinid wackestone (see there). The original definition (Cutbill & Challinor 1965) is insufficiently clear. DESCRIPTION: The mellfjellet Member forms the upper part of the Wordiekarnrnen Formation across Spitsbergen and shows a more uniform facies than the underlying members.

The Tyrrellfjellet Member consists of alternating limestones (mudstones through grainstones) and dolomites. Palaeoaplysinid build-ups are developed in the lower part of the member. Cross-bedded, quartz-rich lime-grainstones and one bed of calcitic quartz sandstone are locally present in the middle part of the member (Biinsow Land). The top of the sandstone bed defines the base of the Finlayfjellet Beds. Gypsum nodules as well as in-situ and transported Micmcodium are scattered throughout the lower and middle parts of the member. Stacked cycles of packstones, grading up into mudstones, comprise the upper part of the member (Finlayfjellet Beds).

The Wellfjellet Member was deposited in marine environments ranging from shallow subtidal to inter-lsubtidal (L8nnry 1981, unpubl.; Dons 1983, unpubl.; Johansen 1994, unpubl.). Palaeoaplysinid build-ups and associated inter- build-up lagoons developed in the early stages of deposition and were followed by bioclastic (and rarely oolitic) shoals prograding across an open to semi-restricted lagoon. During periodic falls of relative sea level the shoals may have been subaerially exposed, producing restricted, locally hypersaline, conditions in the lagoons ( L m q 1981, unpubl.).

Brucebyen Beds (CP-56)

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Brucebyen: An abandoned coal prospecting settlement east of Billefjorden, central Spitsbergen TYPE SECTION FIG. 2-75): Stratotype: Qnellfjellet, Biinsow Land DEPOSITIONAL AGE: Latest Gzhelian - Early Asselian DATING METHOD: Fusulinids REFERENcE(s) FOR AGE: Nilsson 1993 (unpubl.) OVERLYING UNIT(S): Not named UNDERLYING UNIT(S): Cadellfjellet and Kapitol members SUPERIOR UNIT: Tyrrellfjellet Member

l

0 00 NNN

88- 88- * m -

M W P G B

Fig. 2-75: Stratigraphic section CP-56 Stmtotype for: Brucebyen Beds Locality: T~yrrellfjellet N Reference: Nilsson 1993 (unpubl.)

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OTHER USE OF NAME: None THICKNESS: 8-1 1 m, l l m in stratotype MAIN LITHOLOGIES: Limestone LOWER BOUNDARY D E ~ O N : The base is marked by the first occurrence of dark fusulinid lime wackestones above the dolomites of the Cadellfjellet Member. DESCRIPTION: The Brucebyen Beds are dark grey fusulinid wackestones to packstones. They have both a gradational base and top.

The base defines the lower boundary of the Tjmellfjellet Member. The unit occurs from Orustdalen to Ny Friesland, but is not found in St. Jonsfjorden (Cutbill & Challinor 1965).

The total organic content ranges from about 1% to more than 15% and is mainly derived from terrestrial vegetation (unpublished data, Norsk Hydro; Dons 1983, unpubl.). De- position is believed to have occurred during a marine transgression (Sundsbs 1982, unpubl.).

Finlayfjellet Beds (CP-57)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Lamay l981 (unpubl.); Dons 1983 (unpubl.) SYNONYM(S) AND REFERENCE(S): "Limestone B": Gee et al. 1952. The name is changed here because of its inconvenient, informal character. ORIGIN OF NAME: Finlayfjellet: A mountain in Biinsow Land, central Spitsbergen TYPE SECTION (FIG. 2-76): Stratotype: Finlayfjellet SW, Biinsow Land DEPOSITIONAL AGE: ?sakmarian DATING METHOD: Indirect, stratigraphic relationships REFERENCE(S) FOR AGE: Nilsson 1993 (unpubl.) OVERLYING UNIT(S): Gipshuken Formation UNDERLYING UNIT(S): Not named SUPERIOR UNIT: Tyrrellfjellet Member OTHER USE OF NAME: None THICKNESS: 30-50 m, 30 m in stratotype MAIN LITHOLOGIES: Limestone, dolomite LOWER BOUNDARY DEFINITION: The base of the Finlayfjellet Beds is defined by the onset of the thick, prominent carbonate unit described below, in central Spitsbergen overlying a calcite-cemented, very fine-grained sandstone bed. DESCRIPTION: The Finlayfjellet Beds form a prominent, cliff-forming carbonate unit at the top of the mellfjellet Member in central Spitsbergen. They have a composite thickness of several tens of metres and are made up of stacked units of bioclastic packstones grading upwards into unfossiliferous to sparsely fossiliferous mudstones. Each unit is from a few tens of cm to 6 m thick.

Packstones have an open marine fauna of mainly echino- derm fragments, brachiopods, coral fragments, bryozoans and fusulinids. The lowermost and especially the upper part of the succession are dolomitised. The transition to the overlying Gipshuken Formation is not exposed.

The Finlayfjellet Beds have been interpreted as bioclastic banks migrating across a lagoonal environment (Dons 1983,

Tm - unb M W P G B cldvf f mcvcg pcbb

Fig. 2-76: Stratigraphic section CP-57 Smtotvpe for: Finlayfjellet Beds Locality: Finlayfjellet SW Reference: L m q , A. (unpubl.)

Gipshuken Formation

unpubl.) The lagoon may have been periodically enclosed causing alternating open marine and semi-restricted conditions (Lonary 1981, unpubl.).

-

Kiaerfjellet Beds (CP-58)

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: CutbiU & Challinor 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Kiaerfjellet: A mountain on Brsgger- halvsya, Oscar I1 Land TYPE SECTION (FIG. 2-70): Stratotype: Traudalen, Brsggerhalvsya The stratotype was originally defined at the northwestern slope of Scheteligfjellet (Cutbill & Challinor 1965), but no documentation is available. The two localities are situated close to each other. DEPOSITIONAL AGE: ?Sakrnarian DATING METHOD: Indirect, stratigraphic relationships REFERENCE(S) FOR AGE: Nilsson 1993 (unpubl.) OVERLMNG UNIT(S): Gipshuken Formation UNDERLYING UNIT(S): Not named SUPERIOR UNIT: Tyrrellfjellet Member OTHER USE OF NAME: None

(Sakmarian)

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http://jurassic.ru


THICKNESS: 100 m in stratotype MAIN LITHOLOGIES: Dolomite LOWER BOUND- DEFINITION: The lower boundary corresponds to the base of the soft dolomite succession in the upper part of the T@ellfjellet Member. DESCRIPTION: The Kieerfjellet beds form the upper part of the mellfjellet Member from Brarggerhalvqa to Orust- dalen (except for St. Jonsfjorden) and are probably mappable to Ekmanfjorden ("Lower Dolomite members" of Bates & Schwarzacher, 1958) and to Biinsow Land (Fin- layfjellet Beds). They consist of thinly bedded, soft dolomite. They form a marker horizon above resistant limestones with fusulinids. Their lateral relationship with the Finlayfjellet Beds has not been described.

Idunfjellet Member (CP-59)

STATUS OF UNIT: Formal FIRST USE OF NAME: Lauritzen 1981 CURRENT DEFINITION: Lauritzen 198 1 SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Idunfjellet (from the Old Nordic goddess "Idun"): A mountain at Wahlenbergfjorden, Nordaustlandet TYPE SECTION FIG. 2-77): Stratotype: Idwellet, Nordaustlandet DEPOSITIONAL AGE: Moscovian (lower part of member) DATING METHOD: Foraminifera REFERENCE(S) FOR AGE: Lauritzen 198 1 OVERLYING UNIT@): Gipshuken Formation UNDERLYING UMT(S): Htkbardbreen Formation SUPERIOR UNIT: Wordiekammen Formation OTHER USE OF NAME: None THICKNESS: 135 m in stratotype MAIN LITHOLOGIES: Dolomite LOWER BOUNDARY DEFINITION: The base of the member is defined by the introduction of carbonates above the clastic Hilrbardbreen Formation. DESCRIPTION: The Iddjellet Member constitutes the entire Wordiekammen Formation on Nordaustlandet. The lowermost part of the type section shows a 10 m thick sandy dolomite overlain by a 3.5 m thick, partly dolomitised and silicified biosparite which is resistant to weathering. Over- lying this is, a 78 m thick sequence of limestone and dolomite and a 16 m thick succession of sandy dolomite.

The uppermost part of the member consists of dolomites with erosive surfaces, intrafonnational conglomerates and cross-bedded units. The top of the member is defined by the base of a dolomite breccia which is assigned to the Gips- huken Formation.

The unit was deposited in shallow marine to open shelf environments, with input of quartz in the lower and upper parts. The upper part shows shallowing of the sea with possible tidal influence (Lauritzen 1981).

Pre- Old Red

yellowish grey -grey

yellowish - bmwnish grey

light -dark grey

lismsrev - yel- grey

light gray - II'OWiSh

grey - bluish gley

Q

light yelawish grey

light yellowish grey

dark brownish grey

size not to scale

m ' - M W P G B

Fig, 2-77: Stratigraphic section CP-59168a Stmtotpefac Idtmfjellet Member Boundary sbntotype for: HMxdbreen Formation Locdiw: Idunfjellet Re/eme: Lauritzen 1981

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. DISTRIBUTION SHOWN ON RG(s).: 2-06, 2-07, 2-08, 2-09, 2-10 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): "Gypsum beds": Nathorst 1910 ORIGIN OF NAME: Gipshuken (transl. "Gypsum Point"): A cape at Sassenfjorden TYPE SECTION (FIGS. 2-80,2-81): Stratotype: Bredsdorffberget, Dickson Land Hypostratotype: Skansdalen, Dickson Land The stratotype was originally defined at the southwestern ridge of Cowantoppen, close to Gipshuken (Cutbill & Challinor 1965), but no documentation is available. STRUCTURAL SETTING: Late Pdaeozoic platform of Sval- bardfBarents Sea Shelf DEPOSITIONAL A M : Sab.marian - Artinskian DATING METHOD: Brachiopods, bryozoans, conodonts, foraminifem and palynomorpbs REFERENCE(S) FOR AGE: Nakrem et d. 1992; Nakrem 1993; Mangerud & Konieczny 199 1; Sosipatrova 1967 OVERLMNG UNIT(S): Kapp Starostin Formation UNDERLYING UNIT(S): Wordiekammen Formation, Treske- lodden Formation SUPERIOR UNIT: Dickson Land Subgroup OTHER USE OF NAME: None THICKNESS: Up to ca. 280 m, ca. 245 m in stratotype MAIN LITHOU)GIES: Dolomite, limestone, anhydritelgypsum, carbonate breccias LOWER BOUNDARY DEFINITION: The formational base is defined where anhydrite, besides dolomite, becomes dominant in the section, or at the first occurrence of a massive carbonate breccia which regionally replaces the anhydrite-rich facies. DESCRIPTION: The Gipshuken Formation (Figs. 2-78,2-79) is exposed across large parts of Svalbard and is thought to have been deposited over the entire archipelago, except for the southernmost part of Spitsbergen, where it seems to interfinger with the clastic sediments of the Treskelen Sub- group against the margins of the Smkapp-Hornsund High.

The formation represex@ platform deposits of interbedded anhydritelgypsum and dolomite/limestone units with thin mar1 beds and possibly two types of carbonate breccia.

An erosional surface on top of a caliche succession marks the top of the Gipshuken Formation. It represents the end of a period of cyclic sabkha deposition with intermediate marine transgressions over a large platform area. A 2-5 cm

p- - - -

Fig. 2-78: The carbonate rocks of the Gipshuken Formation (Templet and Skansdalen members) form steep cliffs on central Spitsbergen, here at Sindballefjellet, Tempelfjorden. They form the middle third of the cliff, while the lower third is made up of the gypsum/anhydrite-dominated Vengeberget member. The succession is capped by the cherts and siliceous limestones of the Kapp Starostin Formation. Photo: W.K. Dallmann

thick, shaley, dark brown to black bed usually defines the marine transgression represented by the Vmingen Member of the overlying Kapp Starostin Formation.

The Gipshuken Formation is subdivided into the Venge- berget, Zeipelodden, Kloten, Skansdalen, Templet and Ssr- fonna members (both vertically and laterally arranged; see these for detailed descriptions). In general, the subdivision underlines the prominent vertical twofold subdivision of the Gipshuken Formation. Collectively, they comprise most of the formation in central and northern areas, and in western Spitsbergen north of St. Jonstjorden. In western Spitsbergen south of Isfjorden, the formation is not described well enough to apply member names. "Cancrinella limestone" (Birkemajer & Logan 1969) has informally been used for a local facies at Kopernikusfjellet (Wedel Jarlsberg Land).

Fig. 2-79: Carboniferous-Perniian stratigraphy at the mountain Kolos- s e w (Ekmantjorden, James I Land): Above the carbonate rocks of the Wordiekammen Formation, white gypdanhydrite layers indicate the Vengeberget member of the Gipshuken Formation, upwards succeeded by the carbonates of the Skansdalen member. The succession is capped by the cherts and siliceous limestones of the Kapp Stamstin Formation. Photo: H.B. Keilen

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Kapp Starostin Formation

( A r t i n s k k

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z . 2 : a:& - < g 2 1 - K z :

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Wrdiekammen Forrnation

(Salonarlan)

Fig. 2-80: Stratigraphic section CP-60a Stmtotype for: Gipshuken Formation Locality: Bredsdofirget

Reference: Keilen, H.B. (unpubl.)

All members are suggested to have informal status until their use has been established in the geological literature and proven to be appropriate.

Vengeberget member (CP-61)

STATUS OF UNIT: Informal FIRST USE OF NAME: Here CURRENT DEFLNITION: Here SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Vengeberget: A mountain in James I Land, between Dicksonfjorden and Ekmaufjorden TYPE SECTION (FIG. 2-83): Stratotype: Vengeberget, James I Land DEPOSITIONAL AGE: Sakmarian - ?Artinskian DATING METHOD: See Gipshuken Formation REFERENCE(S) FOR AGE: See Gipshuken Formation OVERLYING UNIT@): Skansdalen member UNDERLYING UNIT(S): 'Ijnrellfjellet Member (Wordiekam- men Formation)

units m 11111111111

M W P G B

Ng. 2-81: Stratigraphic section CP-6ObJ64 Hyostmtotype for Gipshuken Formation Stmtotype for: Skansdalen member Locality: Skansdalen Refmence: Keilen, H.B. (unpubl.)

SUPERIOR UNIT: Gipsdalen Formation OTHER USE OF NAME: None THICKNESS: 100-120 m, 109 m in stratotype

LITHOLOGIES: Anhydritelgypsum, dolomite, mar1 LOWER BOUNDARY DEFINITION: The base of the member is defined by the first occurrence of massive anhydrite beds on top of the dolomite/marl dominated Tyrrellfjellet Member. DESCRIPTION: The Vengeberget member is the lower, gyp- sumlanhydrite-dominated part of the Gipshuken Formation.

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Fig. 2-82: Gypsum layers of the Vengeberget member at Palatium- fjellet (James I Land). Photo: H.B. Keilen

It occurs within a NNW-SSE trending, ca. 30 km wide zone from east of Kongsfjorden through E m o r d e n to eastern Nordenskiold Land. It shows relatively abrupt lateral transi- tions with the Kloten breccia member to the southwest, and with the Zeipelodden breccia member to the north-east.

Rhythmtes of anhydriitegypsum, dolomite and marl dominate the member (approximately 90-1 10 m) in the western part of James I Land (Palatndjella, fig. 2-82) to Rejmyre- fjellet east of Tempelfjorden. The dominant white to light grey colour of this unit is ch r t tWMc in central Spits- bergen. The dolomites are dominated by finely laxninated algal mats. Occasional srrmall grntropods and bivalves are seen. Polygonal ,cracks, tepee s t r u m s and stylolites occur fkequently. Oolitic bestone beds occur occasionally (5- 50 cm thick). Various fabrics of anhydrite are seen, for instance anhydrite nodules, enterolithic layers and chicken- wire textures. The anhydrite and dolomite beds vary from 2 cm to 5.5 m thick. Marly units are up to 50 cm thick, although most commonly only 3-5 cm. Between 30-40 rhyth- mically repeated units of anhydrite/dolomite/marl are seen through the unit. Internal deformation structures are seen in anhydrites throughout the unit.

The top of the Vengeberget member is marked by the disappearance of anhydrite and dolomite, limestone and marl become the dominant lithologies.

The facies of the Vengeberget member reflects a sabkha environment and consists of stacked sabkha units of anhydrite, dolomite and marl, deposited in a shallow marine, occasionally restricted langoonal to supratidal environment with very slow subsidence. The climate is interpreted to have been semi-arid (Steel & Worsley 1984). Rhythms may be caused by occasional storms or relatively small sea-level changes. Oolites are interpreted to be nearshore bars or tidal channel infillings. Flora and fauna show very little diversity, but individual populations are large when seen, a feature typical for a hypersaline environment.

Zeipelodden member (CP-62)

STATUS OF UNIT: Informal FIRST USE OF NAME: Lauritzen 198 1

- 2 S W Locar Refen

nation narian)

rth. sirat units

3 m r h'" *

.83: Stratigraphic section CP-61 W*: maber ty: Vengeberget nce: Keilen, H.B. (~publ.) , modified from Lauriaen

CURRENT DEFINITION: LaUritZen198 1 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Zeipelodden: The cape between Palander- bukta and Wahlenbergfjorden on Nordaustlandet

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m

< 4 m high caverns

light brown

strongly weathered

a g e m lllllllrll1 M W P G B

Fi. 2-84: Stratigraphic section CP-62 Stratotype for Zeipelodden member Localiv: Zeipelodden

Re$en!nce: Keilen, H.B. (unpubl.), modified from Lauritzen 1981

TYPE SECTION (FIG. 2-84): Stratotype: Zeipelodden, Nordaustlandet DEPOSITIONAL AGE: Sakmarian - ?k thk ian DATING METHOD: See Gipshuken Formation REFERENCE(S) FOR AGE: See Gipshuken Formation OVERLYING UMT(S): Smfonna and Skansdalen members UNDERLYING UNIT@): Idunfjellet Member (Wordiekammen Formation) SUPERIOR UNIT: Gipsdalen Formation OTHER USE OF NAME: None THICKNESS: 40-50 m, 8 m in stratotype MALN LKTHOLOGIES: Carbonate breccia, limestone LOWER BOUNDARY DEFINITION: The base of the member is defined at the stratigraphic onset of limestone breccias above the dolornites of the Idunfjellet Member. DESCRIPTION: The Zeipelodden member occurs on eastern Svalbard and passes laterally into the evaporitic Venge- berget member of central Spitsbergen. It consists of alternating, unstructured carbonate breccias and algal-laminated limestones. The original dolomite breccias are widely dedolomitised. Irregularly bedded horizons are weathered into up to 5 m high caverns, a property which makes them visible from a dishce. The sediments are highly porous.

The member occurs north of a line striking NW-SE from Torfjellet, west of Pyramiden (Dickson Land) to Sindballe- fjellet (Biinsow Land) and Rejmyrefjellet (Sabine Land). The thickness of this unit varies considerably, but it is reported to be approximately 40-70 m at Mjerlnerfjellet (east of Lomfjorden), at Sindballefjellet and at Tyrrellfjellet (Biinsow Land). Irregular breccia fragments of different sizes (1-30 cm) and shape, with a chaotic appearance, are seen, and a secondary porosity is well developed. The weathered surface is light brown with a brecciated appear-

ance and well-developed cavities. On Nordaustlandet (localities of Idunfjellet and Zeipelfjella) the unit is subdivided into two separate breccias with intervening laminated dolomite and marls.

The Zeipelodden member is interpreted as a solution breccia. During deposition of the sabkha sediments of the Vengeberget member, eastern areas formed a hinterland exposed to weathering and karstification and hence solution of earlier deposited anhydrite. This unit may represent a lateral time equivalent of upper parts of the Tyrrellfjellet Member. Collapse of dolomite beds and an extensive karstification occurred due to semiarid climate (Steel and Worsley 1984) and dissolution of the anhydrite. On Nordaustlandet, a local transgression, producing a supratidal to intertidal lagoonal environment, split up this member into two distinct (lower and upper) units.

1 ; L

1 , . Kloten member (CP-63)

STATUS OF UNIT: Informal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Kloten (transl. "The Heap"): A mountain on Brcaggerhalverya, Oscar I1 Land TYPE LOCALITY: Scheteligfjellet NE, Braggerhalverya DEPOSITIONAL AGE: Sakmarian - ?Artinskian DATING METHOD: Indirect, stratigraphic relationships. See Gipshuken Formation REFERENCE(S) FOR AGE: See Gipshuken Formation OVERLYING UNIT(S): ?Skansdalen members UNDERLYING UNIT(S): Tyrrellfjellet Member (Wordie- kammen Formation) SUPERIOR UNIT: Gipsdalen Formation &TIER USE OF NAME: None THICKNESS: 88 m in stratotype MAIN LITHoLoGIES: Limestone and dolomite breccia LOWER BOUNDARY DEFINITION: Kloten breccia type sediments occur with upward increasing thickness and fre- quencey in the Gipshuken Formation of northwestern Spits- bergen. The base of the member is arbitrarily defined at the first occurrence of carbonate breccia units thicker than 2 m. DESCRIPTION: The Kloten breccia occurs on western Spits- bergen in Permian outcrops of the Tertiary fold belt. It has been observed as far south as Bellsund. Breccias and conglomerates that occur in the Gipshuken Formation even farther south, are not correlated with certainty. The Kloten member probably interfingers with the Vengeberget member to the NE along the eastern margin of the St. Jonsfjorden Trough.

Along the west coast of Spitsbergen, from Brargger- halverya to St. Jonsfjorden and possibly farther south - from Outer Isfjorden to Bellsund - dolomite dissolution breccias (in-place brecciation) occur together with the dolomite/marl beds seen elsewhere on Spitsbergen. Breccia fragments are sharp-edged and occur as rectangular, raudomly mixed 2- 15 cm long fragments of cracked and ruptured dolomite beds in a microcrystalline dolomite matrix. Only scattered occurrences of anhydrite in the lowermost part in the unit

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are reported from the southern parts of the exposure area. The Kloten member is interpreted as a tectonic dissolution

breccia. Anhydrite is thought to have been primarily deposited in the area. It was dissolved and dolomite beds collapsed. There are no signs of karstification.

Skansdalen member (CP-64)

STATUS OF UNIT: Informal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Skansdalen: A valley in Dickson Land, named after Skansen, transl. "The Rampart", an adjacent mountain TYPE SECTION (FIG. 2-81): Stratotype: Skansdalen, Dickson Land DEPOSITIONAL AGE: Sakmarian - Artinskian DATING METHOD: See Gipshuken Formation REFERENCE(S) FOR AGE: See Gipshuken Formation OVERLYING UNIT@): Vsringen Member (Kapp Starostin Formation) UNDERLYING UNIT@): Vengeberget, Kloten and Zeipel- odden members SUPERIOR UNIT: Gipsdalen Formation OTHER USE OF NAME: None THICKNESS: Up to 150 m, ca. 100 m in stratotype MAIN LITHOLOGIES: Dolomite, limestone, marl, anhydritelgypsum and caliche LOWER BOUNDARY DEFINITION: The member base is defined at the base of massive dolomites above the evaporite- dominated Vengeberget member or above the carbonate breccias of the Zeipelodden and Kloten members. DESCRIPTION: The Skansdalen member forms the upper part of the Gipshuken Formation in western areas of Spits- bergen, from Br~ggerhalvwa in the NW to Torell Land in the SE, and in central Spitsbergen including Dickson Land. It interfingers laterally with the limestones of the Templet member in the east. The lateral transition to the Slarfonna member on Nordaustlandet has not yet been defined.

The Skansdalen member consists of regularly bedded dolomites (5-15 cm thick) intercalated with 2-10 cm marly beds. Finely laminated dolomites dominate towards the top of the formation (150-180 m). Bioturbation is common. Caliche beds, erosional surfaces and oolite beds (10-50 cm thick) occur more frequently towards the top. A 10-20 m thick unit of anhydrite/dolomite/marl occurs throughout central Spitsbergen 10-15 m below the top.

The member is interpreted as a supra- to intertidal sediment. Finely laminated dolomite beds with root structures and desiccation cracks are interpreted as shallow marinella- goonal algal mats. Periodic minor sea-level fluctuations are suggested. Erosional surfaces, oolite bars and caliche are recognised, as well as open marine faunas (brachiopods, crinoids, bryozoans, corals). A short regressive period with renewed sabkha environments is interpreted at 10-15 m below the upper formation boundary.

Templet member (CP-65)

STATUS OF UNIT: Informid -T USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Templet (transl. "The Temple"): A mountain in Biinsow Land TYPE SECTION (FIG. 2-85): Stratotype: Templet NW, Biinsow Land DEPOSITIONAL AGE: Sakmarian - Artinskian DATING METHOD: See Gipshuken Formation REFERENCE(S) FOR AGE: See Gipshuken Formation OVERLYING UNIT@): Skansdalen member UNDERLYING UNIT(S): Skansdalen member SUPERIOR UNIT: Gipsdalen Formation OTHER USE OF NAME: None THICKNESS: 100-135 m, ca. 135 m in stratotype MAIN LITHOLOGIES: Limestone LOWER BOUNDARY DEFINITION: The base of the member is defined where limestones start to dominate the succession above dolomites of the Skansdalen member. Although all beds are conformable, the onset of dominant lime content in the carbonate rocks is laterally moving up-section. DESCRIPTION: The Templet member represents a local limestone facies in the upper part of the Gipshuken Formation. It forms a wedge within and interfingers with the dolomite- dominated Skansdalen member.

Both fauna1 and floral diversity are high. Large bivalves (up to 5 cm long), brachiopods, gastropods, crinoids, bryozoans, rugose corals, algal mats and small foraminifera are common. Bioturbation is commonly seen (Rhizocorallium, Thalassinoides, Zoophycos). Crossbedded carbonate sands (size order 1 m) are seen at several levels. Chert nodules are common, generally spacially related to the occurrence of ~alassinoides. Scattered sponge spicules are observed in thin section and may form spiculite beds a few cm thick. Erosional surfaces are seen. Caliche occurs and forms 10- 100 cm thick beds. Root structures and Micmcodium are common. Oncolites have been observed in one bed in the uppermost part of the unit. Stylolites are present in dolomite beds throughout the unit.

This unit is interpreted as representing a mixed open marine to sublinterlsupratidal environment. The fauna is very diverse in the marine facies. Oolite barriers separated the open marine from the restricted lagoonal environments. The latter are dominated by algal mats, gastropods and small bivalves. Supratidal sabkha environments occur at 10-15 m below the top of the formation boundary.

Ssrfonna member (CP-66)

STATUS OF UNIT: Informal FIRST USE OF NAME: Here CURRENT DEFINITION: Here, following Lauritzen 198 1 SYNONYM(S) AND REFERENCE(S): ''Calciferous Sandstone Series": Holland 1961 ORIGIN OF NAME: Smfonna (transl. "The Southern Ice Cap"): A large plateau glacier on Nordaustlandet

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o-l i m 111111TIIII

M W P G B clsivf f mcvcg pcbb

Fig. 2-85: Stratigraphic section CP-65 Stmto@pe for: Templet member Localiw: Templet NW Reference: Keilen, H.B. (un~ubl.)

Kapp Starostin Formation

( A r t i n s .

z 0

m - .- C

z z < :

5 n

@ C Z d m m a .-

W L M O

s ': Y m v l m m 2

0

- Zeiplodden

member (Sahr ian) 4 .... C...-: l

m 11111111111 M W P G B

dsivf f mcvcg pcbb

Rig. 2-86: Stratigraphic section CP-66 Stmtofype for: Ssrfonna member Localiv: Zeipelfjella E Reference: Keilen, H.B. (unpubl.)

TYPE SECTION (FIG. 2-86): Stratotype: Zeipelfjella E, Nordaustlandet DEPOSITIONAL AGE: Sakmarian - Artinskian DATING METHOD: See Gipshuken Formation REFERENCE(S) FOR AGE: See Gipshuken Formation OVERLYING UNIT@): Vmhgen Member (Kapp Starostin Formation) UNDERLYING UNIT@): Zeipelodden member SUPERIOR UNIT: Gipsdalen Formation &HER USE OF NAME: None THICKNESS: 60 - 66 m, 66 m in stratotype MAIN LITHOLOGIES: Limestone, dolomite, coal LOWER BOUNDARY DEFINITION: The base is defined where

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bedded or laminated biomicritic and biosparitic limestones overlie the breccias of the Zeipelodden member. DESCIUPTION: The Sorfonna member forms the upper part of the Gipshuken Formation on Nordaustlandet. The lateral transition to the Skansdalen and Templet members of central Spitsbergen is not preserved, but is thought to have occurred in Ny Friesland. Though distinct boundary is seen between the Smfonna member and the underlying breccias of the Zeipelodden member in the exposures on Nordaust- landet, the overall relation of the two members is interpreted as a diachronous interfingering.

This unit is dominated by fine-grained algal laminated dolomites and limestones, abundant root structures and plant fragments, caliche beds and erosional surfaces. Sponge spicules occur, occasionally forming spiculites. Re- placement of carbonate by chert is more frequent here than elsewhere in the Gipshuken Formation. Minor coal beds (up to 2 cm thick) occur fiequently throughout the member. Brachiopods, ostracods, bryozoans and rugose corals are present. Algae are commonly found.

Erosive surfaces separate several coarsening-upward sequences on a metre- to 10 m-scale. Caliche occurs in the upper parts of the member. On the southwestern slopes of Zeipelfjella, greyish to brownish, thickly bedded, medium- grained dolomites with scattered chert nodules occur. No evaporites have been described from this unit.

The much higher frequency of plant fragments, the onset of thin coal beds intercalated with finely laminated lagoonal algal dolomite, and more open marine conditions represented by limestones and an open marine fauna (corals, bryozoans, brachiopods) suggest increasing humidity subsequent to the previous arid conditions during the late Sakmarianlearliest Artinskian.

DISTRIBUTION SHOWN ON hG(s).: 2-10 STATUS OF UNIT: Formal FIRST USE OF NAME: Here, following Olaussen et al. (1986, unpubl.) CURRENT DEFINITION: Here SYNONYM(S) AND REFERFXCE(S): None ORIGIN OF NAME: Malte Brunfjellet: A mountain in N Sabine Land TYPE SECTION ( h G . 2-88): Stratotype: Malte Brunfjellet, N Sabine Land STRUCTURAL SETTING: Ny Friesland High DEPOSITIONAL AGE: Early Moscovian (upper part of formation)

Fig. 2-87: Limestone gravel conglomerate intercalated with massive limestones, a typical rock association of the upper parts of the Malte Brunfjellet Formation, indicating the transition from clastic to carbonate deposition. Malte Brunfjellet (northern Sabine Land). Photo: W.K. DalImann

DATING METHOD: Foraminifera REFERENCE(S) FOR AGE: I. Nilsson in O l a ~ ~ ~ e n et d. 1986 (unpubl.) OVERLYING UNIT@): Wordiekammen Formation UNDERLYING UNIT(S): he-Old Red LATERALLY ADJACENT UNIT(S): ?Md@ellet Formation, ?HArbardbreen Formation SUPERIOR UNIT: Gipsdalen Group OTHER USE OF NAME: None THICKNESS: Up to 100 m, ca. 70 m in stratotype MAIN LITHOLOGIES: Sandstone, conglomerate, limestone LOWER BOUNDARY DEFINITION: The lower boundary is an angular unconformity above folded, but unmetamorphosed Vendian basement correlated with the Wilsonbreen Forma- tion (interbedded red and green siltstone, very fine sandstone, mudstone and thin dolomite beds). DESCRIPTION: Above the basal unconformity, a 2-3 m thick transitional zone of red and green "mottled shale" occurs, probably representing a weathering zone or paleosol. Above this zone, the lower part (A) of the Malte Brunfjellet For- mation shows 18 m thick interbedded sandstones, conglomerates, red shales and sandy red shales. These beds are interpreted as distal alluvial fan deposits, including stream channels, overbank levees, sheet floods and paleosols.

The overlying part (B) is about 30 m thick, though mainly covered, but small outcrops show coarse sandstones, conglomerates and carbonate rocks.

The upper part (C) is 20 m thick and comprises coarse sandstones and conglomerates interbedded with biogenic carbonates including stromatolites and intraformational conglomerates (Fig. 2-87). These beds are interpreted as fan delta deposits with fluvio-marine channels, subtidal channels, subtidal to intertidal bars, intertidal flats and beach spits.

Different authors provided variable thickness measurements of the entire formation: Winsnes (1966): 92 m; Cut- bill (1968): 97 m; Olaussen et al. (1986, unpubl.): 69 m.

The upper boundary is transitional to the overlying, pure carbonates of the Wordiekammen Formation, indicating a continuous transgression.

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z 0 W

B h

4 al

.;; c W -

a x ; - " > C , - 3 0 < - 0 E z ; ; K .- P W ' - "

, a n , 6%

g y o O Z 3 m .- K ,' a U U m

a Z- 2

0 Ls H m el

d m W

3 2:

Pre- Old Red basement

.............., grain size not to scale

1

m - M W P G B

dsiHf mcvcg pcbb

Fig. 2-88: Stratigraphic section CP-67 Stratotype for: Malte Brunfjellet Formation Locality: Malte Bmfjellet Reference: Olaussen et al. 1986 (unpubl.)

- Pre- Old Red

UPPER PALAEOZOIC LITHOSTRATIGRAPHY

Wrdlekammen Form*

z 0 C3

k 4 Z 6% 0

W

6%

W c. cl < X

" 3

0

W

e 0

basement v

c g o t - .- k > d - 0 4 2 0 2 0 " m O ; w = E J mostly covered

m - M W P G

dsivf f mcvcg

red mottled

green mottled

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The Malte Brunfjellet Formation has previously been regarded as a correlative of the Midadjellet Formation because of its probably similar age (Cutbill 1968), while Olaussen et al. (1986, unpubl.) noted its lithological similarities to the Ebbadalen and H&%ardbreen formations. The lithostratigraphic correlation with the Minkinfjellet Forma- tion is abandoned. They are lithologically not similar, and the two formations occur far (20 km) from each other. A lateral transition has not been shown, although it may be expected

Similar rocks at a comparable stratigraphic level at Lom- fjorden may be correlatives of the Malte B d j e l e t Forma- tion, but documentation is lacking.

DISTRIBUTION SHOWN ON FIG@).: 2-10 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: The type section description of Lauritzen (1981) is supplemented by Olaussen et al. (1984b unpubl.). SYNONYM(S) AND REFERENCE(S): HArbardbreen "Member": Cutbill & Challinor 1965 ORIGIN OF NAME: HArbardbreen: A glacier near Wahlen- bergfjorden, Nordaustlandet TYPE SECTION (FIGS. 2-77,249): Boundary stratotype: Idunfjellet, Nordaustlandet Unit stratotype: Ismisestranda, Nordaustlandet STRUCTURAL SETTING: ?Ny Friesland High DEPOSITIONAL AGE: Serpukhovian - Moscovian DATING METHOD: Indirect, stratigraphic relationships (very uncertain) REFERENCE(S) FOR AGE: Olaussen et al. 1984b (unpubl.) OVERLYING UNIT@): Wordiekammen Formation UNDERLYING UNIT@): Pre-Old Red SUPERIOR UNIT: Gipsdalen Group OTHER USE OF NAME: None THICKNESS: 15-140 m MAIN LITHOLOGIES: Sandstone, conglomerate, shale LOWER BOUNDARY DEFINITION: The lower boundary is defined at the angular unconfomity with the underlying Pre- cambrian basement. DESCRIPTION: The base of the formation at Idunfjellet consists of an 8 m thick conglomerate containing mostly clasts of dolornitic mudstones, but clasts from underlying, red- coloured basement are also common. A 7.5 m thick light yellowish-grey sandstone overlies the conglomerate.

The thickness varies from 15.5 m on Idunfjellet to ca.

Pre- Old Red basement

eoliin sediment

* % - eoliin

sediment " 1 I -

cisivf f mcvcg pcbb

Fig. 2-89: Stratigraphic section CP-68b Unit stratotype for: HBrbardbreen Formation Locality: Isdsestranda, H&ardbreen Reference: Olaussen et al. 1984b (unpubl.)

?40 m at Ismbestranda. The variation is caused by the local development, dependent upon topography of the underlying basement peneplain. The most completely developed and best investigated section at Ismbestranda (type section)

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lacks the basal part (10-20 m) of the formation; the Idun- fjellet section is therefore used as a boundary stratotype.

At Hhbardbreenfismiisestranda, the formation is divided into two units. The lower unit comprises red sandstones interpreted as stream channels and overbank deposits separated by aeolian dune deposits. A muddy, mottled paleosol is also observed. The upper unit comprises yellowishlgrey- ish sandstones interpreted as an estuarine channel complex and shoreface deposits. This coastal section is interrupted by a conglomeratic braided stream channel and a muddy paleosol.

The upper boundary is transitional to sandy dolomites of the Idunfjellet Member (Wordiekammen Formation).

- I , 1 1 1 n

DISTRIBUTION SHOWN ON FIG@).: 2-05. STATUS OF UNIT: Formal I

FIRST USE OF NAME: Krasil'HEikov & LivHic 1974 CURRENT DEFINITION: Womley dEdwards 1976 SYNONYM(S) AND REFERENCE(S): "Red Conglomerate": Andersson 1900 ORIGIN OF NAME: Landnmdingsvika (transl. "The Bay of the 'Landnmding' [northeastern wind],,): A bay on SW Bj-a TYPE SECTION (FIGS. 2-91,2-92): Stratotype: Landnmdingsvika, Bjmwya SW Hypostratotype: Kobbebukta, Bjrmnerya N STRUCTURAL SETTING: West Bjmwya Trough DEPOSITIONAL AGE: Ba~hkirian

clsivff mcvcg pcbb

Fig. 2-90: Altermthg alluvial red mudstones and conglomerates Fig. 2-91: Stratigraphic section CP-6% (fan and overbank deposits) and grey, shallow-marine sandstones Stmtorjpefor: Landwrd'mgsvika Formation (reworked in coastal areas) in the Landwrdingsvika Formation Locality: Landwrdingsvika (Bjmwya). Photo: GB. Lmsen Reference: Gjelberg 1981

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age- m units - d sivf f m cvcg pcbb

Fig. 2-92: Stratigraphic section CP-69b Hypshatotype for: Landrwrdingsvika Forination Locality: Kobbebukta Reference: Gjelberg, J.G. (mpubl.)

DATING METHOD: Fusulinids REFERENCE(S) FOR AGE: Worsley & Edwards 1976 (not documented); Sirnonsen 1988 (unpubl.) OVERLYING UNIT(S): Kapp m e Formation, locally Ham- bergfjellet Formation UNDERLYING UNIT(S): Nordkapp Formation SUPERIOR UNIT: Gipsdalen Group OTHER USE OF NAME: None THICKNESS: Up to 200 m MAIN LITHOLOGIES: Red mudstone, conglomerate, sandstone LOWER BOUNDARY DEFINITION: The base of the formation in the type section is placed at the appearance of thick, red mudstones (Worsley & Edwards 1976) above the coarser- grained clastics of the Nordkapp Formation. DESCRIPTION: The lower part of the formation consists of red mudstones, interstratified with relatively thin sandstone beds. The middle part consists of relatively thick, red to yellow conglomerates interbedded with red and green mudstones and grey and red sandstones of marine origin (Fig. 2- 90). The upper part comprises calcareous sandstones in alternation with red and green mudstones and siltstones.

Most of the sandstones contain marine trace fossils, and indications of tidal influence. The red mudstones in the lower part of the formation most likely represent flood plain or coastal plain deposits (qelberg 1981), although marine plankton have been recorded fiom some samples in the basal part of the type section (Vigran 1994, unpubl.). The presence of calcrete paleosols contrasts with the coals seen in underlying units.

The ratio of marine influenced sediment increases upwards, together with increasing carbonate content. The top of the formation has been placed at the first appearance of thick carbonate beds. Environmental interpretations have also been given by Gjelberg (1 978), Gjelberg & Steel (1 98 1, 1983) and Worsley et al. (in press).

DISTRIBUTION SHOWN ON FIG(s).: 2-05 STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley & Edwards 1976 CURRENT DEFINITION: Worsley & Edwards 1976 SYNONYM(S) AND RE~RENCE(S): "Ambigua limestone": Andersson 1900; "Kobbebukta Formation": Krasil'SEikov & LivSic 1974 Although Krasil'SEikov & LivSic's (1974) publication with the name "Kobbebukta Formation" was issued earlier, the manuscripts were written simultaneously. This is valid for

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2. UPPER PALAEOZOIC LITHOSTRATICRAPHY

several units on Bjsmsya. We recommend the use of Wors- . ley & Edward's (1976) nomenclature, because this is better 1 established in the published literature (see Section 2.5.1). ORIGIN OF NAME: Kapp W e : A point on SW Bjsrn0ya TYPE SECTION (FIG. 2-94): Boundary stratotype: Landnsrdingsvika - Kapp W e , SW Bjsrnsya STRUCTURAL SETTING: West B j m y a Trough DEPOS~TIONAL AGE: Bashkirian - Moscovian DATING METHOD: Fusulinids REFERENCE(S) FOR AGE: SimOnsen 1988 (unpubl.) OVERLYING UNIT(S): Kapp Hanna Formation, Miseryfjellet Formation UNDERLYING UNIT@): Landnsrdingsvika Formation SUPERIOR UNIT: Kapp W e Formation OTHER USE OF NAME: None THICKNESS: Up to 200 m (composite) MAIN LITHOLOGIES: Cherty limestone, shale, sandstone, intraformational conglomerate biomicrites with marine faunas increase upwards to the LOWER BOUNDARY DEFINITION: The transition with the un- junction with the overlying, totally limestone-dominated derlying coarse-clastic dominated Landwrdingsvika For- Efuglvika Member. Northern coastal exposures in Kobbe- mation is marked by the disappearance of thick conglomer- bukta show less sandstone, a more shaley grey development ates and the introduction of carbonates. The boundary is and more marine influence. defined at the base of the first distinct carbonate bed. The rhythmic development of the unit also displays nu- DESCRIPTION: The formation is fully developed and well merous karst and discontinuity surfaces, suggesting an in- exposed, but poorly accessible, in the cliffs of Land- terplay of local tectonic activity with ongoing regional sea- mdingsvika on the southwestern coast of Bjsmraya. More level rise m k e m o 1979, unpubl.; Worsley et al, in press). accessible, although faulted, exposures show incomplete sections through the three members of the formation in Kobbebukta on the northern coast. For more detail see the Efuglvika Member (CP-72) Bogevika, Efuglvika and Kobbebukta members. Kirkemo (1979, unpubl.) provided detailed descriptions. STATUS OF UNIT: Formal

FIRST USE OF NAME: Worsley & Edwards 1976 CURRENT DEFINITION: Worsley & Edwards 1976

Bogevika Member (CP-71) SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Efuglvika = ffirfhglvika (transl. "The

STATUS OF UNIT: Formal Eider Duck Bay"): A bay on western Bjnrnuaya FIRST USE OF NAME: Worsley & Edwards 1976 TYPE SECTION (FIG. 2-95): CURRENT DEFINITION: Worsley & Edwards 1976 Stratotype: Landnsrdingsvika - Kapp W e , SW Bjsrnsya SYNONYM(S) AND REFERENCE(S): None DEPOSITIONAL AGE: Early Moscovian ORIGIN OF NAME: Bogevika (transl. "The Bow Bay"): A bay DATING METHOD: Fwulinids On SW Bjerrnsya REFERENCE(S) FOR AGE: Sim01l~en 1988 (unpubl.) TYPE SECTION (FIG. 2-94): OVERLYING UNIT@): Kobbebukta Member, locally Kapp Stratotype: Landnsrdingsvika - Kapp W e , SW Bjnrrnsya Hanna Formation DEPOSITIONAL AGE: Bashkirian - Early Moscovian UNDERLYING UNIT@): Bogevika Member DATING METHOD: Fwulinids SUPERIOR UNIT: Kapp W e Formation REFERENCE(S) FOR AGE: Simnsen 1988 (unpubl.) OTHER USE OF NAME: None OVERLYING UNIT(S): Efuglvika Member Tmcmss: 77 m in stratotype UNDERLYING UNIT@): Landnsrdingsvika Formation lMALN LITHOLOGIES: Cherty limestone SUPERIOR UNIT: Gipsdalen Formation LOWER BOUNDARY DEFINITION: The Efuglvika Member OTHER USE OF NAME: None starts where the succession of the Kapp Khe Formation be- THICKNESS: 92 m in stratotype comes dominated by limestones. Shales and sandstones, MAIN LITHOLOGIES: Limestone, dolomite, sandstone, shale building up the major part of the underlying Bogevika LOWER BOUNDARY DEFINITION: See Kapp m e Formation Member, occur only as thin intercalations between lime- DESCRIPTION: In type section both upwards coarsening and stones above the boundary. upwards fining rhythrtes are seen (Fig. 2-93): a significant DESCRIPTION: Thinly bedded to massive cherty limestones sandstone content decreases upwards as first shales and show textures ranging from wackestone to grainstone. Both then limestones become more prominent. Many beds here discontinuity and karstic surfaces are common, but stenoha- have greyish-red or variegated green-red colours; caliche line marine faunas occur throughout. The unit typically con- horizons are common in the lower parts of the member, but sists of a series of upwards coarsening rhythrmtes passing

Fig. 2-93: Coarsening-upward unit in the Bogevika Member, Kobbe-

bukta, Bjlarnraya. Photo: D. Worsley

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(unpubl.)

0

0 m K

0

, . 11111111111 M W P G B

cleivf f mcvcg pcbb

Fig. 2-94: Stratigraphic section CP-70171 Boundary stratotype folr Kapp Kitre Eonnation Simtotypefor: Bogevika MW& Locality: LandoLndingsvika - Kapp Kdre Referance: Worsley, D. (in press), modified from Kirkemo 1979

106

c n ; 3.;

0

= U

- , Z C <

.F c

a ; m

a O M

b

: F4

0 0 . 4 0 W O M W L 5 , O

M

IS$ III

55s 11111111111

M W P Q B clsivf f mcvcg pcbb

f c

0 2 D

W *

d.;

& m

I B I 2

%B

B

$$I6 Boo b IIIh g5 v 6

1 .

Ym units

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3

CA

RB

ON

IF

ER

OU

S

Mo

sc

ov

ia

n

KA

PP

K

AR

E

FO

RM

AT

IO

N

W

Efu

glv

ika

Me

mb

er

CA

RB

ON

IF

ER

OU

S

Mo

sc

ov

ia

n

KA

PP

K

AR

E

FO

RM

AT

IO

N

Efu

glv

ika

Me

mb

er

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V unlb

section thickness Location: east

V)

2

-. ..................

correlation between sections 1

lateral interlingering

appmximate

H

F-. 0 , 4 8 . Z @ Z 0 W . - & Z L ' o m - o h - Z O W X

section thickness approximate

Z k 0 0

=

a v

Location: west

0

0

0

0 grain size approximate

Member (Moscovian)

ss

Efuglvika

- M W P G B

dsivf f mcvcg pcbb

R 0

< M

-

from bioturbated chert-rich wackestones with Thalassi- noides burrows up into chert-free grainstones, sometimes with clearly erosive or karstified tops. Some small phyl- loidhryozoan build-ups occur locally uppermost.

Rhythmicity, discontinuity surfaces, karst and chert dikes indicate ongoing local tectonic activity during relative high stand with generally open marine conditions.

Kobbebukta Member (CP-73)


m M W P G B

dsivf f mcvcg pcbb

Fig. 2-96: Stratigraphic section CP-73 Stmtotype for: Kobbebukta Member

Locality: Kobbebukta

Reference: Worsley, D. (in press), modified from Kirkemo 1979 (unpubl.)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here, after Kirkemo 1979 (unpubl.) SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Ubbebukta (transl. "The Seal Bay"): A bay on northern BjPrmerya TYPE SECTION (FIG. 2-96): Stratotype: Kobbebukta, northern BjPrmerya DEPOSITIONAL AGE: Late Moscovian DATING METEIOD: Fusulinids REFERENcE(s) FOR AGE: ShlOIlSeIl1988 (UIlp~bl.) OVERLYING -(S): Kapp Hanna Formation _ UNDERLYING UNIT@): Efuglvika Member SUPERIOR UNIT: Kapp Kilre Formation Orm~ USE OF NAME: "Kobbebukta Formation": KrasilY- S a w & LivSic 1974

Although Krasil'SEikov & LivSic's (1974) publication with the name "Kobbebukta Formation" was issued earlier, the manuscripts were written simultaneously. This is valid for several units on Bjnrmsya. We recommend the W of Wors- ley & Edward's (1976) nomenclature, because this is better established in the published literature (see Section 2.5.1). Tmcmss: Up to 45 m (stratotype)

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- ......-.. .... - POZOIC LITHOSTRATIGRAPHY

MAIN LITHOLOGIES: Conglomerate, limestone LOWER BOUNDARY DEFINITION: The boundary is defined where distinctive intraformational conglomerates rest with an erosive contact on the underlying bedded limestones and cherts of the Efuglvika Member. DESCRIPTION: The conglomerates were deposited both subaerially and in submarine debris flows and locally infill small half-&bens formed in the uppermost Efuglvika Member. Interbedded limestones, shales and siltstones contain marine faunas. Exposures on the SW coast show a much thinner development of only a few metres of debris flows; alternatively the Kapp Hanna Formation's extrafor- mationalconglomerates infill small fault-controlled depressions cutting directly into the Efuglvika Member carbonates.

Synsedimentational tectonism reflected by the member's conglomerates reflects formation of an exposed block over the eastern parts of present-day Stappen High. Eroded material was transported westwards into the West Bjnrrnnrya major half-graben through a series of small gullies; these reflect drainage control on the generally westwards-dipping topography by sets of small faults conjugate to the main N-S directed block faulting (Worsley et al., in press).

DISTRIBUTION SHOWN ON FIG(s).: 2-05 STATUS OF UNIT: Formal FIRST USE OF NAME: Krasil'BEikov & LivSic 1974 CURRENT DEFINITION: W0pley & & h d S 1976 SYNONYM(S) AND REFERENCE(S): "Yellow sandstone": Andersson 1900 ORIGIN OF NAME: Kapp Hanna: A point on western B jm- arya TYPE SECTION (FIGS. 2-98,2-99): Bmdary stratotype: Efuglvika N, SW Bjnrrnnrya Unit stratotype: Kobbebuh - Nordvestbukta, NW B j m - q a (compasite section) ~ U C T U R ~ L SETTING: West Bjmwya Trough ~ P O S I T l 0 N A L AGE: Late MOSCOViWl- ?hhOVi8tl DAT~G MEHOD: Fusulinids REFERENC~S) FORAGE: Sh011sm 1988 (unpubl.), Nilsson 1994 (unpwbl.)

Fig. 2-98: Stratigraphic section CP-74a Boundary stmtof)tpe for: Kapp Hanna Formation Locality: Efuglvika Reference: Worsley et al. (in prep.)

Fig. 2-97: Syntectonically deposited sandstones with erosive base in

the Kapp Hanna Formation, Kapp Hanna, B j e w a . Photo: D. Worsley

- r

Tllltlillll M W P G B

drivff mcvcg pcbb

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c m .- z

V ) '

3 0 2

0%

2: c -4

z m z 0 '- z m : ; K 0

a:: 0 -4 f. 24

(L Y

correlation between sections

grain size

c j approximate l I 1. ........ .' m 11111111111

M W P G B clsivf f mcvcg pdsb

Fig. 239: Stratigraphic section CP-74b Composite unit stratotpe for: Kapp Hanna Formation Locality: Kobbebukta - Nordvestbukta Refemnce: Worsley et al. (in prep.)

OVERLYING UNIT(S): Kapp Dun& Formation UNDERLYING UNIT(S): Kapp Kilre Formation; see also 'description' SUPERIOR UNIT: Gipsdalen Group ~ T H E R USE OF NAME: None THICKNESS: Up to ca. 150 m MAIN LITHOLOGIES: Sandstone, shale, conglomerate, dolomite LOWER BOUNDARY DEFINITION: The base is defined by a basal extraformational conglomerate overlying various lithologies of the Kapp K&re Formation. The conglomerate contains clasts of various underlying lithologies and is the

Duner

- M W P G B

dsivf f mcvcg pcbb


result of fault movements giving rise to an angular uncofor- mity at the boundary. DESCRIPTION: Much of the formation shows both upwards coarsening and upwards flning intercalations of sandstone and shale deposited in coastal environments. More complex developments are seen at several levels where gulhes cut down into pre-existing deposits, in some cases with marked angular unconformity (Fig. 2-97); these gullies are associated with intraformational faulting and are ididled by extraformational conglo~~~erates deposited by both ephemeral stream flood deposits and submarine debris flows. Clast composition varies markedly stratigraphically and geo-

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graphically. An increasing frequency of clasts derived from progressively older stratigraphic units upwards and southwards on Bjrsrnraya reflects exhumination of strata from the newly developed block over the East of the island and the greater proxhity of southern exposures to this block. Most of the faults seen cutting the Upper Palaeozoic succession on Bjrsrnraya today apparently formed during deposition of the Kapp Hanna Formation.

Basal conglomerates of the Kapp Hanna Formation locally infill faulted relief in the top of the Kapp Kilre Forma- tion (e.g. at Raudnuten); at Alfredfjellet and Hambergfjallet local half-grabens contain local representatives of the Kapp Hanna FO-tion unconformably overlying the Ymerdalen (Pre-Old Red), Rsedvika and Nordkapp formations; suspected basal conglomerates of the Kapp Hanna Formation Fig. 2-101: Vertically stacked Pafaeoaplysina buildups at -et, near

rest directly on the Pre-Old Red southwest of Miseryfjellet. Kapp Duner (Bjimqa) in the Kapp Dunk Formation. Photo: G.B.

The E-W trending grabens and half-grabens seen in the southern cliffs represent the conjugate minor fault systems referred to under the Kobbebukta Member.

Kapp Duner Formation

'7..

6 km - 'L W0RN0YA

Unit stratotype: Amfiet-Teltvika-Kapp Elisabeth, NW Bj-a (composite section) STRUCTURAL SETTING: West Bjsmaya Trough DEPOSITIONAL AGE: Middle Gzhelian - Asselian DATING METHOD: Fusulinids REFERENCE@) FOR AGE: Simonsen 1988 (unpubl.), Nilsson 1994 (unpubl.) OVERLYING UNIT(S): Hambergfjellet Formation, ?Misery- fjellet Formation UNDERLYING UNIT(S): Kapp Hanna Formation SUPERIOR UNIT: Gipsdalen Group OTHER USE OF NAME: None THICKNESS: Up to ca. 90 m MAIN LITHOLOGIES: Dolomite, limestone LOWER BOUNDARY DEFINITION: The base is defined by the

DISTRIBUTION SHOWN ON FIG(s).: 2-05 onset of palaeoaplysinid reef carbonates or associated bed- STATUS OF UNIT: Formal ded dolomites above the alternating carbonateJclastic suc- F m s ~ USE OF NAME: Krasil'BEikov & LivBic 1974 cession of the underlying Kapp Hanna Formation. CURRENT DEFINITION: Worsley & Edwards 1976 DESCRIPTION: Both tabular and lenticular palaeoaplysinid SYNONYM(S) AND REFERENCE(S): "Fusulina limestone": bioherms (Figs. 2-100,2-101) as well as fore-reef carbon- Andersson 1900 ates (Fig. 2-102) occur in the lower parts of formation, often ORIGIN OF NAME: Kapp Dun&: A point on northwestern Bjsrnsya TYPE SECTION (FIGS. 2-103,2-104): Boundary stratotype: Snyta, NW Bjmwya

l

l .. '

l Fig. 2-1Q2: Foreteef

faoies in fhe -p DrmCr l%r!mtion,

Flp;Z-l~.AlmM&diEatGpg . KaPP-, & n a t c d B B o s i t d d & r n M EJjmmya. Plaato: Fahmqplysim Wdups. Photo: G.B. Larssen D. Wrsley

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- - grain size

I l l 1 1 I approximate y m 11111117111

units M W P G B dsivf f mcvcg pcbb

Fig. 2-103: Stratigraphic section CP-75a Boundav stmtofpe for: Kapp Dun& Formation Localiiy: Snyta Reference: Simonsen 1988 (unpubl.)

with marked karstic tops. A sigmficant hiatus around the latest Gzhelian to early Asselian interval is marked by a particularly prominent karst surface. Upper (bedded dolomitic limestone) parts of the formation onlap the topography caused by synsedimentary tectonism responsible for deposition of the Kapp Hanna Formation.

Mineralogical and sedimentological descriptions of different aspects of the formation are given by Siedlecka (1972a, 1975), L o w (1988), Stemmerik & Larssen (1994), Stem- merik et al. (1994), Worsley et al. (in press).

Immediately post-depositional uplift produced tilting and erosion of the formation's topmost beds. Marked karstic features in the type area are infilled with conglomerates showing lithologies similar to those of the Miseryfjellet Forma- tion. Representatives of the formation in small grabens in the island's southern cliffs are overlain by the Hambergfjel- let Formation (Simonsen 1988, unpubl.; Worsley et al., in press).

2.6.3 Bjarmeland Group

BJARMELAND GROUP (CP-76)

STATUS OF UNIT: Formal FIRST USE OF NAME: Committee on Upper Palaeozoic Stratigraphy of the Barents Sea Shelf (in prep.) CURRENT DEFINITION: Here, following the proposal of the

Committee on Upper Palaeozoic Stratigraphy of the Barents Sea Shelf. SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Bjarmeland: An Old Norse name assigned to an area at the White Sea and the river Dvina (northwestern Russia). The group name is derived from the Bjarmeland Platform, a structural element on the southern Barents Sea Shelf. TYPE AREA: Bjarmeland Platform, southern Barents Sea Shelf STRUCTURAL SETTING: Late Palaeozoic platform of Sval- bardBarents Sea Shelf DEPOSITIONAL AGE: Sakmarian - Artinskian OVERLYING UNIT@): Tempelfjorden Group UNDERLYING UNIT(S): Gipsdalen Group SUPERIOR UNIT: None OTHER USE OF NAME: Bjarmeland Platform (Gabrielsen et al. 1990): A syndepositional structural element on the southern Barents Sea Shelf, where the group is typically developed. THICKNESS: 233-488 m on the Bjarmeland Platform, 88- 105 m on the southern Finnmark Platform, up to 70 m on Bj-a MAIN LITHOLOGIES: Limestone, chert, sandstone, siltstone DESCRIPTION: The Bjarmeland Group occurs on the southern Barents Sea Shelf, with a wedge extending onland on Bjorwya. It is thickest throughout the BjarmelandPWom including the eastern flank of the Loppa High and northern areas of the Fhmark Platform. The group onlaps palaeo- highs within the platform and the margins of the depositional basin such as the eastern flank and crestal areas of the Loppa High and the southern parts of the Finnmark Plat- form. In these areas the uppermost part of the group was subaerially exposed and karstified before flooding in the late Permian. Bjsrnsya - situated on the Stappen High which had a similar Permian upliR history - shows a similar overall development to that of the Loppa High. The lower parts of the group, developed in platform and basinal areas offshore, are probably not represented by the onshore exposures on ~~~a.

Lithologies are dominated by white to light grey bioclastic limestones, although dark grey to black and argdlaceous, locally bituminous limestones also occur. Minor amounts of cherts occur, especially in the uppermost part. Minor intercalations of silt- and sandstones are locally recognised. In the reference area on the Polheim Subplatform fine-grained siliciclastics and marls dominate the succession.

Deposition took place in a marine environment d-g an overall rise in relative sea level, except for the lowermost parts of the group that were deposited during a relative low sea level. These "lowstand" sedimenb are confined to the distal and more rapidly subsiding parts of the Bjameland Platform and nortBern areas ofthe Finnmark Plafiorm. Dur- ing the Late kthk ian both basinal margins and structural highs were f l o h d In shallow marine areas coolwater carbonate sedimentation took place giving rise to an abundant fauna of bryozoans, crinoids, echinoderms and brachiopods.

The lower part of the Bjarmeland Group typically comprises large carbonate build-ups dominated by bryozoans

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Location: Amfiet

- M W P G B

dsivf f m cvcg pcbb

Fig. 2-104: Stratigraphic section CP-75b Composite unit stratotype for: Kapp Jhdr Formation Locality: Amfiet - Teltvika - Kapp Elisabeth Reference: Sirnomen 1988 (unpubl.)



....................... ..*

lii. strat m 17111111111 l units

dsivf f mcvcg pcbb

Location: Kapp Elisabeth

l units M W P G B clsivf f rncvcg pcbb

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and Itrbiphytes. These represent major structures, up to 600 m or 700 m thick, which are easy to map on seismic profiles. Inter-reef facies are f i e - m e d carbonate rocks and shales, locally with mass transport sediment5 derived from the reeves. The bioclastic grain-lpackstone to locally wackestone facies of the upper and geographically widespread formation of the Bjarmeland Group contains a fully marine fauna of crinoids, brachiopods, echinoderms, bryozoans and occasional locally sponges, suggesting that sedimentation most probably took place in an open high energy shelf environment.

Although Krasil'SEikov & LivSic's (1974) publication with the name "Alfredfjellet Formation" was issued earlier, the manuscripts were written simultaneously and the original paper in Russian was not readily available to geologists outside the USSR. This is valid for several units on Bjnnnsya. We recommend the use of Worsley & Edward's (1976) nomenclature, because this is better established in the published literature. ORIGIN OF NAME: Hambergfjellet: A mountain on southern Bjarmraya TYPE SECTION (FZGS. 2-105,2-106): Stratotype: Hambergfjellet, southern Bjnnnsya Hypostratotype: Alfredfjellet, southern Bjmrmsya STRUCTURAL SETTING: West Bjarmraya Trough DEPOSITIONAL AGE: ?Salanarian - Artinskian DATING METHOD: Fusulinids, conodonts REFERENCE(S) FORAGE: Sh011sen 1988 (unpubl.); Nakrem et al. 1992 OVERLYING UNIT(S): Miseryfjellet Formation UNDERLYING UNIT(S): Pre-Old Red, Nordkapp, Land- wrdingsvika and Kapp Dunk formations SUPERIOR UNIT: Bjanneland Group

DISTRIBUTION SHOWN ON FIG(s).: 2-05 STATUS OF UNIT: Formal F h S T USE OF NAME: W0rSley & Edw~fds 1976 CURRENT DEFINITION: W0rSley & Edwards 1976 SYNONYM(S) AND REFERENGE(S): "Cora limestone": Andersson 1900; "Alfredfjellet Formation": Krasi17BEikov & LivBic 1974.

Mityfjjllet Formatjon

(Kungunan) correlation between sedlons

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E 0 X P: m W U)

a * 2 4 m grain size grain size

approximate approximate

Tm 11111111111 unrts M W P G B

- M W P G B

clsivf f mcvcg pcbb clsivf f mcvcg pcbb

Fig. 2-105: Stratigraphic section CP-77a Fig. 2-106: Stratigraphic section CP-7% Stmto&pe for: Hambergfjellet Formation Hypostmtotypefor: Hambergfjellet Formation Locality: Hambedellet Locality: Alfredfjellet Reference: Simonsen 1988 (unpubl.) Reference: Simonsen 1988 (unpubl.)

G-

114

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The formation was placed in the Gipsdalen Group by Cut- bill & Challinor (1965) and in the Tempelfjorden Group by Dallmann & Krasil'SEikov (1996), the latter due to its fau- nal relation with the Varingen Member. It is now correlation with intermediate, thickly developed lateral equivalents on the Barents Sea Shelf, the Bjarmeland Group. OTHER USE OF NAME: None THICKNESS: 31.5 m (stratotype), 50 m (hypostratotype), 0-70 m elsewhere on Bjmwya MAIN LITHOLOGIES: Sandy limestone, sandstone LOWER BOUNDARY DEFINITION: The base is defined by an erosional unconformity andlor karst surface below the typical lithologies of the Hambergfjellet Formation. DESCRIPTION: The formation is only preserved on Bj~rmsya's southernmost mountain tops and wedges out rapidly northwards. Basal pebbly and fossiliferous sandstones pass up into bioclastic sandy limestones in the most complete southernmost cliff exposures. The faunas suggest a correlation to uppermost parts of the Gipshuken Forma- tion of Spitsbergen andor to the Varringen Member of the Kapp Starostin Formation. The Hambergfjellet Formation shows some thickness variations over pre-existing half- grabens in the underlying basement and was slightly de- formedslumped prior to deposition of the overlying Miseryfjellet Formation.

2.6.4 Tempelfjorden Group

TEMPELFJORDEN GROUP (CP-78)

SVA

DESCRIPTION: The group consists of siliceous (spiculitic) shales, siltstones and cherts with intercalated minor sandstones and limestones of mid- to late Pennian age, overlying the carbonates of the Gipsdalen Group. Both litho- and bio-l facies contrast strongly with those of the underlying group,, indicating a hydrographic shift to cooler water conditi0ns.l The generally deeper water facies represented in this group also suggest large-scale sea level rise accompanying rifting and establishment of a marine passage from the Boreal Sea in the Barents Sea Region to the North Sea area. The Tempelfjorden Group at present comprises thrbe laterally equivalent formations: Kapp Starostin Formation (Spits- bergen and eastern islands), Tokrossnrya Formation (Sm- kapp area) and MiseTyfjellet Formation (Bjsrwya). Similar successions seen in offshore wells throughout the Barents Sea Shelf will undoubtedly augment present knowledge of the group's development.

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Tempelfjorden (transl. "Temple Fiord"): A fiord between Biinsow Land and Sabine Land, central Spitsbergen TYPE AREA: Mountain areas in Dickson Land and Biinsow Land, central Spitsbergen STRUCTURAL SETTING: Late Palaeozoic platform of Sval- bard/Barents Sea Shelf DEPOSITIONAL AGE: Late Artinskian - Kazanian (?Tatarian) OVERLYING UNIT(S): Sassendalen Group UNDERLYING UNIT@): Gipsdalen Group, Bjarmeland Group SUPERIOR UMT: None OTHER USE OF NAME: None THICKNESS: Up to 460 m MAIN LITHOLOGIES: Chert, siliceous shale, sandstone, limestone

DISTRIBUTION SHOWN ON FIG(s).: 2-06, 2-07, 2-08, 2-09, 2-10 STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): "Brachiopod formation": Nordenskiiild 1863; "Brachiopod Cherts": Gee et al. 1952; "Starostin Formation": Burov et al. 1965. The "Starostin Formation" as defined by Burov et al. (1965) does not contain the Selandemeset member, which is considered as an individual formation by them. ORIGIN OF M: Kapp Starostin: A point on the southern coast of outer Isfjorden. TYPE SECTION (FIG. 2-110): Stratotype: Kapp Starostin, outer Isfjorden STRUCTURAL SETTING: Late Palaeozoic platform of Sval- bard/Barents Sea Sheif DEPOSITION& AGE: hk Artinskian - Kazanian DATING METHOD: various fossils REFERENCE(S) FOR AGE: Biernat & Birkenmajer 1981; Nalcamura et al. 1987; Stemmerik 1988; Nakrem 1988, 1991; Nakrem et al. 1992 OVERLYING UNIT(S): Vardebukta and Vikinghagda formations UNDERLYING UNIT(S): Gipshuken Formation SUPERIOR UNIT: Tempelfjorden Group C ~ ' H E R USE OF NAME: None Tarcmss: Up to 460 m, 380 m in stratotype

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L L

Fig. 2-107: A typical cliff formed by the cherts, spiculitic limestones and sandstones of the Kapp Starostin Formation (upper half of slope) at Skansen (Billefjorden). Photo: J. Nagy

Pig. 2-108: Alternating cherts and spiculitic carbonate rocks of the Kapp Starostin Formation at Skansbukta (Billefjorden). Photo: J.

Fig. 2-109: Section through the Kapp Starostin Foxmation in western Nordenskiold Land showing five depositional units of cherts and other spiculitic lithologies. Photo: E.P. Johannessen

Vardebukta Formation

~drmation (Artinskian)

age I lith. strat m illl11llrn l units M W P O B

dsivf f mcvcg pcbb

Fig. 2-110: Stratigraphic section CP-79/80/8 1/82

Stratotype for: Kapp Starostin Formation, Vsringen, Svenskeegga Hovtinden members

Locality: Kapp Starostin, Festningen section Reference: Hellem 1980 (unpubl.)

and

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MAIN LITHOLOGIES: Chert, siliceous shale, sandstone, limestone LOWER BOUNDARY DEFINITION: The base of the formation is almost everywhere defined by the onset of the Vsringen Member, a distinct marker bed composed of bioclastic limestone, overlying the dolomitic lithologies of the Gipshuken Formation. DESCRIPTION: The Kapp Starostin Formation is developed throughout Spitsbergen and Nordaustlandet in all localities east and north of the Swkapp-Hornsund High (Figs. 2-107, 2-108, 2-109). Its upper parts are also poorly exposed on Edgesya and Barentssya. It is 460 m thick in the St. Jons- fjorden Trough, 380 m in the type section at Isfjorden, and thins to a few metres, and finally pinches out, on the eastern margins of the Ssrkapp-Hornsund High. Lithologies are spiculitic cherts, shales and siltstones, siliceous sandstones and limestones, and dolomites. The overall stratigraphic development is not understood well yet, and the member subdivision of the formation is largely of a preliminary, informal character.

Detailed local descriptions are provided by a number of unpublished theses: Bottolfsen (1994), Cutler (1981), Fredriksen (1988), Hellem (1980), Henriksen (1988), Knag (1980), Saalmann (1995).

Veringen Member (CP-80)

STATUS OF UNIT: Formal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): "Limestone A": Forbes et al. 1958 ORIGIN OF NAME: Vnrringen (named after a vessel): A mountain in western Nordenskiold Land, close to the type locality TYPE SECTION (FIG. 2-110): Stratotype: Kapp Starostin, outer Isfjorden DEPOSITIONAL AGE: Late Artinskian - Kungurian. The V h - gen Member probably corresponds in age to the upper part of the Hambergfjellet Formation andtor the hlatus between the Hambergfjellet and Miseryfjellet formations on Bjmaqa. DATING METHOD: See Kapp Starostin Formation REFERENcE(s) FOR AGE: See Kapp Starostin Formation OVERLYING m @ ) : Svenskeegga member UNDERLYING UNIT@): Gipshuken Formation SUPERIOR UNIT: Kapp Starostin Formation OTHER USE OF NAME: None THICKNESS: Up to 40 m, 22 m in stratotype MAIN LITHOLOGIES: Bioclastic limestone LOWER BOUNDARY DEFINITION: The base is defined at the onset of bioclastic limestone above the dolomitic lithologies of the Gipshuken Formation. DESCRIPTION: The Vnrringen Member consists of limestones rich in brachiopods, bryozoans, crinoids and other marine fossils. It is a transgressive unit and forms widespread and prominent cliffs above the more easily weathered dolomitic limestones of the upper Gipshuken Forma- tion. The member is used as a marker almost throughout Svalbard. It does not occur in northern Oscar 11 Land including Bmggerhalv~ya.

Svenskeegga member (CP-81)

STATUS OF UNIT: Informal FIRST USE OF NAME: C ~ t b a & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Svenskeegga (transl. "The Swede Crest"): A mountain crest in southern Oscar I1 Land TYPE SECTION (FIG. 2-110): Stratotype: Kapp Starostin, outer Isfjorden DEPOSITIONAL AGE: Kungurian - ?Kazanian DATING METHOD: See Kapp Starostin Formation REFERENCE(S) FOR AGE: See Kapp Starostin Formation OVERLYING UNIT(S): Hovtinden member UNDERLYING UNIT(S): Vmingen Member SUPERIOR UNIT: Kapp Starostin Formation OTHER USE OF NAME: None THICKNESS: 150-230 m, 165 m in stratotype MAIN LITHOLOGIES: Spiculitic shale, chert, siltstone, limestone LOWER BOUNDARY DEFINITION: The lower boundary is defined, where clastic lithologies conformably overly the bioclastic limestone of the Vsringen Member. DESCRIPTION: The Svenskeegga member is only defined in its type area at outer Isfjorden. Stratigraphic relations to other sections of the Kapp Stqrostin Formation are not yet understood.

The unit consists of cherts and spiculitic shales as well as siliceous limestones with sponges and sponge spicula, brachiopods (abundant productids and spiriferidi), bryozoans and trace fossils (e.g. Zbophycos). A bioclastic limestone marker bed occurs uppermost in the unit in the Festningen section. Bioturbation and faunas suggest deep marine shelf conditions.

Hovtinden member (CP-82)

STATUS OF UNIT: Informal FIRST USE OF NAME: Cutbill & Challinor 1965 CURRENT DEFINITION: Cutbill & Challinor 1965 SYNONYM(S) AND RE~RENCE(S): None ORIGIN OF NAME: Hovtinden (transl. "The Hoof Pinnacle"): A mountain summit in southern Oscar 11 Land TYPE SECTION (FIG. 2-110): Stratotype: Kapp Starostin, outer Isfjorden DEPOSITIONAL AGE: ?Kazanian DATING METHOD: See Kapp Starostin Formation REFERENcE(s) FOR AGE: See Kapp Starostin Formation OVERLYING UNIT@): Vardebukta Formation UNDERLYING UNIT(S): Svenskeegga member SUPERIOR UNIT: Kapp Starostin Formation OTHER USE OF NAME: None THICKNESS: 200-230 m, 196 m in stratotype MAIN LITHOLOGIES: Silicified shale, siltstone, sandy limestone LOWER BOUNDARY DEFINITION: The base is defined, where shales, sandy cherts or cherty sandstones conformably overlie the bioclastic limestone interval in the upper part of the Svenskeegga member. The boundaj is not defined outside the type area.

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DESCRIPTION: The Hovtinden member is only defined in its type area at outer Isfjorden. Stratigraphic relations to other sections of the Kapp Starostin Formation are not yet understood.

The unit consists of silica-cemented shales, siltstones and sandstones, as well as thin intercalated limestones. The uppermost part of the unit at Festningen shows a slight upwards coarsening trend into silty shales with a decreasing spiculite content.

Revtanna member (CP-83)

STATUS OF UNIT: Informal FIRST USE OF NAME: Here CURRENT DEFINITION: Here, following Knag (1980, unpubl.) SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Revtanna (transl. "The Fox Tooth"'): A mountain in northern Wedel Jarlsberg Land TYPE SECTION (FIG. 2-111): Stratotype: Revtanna, northern Wedel Jarlsberg Land DEPOSITIONAL AGE: ?]Kazanian

D ~ G METHOD: Indirect, s tmipphic relationships REFERENCE(S) FOR AGE: See S&- Formation OVERLYING m(s): Vs* Formation UND-G m(s): Not named SWPEFUOR UNIT: Krrpp Starwtin Formation OTHER USE OF NAME: None THICKNESS: Up to 85 m lMAIN LFFHOLQCJIES: SimWom, shtrle, siltstone, limestone LOWER BOUNDARY DEFINITEON: The bou1dary of the member in the type section is defied at the bottom of a distinct sandstone interval, resting conformably on a limestone bed 58 m above the base of the Kapp Starostin Formation. DESCRIPTION: The Revtanna member comprises the sandstone-dominated, upper part of the Kapp Starostin Forma- tion in SW Spitsbergen, along the eastern margins of the Smkapp Hornsund High. The unit oonsists of three coarsening-upward sequences, each starting with a thin limestone grading up via dark shales or siltstones into very fine or f i e clayey quartz sandstones oRen rich in glauconite. The thickness of the member (82 m in the type section) decreases southward towards the Smkapp-Hornsund High. North- war4 the member interfingers with the dark spiculitic mudstones, limestones and siltstones of the Hovtinden Member.

Stensiiifjellet member (CP-84)

STATUS OF UNIT: Informal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFIERENCE(S): None ORIGIN OF NAME: Stensi6fjeUet: A mountain in Sabine Land TYPE SECTION (FIG. 2-112): Stratotype: Stensiofjellet, Sabine Land DEPOSITIONAL AGE: ?IbZtllign DATING METHOD: Indirect, stratigraphic relationships

- l 7 m units -

clslvf f mcvcg pcbb

Fig. 2-111: Stratigraphic section CP-83 StmtotypeJbr: RRevtanna member Locnliw: Rwkxma Reference: Knag 1980 (unpubl.)

REFERENCE(S) FOR AGE: See h p p Star0sh Formation OVERLYING UNIT(S): Vardebukta and Vikinghag& formations UNDERLYING UNIT(S): Not named SUPERIOR UNIT: Kapp Starostin Formation ~ H E R USE OF NAME: None THICKNESS: Up to 60 m, 27 m in stratotype MAIN LITBOLOGIES: Sandstone, chert LOWER BOUNDARY DEFINITION: The base of the member occurs 30 m below .the Triassic base on the western slope of Stensiofjellet (type locality), at the base of a massive sandstone succession. DESCRIPTION: The Stemiiifjellet member forms a thick sandstone wdge in the uppermost part of the Kapp Starostin Formation in northwestern and central Spits- bergen. The member consists of irregularly interbedded

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(Induan)

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glauconitic sandstones and sandy, spiculitic cherts. Sporadic coquina lags and brachiopod shells occur. The unit's greenish colour in the field reflects its high glauconite content. The lower boundary is gradational from light spiculitic cherts or silicified coquina limestones. The maximum thickness of ca. 60 m occurs in the Billefjorden area and on Brsggerhalvqa. The unit is not correlative with or laterally equivalent to the Selanderneset member.

Palanderbukta member (CP-85)

STATUS OF UNIT: Informal FIRST USE OF NAME: Lauritzen 198 1 CURRENT DEFINITION: Lauritzen 1981 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: PdanderbukW A fiord in southwestern Nordaustlandet TYPE SECTION (FIG. 2-113): Stratotype: Zeipelfjella W, Palanderbukta, Nordaustlandet DEPOSITIONAL AGE: Kungurian - ? U f i a n DATING METHOD: Conodonts REFERENCE(S) FOR AGE: Nakrem et al. 1992 OVERLYING UNIT@): Not named UNDERLYING UNIT@): Not named SUPERIOR UNIT: Kapp Starosh Formation OTAER USE OF NAME: None THICKNESS: 17.5 m in stratotype MAnv LITHOLOGIES: Limestone, chert LOWER BOUNDARY DEFINITION: The base df the member is marked by a sharp lithological break at 46.5 m (in the type section) above the base of the Kapp Starostin Formation. DESCRIPTION: The Palanderbukta member is only observed on Nordaustlandet. It is dominated by limestones which are extremely fossiliferous (brachiopods, subordinate corals). Prevailing lithologies are sandy biosparites, subordinate cherty biosparites and chert. An almost white, 2 m thick chert bed is found in the lower part of the unit. The member offen has a characteristic green colour caused by the presence of glauconite, and some beds consist of almost pure glauconite sandstone.

Selanderneset member (CP-86)

STATUS OF m: Informal FIRST USE OF NAME: BUTOV et d. 1965 CURRENT DEFINITION: Here SYNONYM(S) AM) REFERENCE(S): "Selander Suite": Burov et d. 1965 ORIGIN OF NAME: Selanderneset: A cape on southwestern Nordaustlandet, at Hinlopenstretet TYPE SECTION (FIGS. 2-114,2-115): Unit stratotype: Angelinberget, Selanderneset, Nordaust- landet Boundary and Hypostratotype: Eremitten, Vaigattbogen,

Fig. 2-112: Stratigraphic section CP-84 olav v Land Stratotype for: Stensiofjellet member DEPOSITIONAL AGE: ?Kazanian Locality: Stensiofjellet DATING METHOD: Indirect, stratigraphic relationships Reference: Hellem, T. & Worsley, D. (unpubl.) REFERENCE(S) FOR AGE: Nakrem et al. 1992

119

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?. UPPER PALAEOZOIC LtTHOSTRATlGRAPHY

F A A A A A A A

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Fig. 2-115: St&$raphic section CP-86b Boundary stmto@pe&r: Selanderneset member Locality: bmiitan Refkrcm: Hellem, T. & Worsley, D. (unpubl.)

OVERLYING UNIT(S): Not named UNDE-G UNIT(@: Not named SUPERIOR UNIT: K q p Starostin Formation

OTHER USE OF NAME: None THICKNESS: 30-300 (?) m MAIN LITHOLOGIES: Sandstone, sandy limestone LOWER BOUNDARY DEFINITION: The lower boundary is defined by beds of glauconitic sandstones resting conformably on spiculitic cherts of the underlying part of the formation. DESCRIPTION: Glauconitic sandstones and sandy coquina limestones herein defined as the Selanderneset member occur in the upper part of the Kapp Starostin Formation on Nord- austlandet and in the Lomfjorden area, northeastern Spitsber- gen. This usage is more restricted - both stratigraphically and geographically - than the original "Selander Suite" introduced by Burov et al. (1965). The top is defined by a higher level of spiculitic cherts. Though the member is defined by a higher level of spicitalitic cherts. Though the member is defined by the type locality at Selanderneset, the good exposure at Eremitten (Vaigattbogen, northern Olav V Land) are used as a boundary and hypostratotype. The member is 85 m t5lick here and outcrops between 135 m and 220 m above sea-level on the mountain's northeastern slopes. The member thins westward and passes into spiculitic cherts and shales. It consists of three course sandy limestone to sandstone units with spiculitic interbeds between each of these.

Tokrosssya Formation (CP-87)

DISTRIBUTION SHOWN IN FIG@): 2-06 STATUS OF UNIT: Formal FIRST USE OF NAME: Siedlecki 1964 CURRENT DEFINITION: S id - 1970 SYNONYM(S) AND REFEREIYCE(S): Tokross~ya "Beds": Siedlecki 1964; Brahiopod Cherty Limestone: Birkenmajer & Czamiecki 1960. Formation rank was introduced by Cut- bill & Challinor (1965). ORIGIN OF NAME: TokrOsssya (transl. "Island of the two crosses"): A small island close to the southernmost tip of Spitsbergen TYPE SECTION (FIG. 2-116): Strat0type:Tokrosssya N, Ssrkapp Land STRUCTURAL SETTING: Late Palaeozoic platform of Sval- bardmarents Sea Shelf DEPOS~TIONAL AGE: ?KUIl@aIl- ?KaZaJliaIl DATING MET-FIOD: Invertebrate fossils REFERENCE(S) FOR AGE: Nakrem et al. 1992 OVERLYING UNIT(S): Vardebukta Formation UNDERLYING UNIT(S): Not exposed SUPERIOR UNIT: Tempelfjorden Group OTHER USE OF NAME: None THICKNESS: Up to ca. 425 m exposed MAIN LITHOLOGIES: Chert, siliceous limestone, sandstone

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- m -

dsivf f mcvcg pobb

Y s Y s Y s VVYSYSYS grain size approximate

Fig. 2-116: Stratigraphic section CP-87 Shatotype for: Tokrossarya Formation Localiv: Tokrossqa N Reference: Daham et al. 1993, redrawn from Siedlecka 1970

LOWER BOUNDARY DE-ON: The 10- boundary is m t exposed. DESCRIPTION: The Tokrossaya Formation represents the Tempelfjorden Group on the! smith- side of the Sm- kapp-Hornsund High. The p e n t cxpomes are probably thrust in from the west during the Palaeogene tectonic event.

The basal part of the Tokrosssya Formation is not exposed. The most complete section of 300 m thickness is ex-

posed on Tokrosssya (type section). Siedlecka (1970) pointed out that the original description of Siedlecki (1964) presented the unit in inverted succession; these authors divided the succession into Lower and Upper 'Tokrosssya beds", the lower being dominated by arenaceous, calcareous, spiculitic cherts or spiculites, and the upper by arenaceous, cherty limestones and overlying calcareous sandstones and siltstones. On 0yrlandet and Tokrosssya, the two members are divided by one or several, up to 20 m thick layers of silica-cemented, medium-grained quartz sandstones (Sandhamna beds). Glauconite is present in nearly all rock types. Macrofossils (spiriferids, productids, bryozoans and occasionally sponges) occur predominantly and abundantly within the upper member, but also less frequently at certain levels of the lower member. Pectenids are found in some places within the lower member. Plant remains occur within the quartz sandstones and intercalated arenaceous limestones on 0yrlandet.

Siedlecka (1970) provided a detailed sediment-petrologic analysis of the individual rock types and concluded that the sediments were deposited in an epicontinental marine environment with a maximum transgression during the deposition of the cherts of the lower member under relatively deep, quiet, restricted conditions, probably within depressions on the outer shelf. The arenaceous rocks of the upper member indicate shallowing and littoral influx.

Sandhamna beds (CP-88)

STATUS OF m: Informal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Sandhamna: A bay in SW @yrlandeet, southern S&pp Land TYPE SECTION (FIG. 2-117): Sandhamm, 0yrlandet SW Ssrkapp Land DEPOS~IONAL AGE: ?Ufh lk - ?Kazanian DATING METHOD: Indirect, stratigraphic relationships REFERENCE(S) FOR AGE: See Tokrosssya Formation OVERLYING UNIT(S): Not named UNDERLYING UNIT(S): Not named SUPERIOR UNIT: Kapp Starostin Fonnation CY~EER USE OF NAME: None THICKNESS: ca. 70 m stratotype MAIN LLTHOLOGIES: Sandstone LOWER BOUNDARY DEFINITION: The base of the unit is the first massive sandstone bed in the middle part of the Tokross@ya Formation. DESCRIPTION: The San- beds occur on both sides of the NNW-SSE trending synciine passing though 0yrIandet. On the SSW fold limb, they run from San- to Skjer- odden; on the NNE fold limb, they occur on 0yrlandsodden and Tokrosserya. They reappear on Smkappsya.

The Sandhamna beds comprise one or up to four, up to 20 m thick sandstone beds, intercalated with arenaceous cherty limestones of the middle part of the Tokrosssya For- mation. The sandstones are silica-cemented, medium- grained quartz sandstones with a distinct glauconitic component.

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2. UPPER PALAEOZOIC L ITHOSTRATIc~aDYV

- c , 8

- - d d v f f m cvcg pcbb

Fig. 2-117: Stratigraphic section CP-88 StmtotJpe for: Sandhamna beds Locality: Sandhamna Reference: Dallmann et al. 1993, redrawn from Siedlecka 1970

Fig. 2-118: Miseryfjellet on Bjemeya, seen from the east. The steep wall in the middle of the slope consists of the siliceous rocks of the Miseryfjellet Formation, morphologically well distinguished from the underlying Late Devonain Rsedvika Formation and the overlying Triassic strata (Urd and Skuld formations). Photo: W.K. Dall- mann

STRUCTURAL SETTING: Late Palaeozoic platform of Sval- bard1 Barents Sea Shelf DEPOSITIONAL AGE: Kun@an- Uf f i an DATING METHOD: Conodonts REFERENCE@) FOR AGE: Nakrem 1991 OVERLYING UNIT@): Urd Formation UNDERLYING UNIT@): Rsedvika, Nordkapp, Landwrdings- vika, Kapp m e , Kapp Dun& and Hambergfjellet formations SUPERIOR UNIT: Tempelfjorden Group OTHER USE OF NAME: "h4isery Subformation": Pavlov et al. 1983 (see section 2.7.1) THICKNESS: 90-1 15 m MAIN LITHOLOGIES: Siliceous limestone, sandstone LOWER BOUNDARY DEFINITION: The basis is defined at the overstep unconformity, where Kungurian sandstones and conglomerates overlie various older formations. DESCRIPTION: Basal sandstones and conglomerates onlap and overstep all older units on Bjsmnrya. Locally these basal beds fill up to 10 m deep karstic features in underlying dolomites of the Kapp Dun& Formation. Most of the formation consists of partially silicified grainstones and packstones, with a 12 m thick cross-bedded quartzitic sandstone developed 20 m above the base of the unit. A rich fauna of brachiopods, bryozoans and crinoids is very similar to that of correlatives on Spitsbergen (e.g. Gobbett 1963). Outliers on the island's northern coast preserve only the lowermost 10 m to 15 m of the formation. (Fig. 2-1 18)

DISTRIBUTION SHOWN ON FIG@).: 2-05 STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley & Edwards 1976 CURRENT DEFINITION: Worsley & Edwards 1976 SYNONYM(S) AND REFERENCE(S): "Spirifer limestone": Andersson 1900; "Laksvatnet Formation": Krasil'BEikov & LivBic 1974. Although Krasil' SEikov & LivBic (1974) publication with the name "Laksvat.net Formation" was issued earlier, the 2.7 Abandoned lithostratigraphic unit names manuscripts were written simultaneously. This is valid for several units on B j m q a . We recommend the use of 2.7.1 Names with aplace name segment

Worsley & Edward's (1976) nomenclature, because this is Names listed in this section are not recommended for future better established in the published literature. use. They are either synonyms of other, preferred names, or ORIGIN OF NAME: Miseryfjellet: A mountain on Bj~rmnrya describe units that overlap, or are incompatible, with an- TVPE SECTION @G. 2-119): other, preferred stratigraphic subdivision. Preferences are Stratotype: Brettingsdalen, Miseryfjellet, Bjsmnrya discussed in sections 2.3 and 2.5.

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E

RBledvika Formation

(Tournaisian- Famennian) -

M W P G B clsivf f mcvcg pcbb

Fig. 2-119: Stratigraphic section CP-89 Smtotypefor: Miseryfjellet Formation Locality: Brettingsdalen, Miseryfjellet Reference: Hellem, T. & Worsley, D. (unpubl.)

Some names describe local facies that SKS does not consider to deserve lithostratigraphic names in order to keep the number of names low. Such names should only be used for detailed, local investigations, but they should not form part of the regional lithostratigraphic scheme.

Within every entry, the synonym or superior unit name which should be consulted in the lexicon (section 2.6) is indicated with its ID number.

Alfredfjellet Formation (Krasi17SCikov & Livgic 1974): Syn- onym of Hambergfjellet Formation (Worsley & Edwards 1976). Due to little scientific contact between West European and Soviet geologists at that time, stratigraphic schemes were developed contemporaneously and independently. The name Hambergfjellet Formation (CP-77) is preferred because it is better established in the geological literature.

Anservllra beds (Cutbill & Challinor 1965): Part of the Mdanfjellet Formation (Moscovian). Proposed member rank (Dallmann 1993). It is correlative to the Terr'er$ellet member of the Minkinjellet Formation. The name has been confused with the "Anservika Member" of Gjelberg (1984, unpubl.) which was assigned to the redbeds of the "Hultberget Member" of the "Svenbreen Formation" (Ser- pukhovian/?Bashkirian). Due to this confusion, the name should be avoided. See Tewer$ellet member (CP-32) and Hultberget Fonnation.

Drevbreen beds (Nys~ther 1977): Local equivalent of the Treskelodden Formation in central Torell Land; the latter name has clear priority. The name 'Drevbreen' has also been used for a Triassic unit in the same area (Birken- majer 1977). See Tmskelodden Formation (CP-45).

Ebbabreen sandstone beds, E. shale beds (Holliday & Cut- bill 1972): The names describe very local facies within the Ebbaelva Member of the Ebbadalen Formation. There is no need for these names. See Ebbaelva Member (CP-27).

Elsabreen (conglomerate) beds (Cutbill & Challinor 1965): Local name for an equivalent of the OdelEellet Member of the Ebbadalen Formation. Odel&jellet Member (CP- 28) has priority due to its established position in the geological literature.

FerrierfSellet Breccia (McWhae 1953): Local breccia at base of Minkinjellet Formation (Carmnelva member; CP-31) at Ferriefjellet.

Fortet Breccia (McWhae 1953): See Fortet member (CP- 33).

Fugle Subformation (Pavlov et al. 1983): Incomplete place name (Fugleodden; could be confused with Fuglefjellet). Upper, coal-barren part of the Tunheim Member of the Reedvika Formation on Bjmwya. The reason for a revision of the member subdivision of the Rktedvika Forma- tion is not obvious. See nnheim Member (CP-19).

Gerritelva sandstone Member (Holliday & Cutbill 1972): The name is superfluous, since the unit is correlated with Ebbaelva Member (CP-27) of the Ebbadalen Formation. The latter name is preferred because it is well-established in the geological literature.

Grytvika Bed (Sirnomen 1988, unpubl.): Fusulinid limestone bed in the Kapp Dunkr Formation (CP-75), Bjm- oya. The lower one of three correlatives (see also Knort- odden and Teltvika beds) of the Brucebyen Beds (CP-56)

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of Spitsbergen. The bed has a limited exposure and is probably not useful as a marker bed. The use of the name should be restricted to specialised local investigations.

Jotunfonna beds (Cutbill & Challinor 1965): A section within the former 'TJordenskioldbreen Formation", defined only by its fusulinid content. The name has no lithostratigraphic application. See Kapitol Member (CP- 49) and Msrebreen Member (CP-48).

Kapp Fanshawe Formation (Nordenskiold 1863): Outdated name comprising the Billejorden and Gipsdalen p u p s in the Lomfjorden area.

Kapp Ziehen unit (Lock et al. 1978): Synonym of Kapp Stamstin Formation (CP-79) on the islands of Barentsnrya and Edgeraya. Exposures are poor and no individual units within the formation should be defined here.

Knortodden Bed (Simonsen 1988, unpubl.): Fusulinid limestone bed in the Kapp Dun& Formation (CP-75), Bjsmsya. The upper one of three correlatives (see also Grytvika and Teltvika beds) of the Brucebyen Beds (CP-56) of Spitsbergen. The bed has a limited exposure and is probably not useful as a marker bed. The use of the name should be restricted to specialised local investigations.

Kobbebukta Formation (Krasil'SEikov & LivSic 1974): Synonym of Kapp Kdre Formation (Worsley & Edwards 1976). Due to little scientific contact between West Euro- pean and Soviet geologists at that time, stratigraphic schemes were developed contemporaneously and independently. The name Kapp Kdre Formation (CP-70) is preferred because it has been established better in the published geological literature and designates better exposure of the formation.

Labvatnet Formation (Krasil'SEikov & LivSic 1974): Syn- onym of MiseMellet Formation (Worsley & Edwards 1976). Due to little scientific contact between West Euro- pean and Soviet geologists at that time, stratigraphic schemes were developed contemporaneously and independently. Though the formation underlies the lake Laks- vatnet, there are no satisfactory outcrops of the formation in the vicinity of the lake. The name MiseMellet Forma- tion has been established better in the published geological literature. Though the place name 'Misery' previously was used for a part of the Upper Devonian Raedvika For- mation (Horn & Orvin 1928; Evdokimova et al. 1986), by the latter in a biostratigraphic context, the name Miseryf- jellet Formation (CP-89) should be preferred.

Margaretbreen Conglomerate Facies (Holliday & Cutbill 1972): A local succession of dolomite breccias, conglomerates and sandstones at the base of the ~ikolorjellet Member (CP-29).

Misery Subformation (Pavlov et al. 1983): Incomplete place name (Mueryfjellet). The name 'Miserytjellet' has also been used for the "Laksvat.net Formation" by Worsley & Edwards 1976. Part of the Vesalsmda Member og the Rsedvika Formation, based on biostratigraphic evidence. The reason for a revision of the member subdivision of the Rsedvika Formation is not obvious. (See Vesalstmnda Member {CP-17).

Nordenskiiildbreen Formation (Cutbill & Challinor 1965): A unit composed of 9 members, if all later defined

changes are considered (7Jwel@ellet, Cadellfjellet, Kapi- tol, Minkinfiellet, Msrebreen, Scheteli&ellet, Jutulslottet (unpubl.), Idunflellet and Hdrbardbreen members). The 'formation'is too complex and heterogeneous and is not compatible with recent advances in our understanding of the stratigraphic development. Several of its members have been raised to formation rank (see Minkinjellet, Schetelidellet and Hdrbardbreen formations). The remaining members (lj~rellfjellet, Cadel@ellet, Marebeen, Kapitol and IdunJjllet members) are assigned to a new formation; see Wordiekammen Formation (CP-47).

Petrelskardet Shale Formation: See Petrellskaret Forma- tion.

Pyramiden bedslconglomerates (Gee et al. 1952), F! For- mation (LjutkeviE 193713, Ustrickij 1967): equivalent of OdelGellet Member (CP-28). The latter name has clear priority due to its established position in the geological literature. Cutbill & Challinor's (1965) correlation with the Minkinjellet Formation ("Member") is rejected by more recent investigations (Johannessen 1980, unpubl.; Johan- nessen & Steel 1992; Dallmann 1993).

Ragnarbreen Breccia (McWhae 1953a): Local breccia at base of Minkinfiellet Formation (Camnelva membe,: CP- 31)) at Ragnarbreen and Ebbabreen.

Reinodden Formation (Cutbill & Challinor 1965): The name has been used by several authors for Upper Car- boniferous to Lower Permian conglomerates and sandstones in the Bellsund area. These were tentatively correlated with the Hyrnejellet Formation by Cutbill & Challinor (1965), but after detailed mapping been correlated with the Treskelodden Formation in the Homsund area (Johannessen et al. 1984, unpubl. report, Statoil; Dallmann et al. 1990; Ohta & Dallmann 1994). The name Treskelodden Formation (CP-45) has priority due to better definition and type descriptions.

Ritleodden Conglomerate Bed (Worsley & Edwards 1976): A local conglomerate in the lower part of the Zbnheim Member (CP-19) of the Rsedvih Formation on Bjnrmraya. It is not easily distinguished from other conglomerate beds and has no lithostratigraphic d u e .

Selander Suite/Fonn;ition (Burov et al. 1965): An incomplete place name; see Selanderneset member (CP-86).

Skrekk Subformation (Pavlov et al. 1983): Incomplete place name ('Slareklguvet' or 'Skrekkodden'?). Part of the Vesalsfrunda Member of the Rgedvika Formation, based on biostratigmtphic evidence. The reason for a revision of the member subdivision of the RBedvika Formation is not obvious. See Vesalshnda Member (CP-17).

Starostin Formation (Burov et al. 1965): An incomplete place name; see Kapp Starostin Formation (CP-79).

Svenbreen Formation (Cutbill & Challinor 1965): This formation contains a major hiatus and change in sedimentary environment. The upper member of the formation is raised to formation rank (see Hultberget Formation, CP-25), while the two lower members (Sporehagda and Birger Johnsonfjellet members) form the Murnien Formation (CP-05).

Teltfjellet Member (Holliday & Cutbill 1972): The name is superfluous, since the unit is correlated with the Triblor- flellet Member (CP-29) of the Ebbadalen Formation. The

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latter name has priority because it is well-established in the geological literature.

TelMka Bed (Simonsen 1988, unpubl.): Fusulinid limestone bed in the Kapp Dunkr Formation (CP-75), B j m y a . The middle of three correlatives (see also Gryt- vika and Knortodden beds) of the Brucebyen Beds (CP- 56) of Spitsbergen. The bed has a limited exposure and is probably not useful as a marker bed. The use of the name should be restricted to specialised local investigations.

Tokrosseya Beds, Lower and Upper (Siedlecki 1964; Siedlecka 1970), with member rank (Dallmann et al. 1993): Informal subdivision of the Tokross~ya Formation (CP-87) into a lower (mainly calcareous spiculitic cherts) and an upper (mainly siltsones, sandstones and cherty limestones) unit. The subdivision is useful, but formal member names should be found with knowledge of suitable localities.

Trygghamna Formation (Dineley 1958): A Lower Car- boniferous sandstone unit of the Trygghamna area correlated with the Orustdalen Formation. Although 'Trygg- hamna' is the first published name, the name Orustdalen Formation (CP-08) is better established in the geological literature.

Tunheim Subformation (Pavlov et al. 1983), according to "'Ihheim series" (Horn & Orvin 1928): Lower, coal-bearing part of the Tunheim Member (CP-19) of the medvika Formation. The extended meaning of the Tunheim Mem- ber (Worsley & Edwards 1976) is better established in the literature and should be preferred.

Urmstonfjellet Limestone Bed (Holliday & Cutbill 1972): A limestone bed in the lower part of the Camnelva member (CP-31). There is no reason for specially naming this bed which is one among other equal ones.

Vegard Formation (Dineley 1958): Incomplete place name, see Vegardjella Formation (CP-09).

2.7.2 Names without a place name segment

Names without a place indicative segment are in general old, informal names that meanwhile have been substituted by formal names. For a number of names, the grouping of strata does not correspond to the more recent lithostratigraphic subdivision. Almost all of these names are today out of use. They are listed here with their reference (first published) and indication of stratigraphic range for the purpose of understanding older geological literature in a modem context.


Ambigua limestone (Andersson 1900): Synonym of Kapp Kdre Formation (CP- 70)

Anhydrite member (Bates & Schwarzacher 1958): Part of Gipshuken Formation (CP-60)

Brachiopod cherts (Gee et al. 1952): Synonym of Kapp Starostin Formation (CP- 79)

Brachiopod Cherty Limestone (Birkenmajer & Czarniecki 1960): Synonym of Tokrosstaya Formation

(CP-87) Brachiopod formation (Nordenskiold 1863): Synonym of

Kapp Starostin Formation (CP- 79) Calciferous Sandstone Series (Holland 1961): Synonym

of S~r$onna Member (CP-66) Cancrinella limestone (Birkenrnajer & Logan 1969): Local

variant of Gipshuken Formation (CP-60) Carbonate Member (Lowell 1968): Synonym of Wordie-

kammen Formation (CP-47) Cora limestone (Andersson 1900): Synonym of Hamberg-

fiellet Formation (CP-77) Culm sandstones (Nathorst 1910): Synonym of Bille-

fiorden Group (CP-01) Cyathophyllum limestones (Nordenskiold 1875): Name

for the entity of Minkinjellet, Wordiekammen and Gips- huken formations (CP-30,47, 60)

Evaporite series (Bates & Schwarzacher 1958): Parts of Wordiekammen and Gipshuken formations (CP-47, 60)

Fusulina limestone (Andersson 1900): Synonym of Kapp Dunkr Formation (CP- 75)

Gypsum beds (Nathorst 1910): Synonym of Gipshuken Formation (CP-60)

Gypsum member (Bates & Schwarzacher 1958): Synonym of Vengeberget member (CP-61)

Limestone A (Forbes et al. 1958): Synonym of V~ringen Member (CP-80)

Limestone B (Gee et al. 1952): Synonym of Finladellet Beds (CP-57)

Lower Dolomite member (Bates & Schwarzacher 1958): Synonym of Kiarjellet Beds (CP-58) at Ekmanfjorden

Lower Gypsiferous series (Gee et al. 1952): Synonym of Ebbadalen Formation (CP-26) without Odelljellet Member

Lower Gypsum zone (Cutbill & Challinor 1965): Synonym of Vengeberget member (CP-61)

Lower Redbed Facies (Holliday & Cutbill 1972): Lower part of Odel@ellet Member (CP-28)

Passage beds (Wordie 191 9; Gee et al. 1952): Minkinjellet Formation (CP-30) with part of Ebbadalen Formation (CP-26)

Productus-bearing limestones and cherts (Nordenskiold 1871): Synonym of Kapp Starostin Formation (CP-79)

Red conglomerate (Andersson 1900): Synonym of Land- n~rdingsvika Formation (CP-69)

Spirifer limestone (Nordenskiold 1871): Synonym of V~ringen Member (CP-80)

Spirifer limestone (Andersson 1900): Synonym of Misery- Jellet Formation (CP-89)

Upper Gypsiferous series (Gee et al. 1952): Synonym of Gipshuken Formation (CP-60)

Upper Gypsum Zone (Cutbill & Challinor 1965): Upper part of Gipshuken Formation (CP-60) in western Spits- bergen

Upper Redbed Facies (Holliday & Cutbill 1972): Upper part Odelljellet Member (CP-28)

Ursa sandstone (Holtedahl 1920): Synonym of R~edvika and Nordkappformations (CP-16,20)

Yellow sandstone (Andersson 1900): Synonym of Kapp Hanna Formation (CP-74) .

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3. MESOZOIC LITHOSTRATIGRAPHY

3.1 Stratigraphic development of Svalbard and the Barents Sea Shelf

The chapter on Mesozoic stratigraphy of Svalbard also comprises the offshore deposits of the western Barents Sea Shelf, although offshore deposits are not included in the discussions of the Upper Palaeozoic and Tertiary of Svalbard. The present knowledge of the essentially continuous stratigraphy and spatial relations of the Mesozoic succession of the entire Barents Sea Shelf supports the establishment of a common stratigraphic framework. The offshore units are included in the lexicon text (Chapter 3.5) and in the Correla- tion scheme (Fig. 3-05), but are not represented by maps and type sections. The reader is referred to the cited publications on the Barents Sea Shelf.

The Barents Sea Shelf, with Svalbard forming its exposed northwestern corner, was an area of clastic deposition during the entire Mesozoic. While carbonate sedimentation had prevailed from the late Carboniferous into the Pennian, the late Permian had seen a transition to cherty/spiculitic mudstone deposition in basinal areas and interbedded bioclastic limestones and shales in platform settings. An extensive late Permian hiatus, seems to have developed everywhere. This hiatus was submarine in basinal areas, while marginal areas were exposed and locally not transgressed before the late Early Triassic. Major sedimentary basins were developed over the main Svalbard islands, the Bjorn0ya Basin, Hammerfest Basin and Nordkapp Basin of the Western Barents Sea Shelf and the Central Barents Sea Depression west of Novaja Zemlja (Fig. 1-02). These basins were separated by shallow shelf or platform areas, surrounding land areas or local highs. An extensive seaway connected these basins - and other basins southward to the North Sea area - during most of the Mesozoic, and deltaic and coastal sediments prograded into the sea from different land areas, cre- ating a complex pattern of sedimentary units. Erosion and redeposition of the clastic sediments was important during long periods.

During most of the Mesozoic, the main land and sedimentary provenance area for the successions deposited in Svalbard was situated to the west of Svalbard (eastern North Greenland), from where most sediment bodies built out into the easterly basin. An additional northern to northeastern source area became evident from the Late Triassic (Steel & Worsley 1984), and at Kong Karls Land also from north and east (Olaussen et al., in prep.). All Mesozoic sedimentary episodes led to sedimentation across all of Svalbard, possibly except northemmost areas, where the record is lacking, both due to the periodical absence of sedimentation and to later stripping off of sediments.

In the Barents Sea, a complete stratigraphic nomenclature is only established for the Hammerfest Basin, while in other areas only a few units are defined at present.


TraQtionally, three lithostratigraphic groups have been defined in the Mesozoic succession of Svalbard (Sassendalen, Kapp Toscana and Adventdalen groups: Buchan et al. 1965; Parker 1967) and five in the southwestern Barents Sea (Ing~rydjupet, Realgrunnen, Teistengrunnen, Nordvest- banken and Nygrunnen groups: Worsley et al. 1988; Fig. 3- 02). In the present proposal, those Barents Sea Shelf groups that have equivalents on land apply the group names defined on land. For the Triassic to Middle Jurassic of the Barents Sea Shelf, the previous subdivision is taken care of by con- verting previous groups into subgroups (Fig. 3-01). One group (Nygrunnen Group) was only deposited on the Bar- ents Sea Shelf when Svalbard was uplifted at the end of the Mesozoic.

The Sassendalen Group was defined on Spitsbergen by Buchan et al. (1965) and comprises shales, siltstones and sandstones of Early and Middle Triassic age. The group's coastal to deltaic sediments exposed on western Spitsbergen grade into organic-rich shelf mudstones eastwards in Sval- bard and southwards into the Barents Sea Shelf, however, a thick marine to coastal clastic succession is deposited in the Hammerfest Basin (southwestern Barents Sea Shelf).

Worsley et al. (1988) defined the "Ingsydjupet Group" in the Hammerfest Basin for the Induan to Anisian shales and claystones grading upwards into Ladinian and Carnian compositionally immature sandstones. In the present nomenclature, the name Ingoydjupet Subgroup is reserved for the finer-grained Induan - Anisian succession of the Barents Sea Shelf. The subgroup is correlated with and included in the Sassendalen Group. The Ladinian - Carnian sandstone- rich succession is correlated with and included in the overlying Kapp Toscana Group.

The Kapp Toscana Group, originally defined by Buchan et al. (1965) as a formation, comprises sandstones and mudstones of late Middle Triassic to Middle Jurassic age. The group represents a significant change in sedimentary regime from the underlymg groups, and a turn into similar shallow marine to deltaic depositional environments across the entire Barents Sea Shelf.

The StoMorden Subgroup (new name) comprises the compositionally immature sandstones and mudstones oflate Middle (Ladinian) and early Late Triassic age deposited in coastal to shallow marine environments. The subgroup comprises the lower part of the Kapp Toscarra Group, includmg

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prises a basinal, shaley development, with condensed calcareous sandstones in plat-

Fig. 3-01: Group and subgroup subdivision of Mesozoic rocks

the upper, compositionally immature part of the "Ingray- djupet Group" on the southwestern Barents Sea Shelf as defined by Worsley et al. (1988).

The JFTlhelm0ya Subgroup corresponds to the "Wilhelm- sya Fonnation" (Worsley 1973; Bjaerke & Dypvik 1977; Edwards et al. 1979) ip the Svalbard area. The variedly condensed development in different areas of Svalbard led to the establishment of several formations within the succession and the change of the Wilhelmsya unit from formation to subgroup rank. The subgroup consists of texturally mature sandstones deposited on coastal plains and in deltaic through shalloy marine environment; it shows an increasingly condensed development towards the west.

The Realgrunnen Subgroup was defined with group rank by Worsley et al. (1988) in the Hammerfest Basin. The recent understanding of the intermediate nature of the coeval deposits of Kong Karls Land, and data fiom numerous cored wells in the Barents Sea, correlate this succession with its condensed counterpart in Svalbard, the Wilhelm~a Sub- group and makes it appropriate to include the succession in the Kapp Toscana Group.

The Adventdalen Group was defined on Spitsbergen by Parker (1967) for the shales and minor sandstone successions of latest Middle Jurassic to Early Cretaceous age. The group is here laterally extended to include correlative sediments on Kong Karls Land and in the southwestern Barents Sea, previously referred to as the "Teistengrunuen" and 'Wordvestbanken groups" (Worsley et al. 1988). Dark organic-rich shales of Late Jurassic age occur throughout the area. A hiatus of varying magnitude above these shales reflects a period of tectonic disturbance at the Jurassic - Cre- taceous transition, well established in the Barents Sea. This is followed by calcareous sedimentation on platform areas and dark, but organic-lean, shales in the basins. In the north, in Svalbard, deltaic sedimentation gave rise to the deposition of prominent sandstone bodies.

The JanusBellet Subgroup (Parker 1967) comprises the dark shale succession of latest Middle Jurassic to Hautenv- ian age in Svalbard.

The Nygrunnen Group (Worsley et al. 1988) is only documented in the southern part of the Barents Sea and com-

l form setting. The group is of Late Cretaceous age.

3.3 Previous stratigraphic schemes

Most authors who have elaborated previous stratigraphic schemes for Svalbard worked either on the Triassic to Middle Jurassic (Swendalen and Kapp Toscana groups; Fig. 3-03), or the Middle Jurassic

to Early Cretaceous (Adventdalen Group; Fig. 3-04). This was a natural consequence of the major sequence boundary between these two groups which also is reflected in the quite different lithologies below and above. Exceptions are PEelina (1980, 1983), presenting results of the Russian research on the archipelago, and stratigraphers workmg on some of the eastern islands (Worsley 1973; Smith 1975; Smith et al. 1975, 1976).

The Triassic to Middle Jurassic of Svalbard has histori- cally often been referred to as the Triassic only, due to the fact that the Jurassic represents a very condensed succession in the best accessible (western and central) parts of Sval- bard, often only a few metres thick. This changed with the recognition of the much thicker Jurassic sections on Wilhelmsya (Worsley 1973; Smith 1975), Hopen (Smith et al. 1975) and Kong Karls Land (Smith et al. 1976).

The "Triassic" stratigraphy was first summarised into a common scheme by Buchan et al. (1965) which was widely applied until the early 1980s. Several local adjustments were then made (Flood et al., 1971, and Lock et al. 1978, on Edgeraya and Barentssya; Worsley & Mnrrk, 1978, in southem Spitsbergen), until Marrk et al. (1982) summarised the revised view into a new scheme, this time paying attention to the differential stratigraphic development on western and centralleastern Spitsbergen.

The "Jurassic-Cretaceous" stratigraphy was firstly summarised into a common scheme by Parker (1967). Minor adjustments or supplements for individual regions were made by Norwegian and British authors (Nagy 1970; Smith et al. 1976). A detailed subdivision of the Janusfjellet Subgroup in central and eastern Spitsbergen was presented by Dypvik et al. (1991).

More or less simultaneously with Mwk et al. (1982), a different stratigraphic nomenclature was developed by PEelina (1980,1983), also reflecting the regional@ varying stratigraphic development, but showing a greater influence of chronostratigraphic thinking, i.e. a trend to summarise lithologies into formations (Russian: svity, lit. transl. "suites"') according to their related stage.

A major effort was undertaken by the Stratigraphic Com- mittee of Svalbard in the context of the present compilation to elaborate a synthesis of the Russian and Norwegian schemes, while maintaining as many names as possible

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by upward coarsening shale-siltstonelsandstone sequences, and the upper unit by phosphatic, organic-rich shales and subordinate sandstones.

B u c b et al. (1965) defmed three formations within this group, the Vardebukta Fonnation, "Sticky Keep Formation" and Botneheia Forma- tion, of which the two upper units formed the "Kongressfjellet Sub- group". The latter was

Ing~ydjupet Group Sassendalen Group

changed to formation rank by FIood et al. (1971), but this was only applied on the map sheet Adventdalen (Major & Nagy 1964,1972), and has been rejected by subsequent authors. This rejection may have been a- consequence of the problems arising when defining the lower boundary of this unit.

From the 1970s onward, separate subdivisions were introduced for centraYeastern and western Svalbard, due to the different facies development in both areas. The two developments are thought to have a transition at depth below the younger fill of the Central Tertiary Basin, with a proximal, coarse-grained facies to the west, and a more distal, shale- dominated facies to the east.

The suggested member subdivision of the Sassendalen Group's formations in Svalbard (Fig. 3-05) is a synthesis of the units of Buchan et al. (1965), Birkentmjer (1977), Mmk et al. (1982) and PEelina (1983), some of them with a revised rank. A few members, from all of these authors, may be subjected to further refinements after more thorough fieldwork. These units are provisionally maintained with an informal status (Fig. 3-05).

Fig. 3-02: Revision of Mesozoic group/subgroup subdivision of the Barents Sea Shelf

shown on published maps without major redefiitions, and at the same time taking care of as many as possible priori- ties by first publication. This resulted, of course, in a number of compromises. Still, the revised scheme (Fig. 3-05) has preserved the traditional group subdivision and most formation names f d a r from published maps. At the same time, it takes into account important stratigraphic units and correlations from the Russian scheme represented by PEelioa (1980, 1983), though this is not always reflected by the names themselves (for account of choice of names: see chapters 3.4,3.5 and 3.6.1).

Historic priority is the main criterion for recognition and acceptance of lithological unit names, however, many terms have been poorly defied in the past or have first been mentioned in areas where they are poorly exposed or developed Several units have been emended or redefined to adjust the stratigraphic framework to the meanwhile improved knowledge level, or to enable correlations between these areas and the Barents Sea Shelf. The present synthesis also tries to incorporate regional variations, often by redefining type tections (stratotypes), or by defining reference sections (hy- postratotypes) in addition to the type sections, or by accept- ing locally or regionally developed subdivisions at member level.

Central and eastern areas: Lock et al. (1978) included all shales of Early and Middle Triassic age on the islands Barentsarya and Edgenrya in the "Barentwya Fonnation", with the organic-rich dark shales (previously named Botneheia Fornation) distinguished as the "Oil Shales Member". For central and eastern Spits- bergen, Msrk et al. (1982) kept the terminology of Lock et al. (1978), but retained the three previously defined formations of Buchan et al. (1965) at member level. PEelina (1983) also retained a tripartite subdivision of the Lower and Middle Triassic, and introduced the new name "Wiche- bukta Formation" for the upper Lower Triassic (Olenekian) of eastern Svalbard, while restricting the Botneheia Forma- tion to the organic-rich shale lithologies in central and eastern Spitsbergen, Barentsnrya and Edgesya.

As indicated above, there were difficulties in recognising the boundary between the two lower subunits of the group (Deltadalen and "Sticky Keep" members) in central Spits- bergen. This may be due to the circumstance that there is another similar, distinct lithological boundary within the "Sticky Keep Member". Even the best available regional survey, Major & Nagy's (1964) map sheet Adventdalen has

3.4 Regional descriptions and major revisions

3.6.1 Sassendden Group

The Sassendalen Group is maintained as originally defied by Buchan et al. (1965) on central Spitsbergen. The major revision is the lateral extension of the group to include the Ing~ydjupet Subgroup of the Barents Sea.

In Svalbard (except Bjmwya) the subdivision of the group into three units h been applied in all previous stratigraphic work, although with different hierarchies and regional implications. The lower unit is characterised by shallow marine to coastal silt- and sandstones, the middle unit

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- ms- Famatkm KetlhaufidleY Fmatbon W@Wma/a S m W M b . S m W * mc)mWr Formation Fwm&iw

fw&upbr lsfjorden Formation

nFor m De Gwdslen Formation De Geenlalen m Mb.

h Qwrdalen Formation F ~ M Hehnrjella Formation

TSDhwa Tschemakfjelket Fornetion Awstl&den Formation T.WtermaIdje1let Formation M b 6 r

Van Keuienfjwden Formation Van Kwkrd]. Mb rmation ~om~lbfirm b. m m e ~ 8~""atren b. Bravaisbergst Somovbreen Mb- 0Bravsbtqex ~~ Mb

pamhmn m. Formation Mb, Hymefjdlet Formation F ~ a t i o n "m&OPW m- Formation k-pen Mb Paaabmen Mb. Pawhatten Mb.

Sticky Keep Fomation Sticky Keep Formation Pitnerodden Formation Tvfl'lnwdden Tvlllingoddsn

Vardebubta Wlbsbr-n Mb. 7 C-tmatinn Formation Vmbb~kte

%%F P Formation

Kapp Toscar l Cnnn&inn I

Tffihmna#Jelkt M a n k

Tschemwrkqedlat Formsitlon TmhemmQetM Formation

Neperfjellet Isfiordbn Fm. Fhmd Re Gedalen Formation Formation De De Gwrdalen Formation De Geerdalen Formation

Hahnfjella Bbemdm Tachermakfjellet ~or&ation Tschemakfi' Tschermaktjeliet Formation Tschermakfjellet Formation on Formation

I I Botneheh Formation

Ban&& Batneheia I Bbknuten Mb. 1 Member I Formation

rdebukta Formation Mambr

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Mohnh- 9j6gm@eflet Sv~ekPqw Mohrh@aMb, Sandslone Sandaone Fmation sp@rmrnllrt Mb. LenskW M e m h

Formation A- Mm& lL Flatgalen Fwmatian mu. Bed

- in many places - mixed up the base of the "Sticky Keep Member" (base of "Kongressfjellet Formation") with the other boundary (M~rk et al. 1999).

The two lower units, consequently, are here assigned to only one formation, the Wkingkda Formation, with its type section at Vikin&gda (M0rk et al. 1999), a mountain separated from the neighbouring mountain Sticky Keep by the valley Deltadalen, i.e. in the traditional type area for several of the units (Buchan et al. 1965; Mark et al. 1982). To avoid

, redefinitions and to facilitate boundary recognitions in the field, a threefold subdivision of the Vikinghsgda Fonnation is proposed. These three units are the Deltadalen Member (unchanged defmitiod, Lusitaniadalen Member and En- domdalen Member, the latter two replacing the "Sticky Keep Member". All member names are now from tributary valleys of the major valley Sassendalen in the type area.

Western Spitsbergen: Along western Spitsbergen, the threefold subdivision of Buchan et al. (1965) is retained, with the Vardebukta For- mation (Induan; Buchan et al. 1965) at its base, followed by the Tvillingodden Formation (Olenekian) and the Bmvais- berget Formation (Anisian and Ladinian) (Msrk et al. 1982). This subdivision is also followed by PEelina (1983) although she used a different name for the middle unit ('Pitnerodden Formation").

Bj~rnllya and Barents Sea: The coeval units of the southwestern Barents Sea, the Havert, Klappmyss and Kobbe formations (Worsley et al. 1988) are summarised in the Ingsydjupet Subgroup. It is defined in the Hammerfest Basin and contains shales and sandstones of Early and partially Middle Triassic age (Ingarydjupet "Group" of Worsley et al. 1988). With the southward extension of the Kapp Toscana Group into the Barents Sea and the incorporation of the Snadd Fonnation into the latter, the Ingqvq'jupet Subgroup is restricted to the southwestern Barents Sea.

The Steinkobbe Formation (Mark & Elvebakk 1999), overlying rocks of the Ingaydjupet Subpup on the Loppa

Fig. 3-03: Previous and proposed stratigraphic schemes for the Trias- sic to Middle Jurassic showing the formation and member levels. The tables are sotted according to area and present the general development of the lithostratigraphic nomenclature. The references do not necessarily indicate the author(s) introducing the individual names. In each table, the column to the right shows the presently recommended scheme. The Russian rank "svita" is translated with "formation". The white fields in the bottom of the Smkapp Land- Hornsund table represent the basement high with a later onset of Tri- assic sedimentation. I, ..-, . . - I

c I . # -

High, shows more similarities with its time-equivalents in Svalbard.

The Sassendalen Group also includes the coeval deposits on Bjemqa, the Urd Formation (Krasii'lEikov C Liv3ic 1974; Mmk et al. 1982).

3.4.2 Kapp Toscana Group

The Kapp Toscana Group was defined in Svalbard by Buchan et al. (1965) with formation rank, and later modified by the inclusion of the Wilhelm~ya "Formation" (Mmk et al. 1982), after the recognition of the latter in eastern Svalbard (Worsley 1973) and subsequent tracing of its equivalents throughout Spitsbergen. Due to a threefold subdivision into successions of common characteristics, the Kapp Toscana Group is subdivided into subgroups.

The StorJorden S u b p p (established here) comprises shallow marine and coastal deposits of compositionally immature sandstones and claystones that can be traced across major parts of Svalbard, including Hopen (Tschenna@ellet Fonnation and De Geerdalen Fonnation; Buchan et al. 1965; Harland et al. 1974), and into the Barents Sea (Snadd Formation; Worsley et al. 1988). The immature sandstones of the Skuld Formation (Mnnk et al. 1982,1990; name proposed by Krasil'BEikov & Livlic, 1974) on Bjnrmnrya are also included here. The subgroup is of late Middle Triassic (Ladinian) to Late Triassic (Norian) age.

131

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Fig. 3& Previous and proposed stratigraphic schemes for the Mid- dle Jurassic to Cretaceous showing the formation and member

--. k a p ~ --. PARKER 1967

. S 'i

C ~ i i n e ~ b f l".**

m, Fonnatian In-Mb. FMhFmj F W w n m ~ b .

mHctell*m D&&glaFm. Dew* m. ~ r s f ~ k L

Hebetlafjdlet Msrnbr l b h w j d l a t Fmatbn F- m i e n

levels. For further notes see Fig. 3-03.

HOEL & ORVlN I ~ E L I N A ISBO. I SKS, pr-t volume

carolin-@ -R Mb. I cmanefjebt Formalicn ~ ~ O Y f d b .

anciefll.Ma DaJkjeOlaFm, [ M Mb. aMpaSch*h*n Pitmw- - Helvetkfjelbt hdrmbr Hw@bi@a@ H&tMjdet

G m Formation bm&0n h-

WWlK et al. l99

5-U Shcwsam%m Helvetlafjellsl Hdvetiafjdbt Member

Formation Formation I I Hehretiafjellet Formation

I . I 1 ~Ihbegst Mb.

I Janusflellet Formation

2 rnrdhfjdbt Formation

Kong Kda Land Fm.

Kongaerytr Formation

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The Realgrunnen Subgroup (Worsley et al. 1988) is most completely developed in the southwestern Barents Sea where it consists of mature sandstones deposited in coastal plain and deltaic through shallow marine environments. The Realgrunnen "Group" was defined in the Hammerfest Basin as comprising four sandstone formations (Fruholmen, Tbbden, Nordmela and Stu; Worsley et al. 1988). The close lithological similarities between the Hammerfest Basin and Kong Karls Land were first described by Johannessen & Embry (1989), and further elaborated since (Olaussen et al., in prep.).

The Rlhelmuya Subgroup (Wilhelmarya "Formation"; Worsley 1973) which occurs in large parts of Svalbard represents the condensed, marine equivalents of the Real- grunnen Subgroup. The inclusion of the Late Triassic to Middle Jurassic units of Kong Karls Land into the m1- helmuya "Formation" as suggested by Edwards et al. (1 979) further demonstrated the similar development of sandstone facies across both Svalbard and the western Barents Sea. Correlations are, however, hampered by the numerous and extensive hiati, and by the poor biostratigraphic resolution in the condensed Wilhelmuya Subgroup, especially as it occurs on central Spitsbergen (Knommn&ellet Formation) and southern Spitsbergen (Smalegga Formation).

The late Triassic (Norian) to latest Middle Jurassic (Bathonian) lithostratigraphy of Svalbard is rather complex, with more than 20 lithostratigraphic units recognised within it during the past 20 years. On Wilhelmsya, Kong Karls Land and Hopen, different nomenclatures were introduced (Smith 1975; Smith et al. 1975, 1976). Newly improved regional understanding has allowed integration of these units within the mlhelm0ya Subgroup (Olaussen et al., in prep.) and the resultant reduction of the number of unit names in eastern Svalbard (Flatsalen, Svensbya and Kongsuya formations). The lack of suitable place names on these islands made a redefition of several of Smith's et al. (1976) formation and member names necessary (Olaussen et al., in prep.; for individual names see Chapter 3.6.1). The transitional nature of the Kong Karls Land succession between the remaining part of Svalbard and the Barents Sea Shelf is the key for the correlation across this long distance. Seismic interpretation indicates that the group also is present in the subsurface between the exposed and drilled areas (Olaussen et al., in prep:).

The stratigraphic interval including the upper part of the Wilhelmt?ya Subgroup and the lower part of the Adventdalen Group is formed by the Brentskardhaugen Bed (Parker 1967) and locally the overlying Marhugda Bed (Backstrom & Nagy 1985). The Brentskardhaugen Bed is a thin conglomeratic unit rich in phosphatic nodules with fossils of different ages that document an underlying unconformity

I representing a hiatus. The bed has been interpreted by several authors, mainly working in central Spitsbergen (Birken- majer 1972% 1975, 1980; Birkenmajer & Pugaczewska 1975; Birkenmajer et al. 1982; Backstrom & Nagy 1985; Dypvik et al. 1985; Dypvik et al. 1991) as a remani6 deposit and placed at the base of the Janusjellet Subgroup (Agardh- jellet Formation). The Wilhelmlrya Subgroup outside central Spitsbergen contains several phosphatic nodular beds, and at least two hiati on Wilhelmsya and in Smkapp Land,

which by several other authors is interpreted to support the integrated nature of the Brentskardhaugen Bed within the condensed succession of the Wilhelmuya Subgroup (Parker 1967; Worsley 1973; Worsley & Mmk 1978; PEelina 1980; MQ1.k et al. 1982; Maher 1989; Krajewski 1992; Olaussen et al., in prep.). The overlying, oolitic Marhugda Bed seems to show a close genetic relation to the Brentskardhaugen Bed. Another hiatus above the Marhugda Bed is suggested by PEelina (1980) and Kopik & Wierzbowski (1988). The Brentskardhaugen and Marhsgda beds thus are interpreted to occupy either a stratigraphic position at the top of the condensed shallow-marine succession of the Wilhehwya Subgroup, or at the base of the renewed development of a basin, where the sediments of the Adventdalen Group were deposited. In the present scheme (Fig. 3-05) and the type sections (Chapter 3.5), the beds are included in the Wilhelmerya Subgroup due of to their lithological affiliation, regardless of their diverging genetical interpretations.

3.4.3 Adventdalen Group

The Adventdalen Group was defined on central Spitsbergen by Parker (1967), extended to include correlative units on Kong Karls Land by Smith et al. (1976), and is herein further extended to comprise both the "Teistengrunnen" and 'Wordvestbanken groups" as defined by Worsley et al. (1988) in the Hammerfest Basin.

The group consists of claystones, shales'and sandstones deposited in shelf settings of latest Middle Jurassic and Early Cretaceous age. Important hydrocarbon source rocks occur in the upper Jurassic succession both in Svalbard (Agardhjellet Formation) and in the Barents Sea (Hekkin- gen and Fuglen Formations.). A significant sandstone unit, the Helvetiajellet Formation, in the middle of the group in Svalbard is the result of regional upliR, relative sea level fall and deltaic progradation (Gjelberg & Steel 1995), while in platform settings in the Barents Sea, a condensed limestone interval developed in the earliest Cretaceous (Klippfisk For- mation, Smelror et al. 1998) which grades into marls and calcareous claystones in the basins. A hiatus occurs around the Jurassic - Cretaceous boundary. In the Barents Sea this is separating the Kimmerian disturbed sediments (Gabrielsen et al. 1990) from Cretaceous calcareous shales, while in central and eastern Spitsbergen this hiatus is associated with the Mjkiegardjellet Bed (Birkenmajer 1980), a complex, plastic claystone marker unit. Tectonic distur- bances have obscured this boundary at many localities on western and southern Spitsbergen.

The Shnusjellet Subgroup (Parker 1967; Dypvik et al. 1991) was established in central and eastern Spitsbergen as comprising the Agardhjellet Formation (Jurassic) and Ruri@ellet Formation (Cretaceous). Dypvik et al. (1991) defined seven members in these areas. In southern Spits- bergen (i.e. mainly in Torell Land), Birkenmajer (1975) followed Rbiycki's (1959) definition of three members within their Janusjellet "Formation". The lower and upper members show a clear parallel development in central Spits- bergen, while the middle member spans the Jurassic - Cre-

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vq Janusfiellet subgroup

I 3 - -,M - - -+-_-h

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taceous boundary. Reconnaissance studies in the summer of 1996 (A. Mmk, H. Dypvik, and others) reconfirmed previous notes (Dallmann et al. 1990,1993) that the subgroup is affected by tectonics and the previously assigned lithostratigraphy and sequence thickness should be treated with care. Consequently, the Jan@ellet Subgroup applies to all of Spitsbergen, although it should be recognised that the boundary between the Agardhjellet and RuriMelletfomta- tions may be difficult to trace in western Spitsbergen. How- ever, major parts of the sediments can easily be referred to either unit. The present extension of the use of the name JanurJjllet Subgroup to all exposure areas of Svalbard also implies that coeval sediments on Wilhelmaya and Kong Karls Land ("Retziusfjellet Shale Member" and parts of "Dunkrtjellet" and "Nordaustpynten Shale members", Smith 1976) are included in the Agardhfjeet Formation.

The Fuglen Formation is retained as defined by Worsley et al. (1988) in the Hammerfest Basin, where dark, pyritic mudstones with limestone interbeds dominate, while it has a more proximal, highly bioturbated sandy development towards the south. Thin correlative units further north in the Barents Sea are also present (data from Norwegian Petro- leum DirectorateIIKU Petroleum Research). The Fuglen Formation is unconformably separated by a hiatus from the underlying St0 Formation, and the boundary youngs northwards.

The Hekkingen Formation consists of the dark organic- rich claystones with a pronounced gamma peak and a very high organic content in the lower Alge Member, overlain by the Krill Member that also is a good hydrocarbon source rock (Worsley et-al. 1988). The formation is defined in the Hammerfest Basin, but extends over a large part of the Barents Sea (i.e. well documented on the Bjarmeland Plat- form; Leith et al. 1993) where it is one of the most important hydrocarbon source rocks. The basal hiatus has different durations in different areas.

On the Barents Sea Shelf, a major break in deposition took place at the Jurassic - Cretaceous boundary, associated with the Late Kimmerian tectonic movements. When deposition resumed in the early Cretaceous, dark grey to greyish brown claystones of the Knurr Formation were deposited in the Hammerfest Basin (Worsley et al. 1988), while a condensed mar1 and limestone succession is developed in platform areas and is assigned to the Klippfisk Formation (Smelror et al. 1998). On the Bjarmeland Platform several shallow cores penetrate the unit which here is assigned to the Kutling Member (Smelror et al. 1998), while similar sediments on Kong Karls Land, although poorly exposed, are assigned to the Tordenskjoldberget Member (Smith et al. 1976).

Following the episode of carbonate deposition, basinal conditions again developed over major parts of the south-

western Barents Sea with deposition of dark brown to grey shales and claystones with interbeds of pale limestone and dolomite. These sediments are defined as the Kolje F o m - tion in the Hammerfest Basin (Worsley et al. 1988). The unit can also be traced over larger areas and is well developed on the Bjarmeland Platform. A thin wedge of shales of this formation has recently been recognised on Kong Karls Land (Smelror et al. 1998).

The Helvetiajellet Formation with its lower sandstones (Festningen sandstone member) and overlying deltaic shale- sandstone development (Gjelberg & Steel 1995) was defined by Parker (1967) on Spitsbergen. This unit is here extended to include the sandstones of Kong Karls Land, singled out as the Hdr$agrehuugen Member (Smith et al. 1976, Olaussen et al., in prep.). Basalts intercalated with and overlying the upper part of the Hbrfagrehaugen member are referred to as the Kong Karls Land Flows. ,

The youngest Mesozoic sediments of Svalbard are the shales and sandstones of the Camlinejellet Formation (Parker 1967). Only the two lower subunits, the Dalkjegla and InnkJegla members, are preserved in central Spitsbergen due to late Mesozoic and Cenozoic uplift and erosion, but the unit is most completely developed in southeastern Spits- bergen -where three additional subunits (Langstakken, Zillerberget and Schonroc~ellet members) are preserved (Nagy 1970; Dallrnann et al. 1994).

In the Barents Sea Shelf a dark grey to green claystone unit (Kolmule Formation), correlative to the Carolinefjellet Formation, is defined in the Hammerfest Basin (Worsley et al. 1988), but extends over wider areas as documented on the Bjarmeland Platform (khus 199 1; Leith et al. 1993).

3.4.4 Nygrunnen Group

Late Cretaceous sediments are only preserved on the Barents Sea Shelf, where they form the Nypnnen Group (Worsley et al. 1988). The thick basinal development in the Hammerfest Basin is assigned to the Kveite Formation and consists of a more than 1 lcm thick succession of greenish to grey claystones. Its thinly developed platform equivalent, the Kviting Formation, consists of calcareous sandstones and claystones. A major unconformity is assumed below the group.

3-45 Intrusive rocks

The name Diabasodden Suite is proposed for the dolerite sills and dikes of latest Jurassic to Early Cretaceous age that intruded older rocks all across Svalbard.

Fig. 3-05 (p. 134-135): Proposed lithostrati&raphic scheme for the Mesozoic of Svalbard and the Barents Sea Shelf. The diagram contains all names recommended by SKS at group, subgroups formation, member and bed levels. Member and bed names m italics represent informal units. The ages and age boundarim of the units are indicated in accordance with existing data, but are admittedly s e h d c . Possible dischronous boundaries are drawn straight unless reliable data can document the diachronism. The indicated major hiati are also drawn schematically and do not claim any precision concerning their age range. Minor hiati are omitted. Vertical lines between formations may represent interfingering relationships.

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Ffs. E W i h t i ~ ~ map M-I: M-k of* SarrEepp-n.od area (Southern ngen)

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Late Palaeozoic cover rocks ' "-+Old Red baw",ent

Fig. 3-07: Distribution map M-II: Mesozoio of Torell Land and the Bellsund- Isfjorden area (southwestern Spitsbergen)

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F@. 3-08: Mbution map M-IIL Mesozoic of the southern Storfjoden area (southeastern Spitsbergen)

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Fig. 3-09: Distribution map M-IV Mesozoic of Oscar 11 Land and Dickson Land (Central western Spitsbergen)

140

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I Tertiary cover rocks -

Helvetlafjellet Fm.

De Geerdalen Fm.

TschermakfJellet Fm.

Botnehek Formation

Fig. 3-10: Distribution map M-V: Mesozoic of northeastern Nordenskiold Land and Sabine Land (Central eastern Spitsbergen)

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Fig. 3-11: Distribution map M-VI: Mesozoic of Kong Karls Land

Fig. 3-12: Distribution map M - W : Mesozoic of Barentsraya, Edgeeya, Hopen and Olav V Land (Eastern Svalbard)

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3. MET^'^" ' "" OSTRATIGRAPHY

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3.5. l Sassendalen Group

SASSENDALEN GROUP (M-01)

Sassendalen I -

STATUS OF m: Fonnal FIRST USE OF N-: Buchan et al. 1965 CURRENT DEFINITION: Mmk et al. 1982; herein extended to include the correlative Ing~rydjupet Subgroup of the Hammerfest Basin (Worsley et al. 1988) SYNONYM(S) AND REFERENCE(S): None ORIGIN OF m: Sassendalen: A major valley in central Spitsbergen TYPE AREA: Sassendalen, central Spitsbergen STRUCTURAL SETTING: Barents Sea Shelf (including Sval- bard) DEPOSITIONAL AGE: Early and Middle Triassic OVERLYING UNIT(S): Kapp Toscana Group UNDERLYING UNIT(S): Tempelfjorden Group, locally Bille- fjorden Group, Gipsdalen Group or Pre-Old Red on the Ssrkapp-Hornsund High SUPERIOR UNIT: None OTHER USE OF NAME: None TEFICKNESS: Up to 700 m in Svalbard, up to 1000 m on Barents Sea Shelf

Fig. 3-14: The mountain Hyrnefjellet at Hornsund, seen from the southeast, showing the grey-coloured Sassendalen Group as it typically occurs in the Hornsund area. Vardebukta Formation: lower part of the grey succession, mostly covered by scree; Tvilligodden For- mation: succeeding coarsening-upward unit with two massive sandstone beds in upper part; Bravaisberget Formation: scree-covered shale succession (Passhatten Member) and overlying sandstone succession (Somovbreen Member); Kapp Toscana Group: succession with yellow intercalations just visible to the right. For underlying, multicoloured, Palaeozoic rocks on the left side of the photograph compare Fig. 2-61. Photo: WK. Dallmann

MAIN LITHOLOGIES: Shale, siltstone, sandstone DESCRIPTION: The Sassendalen Group comprises clastic sediments of Early and Middle Triassic age in Svalbard and on the Barents Sea Shelf. Dominant lithologies are shales and siltstones with subordinate sandstones and minor amounts of carbonate rocks.

The group is exposed along the Tertiary fold-thrust belt on western Spitsbergen, in central and eastern Spitsbergen, as well as on Barentssya, Edgesya, southwestern Nordaust- landet and Bjsrnnrya (Figs. 3-13, 3-14, 3-15, 3-16, 3-19, 3-24,3-27). It continues in the subsurface between these is-

Fig. 3-13: The succession of the Sassendalen Group at Bravaisberget, Fig. 3-15: The succession of the Sassendalen Group at Hegrinden, Van Keulenijorden, showing a typical development of the western Barentssya, showing a typical development of the eastern areas. The areas. The resistant beds to the lower left belong to the Pennian base is not exposed. The strata is assigned to the Vikinghnrgda (lower Kapp Starostin Formation. The overlying section is assigned to the part) and Botneheia formations (upper part). Photo: A. Mmk Vardebukta Formation (first coarsening-upward unit), Tvilligodden Formation (subsequent three units) and the Bravaisberget Formation (dark mudstones: Passhatten Member, overlying sandstones: Somovbreen and Van Keulenfjorden members). Photo: A. Msrk

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Fig. 3-16: The succession of the Sassendalen Group at Waveltoppen, Torell Land. The resistant beds in the lower half of the dope belong to the Pennian Kapp Starostin Fonnation. The overlying section is assigned to the Vatdebukta Fonnation (fi coarsening-upward cycle), Tvillingodden Formation (subsequent two cycles) and the dark mudstones of the Bdsberge t Formation on the very top. Photo: W.K. Dallmann

lands southwards in the Barents Sea Shelf to the Hammer- fest Basin.

The Sassendalen Group (Early and Middle Triassic) represents a series of stacked transgressive-regressive succession~, each formation being initiated by a regionally significant transgression (Mmk et al. 1989). These successions can also be traced across the Barents Sea Shelf to Arctic Canada and Eastern Siberia (Mslk et al. 1989; Egorov & Mnrrk, in press).

The subdivision into ten formations reflects both lateral and vertical facies variation; there are three formations (Vardebukta, Tvillingodden and Bravaisberget formations) on western Spitsbergen, two (Vikinghsgda and Botneheia formations) in central and eastern Svalbard, one (Urd For- mation) on Bjmnqa, and one (Steinkobbe Formation) only documented on the Svalis Dome in the western Barents Sea. Three fornations defined in the Hammerfest Basin (Havert, Klappmyss and Kobbe formations) form the Ingwdjupet Subgroup.

The group represents coastal, deltaic to shallow shelf deposits in western Spitsbergen. These coastal sediments grade eastwards and southwards into shelf mudstones. The upper part is very organic-rich and phosphatic. In the southwestern Barents Sea Shelf shallow to deep shelf sediments were deposited.

STATUS OF UNIT: Fonnal FIRST USE OF NAME: Buchan et al. 1965 CURRENT DEFINITION: NIBzk et d. 1982 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Vardebukta (transl. "The Cairn Bay"): A bay at the Festningen section, outer Isfjorden ME SECTION (FIG. 3-18): Stratotype: Festningen section, outer Isfjorden DEPOSITIONAL AGE: Induan DATING METHOD: Ammonoids, bivalves REFERENCE(S) FOR AGE: Tozer & Parker 1968; KorEinskaja 1982,1986; Weitschat & Dagys 1989 OVERLYING UNIT(S): Tvillingodden Formation UNDERLYING UNIT(S): Tempelfjorden Group, locally Bille- fjorden Group, Gipsdalen Group or Pre-Old Red on the Swkapp-Homsund High SUPERIOR UNIT: Sassendalen Group C ~ H E R USE OF NAME: None THICKNESS: 292 m in the stratotype at Isfjorden, 150-200 m in the Bellsund area, 70-80 m in western Smkapp Land, 16 m on the Smkapp-Homsund High MAIN LITHOLOGIES: Shale, siltstone, sandstone LOWER BOUNDARY DEFINITION: The base is defined by grey shales resting conformably on well-cemented siliciclastic, dark grey shale of the Permian Tempelfjorden Group, or locally above older strata. See also special notes on the Kiste- fjellet Member. DESCRIPTION: The formation is developed in western Spits- bergen and is exposed along the Tertiary fold-thrust belt It is a time-equivalent of the Deltadalen Member (Viking- bgda Formation) which represents a more distal part of the Early Triassic basin. On the Snnkapp-Homsund High, it is only represented by the thin Kistefjellet Member which is age-correlative to the uppermost part of the unit elsewhere, unconformably overlying folded basement and tilted Lower Carboniferous sediments.

In northern parts of the outcrop area, Buchan et al. (1965) defined the lower shaley Selmaneset member and the overlying Siksaken member with type sections in Oscar 11 Land. In southern parts, Birkenmaje~ (1977) defined the Urne- toppen and Wibebreen members. A regional revision of the Vardebukta Formation will probabiy result in the definition of additional members, so these members ate considered to be informal at present.

Grey shale and silly shales with thin siltstone and sandstone interbeds grade upwards into thinly to thickly bedded

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clsivf f mcvcg pcbb

Pig. 3-17: The Myalina limestone in the Vardebukta Formation, Fest- ningen, outer Isfjorden. Photo: A. Mmk

sandstones, which frequently contain shell fragments (Fig. 3-17). The sandstones in the middle part of the unit are cross-bedded. Above this interval sandstone beds thin and become less common towards the top of the formation. Ma- rine fossils like bivalves, ammonoids and bioturbation are common, while fish teeth and vertebrate bones occur here and there. North of the type locality desiccation cracks are present, and southwards along the coast of western Spits- bergen the formation contains several minor coarsening- u~ward successions.

The formation represents a shallow-marine, coastal environment with prograding deltaic lobes. Offshore bars are present.

Selmaneset member (M-03)

STATUS OF UNIT: Informal FIRST USE OF NAME: Buchan et al. 1965 CURRENT DEFINITION: Buchan et al. 1965 SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Selmaneset: A cape on the northern shore of Isfjorden, Oscar I1 Land TYPE SECTION:

Stratotype: Selmaneset, Oscar II Land DEPOSITIONAL AGE: I n d w DATING METHOD: Fossils REFERENCE(S) FOR AGE: See Vardebukta Formation OVERLYING UNIT@): SikSaken member UNDERLYING UNIT@): Tempelfjorden Group SUPERIOR UNIT: Vardebukta Formation OTHER USE OF NAME: None THICKNESS: 136 m in stratotype MAIN LITHOLOGIES: Shale, siltstone, sandstone LOWER BOUNDARY D E ~ I T I O N : See Vardebukta Formation DESCRIPTION: The Selmaneset member is defined by dark, often grey calcareous silty shales and shaley siltstones occurring below the resistant beds of the Siksaken member. Thin, hard calcareous siltstone interbeds are common. The unit becomes more sandy towards its top, where it contains fine-grained sandstones, silty limestones and siderite concretions. Fossils are not common, but bivalves, bone fragments and an ammonoid have been found. The deposits represent coastal to shallow marine environments.

The member is described from the outer Isfjorden area. Southward along the foldbelt of western Spitsbergen it contains several coarsening-upward successions. Although the unit is well-defined in the type section, we recommend informal use of the term only in the type area until sufficient data are available for a consistent revision of the Lower Tri- assic member subdivision.

Pig. 3-18: Stratigraphic section M-02 Shatotype for: Vardebukta Formation Locality: Festningen 1 Reference: Msrk et al. 1982

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Siksaken member (M-04)

STATUS OF UNIT: Informal FIRST USE OF NAME: b & E U l et d. 1965 CURRENT DEFINITION: Buchan et al. 1965 SYNONYM(S) AND REFERENCE(S): None OR~GIN OF NAME: Shaken (transl. from "Mt. Zigzag"): A mountain group in Oscar II Land, on official maps called 'Geitene' (The Goats) TYPE SECTION:

Stratotype: Geitene (Shaken), Oscar I1 Land DEPOSITIONAL AGE: h l d ~ DATING METHOD: Fossils REFERENCE(S) FOR AGE: See Vardebukta Formation OVERLYING UNIT@): Iskletten Member (Tvillingodden For- mation) UNDERLYLNG UNIT@): Selmaneset member SUPERIOR UNIT: Vardebukta Formation OTHER USE OF NAME: None THICKNESS: 104 m in stratotype MAIN LITHOLOGIES: Calcareous siltstone, sandstone LOWER BOUNDARY DEFINITION: The lower boundary of the member is conformable and defined at the base of the lowest distinctly carbonate-cemented (resistant) bed above the shale-dominated part of the Vardebukta Formation. DESCRIPTION: The Siksaken member forms an easily map- able succession, consisting of alternating grey calcareous siltstones and silty limestones, passing into calcarenitic, light grey and white sandstone, hard siltstones and calcareous shales. Fossils are fairly common. The deposits represent coastal, locally exposed, to shallow marine environments.

The member is described from the outer Isfjorden area. Southward along the foldbelt of western Spitsbergen it contains several coarsening-upward successions. Although the unit is well-defined in the type section, we recommend informal use of the term only in the type area until sufficient data are available for a consistent revision of the Lower Tri- assic member subdivision.

Urnetoppen member (M-05)

STATUS OF UNIT: Informal FIRST USE OF NAME: Birkenmajer 1977 CURRENT DEFINITION: Birkenmajer 1977 SYNONYM(S) AND REFERENCE@): None OR~GIN OF NAME: Umetoppen: A mountain north of Hom- sund TYPE SECTION:

Stratotype: Umetoppen SW, Homsund DEPOSITIONAL AGE: Induan DATING METHOD: Fossils, stratigraphic relationships REFERENCE(S) FOR AGE: See Vardebukta Formation; Birkenmajer 1977 OVERLYING UNIT(S): Wibebreen Member UNDERLYING um~(s): Tempelfjorden Group SUPERIOR UNIT: Vardebukta Formation OTHER USE OF NAME: None THICKNESS: 22.5 m in stratotype

MAIN LITHOLOGIES: Shale, siltstone, sandstone LOWER BOUNDARY D E F ~ T I O N : See Vardebukta Formation DESCRIPTION: The Umetoppen member consists predominantly of grey-greenish, grey to black shale with subsrdi- nate siltstones and fine-grained sandstone interdatio~ls. In some sections, siltstones and mdstones may apparently partly or entirely replace the shale component of the member. Sphero-siderite nodules or lenses occur locally within the shale. Glauconitic sandstone and siltstone may appear at the base of the member. Red-weathering, ferrigenous (sideritic-pyritic) limestone, sandstone and shale, as well as light (yellowish, whitish) cross-bedded or mega-rippled thin sandstones usually occur at the top of the member. The member was deposited in shallow marine environments.

The unit is defined in the Homsund area Along the coast of western Spitsbergen several w h g - u p w d successions occur. Although the unit is well d e f i in the type section, we recommend infonnal uiw of the term until sufTi- cient data are available for a consistent revision of the Lower Triassic member rmbdivisi~ft

Wibebreen member (M-06)

STATUS OF UNIT: Informal FIRST USE OF NAME: Birkemajer 1977 CURRENT DEFINITION: Bitkenmaja 1977, although revised here to not include deposits of the Kktefjellet Member (M-07) on the Smkapp-Horns4 High. Smom(s) AND REFEREN~(S): None ORIGIN OF NAME: Wibebreen: A glacier north of Hornsund TYPE SECTION:

Stratotype: Umetoppen S'JB, Homund DEPOSITIONAL AGE: hhlEUl DATING METHOD: Fossils and stratigraphic relationships REFERENCE(S) FOR AGE: See Vardebukta Formation; Birkenmajer 1977 OVERLYING wm(s]: TvdkgSdden Formation UNDERLYING mm(s]: Urnetqpn member SUPERIOR UNIT: Wdeb%tB1 Famation cmma use OF Mr?m: M m m-$$: 47 ln in ~~ MAnv ~ 1 ~ a 0 . m W e 8 siltatone, sandstone LOWER mummy D E ~ O N : The base of the member is d e f d by the b a between an underlying bivalve-rich bed at&ibuted b m@meratic equivalents of the "Brevass- fjellet My- 3edt9, and the overlying shales, siltstones and sands- which constitute the upper part of the Varde- bukta Formation. DESCRIPTION: The Wibebreen member occurs in the Smkappp-Nornsund area, off the Smkapp-Homsund High. It correlates in age with the Kistefjellet Member on the high.

The unit consigts predominantly of two rock types, viz. (1) grey to black shale to marly shale, and (2) grey, greenish- grey, platy siltstone and fine-grained sandstone. The shales predominate in the uppermost, and often also the bottom parts of the member. Siltstone-sandstone horizons may appear as thicker, even cliff-forming bands in the middle part of the unit. Well-developed lamination, small-scale cross-bedding and ripple-marMamination are characteris-

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tic. Subordinate lithologies are ferruginous rnarls, blue, rusty-brown-weathering, silty limestone bands and siderite concretions. In some sections the member is entirely represented by shale. The member was deposited in shallow marine environments.

Although the unit is well-defined in the type section we recommend informal status until sufficient data are available for a consistent revision of the Lower Triassic member subdivision.

Kistefjellet Member (M-07)

STATUS OF UNIT: Formal FIRST USE OF NAME: k 'bk et d. 1982 CURRENT DEFINITION: PEelina 1983 SYNONYM(S) AND REFERENCE(S): Kistefjellet "Formation": PEelina 1983 ORIGIN OF NAME: Kistefjellet (transl. "The Coffin Moun- tain"): A mountain near the southern tip of Ssrkapp Land TYPE SECTION:

Stratotype: Kistefjellet, Sarrkapp Land DEPOSITIONAL AGE: Late Induan DATING METHOD: Brachiopods, stratigraphic relationships REFERENCE(S) FOR AGE: KorEinskaja 1982; Birkenmajer 1977; PEelina 1983; Nakrem & Mmk 1991 OVERLYING UNIT(S): Tvillingodden Formation UNDERLYING UNIT@): Pre-Old Red, in places possibly Upper Palaeozoic sediments of unknown stratigraphic affiliation SUPERIOR UNIT: Vardebukta Formation OTHER USE OF NAME: Kistefjellet "Formation": Mmk et al. 1982

According to Mmk et d.'s definition, the Kistefjellet For- mation includes the Olenekian part of the Sassendalen

Fig. 330: Triassic unconforrnity above folded Caledonian basement, with the conglomeratic Brevassfjellet Bed above the unconfonnity surface, St. Nikolausfjellet, Ssrkapp Land. Photo: WK. Dallmann

Group on the Smkapp-Hornsund High. This definition is not supported, and the Olenekian part is assigned to the Tvillingodden Formation. THICKNESS: 16 m in stratotype MAIN LITHOLOGIES: Sandstone, conglomerate LOWER BOUNDARY DEFINITION: The base of the member is defined by a basal conglomerate or sandstones unconformably overlying folded, Pre-Old Red on the Smkapp- Homsund High (see Brevassfjellet Bed, M-08; Figs. 3-19, 3-20). Locally, a thin horizon of Upper Palaeozoic calcareous rocks may occur below. DESCRIPTION: The Kistefjellet Member consists of a basal polymict conglomerate (Brevassfjellet Be4 M-08; Fig. 3-20) of local provenance. The conglomerate is overlain by silty sandstones which contain brachiopods in their lower parts. The member was deposited in shallow marine environments, starting with a transgressive bed.

Fig. 3-19: The thin development of the Sassendalen Group on the Ssrkapp-Hornsund High, here at Kistefjellet: The lower sandstone succession represents the Kistefjellet Member, a local facies of the Vardebukta Formation, while the overlying Tvillingodden Formation is very thin (minor coarsening-upward unit). The upper scree-coverd part of the slope is the mudstone-dominated Passhatten Member, and the succeeding light, resistant sandstone band the Somovbreen Member of the Bravaisberget Formation. The uppermost sandstone succession is assigned to the Kapp Toscana Group. Photo: W.K. Dallmann

Brevassfjellet Bed (M-08)

STATUS OF UNIT: Formal FIRST USE OF NAME: Birkenmajer 1977 CURRENT DEFINITION: bf0rk et d . 1982 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Brevassfjellet (transl. "The Glacial Water Mountain"): A mountain in western Ssrkapp Land TYPE SECTION:

Stratotype: Kistefjellet, Ssrkapp Land DEPOSITIONAL AGE: Late Induan DATING METHOD: Bivalves, stratigraphtc relationships REFERENCE(S) FOR AGE: k 'bk et al. 1982 OVERLYING UNIT@): Unnamed UNDERLYING UNIT@): Pre-Old Re4 in places possibly Upper Palaeozoic sediments of unknown stratigraphic affiliation SUPERIOR UNIT: Kistefjellet Member OTHER USE OF NAME: "Brevassfjellet Myalina Bed": Birkenmajer (1977)

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The name was used for both the basal conglomerate directly resting on the basement on the Smkapp-Homund High, and for the bivalve-rich beds in the middle part of the Vardebukta Formation east of the high. The name is now restricted to the conglomerates on the Smkapp-Homund High (Worsley & Mnrrk 1978). THICKNESS: <2 m MAIN LITHOLOGIES: Conglomerate LOWER BOUNDARY DEFINITION: See Kistefjellet Member DESCRIPTION: The Brevassfjellet Bed consists of a polymict conglomerate of local provenance. It contains clasts of basement and Upper Palaeozoic (possibly Permian) cherts and limestones. The bivalve Promyalina sp. is locally common (Karentoppen). At Lidfjellet red-weathering, crumbled calcareous rocks may be included in the Brevassfjellet Bed, or may represent remains of an Upper Palaeozoic unit between the basement and the Triassic succession. The bed initiates the Triassic marine sedimentation in its area.

DISTRIBUTION SHOWN ON ~ G ( s ) . : 3-06,3-07,3-09 STATUS OF UNIT: Formal FIRST USE OF NAME: Mnrrk et al. 1982 CURRENT DEFINITION: Mmk et al. 1982 SYNONYM(S) AND REFERENCE(S): "Pitnerodden Formation": PEelina 1983; "Sticky Keep Formation", western outcrop area: Buchan et al. 1965 ORIGIN OF NAME: Tvillingodden (transl. "The %in Cape"): Actually 'Tvillingoddane' (plural), or 'Austre' (Eastern) and 'Vestre (Western) Tvillingodden': two small peninsulas at the Festningen section, outer Isfjorden, where the western one forms the type section. TYPE SECTION (FIG. 3-21): Stratotype: Festningen section, outer Isfjorden DEPOSITIONAL AGE: Olenekian DATING METHOD: Ammonoids, brachiopods REFERENCE(S) FOR AGE: Tozer & Parker 1968; KorEinskaja 1982; Weitschat & Dagys 1989 OVERLMNG mm@): Bravaisberget Formation UNDERLYING m ( s ) : Vardebukta Formation SUPERIOR UNIT: Sassendalen Group OTHER USE OF NAME: "Tvillingodden Formation" (PEelina 1980): The unit name as used by PEelina is replaced by Tverrbekken member (M-44) THICKNESS: 200-250 m in the Isfjorden - Bellsund area (220 m in stratotype), 70-1 10 m in western Smkapp Land, ca. 20-30 m on the San:kapp-Hornsund High MAIN LITHOLOGIES: Shale, siltstone, sandstone

B

m mcvcg pcbb

Fig. 3-21: Stratigraphic section M-09 Stmtoijpe for: Tvillingodden Formation Locality: Festningen 1 Refereizce: W et al. 1982

LOWER BOUNDARY DEFINITION: The base is defined where thinly laminated, unbioturbated shale overlies the distinctly more silly shale of the Vardebukta Formation. DESCRIPTION: The formation is developed in western Spits- bergen and exposed along the Tertiary fokl-thrust belt. It is a time-equivalent of the Lusitatliadalen and Vendomdalen members (Vikinghsgda Formation) which represent more central facies developments in the Early Triassic basin.

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In northern parts of the outcrop area, Buchan et al. (1965) distinguished the Iskletten and Kaosfjellet members with type sections in Oscar I1 Land.

The formation consists of dark grey, laminated shales coarsening upwards to laminated siltstones and sandstones. South of the type area, the formation shows several (up to four) coarsening-upward units. Bioturbation (e.g. Rhimco- mllium) is common or abundant in the upper parts of the individual coarsening-upward units.

A pronounced fossiliferous limestone bed (the Skilisen Bed) occurs in the southern part of western Spitsbergen. At the type locality a fossiliferous bed occurs at the top of the formation. Except for these limestone beds, macrofossils (bivalves, brachiopods, ammonoids) are sparse, though they occur throughout the formation.

The entire formation is of marine origin, deposited in moderately deep to shallow shelf environments, with the thicker limestone units representing bar environments.

Iskletten Member (M-10)

STATUS OF UNIT: Formal FIRST USE OF NAME: Buchan et al. 1965 CURRENT DEFINITION: Buchan et al. 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Iskletten (transl. "The Ice Bluff"): A mountain in Oscar 11 Land TYPE SECTION (FIG. 3-22): Stratotype: Iskletten, Oscar I1 Land DEPOSITIONAL AGE: Olenekian DATING METHOD: Ammonoids and bivalves, stratigraphic correlations REFERENCE(S) FOR AGE: See Tvillingodden Formation OVERLYING UNIT@): Kaosfjellet Member UNDERLYING UNIT@): Vardebukta Formation SUPERIOR UNIT: Tvillingodden Formation OTHER USE OF NAME: None THICKNESS: 154 m in stratotype MAIN LITIIOLOGIES: Shale, calcareous siltstone LOWER BOUNDARY D E ~ T I O N : See Tvillingodden Forma- tion DESCRIPTION: The member forms the lower part of the Tvillingodden Formation and consists of interbedded dark grey, often calcareous silty shale, and grey to grey-green, flaggy and laminated, calcareous shaley siltstone. Grey septarian limestone concretions are common - especially in the upper part, and hard yellow-weathering thin calcareous siltstone interbeds are also common. Fossils are not particularly abundant, but ammonoids and bivalves do occur, especially in the limestone concretions. The unit is easily recognised between the cliff-forming members below and above. Lithologies are fairly uniform. The member was deposited in shallow marine environments.

The unit is recognised in the outer Isfjorden area and in ;) Oscar I1 Land. Southward along the Tertiary fold-thrust belt

several coarsening-upward units occur. The unit is well defined in the type area and we recommend use of the name only in this region until sufficient data are available for a

Bravaisberget Formation (Anisian)

L 0 n

E 5 - m - - m i' 0

;: S 0 C(

h <- z &

0 ' = o .-

f J ' u ; : Q ' m W a ' = n -

m Q

K - 0 L

+o;:

; 4 = CI c

N Vardebukfa Formation (Induan)

-< 4

grain. size approximate

- m -

clsivf f rncvcg pcbb

Fig. 3-22: Stratigraphic section M-1011 1 Stmtotyge for: Iskletten and Kaosfjellet members Locality: Iskletten Reference: Buchan et al. 1965

consistent revision of the Lower Triassic member subdivision. The member is approximately time-equivalent with the Lusitaniadalen Member in central Spitsbergen and eastern Svalbard.

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Kaosfjellet Member (M-11)

STATUS OF UNIT: Formal RRST USE OF NAME: Buchan et al. 1965 CURRENT DEFINITION: B~chan et al. 1965 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Kaosfjellet (transl. "The 7 C aos Moun- tain"): A tectonized mountain in Oscar II Land TYPE SECTION (FIG. 3-22): Stratotype: Iskletten, Oscar 11 Land DEPOSITIONAL AGE: Olenekian DATING METHOD: Fossils, stratigraphic correlations REFERENCE(S) FOR AGE: See Tvillingodden Formation OVERLYING UMT(S): Bravaisberget Formation UNDERLYING UNIT(S): Iskletten Member SUPERIOR UNIT: Tvillingodden Formation OTHER USE OF NAME: None THICKNESS: 76 m in stratotype MAIN LITHOLOGIES: Siltstone LOWER BOUNDARY DEFINITION: The lower boundary of the member is defined at the abrupt onset of continuous siltstones above shales, accompanied by a distinct change in colour. DESCRIPTION: The Kaosfjellet Member forms a distinctive cliff, consisting of yellow-brown weathering, laminated shaley siltstones, thinly alternating with fragmented, hard, thin grey, slightly calcareous, orange and red-brown weathering siltstones. The upper and lower contacts are marked by abrupt changes in colour, lithology and resistance. The member was deposited in shallow marine prodelta environments.

The unit is defined in the outer Isfjorden area and Oscar I1 Land, and is only recognised in the thicker sections of the western outcrop belt north of Wedel Jarlsberg Land. South- ward along the Tertiary fold-thrust belt several coarsening- upward units occur. The unit is well defined in the type area and we recommend use of the name only in this region until sufficient data are available for a consistent revision of the Lower Triassic member subdivision. The member is approximately time-equivalent with the Vendomdalen Member of central Spitsbergen and eastern Svalbard.

Skilisen Bed (M-12)

STATUS OF UNIT: Formal FIRST USE OF NAME: Birkenmajer 1977 CURRENT DEFINITION: Mmk et al. 1982. The unit was introduced by Birkenmajer (1977) and applied by Worsley & Mnrrk (1978) with reference to sections at S d a p p Land, but subsequently redefined by Mmk et al. (1982) according to its F ~ s t description by Lundgren (1887; "Retziakalk"). SYNONYM@) AND REFERENCE(S): "Retziakalk" ("Retzia limestone"): Lundgren 1887 ORIGIN OF NAME: Skilisen (transl. "The Divide Glacier"): A glacier in Torell Land TYPE SECTION (RG. 3-23): Stratotype: Bravaisberget, Van Keulenfjorden DEPOSITIONAL AGE: Olenekian

m P G B

Bravaisbepet

dsivf f mcvcg pcbb

Fig. 333: Stratigraphic section M-12 Simtotype for: Skilisen Bed Locality: Bravaisberget 1 Reference: h&&, A. & Forsberg, A. (unpubl.)

0

V)

DATING METHOD: Brachiopods, stratigraphic correlations REFERENCE(S) FOR AGE: See Tvillingodden Formation SUPERIOR UNIT: Tvillingodden Formation OTHER USE OF NAME: None THICKNESS: <l8 m, 11 m in stratotype MAIN LITHOLOGIES: Sandy limestone LOWER BOUNDARY DEFINITION: The lower boundary is defined at the base of a biosparitic limestone in the middle part of the Tvillingodden Formation, ca. 70 m above the for- matioaal base in the type section. DESCRIPTION: The unit consists of sandy, biosparitic limestone rich in brachiopods and bivalves. It is only a few metres thick in the type locality, but it is developed as an 18 m thick crinoidal biosparite in central Smkapp Land. The unit represents open marine bank deposits.

(Induan) F

Formation

- a : "

V)::

* = Q - @ Q L - 0 k O O


(Anidan)

z 2 H C 3:

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2 'I: .* 24 U2 -

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DISTRIBUTION SHOWN ON FIG@).: 3-08, 3-09,3-10,3-12 STATUS OF UNIT: Formal FIRST USE OF NAME: Mark et al. 1999 CURRENT DEFINITION: Mark et al. 1999 SYNONYM(S) AND REFERENCE(S): "Vardebukta" and "Sticky Keep" formations in central and eastern Svalbard: Buchan et al. 1965; Deltadalen and "Sticky Keep" members: Mmk et al. 1982; "Vardebukta" and "Wichebukta formations" in central and eastern Svalbard: PEelina 1983; Lower part of "Barentsaya Formation": Lock et al. 1978 ORIGIN OF NAME: Vikinghcjgda (transl. "The Viking Hill"): A mountain south of Sassendalen, eastern Nordenskiold Land TYPE SECTION (FIG. 3-25): Stratotype: Deltadalen - Vikingbgda, eastern Nordenskiold Land DEPOSITIONAL AGE: Ind~an - Olenekian DATING METHOD: Ammonoids, bivalves, palynomorphs REFERENCE(S) FOR AGE: Tozer & Parker 1968; KorEinskaja 1975, 1986; Weitschat & Dagys 1989; Mark et al. 1999 OVERLYING UNIT(S): Botneheia Formation UNDERLYING UNIT(S): Kapp Starostin Formation SUPERIOR UNIT: Sassendalen Group OTHER USE OF NAME: None

Fig. 3-24: The Sassendalen Group at Milne Edwardsfjellet, central Spitsbergea The Vikingbgda Formation is rapresented by the lower two thirds of the slope. The Botneheia Fortnation occurs above. the mall plateau towards the top of the cliff, succeeded by the Shales of the Tschermaktjellet Formation (basal Kapp Toscana Group) forming the ridge. Photo: A. h4mk

l unit. clsivf f mcvcg pcbb

Fig. 3-25: Stratigraphic section M-13/14/15/16 Stmtotype for: Vikinghsgda Formation, Deltadalen, Lusitdadalen

and Vendomdalen memben Locality: Deltadalen - Vikinghsgda SE Reference: Mark et al. 1998

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Botneheia Formation

I l l cl sivf

6

66

m f mcvcg pcbb

THICKNESS: 250 m in stratotype, central Spitsbergen 200-220 m in central eastern Spitsbergen MA~N LITHOLOGIES: Shale, siltstone LOWER BOUNDARY DEFINITION: The formational base is defined where soft weathering sandstones or siltstones rest with a sharp boundary on glauconitic cherty sandstones of the Kapp Starostin Formation (Upper Permian) (Fig. 3-26). DESCRIPTION: The formation consists of grey shales and silty shales with subordinate siltstones and carbonate beds. Septarian nodules are abundant at several levels. m .. . 1

The former twofold subdivision of these deposits has recently been revised by a threefold subdivision which reflects better the nature of the stratigraphic sections (Msrk et al. 1999). These three units are the Deltadalen Member (unchanged definition), Lusitaniadalen Member and Vendom- dalen Member, the two latter replacing the "Sticky Keep Member".

The lower part of the formation (Deltadalen Member) is shaley and sandy, the middle part (Lusitaniadalen Member) consists of mudstones and siltstone beds, while the upper part (Vendomdalen Member) is dominated by dark grey mudstone with dolomite beds.

The formation represents a series of stacked transgressive-regressive successions (Fig. 3-24), each member being initiated by a regionally significant transgression (Mmk et

al. 1999; Egorov & Mmk, in press), and deposited in moderately deep marine shelf environments.

The formation is time-equivalent with the Vardebukta and Tvillingodden formations in western Spitsbergen.

Deltadalen Member (M-14)

STATUS OF UNIT: Formal FIRST USE OF NAME: Mark et al. 1982 CURRENT DEFINITION: Merrk et al. 1999 SYNONYM(S) AND REFERENCE(S): Vardebukta Formation: Buchan et al. 1965. The name 'Vardebukta Formation' is now restricted to the western outcrop belt. ORIGIN OF NAME: Deltadalen (transl. "The Delta Valley"): A tributary valley of Sassendalen, eastern Nordenskiold Land TYPE SECTION FIG. 3-25): Stratotype: Deltadalen, Nordenskiold Land DEPOSITIONAL AGE: Induan DATING METHOD: Ammonoids, palynomorphs REFERENCE(S) FOR AGE: KorEinskaja 1982; Mmk et al. 1999 OVERLYING UNIT(S): Lusitaniadalen Member UNDERLYING UNIT(S): Kapp Starostin Formation SUPERIOR UNIT: Vikingh0gda Formation -R USE OF NAME: None THICKNESS: 68 m in stratotype MAIN LITHOLOGIES: Shale, sandstone LOWER B O ~ M DEFINITION: See Tvillhgodden Forma- tion # l \ . .,.l

DESCRIPTIOIY: The Deltadalen Member starts with silty shale and thin to medium thick beds of sandstone. The remaining part of the member consists of greenish-grey, silty shale, siltstone and sandstone. The sandstone beds show hummocky cross-~tra~cation, wave ripples or planar lamination, which often fine upwards. Carbonate concretions and marine fossils are present. The rock weathers to a grey or greenish-grey colour. The member was deposited in shallow to moderately deep shelf environments.

The unit's top has recently been moved to a somewhat lower position (Mark et al. 1999) than that envisaged by (Mmk et al. 1982). Findings of Smithian (lower Olenekianl

W

amrnonoids in what is now the lower part of the overlying 7 Lusitaniadalen Member, hawimpmved corre1ations leading

Fig. 3-26: The Pennian-Triassic boundary in Lusitaniadalen, marked by a red glove, showing the top of the Kapp Starostin Formation and the base of the Vikingh~gda Formation. Photo: A. Mark

to the exclusion of these beds fiom the Deltadalen Member. The member is time-equivalent to the Vardebukta Formation in western Spitsbergen.

Lusitaniadalen Member (M-15)

STATUS OF UNIT: Formal -T USE OF NAME: lMPlrk et d . 1999 CURRENT DEFINITION: Mmk et al. 1999 SYNONYM(S) MD REFERENCE(S): The member corresponds approximately to the lower part of the former "Sticky Keep Formation" (Buchan et al. 1965) or "Sticky Keep Member" (Mmk et al. 1982)

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ORIGIN OF NAME: Lusitaniadalen: A tributary valley of Sassendalen, eastern Nordenskiold Land TYPE SECTION (FIG. 3-25): Stratotype: Deltadalen - Vikinghergda, Nordenskiijld Land DEPOSITIONAL AGE: Smithian (Early Olenekian) DATING METHOD: Ammonoids, bivalves, palynology REFERENCE(S) FOR AGE: Weitschat & Lehmann 1978; KorEinskaja 1982; &rk et al. 1999 OVERLYING UNIT(S): Vendomdalen Member UNDERLYING UNIT(S): Deltadalen Member SUPERIOR UNIT: Vikinghagda Formation OTHER USE OF NAME: None THLCKNESS: 88 m in stratotype MAIN LITHOLOGIES: Shale, sandstone LOWER BOUNDARY D E ~ O N : The base is defined by the change from silty shale and sandstone beds (Deltadalen Member) to laminated dark grey shales. The boundary is often marked by a change in the &ace slope angle. DESCRIPTION: The Lusitaniadalen Member consists of dark grey shales with thin to medium thick beds of yellow- weathering, calcareous siltstones. Limestone nodules (0.1- 1 m) are abundant and o h occur in well-defined horizons. Siltstone beds are common and are between a few milli- metres and several centimetres thick. The base and lower parts of the unit are well-exposed in Deltadalen (the valley between Sticky Keep and Vikinghrgda). The member is an approximate time-equivalent of the Iskletten Member farther west. It was deposited in moderately deep shelf environments.

Vendomdalen Member (M-16)

STATUS OF UNIT: Formal FIRST USE OF NAME: Mmk et al. 1999 CURRENT DEFZNITION: Mmk et al. 1999 SYNONYM(S) AND REFERENCE(S): The member corresponds to the upper part of the former "Sticky Keep Formation" (Buchan et al. 1965) or "Sticky Keep Membery' (Mark et al. 1982) ORIGIN OF NAME: Vendomdalen: (transl. "The Turn-Around Valley") A tributary valley of Sassendalen, western Sabine Land TYPE SECTION (FIG. 3-25): Stratotype: Vikinmgda, Nordenskiold Land DEPO~ITIONAL AGE: Spathian (Late Olenekian) DATING METHOD: Ammonoids, bivalves, palynology REFERENCE(S) FOR AGE: Weitschat & Lehmann 1978; KofEinskaja 1982; Mmk et al. 1999 OVERLYING m(s) : Botneheia Formation UNDERLYING m(s) : Lusitaniadalen Member SUPERIOR m: Vilcinghsgh Formation OTHER USE OF NAME: None THICKNESS: 94 m in stratotype MAIN LITHOLOGIES: Mudstone LOWER BOUNDARY DEFINITION: The base is defined by the change from silty shale with siltstone beds (Lusitaniadalen Member) to the dark grey, comparatively uniform mudstone lithology of the Vendomdalen Member. DESCRIPTION: The main lithology is dark grey mudstone

with medium to thick beds of yellow weathering dolomite. Large septarian nodules occur as horizons in the lower part of the member, while small carbonate nodules occur throughout the member. Ammonoids and bivalves are abundant. On top of the member a thick silty dolomite bed with ammonoid imprints frequently occurs. The member is a time-equivalent of the Kaosfjellet Member farther west. The member was deposited in moderately deep to deep shelf environments.

DISTRIBUTION SHOWN ON FIG(s).: 2-05 STATUS OF UNIT: Formal F m s ~ USE OF NAME: Krasil'SEikov & LivBic 1974 CURRENT D E ~ O N : Mmk et al. 1982 SYNONYM(S) AND REFERENCE(S): "Vardebukta" and "Wichebukta formations" on Bj~rmsya: PEelina 1983 ORIGIN OF NAME: Urd (an Old Norse goddess): One of the mountain summits of Miseryfjellet, Bjnrrnsya TYPE SECTION (FIG. 3-28): Stratotype: Urd, Miseryfjellet (Bjnrrnsya) DEPOSITIONAL AGE: Early to ?Middle Triassic DATING METBOD: Ammonoids, palynology REFERENCE(S) FORAGE: PEelina 1972; h h k et d . 1990 OVERLYING =(S): SMd Formation UNDERLYING UNIT(S): Miseryfjellet Formation SUPERIOR UNIT: Sassendalen Group -R USE OF NAME: None THICKNESS: 65 m in stratotype MAIN LITHOLOGIES: Sandstone, shale

Fig. 3-27: The Triassic succession of B j m q a (Urd and Skuld formations) overlying the cliff-fonning siliceous lithologies of the Per- mian Miseryfjellet Formation. Photo: A. Mnrk

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m mcvcg pcbb

Fig. 3-28: Stratigraphic section M-17/18/36 Stmtotypefar: Urd and SMd formations, Verdande Bed Locality: Urd, Miseryfjellet Reference: Msrk et al. 1982

LOWER BOUNDARY DEFINITION: The base is defied by a sharp boundary with a slight angular unconformity between underlying limestones of the Miseryfjellet Formation and the Triassic sandstone. DESCRIPTION: The lower part of the Urd Formation (22 m) consists of sandstone and siltstones changing upwards into silty shale. The upper 40 m consists of silty shale with thin siltstone laminae and yellow weathering, thin siltstone beds. Poorly preserved ammonoids and bivalves occur in this section. Close to the top several yellowish weathering, dolomitic siltstone beds occur. The top is formed by a 20 cm thick conglomerate bed with phosphatic nodules (Verdande Bed). The formation was deposited in shallow marine shelf environments. Thorough descriptions of the formation are provided by PEelina (1972) and Mmk et al. (1990) (Fig. 3- 27).

Verdande Bed (M-18)

STATUS OF UNIT: Formal FIRST USE OF NAME: Mmk et d. 1982 CURRENT DEFINITION: Mmk et al. 1982 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Verdande (an Old Norse Goddess): One of the mountain summits of Miseryfjellet, Bjsrnarya TYPE SECTION (FIG. 3-28): Stratotype: Ur4 Miseryfjellet (Bjmrmraya) DEPOSITIONAL AGE: ?Late Middle Ttiassic DATING METHOD: Indirect, stratigraphic refationships REFERENCE(S) FOR AGE: PEelina 1972; MfXk et d. 1990 OVERLYLNG UNIT(S): Skuld Formation SUPERIOR UNIT: Urd Formation OTHER USE OF NAME: None THICKNESS: 0.2 m MAIN LITHOLOGIES: Phosphate nodule conglomerate LOWER BOUNDARY DEFINITION: The lower boundary is defined by the sharp onset of the nodular lithology of this bed above siltstones. DESCRIPTION: The Verdande Bed is a remanic conglomerate consisting of phosphate nodules which measure a few centimetres in diameter. The conglomerate rests on dolomitic siltstones. There is a pronounced break in the surface slope angle at the be4 which form8 a small ledge. ?he nodules often have irregular shapes and -er with a bluish-grey colour. The bed is interpreted as representing the winnowed remains of an originally thicker Middle Triassic unit (PEelina 1972; Mmk et d. 1990).

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DISTRIB~ON SHOWN ON RG(s).: 3-06,3-07,3-09 STATUS OF UNIT: Formal

Fig. 3-30: Typical phosphate nodule horizons in the Bravaisberget For- mation, here at Festningen, outer Isfjorden. Photo: A. M k

h R s T USE OF NAME: W k et d. 1982 CURRENT DEFENITION: Mmk et al. 1982 SYNONYM(S) AND REFERENCE(S): "Botneheia Formation": Buchan et al. (1965). The name 'Botneheia Formation' is now only referred to time-equivalent deposits in central DESCRIPTION: The Bravaisberget Formation forms a major Spitsbergen and eastern Svalbard. coarsening-upward succession, where the basal mudstones ONGIN OF NAME: Bravaisberget: A mountain in Nathorst grade into siltstones and sandstones. Small phosphate nod- Land, Van Keulenfjorden ules occur abundantly throughout the formation. Southward TYPE SECTION (hG. 3-31): Stratotype: Bravaisberget, Van Keuleflorden Tschermak- DEPOSITIONAL AGE: Middle Triassic DATING METHOD: Ammonoids, bivalves REFERENCE(S) FOR AGE: Tozer & Parker 1968; IbrCinskaja 1982; Weitschat & Lehmann 1983 OVERLYING UNIT(S): Tschermakfjellet Formation UNDERLMVG UNIT(S): Tvillingodden Formation SUPERIOR UNIT: Sassendalen Group OTHER USE OF NAME: None THICKNESS: 200-250 m in the outer Isfjorden - Bellsund area (209 m in stratotype), ca. 110 m in western Smkapp Land, ca. 70-80 m on the Smkapp Hornsund High MAIN LITHOLOGIES: Mudstone, siltstone, sandstone LOWER BOUNDARY D E F ~ O N : The formational base is de- ,,-, fined by soft, dark mudstone resting conformably on top of the cliff-forming siltstones and sandstones of the underlying - formation.

I Tvillingdden

Formation

ll?A I S v A ISA

I (Olenekian) v m untts -

clsivf f mcvcg pcbb

Fig. 3-29: The Bravaisberget Formation at Bravaisberget, Van Keulen- Fig. 3-31: Stratigraphic section M-19/20b/22b fjorden. The dark mudstones in the middle of the slope represent the Stratotype for: Bravaisberget Formation Passhatten Member, the overlying cliff-forming siltstones and sand- Hypostratotype for: Passhatten and Somovbreen members stones the Somovbreen and Van Keulenfjorden members. Photo: A. Locality: Bravaisberget 2 Mark Reference: Mark et al. 1982

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along the Tertiary fold-thrust belt the siltstones and sandstones show abundant calcite and dolomite cementation which results in a yellow weathering colour. Oolite horizons occur in the northern areas.

Ammonoid, bivalve and brachiopod faunas are common. Trace fossils occur in upward increasing abundance. The unit is rich in organic material (TOC 1-7 %) and represents, together with the time-equivalent (although generally more mudstone-dominated) Botneheia Formation, the most promising hydrocarbon source rock potential of Svalbard. Phosphate nodules occur abundantly throughout the formation (Fig. 3-30).

The formation is subdivided into four members: The lower Passhatten Member is shale dominated, while the overlying Somovbreen Member consists of calcareous siltstones (Fig. 3-29). The Van Keulenijorden Member caps the succession with a silicified calcareous sandstone. The Karentoppen Member in southwestern Spitsbergen represents intercalated deltaic to fluvial sandstones.

The Bravaisberget Formation is interpreted as a deltaic influenced, regressive unit, with several superimposed lower- order transgressive-regressive units representing prograding delta fiont mudstones and siltstones (Mmk et al. 1989).

Passhatten Member (M-20)

STATUS OF UNIT: F o ~ FIRST USE OF NAME: Birkenmajer 1977 CURRENT DEFINITION: Mmk et al. 1982 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Passhatten (transl. "The Pass Hat"): A mountain in Wedel Jarlsberg Land ME SECTION (FIGS. 331,332): Stratotype: Treskelen, Homund Hypostmtotype: B~avaisberget, Van Keulenfjorden The type section was first defined at Passhatten by Birken- rnajer (1977), according to a description by R6Qcki (1959). The redefined type sections reflect easier accessible and meanwhile better described sections that also account for the lateral variation of the unit. DEPOSITIONAL AGE: Anisian DATING METHOD: Ammonoids REFERENCE(S) FOR AGE: Tozer & Parker 1968; KorEinskaja 1982 OVERLYING UNIT(S): Somovbreen and Karentoppen members UNDERLYING UNIT(S): Tvillingodden Formation SUPERIOR m: Bravaisberget Formation OTHER USE OF NAME: None THICKNESS: 53 m in the stratotype, 76 m in the hypostratotype MAIN LITHOLOGIES: Mudstone, siltstone LOWER BOUNDARY DEFINITION: See Bravaisberget Forma- tion DESCRIP~ON: The Passbatten Member forms the lower, Fie-grained part of the Bravaisberget Formation. The main lith01ogy is dark grey, soft mudstone. Siltstone and silty limestone beds, often with phosphate nodular conglomerates, are abundant. These siltstone beds increase in thick-

5 G' g z 'd U

5 -

c m .- E

1- * v 0

m P a 0

Z d 0 D h

D

z E

O

U " 5:

0 p: - 0 V)

V) I-

a : - p:- W l- 2

< > U p: L9

* D P

a = 0

m E .- a ", .- = ; a a

V1

m 5 P,

TvilUngod. Fm. ( m l d a n )

Pprr' -' Fig. 3-32: Stratigraphic d o n M-2M2% L,-. . . Stmto&pe for: Pawhatten and Somwbreen members Locality: Treskelen Re$erence: h&& et al. 1982

157

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ness (dm to m size) and abundance towards the upper boundary, usually with the Somovbreen Member. The unit is poor in fossils. The member was deposited in open marine shelf environments.

Karentoppen Member (M-21)

STATUS OF UNIT: Formal FIRST USE OF NAME: Mark et al. 1982 CURRENT DEFINITION: Mmk et al. 1982 SYNONYM(S) AND REFERENCE(S): None O w m OF NAME: Karentoppen: A mountain in western Sarkapp Land TYPE SECTION (FIG. 3-34): Stratotype: Karentoppen, Smkapp Land DEPOSITIONAL AGE: Middle Triassic DATING METBOD: Indirect, stratigraphic relationships REFERENCE(S) FOR AGE: Mank et al. 1982 OVERLYING UNIT(S): Somovbreen Member UNDERLYING UMT(S): Passhatten Member SUPERIOR UNIT: Bravaisberget Formation HER USE OF NAME: None THICKNESS: 43 m in the stratotype RLm LITHOLOGIES: Sandstone, conglomerate LOWER BOUNDARY DEFINLTION: The bioturbated sandstones of the Karentoppen Member rest with a sharp contact on the phosphatic shales of the Passhatten Member. DESCRIPTION: The Karentoppen Member is restricted to western Smkapp Land and forms a wedge between the Pass- hatten and Somovbreen members. It consists of cross- bedded sandstones (Fig. 3-33) gradmg upward into the Somovbreen Member. It is characterised by an upward-fining, cross- to planar laminated sandstone succession with subordinate conglomerate beds. Herringbone cross-bedding occurs in the lower part of the unit. Trace fossils change gradually from being high-energy protective burrows in the lower part to the typical marine ichnocoenosis of the Somovbreen Member uppermost. The member represents deltaic distributary sandstones. Basement

0

- m 1IITIIITill clsivf f mcvcg pcbb

Fig. 3-34: Stratigraphic section M-2 1

L I Gmtotypa for: Karentoppen Memhr Locality: Karentoppen Reference: Mmk et al. 1982

Somovbreen Member (M-22)

STATUS OF UNIT: Formal FIRST USE OF NAME: Birkenmajer 1977

l CURRENT DEFINITION: Mmk et al. 1982; modified here to exclude the uppermost sandstone unit (Van Keulentjorden Member)

Fig. 3-33: Deltaic channel sedients typical for the Karentoppen SYNONYM(S) AM) REFERENCE(S): None Member, here at Karentoppen, Ssrkapp Land. Photo: A. Mmk ORIGIN OF NAME: Somovbreen: A glacier in Torell Land

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'. MESOZOIC LITHOSTRATIGRAPHY

TYPE SECTION (FIGS. 3-31,3-32): Stratotype: Treskelen, Hornsund Hypostratotype: Bravaisberget, Van Keulenfjorden The type section was first defined at Passhatten by Birken- majer (1977), according to a description by R6iycki (1959). The redefined type sections reflect easier accessible and meanwhile better described sections that also account for the lateral variation of the unit. DEPOSITIONAL AGE: ?Anisian - Ladinian DATING METHOD: Amrnonoids, bivalves REFERENCE(S) FOR AGE: Tozer & Parker 1968; KorEinskaja 1982 OVERLYING UNIT@): Van Keulenfjorden Member UNDERLYING UNIT@): Passhatten and Karentoppen members SUPERIOR UNIT: Bravaisberget Formation ER USE OF NAME: None THICKNESS: 40 m in the stratotype, 89 m in the hypostratotype MAIN LITHOLOGIES: Siltstone, sandstone LOWER BOUNDARY DEFINITION: The lower boundary coincides with the base of the cliff-forming siltstones and sandstones forming the upper part of the Bravaisberget Forma- tion, overlying the dark mudstone-dominated lithologies of the Passhatten Member. DESCRIPTION: The Somovbreen Member comprises the upper siltstone-dominated part of the Bravaisberget Forma- tion, except for the uppermost, massive sandstone. There is a gradual transition from the underlying members. The siltstones contain abundant calcite and dolomite cement. They are strongly bioturbated, and often show a succession of trace fossils reflecting upwards increasing energy levels. Oolitic beds in the northern areas are provisionally included in the member. The unit contains ammonoids, bivalves and reptile bones. The member was mainly deposited in prodelta environments.

Van Keulenfjorden Member (M-23)

STATUS OF UNIT: Formal FIRST USE OF NAME: PEelina 1983 CURRENT DEFINITION: PEelina 1983 SYNONYM(S) AND REFERENCE(S): "Fos~esand~tein": Hoe1 & Orvin 1937 (upper part of Van Keulenfjorden Member) ORIGIN OF NAME: Van Keulenfjorden: A major fiord in western Spitsbergen TYPE SECTION (FIG. 3-35): Stratotype: Bravaisodden, Van Keulenfjorden DEPOSITIONAL AGE: Ladinian DATING METHOD: Fossils, stratigraphic correlation REFERJCNCE(S) FOR AGE: PEelina 1983 OVERLYING UNIT(S): Tschermakfjellet Formation UNDERLYING UNIT(S): Somovbreen Member SUPERIOR UNIT: Bravaisberget Formation OTHER USE OF NAME: None THICKNESS: 27-67 m (27 m in the stratotype) MAIN LITHOLOGIES: Siltstone, sandstone LOWER BOUNDARY DEFINITION: The base of the Van Keulen- fjorden Member is the boundary between underlying alter-

Tschermak- fpllet Fm. (Carnian)

z 2 b S

< B E " iz 2

O = o a - m k 0

W . a W r b k

W 0

a ; o c -

* 0 : g > a 4 - iz + m

Somovbreen Member

(Ladinian)

y units

m T d sivf f m

v'&/ U

v SISVARM IIA v v 8 V A P U

IS ISv

Fig. 3-35: Stratigraphic section M-23 Sfmtotype for: Van KeUtenfjorden Membes Locality: Bravaisadden Refirence: Ma& A. (unpubl.)

nathg siltstones and shales and the overlying, carbonate- cemented, cliff-forming silt- and sandstone succession in the uppermost levels of the Bravaisberget Formation. D E S ~ ~ ~ O N : The Van Keulenfjorden Member is subdivided into two generally coarsening-upward units. The lower one appears more massive and contains carbonate- cemented siltstones, while the upper one is dicecemented, fine-grained sandstone and contains spidites. Bioturbation occurs throughout the unit. The member represents prodelta and delta top sediments.

The member can be traced along the western exposure belt on Spitsbergen by its yellow-grey weathering colour.

- -

159

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DISTRIBUTION SHOWN ON RG(S).: 3-08,3-09,3-10,3-12 STATUS OF UNIT: Formal FIRST USE OF NAME: B U C ~ I et al. 1965 CURRENT DEFINITION: PC&m 1983. The n m e was used by Buchan et al. (1965) for the entire Middle Triassic of Sval- bard. M d et al. (1982) reduced it to member rank ("Bar- entsraya Fo~ t ion" ) , d andesed it to central and eastern Svalbslrd. PEelina (1983) m m b use formation rank, although regionally limited in the sense of W k et al. SYNONYM(S) AND ~ E R E ~ Y C E ( ~ ) : "Oil shale member": Falcon 1928; "Oil hale member": Lock et al. 1978 ORIGIN OF NAME: BoWeia (transl. "The Cirque Glacier Hill"): A mountain in northern Nordemki6ld Land TWE SECTION @G. 3-37): Stratotype: Sticky Keep, Nordemkiisld Land DEPOSITIONAL AGE: Middle T W i c DATING METHOD: Ammmids, bivalves REFERENCE(S) FOR AGE: Tozer 62 Parker 1968; KorEinskaja 1982; Weitschat.& Le- 1983 OVERLYING UNIT@): Tschamddjellet Formation UNDERLYING UNIT@): =kin&gda Formation SUPERIOR UNIT: Sassendalen Group OTEER USE OF NAME: None THICKNESS: 135 m in Dickson Land, 168 m in the stratotype in northern Nordenskiold Land, 90-1 10 m on eastern Spits- bergen, ca. 80 m on Barentssya and Edgesya MAIN LITHOLOGIES: Mudstone, calcareous siltstone LOWER BOUNDARY D E ~ O N : The lower boundary is marked by soft, black mudstone with small phosphate nodules sharply overlying a yellow weathering, silty dolomite

Fig. 3-36: The calcareous siltstones of the Blanknuten Member (cliff), overlying the shaley part of the Botneheia Formation, Blanknuten, Edgeqa. Photo: A. Wrk

160

. - . age I lib. strat. m

l units cisivf f mcvcg pcbb

Fig. 3-37: Stratigraphic section M-24 Simtotype for: Botneheia Formation Locality: Sticky Keep Refirence: Wrk et al. 1982

bed at top of the underlying Vikingbgda Formation in the type section. In eastern areas (Storfjorden, eastern islands), the boundary is less distinct and defined by the first appearance of the characteristic black mudstones. DESCRIPTION: The Botneheia Formation forms a coarsening-upward succession, where the basal mudstones grade into siltstones (Fig. 3-36). The formation consists mostly of bluish weathering black shale with abundant small (up to 3 cm) phosphate nodules. Thin to medium thick, yellow weathering carbonaceous siltstone beds occur throughout the unit. The upper part is highly calcitic due to numerous contained thin-shelled bivalves, and these beds form a pronounced cliff (Blanknuten Member). The top is marked by a siltstone bed with phosphate nodules, and overlain by grey

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"ESOZOIC CITHOSTRATIGRAPHY

shale with purple weathering siderite nodules of the Tscher- makfjellet Formation

Marine fossils and reptile bone fragments (Fig. 3-38) occur and are abundant in the upper part, where it also is intensively bioturbated. The formation is rich in organic material (TOC 1-10 %), especially in the upper part. It represents, together with the time-equivalent, but more silt- and sandstone-rich Bravaisberget Formation, the most promising hydrocarbon source rocks of Svalbard.

The Botneheia Formation is interpreted as a deltaic influenced, regressive shelf deposit, with partly restricted environments in terms of water circulation (Mark et al. 1982, 1989).

Blanknuten Member (M-25)

STATUS OF UNIT: Formal FIRST USE OF NAME: Mark et al. 1982 CURRENT DEFINITION: W k et d . 1982 SYNONYM(S) AND REFERENCE(S): Blanknuten "Beds": Msrk et al. 1982. With the accepted formation rank of Botneheia shales, the Blanknuten unit is raised at member rank ORIGIN OF NAME: Blanknuten (transl. "The Shining Moun- tain Peak"): A mountain on the western coast of Edgesya TYPE SECTION (FIG. 3-39): Stratotype: Blanknuten, Edgesya DEPOSITIONAL AGE: Ladinian DATING METHOD: Ammonites, bivalves REFERENCE(S) FOR AGE: Tozer & Parker 1968; KorEinskaja 1982; Weitschat & Lehmann 1983 OVERLYING UNIT@): Tschermabfjellet Formation UNDERLYING UNIT(S): Unnamed SUPERIOR UNIT: Botneheia Formation OTHER USE OF NAME: None THICKNESS: 20-25 m on the eastern islands (21 m in the stratotype), 30 m in Dickson Land, up to 70 m in eastern Nordenskiijld Land MAIN LITHOLOGIES: Shale, calcareous siltstone, silty limestone LOWER BOUNDARY DEFINITION: The lower boundary is defined at the base of calcareous, cliff-forming siltstones in the upper part of the Botneheia Formation.

Tschermak- fpllet Frn. (Camian)

2 ;i .- .f 8 ' C I S 6 El -I

z 2 0 iii - i- a

0 2 c4 0

VI Fr,

a = < - n: .: 2;

-- z = i- a 0

L9

WMngh@gda Fonation

m 11111111111 dsivf f mcvcg pcbb

Fig. 3-39: Stratijpphic section M-25 Stmtotype for: Blanknuten Member Locality: B l h t e n , Edgeqa Reference: Msrk et al. 1982

DESCRIPTION: The Blanknuten M~~ consists of black, calcareous organic-rich M e s with thin to medium thick, calcareous siltstones and thin, silty limestone beds (Figs. 3- 36,3-38). The high calcite content is due to numerous thin- shelled bivdves. The unit usually forms a cliff along mountain sides. The member represents open marine shelf sedhents. It temiwta the deposits of the Sassendalen Group.

OC~RRENCE: Offshore unit, known from the Svalis Dome (Fig. 1-02) !%ATUS OF UNIT: F o ~ FZRST USE OF NAME: Mnrrk & Elvebakk 1999 CuRRrnT DEFINITION: W k & Elvebakk 1999 LSYNONYM(S) AND REFERENCE(S): None Qmcm OF NAME: Steinkobbe: Norwegian for 'common seal, harbour seal' (Phoca vihrlina) TYPE SECTION:

Sbtotype: Composite, shallow boreholes 7323107-U-03,- Fig. 3-311: Vertebrate Fcmains, mostly phosphoritised bone frrlgments, 04,-01,-07,-09, Svalis Dome

in the Blanknuten Member, Blanknutm, Ed-a. Photo: A. Mefds DEPOSITIONAL AGE: Spathian - Anisian

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DATING METHOD: Ammonoids, palynology REFERENCE@) FOR AGE: Vigran et al. 1998 OVERLYING UNIT@): Snadd Formation UNDERLYING UNIT@): Klappmyss Formation SUPERIOR UNIT: Sassendalen Group OTHER USE OF NAME: None THICKNESS: 107 m in the stratotype MAIN LITHOLOGIES: Mudstone, calcareous siltstone LOWER BOUNDARY DEFINITION: The base is defined at 107.05 m in core 7323107-U-03, where black organic-rich mudstone conformably overlies siltstone of the Klappmyss Formation. At this level there is an abrupt increase in both gamma radiation and organic content. DESCRIPTION: The Steinkobbe Formation is dominated by phosphatic, organic-rich mudstone (TOC 1.5-9 %), but also contains siltstone beds.

The lower part of the formation contains papery, finely laminated, unbioturbated mudstone. Some bioturbation occurs higher up where it partly disturbs the lamination. Phos- phate nodules are abundant, both globular and flattened, and are commonly a few centimetres in diameter, although individual nodules may reach larger diameters than the drill core (>S cm). There are also thin beds of carbonate- cemented siltstone. Pynte is abundant throughout the unit. Siltstones' dominate in the middle part (U-01 and U-07), where ripples are developed locally. Flattened bivalves and ammonoids occur commonly.

The Steinkobbe Formation is a facies equivalent of the Botneheia Formation and represents deep, mostly restricted, open shelf environments. The phosphatic, organic-rich sedimentation, however, started earlier in the Svalis Dome area (Spathian) and also ceased earlier than in Svalbard. The unit is included in the Sassendalen Group, but not the Ingoy- djupet Subgroup, because its lithology and organic content, as well as its depositional environment, are similar as in the Botneheia Formation. The lack of evidence for spatial continuity from the Svalis Dome to Svalbard, and the different age of the lower boundary, suggest retention of separate formational names.

INGOXDJUPET SUBGROUP (M-27)

STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Redefined here, from Worsley et al. (1988), to exclude the Snadd Formation which is correlated with the Kapp Toscana Group. The rank is here revised to subgroup (under Sassendalen Group) in order to achieve a correlative group subdivision for Svalbard and the Barents Sea Shelf. SYNONYM(S) AND REFERENCE(S): Ingsydjupet "Group": Worsley et al. 1988 ORIGIN OF NAME: Ingoydjupet: A deep north of Smoya, northern Norway TYPE AREA: Block 7120112, Hammerfest Basin. Base and top are compositely defined in exploration wells 7120112-2 and 7120112-1. STRUCTURAL SETTING: Barents Sea Shelf

DEPOSITIONAL AGE: Early and Middle Triassic OVERLYING UNIT(S): Storfjorden Subgroup UNDERLYING UNIT@): Palaeozoic SUPERIOR UNIT: Sassendalen Group OTHER USE OF NAME: None THICKNESS: 700-1000 m MAIN LITHOLOGIES: Shale, mudstone, siltstone, sandstone DESCRLPTION: The Ingsydjupet Subgroup is assigned to the Early-Middle Triassic development of the Southern Barents Sea. The subgroup is thick throughout the Hammerfest Basin, and with an attenuated lower part onlapping the crest of the Loppa High to the north. The upper parts have been eroded on the Troms-Finnmark Platform. Grey to black shales and mudstones dominate, but thin grey siltstones and sandstones are also present.

Marine environments in the subgroup suggest coast lines to the south and south-east of the Hammerfest Basin and progressive onlap of the Loppa High to the north.

OCCURRENCE: Offshore unit, known from the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 > CURRENT DEFINITION: W0rSley et al. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Havert: Norwegian for 'grey seal' (Hali- choerus grypus) TYPE SECTION:

Stratotype: Exploration well 7120112-2 Hypostratotype: Exploration well 7 12019-2 DEPOSITIONAL AGE: Induan DATING METHOD: Palyn010gy REFERENCE(S) FOR AGE: Little published documentation available; first referred to by Worsley et al. (1988) on the basis of oil company propriety data. OVERLYING UNIT@): Klappmyss Formation UNDERLYING UNIT@): Palaeozoic succession SUPERIOR UNIT: Ingsydjupet Subgroup OTHER USE OF NAME: None THICKNESS: 105 m (stratotype), 150 m (hypostratotype) MAIN LITHOLOGIES: Shale LOWER BOUNDARY DEFINITION: The base of the Havert For- mation is defined by increasing gamma ray and decreasing density response above underlying, Palaeozoic mixed clastic and carbonate successions. In the reference well the base is also easily recognised, where the basal silty shales directly overlie a 6 m thick limestone bed. DESCRIPTION: In its type section, the Havert Formation consists of medium to dark-grey shales with minor interbedded pale-grey siltstones and sandstones comprising two generally coarsening-upward successions. The reference section farther north in the Hammerfest Basin shows a more monotonous silty shale succession with only a very weak upward coarsening trend. Present information suggests a fining trend from the southern margin of the Hammerfest Basin northwards.

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The formation was deposited in shallow marine to open REFERENCE(S) FOR AGE: Little detailed published documen- marine settings with coastal environments to the south and tation available; first referred to by Worsley et al. (1988) on southeast. the basis of oil company propriety data.

OVERLMNC UNIT(S): Snadd Formation UNDERWING =(S): Klappmyss Formation

KLMPMYSS FORMATION (M-29) SUPERIOR UNIT: Ingsydjupet Subgroup -R USE OF NAME: None

OCCURRENCE: Offshore unit, known fiom the Hammerfest THICKNESS: 168 m (stratotype), 283 m (hypostratotype) Basin (Fig. 1-02) MAIN LITHOLOGIES: Shale, siltstone, sandstone STATUS OF UNIT: Formal LOWER BOUNDARY DEFINITION: The formation is defined by FIRST USE OF NAME: Worsley et al. 1988 upward increasing gamma ray, interval w i t time and neu- CURRENT DEFINITION: Worsley et al. 1988 tron porosity responses into the basal shale. Log responses SYNONYM(S) AND REFERENCE(S): None show much more variation above this unit. ORIGIN OF NAME: Klappmyss: Norwegian for 'hooded seal' DESCRIPTION: A 20 m thick basal shale passes upward into (Cystophom cristata) . interbedded shale, siltstone and carbonate-cemented sand- TYPE SECTION: stone. The formation shows many similarities to the Stratotype: Exploration well 7120112-2 Bravaisberget Formation of Spibbergen. Hypostratotype: Exploration well 7 12019-2 The formation Wkens northwds fn>m 140 m on the DEPOSITIONAL AGE: Olenekian Troms-Finnmark Platform. Thicknesses vary more from DATING METHOD: Palyn~logy platform to basin than for the underlying formations. REFERENCE(S) FOR AGE: Little detailed published documen- A transgressive pdse marking the base of the unit was fol- tation available; first referred to by Worsley et al. (1988) on lowed by renewed buildout of clastic, marginal marine the basis of oil company propriety data. regimes from southern coastal areas. OVERWING UNIT(S): KObbe Formation UNDERLYING UMT(S): Havert Formation SUPERIOR UNIT: Ingoydjupet Subgroup 3.5.2 Kapp Toscana Group OTHER USE OF NAME: None THICKNESS: 457 m (stratotype), 561 m (hypostratotype) MAIN LITHOLOGIES: Shale, siltstone, sandstone KAPP TOSCANA GROUP (M-31) LOWER BOUNDARY DEFINITION: The base of the Klappmyss Formation is defined by clear log breaks, with increasing gamma ray, interval transit time and neutron porosity values. This boundary can be correlated across the southwestern Barents Sea Shelf and reflects an early Olenekian (Smithian) transgression. DESCRIPTION: In the type section, medium to dark grey shales pass upwards into alternating shales, siltstones and sandstones. The reference section shows a similar trend, although more dominated by shale.

Shallow to open marine environments are ind~cated, with renewed north- to westwards coastal progradation following STATUS OF UNIT: Formal the earliest Olenekian transgression. FIRST USE OF NAME: B u ~ et al. 1965

CURRENT DEFINITION: Harland et al. 1974; herein extended to comprise coeval deposits on the Barents Sea Shelf

KOBBE FORMATION (M-30) SYNONYM(S) AND REFERENCE(S): Kapp Toscana "Forma- tion": Buchan et al. 1965

OCCURRENCE: Offshore unit, known fiom the Hammerfest ORIGIN OF NAME: ELBpp Toscana: A cape on the southern Basin (Fig. 1-02) mast of Van Keulenfjorden STATUS OF UNIT: Formal TYPE AREA: Central eastern Spitsbergen FIRST USE OF NAME: Worsley et al. 1988 STRUCTURAL SETTING: Barents Sea Shelf (including Sval- CURRENT DEFINITION: W0r~ley et d. 1988 bard) SYNONYM(S) AND REFERENCE(S): None DEPOSITIONAL AGE: c&an to Bathonim ORIGIN OF NAME: Kobbe: A Norwegian popular, collective OVERLYING UNIT(S): Adventdalen Group name for several Arctic seal species (Phoca vinslina, Erig- UNDERLYING UNIT(S): Sassendalen Gmup nathus barbatus, and others) SUPERIOR UNIT: None TYPE SECTION: HER USE OF NAME: None Stratotype: Exploration well 7120112-2 THICKNESS: Up to >475 m in Svalbard, up to 2000 m (?) on Hypostratotype: Exploration well 7 12019-2 Barents Sea Shelf DEPOSITIONAL AGE: Anisian MAIN LITHOLOGIES: Shale, siltstone, sandstone DATING METHOD: Palyn~logy DESCRIPTION: The Kapp Toscana Group comprises shales,

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upper part forms a condensed clastic sedimentary succession, only a few metres thick in southern and western Sval- bard, which gradually is more completely developed towards the east (Wilhehwya Subgroup). Equivalents on the Barents Sea Shelf show a comparatively thick development (Realgnumen Subgroup; Worsley et al. 1988). Sandstones

m m B STORFJORDEN SUBGROUP (M-32)

Fig. 3-40: Milne Edwardsfiellet, central Spitsbergen: The Kapp Toscana Group fonns the upper third of the slope, starting with the thin shales of the Tschermakfjellet Formation resting on top of the Botneheia Formation. The upper sandstone sucoession is the De Geerdalen Formation. The Iowa two thirds of the mountain represent the Sassendalen Group (Vikmgbgda and Botneheia formations; compare Fig. 3-24). Photo: A. NBrk

siltstones and sandstones of Late Triassic to Middle Jurassic (Bathonian) age in Svalbard and on the Barents Sea Shelf (Figs. 3-40,341).

The group is exposed along the Tertiary fold-thrust belt on western Spitsbergen, in central and emtan Spitsbergen, as well as on Barentsya, Edg- H- k g EIarls Land and BjnrmsYa. It continue8 in fhe sw.Wacs between these islands and soathwards across the h t s Sea Shelf to the Bjarmeland Platform afld the Fhmmmfest and Nordkapp basins (Fig. 1-02).

The group starts with the grey shales of the Tscherdc- fjellet Formation which normally grade upward into the immature sandstones of the De Geerdalen Formation (Stor- fjorden Subgroup). This interval contains a number of coarsening-upward successions with increasing proportions of sandstone towards the SW, NE and E, while shales dominate in the central areas of Svalbard. On Svalbard, the

Fig. 3-41: Blanknuten, Edgeaya: The lower cliiT(B1anknuten Member, Sassendalen Group) is upwards succeeded by the shales of the Tschermakfjellet Formation, while the overlying sandstones and shales of the De Geerdalen Formation build up the upper half of the slope. Photo: A. Mmk

and shales also dominate the group in the Barents Sea. The Kapp Toscana Group has been deposited in a gener-

ally nearshore, deltaic environment and is characterised by shallow marine and coastal reworking of deltaic and fluviodeltaic sediments (MIX% et al. 1982).

STATUS OF UNIT: F d FIRST USE OF NAME: Here CURRENT DEFINITION: Here S Y N O ~ ( S ) AM) WERENCE(S): None ORIGIN OF NAME! Storfjorden (transl. "The Big Inlet"): The strait between Spitsbergen and the eastern islands Edgenya and Bamntwya TYPE AREA: Eastern Spitsbergen -J

STRUCTURAL S ~ G : Barents Sea Shelf (including Sval- bard) DEPOSITJONAL AGE: Late Triassic OVERLMNC UNIT(S): Wilhehwya and Realgrunnen subgroups UNDERLYING UNIT(S): Sassendalen Group SUPERIOR UNIT: Kapp Toscana Group OTIIER USE OF NAME: None THICKNESS: Up to 350 m on Svalbard, up to 1400 m on the Barents Sea Shelf MAIN LITHOLOGIES: Shale, siltstone, sandstone DESCRIPTION: The Storfjorden Subgroup includes the Tschermakfjellet, De Geerdalen, Skuld and Snadd formations, i.e. the compositionally immature lower part of the Kapp Toscana Group representing shallow shelf, pro-delta to delta top depositional environments. .The basal part of the subgroup is dominated by grey

shales (Tschermakfjellet F d o n and lower part of Snadd and Skuld formations). The sediments coarsen upmud into sandstones (De Geerdalen Formation and upper part of S d and Skuld formations). The base of the formation is distinctly diachronous, with an earlier onset on the pouthem Barents Sea Shelf (Fig. 3-05).

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Tschermakfjellet . ~orrnafion

age l 11th. &rat - l units ds~vf f mcvcg pcbb

Fig. 3-42: Stratigraphic section M-33 Shatotype for: Tschermakfjellet Formation Locality: Botneheia Reference: MBlk et al. 1982

DISTRIBUTION SHOWN ON FIG@).: 3-06, 3-07, 3-08, 3-09, 3-10,3-12 STATUS OF UNIT: Formal : . *.,g FIRST USE OF NAME: Buchan et d. 1969-" -' CURRENT DEFINITION: Mork et d. 1982; Slight& ren'wd herein to include the "Austjmrhelen Formation": Mmk et al. 1982 SYNONYM(S) AND REFERENT'-): Tschennakfjellet 'Wein- ber": Buchan et al. 1965 ORIGIN OF NAME: Tscherma illet: A mountain in Dicbon Land TYPE SECTION (FIG. 3-42): Stratotype: Botneheia, northern Nordenskiold Land DEPOSITIONAL AGE: &W& C m DATING METHOD: Ammonoids REFERENCE@) FOR WE: KorEinskaja 1982; Dagys et 1993 OVERLYING UNIT@): De G& Formation UNDERLYING UNIT(&): B ~ ~ e t and Botneheia formations SUPERIOR UNIT: Storfjorden Subgroup OTHER USE OF NAME: None THICKNESS: 0-30 m on western Spitsbergen, 30-65 m in central and eastern Spitsbergen (5 1 m in the stratotype), 65- 140 m on Barentsraya and Edgenrya MAIN LITHOLOGIES: Shale LOWER BOUNDARY DEFINITION: The base is defined where grey, silty shale with red weathering laminae and nodules of siderite occurs on top of the cliff-forming, darker grey silt- and sandstones of the upper part of the Bravaisberget or Botneheia formations. The darker colour of the underlying rocks is due to a higher bitumen content. DESCRIPTION: The Tschermakfjellet Formation consists of dark grey shales with upward increasing intercalated siltstone laminae and corresponding decrease in siderite nodules. Fossiliferous beds with ammonoids, bivalves, gastropods and brachiopods occur in eastern areas.

The formation represents a shale-dominated, coarsening- upward, pro-delta depositional environment.

De Geerdalen

DISTRIBUTION SHOWN ON PIG(s).: 3-06, 3-07, 3-08, 3-09, 3-10,3-12 STATUS OF UNIT: Formal FIRST USE OF NAME: Buchan et al. 1965 CURRENT DEFINITION: Mink et al. 1982 SYNONYM(S) AND REFERENCE(S): De Geerdalen "Member": Buchan et al. 1965

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3. MESOZOlC LITHOSTRATIGRAPHY

Wilhelrnraya Subgroup

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Formation (Carnian)

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Fig. 3-46: Stratigraphic section M-34b Hmostmtotype for: De Geerdalen Fonnation Locality: Dalsnuten Reference: MBrk et al. 1982

may belong to either of the types described below (Figs. 3- 45,3-46). DESCRIBTION: The De Geerdalen Formation consists of repeated coarsening-upward successions from shale to sandstone.

Silly shales that contain siderite nodules alternate with sandstones. The sandstones are texturally and compositionally immature, in contrast to the sandstones of the Sassen- dalen Group and Wilhelmsya Subgroup. Thick sandstones

form cliffs in the mountainsides. live main types of sandstone occur: (1) Massive, argillaceous, medium-grained, locally greenish, pale grey weathering sandstones that coarsen upwards; they are mostly structureless, although some bioturbation and linguoid ripples occur. (2) Upward-fig sandstones with sharp lower contacts, some with intraformational mud conglomerates or gravelstones. Ripple structures and cross-bedding alternating with parallel bedding are common, and channel structures prevail locally (Figs. 3- 43,3-44). These sandstones weather with a brownish colour. Minor sandstone beds showing desiccation cracks, raindrop imprints and flaser bedding are locally found.

In western and central to eastem Spitsbergen, the upper part of the De Geerdalen Formation is dominated by multicoloured shales, alternating with minor coarsening-upward units ta: rminating in silt or sands@ne beds (Isfjorden Mem- ber). Some reddish siderite beds which contain plant fossils, fossilised logs, coal frtqpents id cone-h-cone structures are also present.

The De Geerdalen Formation was deposited in shallow shelf to deltaic environments.

Istjorden Member (M-35)

STATUS OF UNIT: Formal WT USE OF NAME: PEelina 1983 CURRENT DEEWITION: PEelina 1983 SYNONYM(S) AND REFERENCE(S): Isfjorden "Formation": PEelina 1983 ORIGIN OF NAME: Isfjorden: (transl. "The Ice Fiord") A major inlet on central Spitsbergen TYPE SECTION WG. 3-45): Stratotype: Storfjellet, central Sabine Land DEPOSITIONAL AGE: Early Norian DATING METHOD: Bivalves, conchostracans and pdyn010gy REFERENCE(S) FOR AGE: PEelina 1983; J .0 . Vigrall, written commun. 1997 OVERLYING UNIT(S): Wilhelmaya Subgroup UNDERLYING UNIT(S): Unnamed SUPERIOR UNIT: Storfjorden Subgroup c h ' I i E ~ USE OF NAME: None THICKNESS: 55-135 m, 87 m in the stratotype MAIN LITHOLOGIES: Shale, mudstone, siltstone, sandstone LOWER BOUNDARY DEFINITION: The lower boundary is defined at the base of a siltstone bivalve coquina bed which occurs above a thick cross-bedded sandstone unit of the De Geerdalen Formation. DESCRIPTION: The Isfjorden Member constitutes the upper part of the De Geerdalen Formation. It consists of alternating shales and evenly bedded, thin- to thick-bedded siltstone and sandstone beds. A siderite nodule bed often occurs some metres above the base, and bivalve coquina beds occur in several sections. The shales may be multicolowed and contain reddened mudstones. Carbonate beds, phosphate nodules and gravel or conglomerate lenses are characteristic. Wave and ripple lamination are common. Plant fragments are abundant, and conchostracans have been found in this member only, The unit was &posited in shallow marine shelf (?locally lagoonal) environments.

167

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The member is easily recognised fiom a distance, as it is made up of evenly bedded albnmthg sandstones and mudstones that form the upper part of the De Geerdalen Forma- tion, resting on thick pronounced satldstones which vary considerably in thickness.

DISTRIBUTION SHOWN ON FIG(s).: 2-05 STATUS OF UNIT: Formal FIRST USE OF NAME Kmil'SiSikov & Liviiic 1974 CURRENT DEWINITION: Mark et al. 1982 SYNONYM(S) AND REFERENCE(S): "Hzddjella Formation" on Bj~nnsya: PEelina 1983 ORIGIN OF NAME: Skllld (m OldNOW g 0 d d ~ ) : m of the mountain summits of EVIisqdjdl:Uet, Bjsramrya TYPE SECTION 34%): Stratotype: U 4 k%s&~llat (gjmwyft) DEPOS~ONAL AGE: Late WWim - m l y C d a n D ~ G METHOD; Ammrmoids, bivalveg, palynology REFERENcE(s) FOR AGE: Whm 1903; Merk et d. 1990; Dagys et al. 1993 OVERLYING UNIT(S): None UNDERLYING UNIT(S): Urd Formation SUPERIOR UNIT: Storfjorden Subgroup I HER USE OF NAME: None THICKNESS: 140 m (top eroded) MAIN LITHOLOGIES: Shale, siltstone, sandstone LOWER BOUNDARY DEFINITION: The lower bow- is defined where grey shale with spread red weathering siderite nodules rests on top of the phosphate nodularVerdan& Bed. DESCRIPTION: The Skuld Formation (Pig. 3-28) consists of basal shales and four coarsening-upward units from shale to sandstone, the lowermost and uppermost being most pronounced. The sandstones are immature. Siderite nodules occur.

At the top of the unit, i.e. below the present erosion surface, a 20 m thick, bedded, fine-grained sandstone succession rich in bivalves and plant ftagments occurs.

The basal grey shales with red-weathering siderite are re- sembling the Tsch-ellet Formation Eurther north in Svalbard, while the mLhmes mela te lithologidly with the De Geerdalen Fomatian. The SWd Formation thus reflects a similar development like the two other f m t i o n s , but here, on Bjornsya, at an a d e r h e . This demonstrates the diachronism of the Stosijmden Subgroup. The formation was deposited in shallow &eW environments.

The unit is described in detail by P E e b (1972) and Mark et al. (1990).

OCCURRENCE: Offshore unit, known fiom the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFLNITION: Worsley et al. 1988 SYNONYM@) AND REFERENCE(S): None ORIGIN OF NAME: Snadd: A local Norwegian name for 'ringed seal' (Phoca hispida) TYPE SECTION: Stratotype: Exploration well 7120112-2 Hypostratotype: Composite; cored exploration well 7120112-1,9-2 DEPOSI~ONAL AGE: Ladinian - Norian DATING METHOD: Palyn010g~ REFERENCE(S) MIRAGE: Wmley et al. 1988 . OVERLYING UNIT@): Realgnumen Subgroup UNDERLYING =(S): Sassendalen Group SUPERIOR UNIT: Storfjorden Subgroup OTHER USE OF NAME: None THICKNESS: 944 m in the stratotype, 1410 m in the hypostratotype MAIN LITHOLOGIES: Shale, siltstone, sandstone LOWER BOUNDARY DEFINITION: The base of the Snadd For- mation is shown by a clear log break at t h ~ base of a 60 m shale interval above the mixed lithologies of the &lying unit. The break is marked by a sharp increase to a more uniform response in gamma ray, interval transit time and neutron porosity values. DESCRIPTION: Basal grey shales coarsen upward into shales with interbeds of grey siltstones and compositionally immature sandstones. Limestones and calcareous interbeds are relatively common in the lower and middle parts of the formation, while thin, coaly lenses are locally developed at higher levels. Distinctive dusky, red-brown shales conclude the succession. Lateral and vertical lithological variations may provide the basis for a future member subdivision.

The formation is similar to the Tschermakfjellet (basal shales) and De Geerdalen formations in Svalbard, though deposition of the individual facies started earlier on the Barents Shelf. This demonstrates the diachronism of the Storfjorden Subgroup (see also S W Formation, M-36).

The Ladinian succession represents relatively distal marine environments in all drilled wells, following a major transgressive pulse which submerged all structural Eghk and platform areas. The Carnian is marked by large-scale progradation of deltaic systems over the entire region.

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STATUS OF UNIT: Formal WIRST USE OF NAME: Worsley 1973 CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): Wilhelmsya Formation: Worsley 1973; W. Member: Smith 1975 ORIGIN OF NAME: Wilhelmsya: A small island at the southern end of Hinlopenstretet, northeastern Svalbard TYPE SECTION (FIG. 3-47): Wilhelmnrya STRUCTURAL SETTING: Svalbard area of Barents Sea Shelf DEPOSITIONAL AGE: N~!'ian - Bathonian OVERLYING UNIT@): Adventdalen Group UNDERLYING UNIT@): Storfjorden Subgroup SUPERIOR UNIT: Kapp Toscana Group OTHER USE OF NAME: None THICKNESS: 3-25 m on western Spitsbergen, 109 m in the stratotype on Wilhelmnrya, ca. 230 m in Kong Karls Land MAIN LITHOLOGIES: Sandstone, shale, mudstone, conglomerate DESCRIPTION: The Wilhehmya Subgroup in Svalbard comprises the condensed time-equivalent of the Realgrunnen Subgroup on the southern Barents Sea Shelf. Its thickness decreases si&~cantly towards the west and northwest, where hiati become increasingly important. The exact age range and location of the hiati in the individual sections is disputed.

The Wilhehmya Subgroup shows significant lateral variations, reflected by its complex subdivision, with an eastward increasing number of vertical submits. The formational subdivision on Spitsbergen is geographically based, but is stratigraphically based in the more complete sections in eastern Svalbard. The subdivision on Spitsbergen is only at memkr level and of inf-m hw of-&e mentioned nnoertahties. . - . m ' . :+ - ;-.; .; . , ,..; . : : . h f

The type section on Wilhe-a 'co&&ts of one major coarsening-upward succession ftom organic-rich sideritic mudstones to mineralogicdly mature sandstones. The upper part captains a varying number of phosphatic conglomerates or phosphorite nodule horizons.

Phosphatic nodular beds are typical for the subgroup, and two formally defied nodular beds occur at i@ Lee (Slottet Bed) and iEs top (Brentskarmen Bed). ' ;, - ._I,,

The subgroup consists of matme sandstones deposited in deltaic through shallow marine environments, increasingly

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STATUS OF UNIT: Formal P, c

FIRST USE OF NAME: Here CURRENT DEFINITION: Here; based on descriptions by Worsley 1973, Smith 1975, and PEelina 1980 SYNONYM(S) AND RE~RENCE($): None ORIGIN OF NAME: Slottet (tram1. 'The Palace" or "The

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Fig. 3-48: The equivalent of the Slottet Bed (spotted carbonate) at Lyngefjellet on Hopen. Photo: A. Mnrk

Castle"): A mountain in western Sabine Land, central Spits- bergen TYPE SECTION:

Stratotype: Slottet, Sabine Land. The Slottet Bed has traditionally been recognised as an individual unit independently of its position at the base of the Wilhelmsya Subgroup. This explains why the stratotype of the Slottet Bed does not coincide with the boundary stratotype of the Wilhelmsya Subgroup. DEPOSITIONAL AGE: Early Norian DATING METHOD: Fossils, mainly ammonoids (Ptemsiren- ites fauna) REFERENCE(S) FOR AGE: KorEinskaja 1980; Basov et al. 1993 UNDERLYING UNIT(S): De Geerdalen Formation SUPERIOR UNIT: Wilhehmya Subgroup OTHER USE OF NAME: None THICKNESS: 7-1 1 m in eastern Svalbard, 7.5 m on Wilhelm- q a , 5.2 m in the stratotype at Slottet, 1 .5 m on Hopen MAIN LITHOLOGIES: Calcareous sand- and siltstone, polymict conglomerate (locally with phosphate nodules) LOWER BOUNDARY DEFINITION: The lower boundary is defined at the first carbonate sandstone bed containing phosphatic nodules in the Upper Triassic succession. DESCRIPTION: The Slottet Bed forms a prominent marker horizon at the base of the Wilhelmraya Subgroup in Svalbard and occurs at the base of the laterally equivalent Flatsalen, Knorringfjellet and Smalegga formations.

In the type section, the bed is 5.2 m thick and consists of fine- to medium-grained quartzose sandstone with phosphatic nodules and siltstone interbeds. Interbeds or lenses of gravelstones and conglomerate occur at the base, particularly consisting of redeposited phosphatic nodules, as well as fragments of quartz, siderite and siliceous rocks. The upper part of the bed is siderite-cemented sandstone with leptochlorite and glauconite. A yellow-brown, spotted carbonate layer occurs both on Wilhelm0ya and on Hopen (Fig. 3-48). Bivalves, brachiopods and ammonoids occur. The bed represents a condensed shelf deposit.

J ' Smalegga I

C SOUTHERN SPITSBERGEN

DISTRIBUTION SHOWN ON FIG(s).: 3-06 (within 'Kapp Toscana Group, undifferentiated') STATUS OF UNIT: Formal FIRST USE OF NAME: W r k et al. 1982 CURRENT DEFINITION: Mark et al. 1982; herein raised to formation rank SYNONYM(S) AND REFERENCE@): Smalegga "Member": Mark et al. 1982 ORIGIN OF NAME: Smalegga (transl. "The Narrow Ridge"): A mountain ridge in Sarkapp Land TYPE SECTION (FIG. 3-50): Stratotype: Smalegga DEPOSITIONAL AGE: Norian to Bathonian, with two major hiati (late Norian - Pliensbachian and Bajocian) DATING METHOD: Bivalves (pectens, Triassic part), ammonoids (Jurassic part) and stratigraphic relationships REFERENCE(S) FOR AGE: PEelina 1980 OVERLYING UNIT(S): Agardhfjellet Formation UNDERLYING UNIT(S): De Geerdalen Formation SUPERIOR UNIT: Wilhelmsya Subgroup OTHER USE OF NAME: None THICKNESS: 24-45 m, 24 m in the stratotype MAIN LITHOLOGIES: Sandstone, conglomerate LOWER BOUNDARY DEFINITION: The lower boundary is defined by the base of the Slottet Bed (see there). DESCRIPTION: The Smalegga Formation represents the extremely condensed Wilhelmsya Subgroup in the Smkapp- Homund area. There is a gradual transition to its northern equivalent, the Knorringfjellet Formation, in Torell Land.

The formation is dominated by bioturbated, quartzitic sandstones with phosphatic nodular conglomerates at the

Fig. 3-49: Cone-in-cone texture within a yellow, sideritic layer in the Smalegga Formation, Treskelen, Hornsund. Photo: W.K. Dallmann

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Keilhaufjellet member (M-41)

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Fig. 3-50: Stratigraphic section M-40 Stratotypefor: Smalegga Formation Locality: Smdegga Reference: b j e W 6 1992

base (Slottet Bed) and top (Brentskardhaugen Bed). While the unit shows a homogeneous development in its type locality, it increasingly contains shales with siderite beds at the base of the unit when passing northwards (Fig. 3-49). The formation was deposited in shallow marine environments.

A detailed description with several stratigraphic sections of the unit is given by Krajewski (1992).

STATUS OF UNIT: Informal FIRST USE OF NAME: PEelina 1980 CURRENT DEFINITION: PEelina 1980 SYNONYM(S) AND RE~RENCE(S): Keilhaufjellet "Forma- tion": PEeliia 1980 ORIGIN OF NAME: Keilhaufjellet: A mountain in southern smkapp Land TYPE SECTION:

Stratotype: Keilhaufjellet West DEPOSITIONAL AGE: N0ritlU DATING METHOD: Bivalves (pectens) , REFERENCE(S) FOR AGE: PEelina 1980 OVERLYING UNIT(S): Mathiasbreen member UNDERLYING UNIT(S): De Geerdalen Formation SUPERIOR UNIT: Smalegga Formation OTHER USE OF NAME: None THICKNESS: 25-30 m MAIN LITHOLOGIES: Sandstone LOWER BOUNDARY DEFINITION: The lower boundary is defined by the base of the Slottet Bed (see there). DESCRIPTION: The Keilhaufjellet member constitutes the Triassic part of the Smalegga Formation. The reason for the establishment of this member is a suggested disconformity including a major hiatus above the member (PEelina 1980).

The Keilhaufjellet member consists of sandstones with sandy-sideritic intercalations and concretions with lenses of very coarse sandstones and phosphate nodules. The member was deposited in shallow marine environments.

The relationship to the overlying Mathiasbreen member is not lithostratigraphically well defined at present, and the name is suggested to have an infonnal rank until a member subdivision with a lithological boundary definition is presented.

Mathiasbreen member (M-42)

STATUS OF UNIT: Informal FIRST USE OF NAME: PEelina 1980 CURRENT DEFINITION: PEelina 1980 SYNONYM(S) AND REFERENCE(S): "Ssrkapp Formation": PEelina 1980. This name is rejected because it contains a place name far from the exposure area, and is reminiscent of the name 'Smkapp Land Group' for an Ordovician unit (Birkenmajer 1978) which has priority. ORIGIN OF NAME: Mathiasbreen: A glacier adjacent to the type section in southern Ssrkapp Land TYPE SECTION:

Stratotype: Keilhaufjellet West DEPOSITIONAL AGE: ?Pliensbachian - Bathonian DATING METHOD: Ammonoids REFERENCE(S) FOR AGE: PEelina 1981) OVERLYING UNIT(S): Agardhfjellet Formation UNDERLYING UNIT(S): Keilhaufjellet member SUPERIOR UNIT: Wilhelfnsya Subgroup OTHER USE OF NAME: None THICKNESS: 14 m in the stratotype MAIN LITHOLOGIES: Sandstone, siltstone, conglomerate

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LOWER BOUNDARY DEFINITION: The base is defined by a 1

late Norian to 7Pliensbachian hiatus which is not lithostratigraphically well recognised DESCRIPTION: The Mathiasbreen member constitutes the Jurassic part of the Smalegga Formation Tbe reason for the establishment of this member is a suggested underlying disconformity including a major hiatus (PEelina 1980).

The unit consists of sandstanes, sandy siltstones with small pebble conglomerates and wnal beds with phosphate nodules. The unit has an erosive base. The top is formed by the phosphatic nodular Brentskardhaugen Bed. The member was deposited in shallow marine environments.

The relationship to the underlying Keilhaufjellet member Fig. 3-51: A section of the Knorringfjellet Formation at Festningen is not lithostratigraphically well defined at present, and the (type section). Photo: J. Nagy name is suggested to have an informal rank until a member subdivision with an acceptable lithological boundary definition is presented. Wilhelmsya Subgroup throughout most of Spitsbergen

(Figs. 3-51, 3-52), except for the Sorkapp - Homsund area (see Smalegga Formation) and Olav V Land (see Flatsalen, Svenskraya and Kongsaya formations). There is a gradual transition to its southern equivalent, the Smalegga Fonna- tion, in Torell Land, and to the more complete succession in Olav V Land.

The formation consists of shales, sandstones and carbonate rocks with a thin polyrnict (phosphatic) conglomerate at its base (Slottet Bed) and top (Brentskardhaugen Bed). It rests conformably on the De Geerdalen Formation. The unit represents a strongly condensed interval and includes long depositional breaks. The formation was deposited in shallow marine environments

D~STRIBUTION SHOWN ON FIG(S).: 3-07, 3-08,3-09,3-10 (within 'Kapp Toscana Group, undifferentiated' or 'Wilhelmqa Group, undifferentiated') STATUS OF UNIT: Formal FIRST USE OF NAME: Mwk et al. 1982 CURRENT DEFIMTION: Here SYNONYM(S) AND REFERENCE(S): KnorringGellet "Mem- ber": Mmk et al. 1982 I ORIGIN OF NAME: Knorringfjellet: A mountain in northern Nordenskiold Land TYPE SECTION (FIG. 3-53): Stratotype: Festningen, outer Isfjorden DEPOSITIONAL AGE: Norian to Bathonian, with two major hiati (late Norian - Pliensbachian and Toarcian - ?early Bathonian)

I Tverrbekken member (M-44)

I Fig. 3-52: Dunes h the sandstones of the Knorringfjellet Formation,

DATING METHOD: Ammonoids, bivalves, palynology, strati- Tilasberget, Wedel Jarlsberg Land. Photo: W.K. D h a n n graphic relationships REFERENCE(S) FOR AGE: PEelina 1965; Bjzrke & Dypvik 1977; KorEinskaja 1980; BtIckstriim & Nagy 1985 OVERLYING UNIT@): Agardhtjellet Formation UNDERLMVG UNIT(S): De Geendalen Formation STATUS OF UNIT: Informal SUPERIOR UNIT: Wilhehwya Subgroup FIRST USE OF NAME: Here OTHER USE OF NAME: None CURRENT DEFINITION: PEelina 1980 THICKNESS: 3-75 m, 18 m in the stratotype S Y N O ~ ( S ) AND REFERENCE(S): "Tvillingodden Forma- MAIN LITHOLOGDES: Sandstone, shale, conglomerate tion": PEelina 1980 (see Chapter 3.6.1) LOWER BOUNDARY DEFINITION: The lower boundary is de- ORIGIN OF NAME: Tverrbekken (transl. "The Transverse fined by the base of the Slottet Bed (see there). Creek"): A creek in western Nordenskiold Land, close to the DESCRIPTION: The Knorringfjellet Formation represents the type section

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Fig. 3-53: Stratigraphic section M-43 Stmtotype for: Knorringfjelfet Formation Locality: Festningen 2 Reference: Mmk et al. 1982

TYPE SECTION:

Stratotypp: Festningen DEPOSITIONAL AGE: Norian DATING METHOD: Bivalves REFERENCE(S) FOR AGE: PEelina 1965; KorEinskaja 1980 OVERLYING UNIT(S): Teistberget member UNDERLYING UNIT(S): De Geerdalen Formation SUPERIOR UNIT: Knorringfjellet Formation OTHER USE OF NAME: None THICKNESS: 1-21 m MAIN LITHOLOGES: ands stone LOWER BOUNDARY DEFINITION: The lower boundary is defined by the base of the Slottet Bed (see there). DESCRIPTION: The Tverrbekken member constitutes the Tri- assic part of the Knorringfjellet Formation. The reason for the establishment of this member is a suggested disconformity including a major hiatus above the unit (PEelina 1980).

The member starts with the phosphatic nodular Slottet

Bed and consists upwards of sandstones with intercalated shales and calcareous beds, ferruginous carbonate concretions and occasionally coquina and algal limestone interbeds. Bivalves and echinoderms are present. The member was deposited in shallow marine environments.

The relationship to the overlying Teistberget member is not lithostcatigraphically well defined at present, and the name is suggested to have an informal rank until a member subdivision with an acceptable lithological boundary definition is presented.

Teistbsrget member W-45) 8 8

STATUS OF UNIT: Informal FIRST USE OF NAME: PEelina 1980 CURRENT DEFINITION: PEelina 1980 SYNONYM(S) AND REFERENCE(S): Teistberget "Formation": PEelina 1980 ORIGIN OF NAME: Teistberget (trwl. "The Black Guillemot Mountain"): A mountain at the eastern coast of Sabine Land TYPE SECTION: Stratotype: Teistberget NE DEWSITTONAL AGE: Pliensbachian - Bathonian DATING METHOD: Dinoflagellates, ammonites, stratigraphic relationships x.9

REFERENCE(S) FOR A6E: Bjaxke & Mvik 1977; PEelina 1980; Bbkstr6m & Nagy 1985 OVERL~G UND'(S): Agardhfjellet Formation UNDERLYING m($): Tvenbekken member, Flatsalen For- mation SUPERIOR UNIT: Knorringfjeffet Formation OTHER USE OF NAME: X0np , - . a v 7'

THICKNESS: 14-26m L. . v . \ . ' :-L: , . , . . MAIN LITHOLOGES: Sandstone, conglomerate LOWER BOUNDARY DEFINITION: The base is defined by a late Norian to ?Pliensbachian hiatus which is not lithostratigraphically recognised. DESCRIPTION: The Teistberget member constitutes the Jurassic part of the Knorringfjellet Formation. The reason for the establishment of this member is a suggested discon- fonnity including a major hiatus below this unit (PEelina 1980).

The member consists of two submits. The lower subunit comprises ofien poorly consolidated sandstones with abundant plant remains, while the upper subunit consists of glauconitic sandstones. The member is capped by the Brent- skardhaugen Bed (see there). The member was deposited in shallow marine environments.

The relationship to the underlying Tverrbekken member is not lithostratigraphically well defined at present, and the name is suggested to have an informal rank until a member subdivision with an acceptable lithological boundary definition is presented.

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Fig. 3-54: Stratigraphic section M-46a Stmtofype for: Flatsalen Formation Locality: Lyngefjellet, Hopen Reference: Larssen et al. 1995 (unpubl.)

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DISTRIBUTION SHOWN ON FIG(s).: 3-10,3-11,3-12 (partly within 'Kapp Toscana Group, undifferentiated' or 'Wilhelmqa Group, undifferentiated') STATUS OF m: Formal FIRST USE OF NAME: Smi€h et al. 1975 CURRENT DEFINITION: Herein. The formation was first defined on Hopen, but is here extended to Kong Karls Land, Wilhehmya and eastern Spitsbergen Smom(s) AND REFERENCE(S): ccBasal member", "Bjm- bogen Member" and 'Transitional member" on Wilhelm- oya: Worsley 1973; "Arnesenodden Shale Bed" on Sven- shsya: Smith et al. 1976; "Kapp Koburg Formation": Worsley & Heintz 1977; "Bjmbogen Formation" in eastern Svalbard: PEelina 1980. ORIGIN OF NAME: Flatsalen (transl. "The Flat Saddle"): A mountain pass at Lyngefjellet, Hopen TYPE SECTION (FIGS. 3-54,3-55): Sfratotype: Flatsalen, Lyngefjellet, Hopen Hypostratotype: Hwagrehaugen, Kongswa DEPOSITIONAL AGE: Norian DATING METHOD: Ammonoids, bivalves REFERENCE(S) FOR AGE: Smith et d. 1975, 1976; Bjzrke 1977; KorEinskaja 1980; Olaussen et al., in prep. OVERLYING UNIT(S): Svenshsya Formation, Knorringfjellet Formation UNDERLYING UNIT(S): De Geerdalen Formation SUPERIOR UNIT: Wilhebya Subgroup OTHER USE-OF NAME: None THICKNESS: Up to 52 m (stratotype) MAIN LITHOLOGIES: Shale, siltstone, sandstone

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LOWER BOUNDARY DEFINITION: The lower boundary is defined by the base of the Slottet Bed (see there). DESCRIPTION: The Flatsalen Formation is often characterised by a gentler slope between the cliff-forming sandstones of the De Geerdalen and Svensksya formations. The slqpe is interrupted by several steps reflecting slight coarsening-upward successions. The dominant lithology is dark grey silty shales, which grade into, and are interbedded with, siltstones and fine-grained sandstone in the more resistant horizons. The shales contain beds of nodular clay- ironstone, bright red-brown to purplish weathering, which are particularly abundant immediately above the resistant, coarser horizons. The sandstones usually weather yellow or brownish and are very thinly bedded. Overlying a prominent calcareous bed near the base (Slottet Bed), a horizon of The - exPsmg -y

brown weathering, bioturbated siltstone occurs. Bivalves are clifFs Of the Svensknrya Photo: Johannessen

common in the siderite, and ammonoids are found. The formation is marine throughout, and the palynomorph assemblages suggest shallow, near-shore conditions (Smith et al. REFERENCE(S) FOR AGE: Smith et al. 1975, 1976; Bjsrke 1975). -1977; PEelina 1980; Olaussen et al., in prep.

The Flatsalen Formation is a lateral time equivalent of the OVERLYING UNIT(S): Kongs~lya Formation Tverrbekken member of the Knorringfjellet Formation in UNDERLYING UNIT(S): Flatsalen Formation eastern central Spitsbergen. The transition has not yet been SUPERIOR UNIT: Wilhelmeya Subgroup located. USE OF NAME: None

THICKNESS: 20-ca. 190 m (stratotype) MAIN LITHOLOGIES: Sandstone, mudstone LOWER BOUNDARY DEFINITION: The base is covered in the

DISTRIBUTION SHOWN ON ~ G ( s ) . : 3-1 1,3-12 STATUS OF UNIT: Formal FIRST USE OF NAME: Sfith et al. 1976 CURRENT DEFINITION: Here; Olaussen et al., in prep. The formation was first defined in Kong Karls Land, but is herein extended to Hopen, Wilhelmsya and Olav V Land. The stratigraphy of Kong Karls Land has been substantially revised as a result of recent investigations. The lower part of the Svenskoya Formation as originally defined is now correlated with the Flatsalen Formation (M-46), while the upper part is referred to the revised Svensksya Formation (see chapters 3.4.2, 3.6.1). SYNONYM(S) AND REFERENCE(S): Lower part of "Tumling- odden Member" on Wilhelmeya: Worsley 1973; "Lyngefjel- let Formation" on Hopen: Smith et al. 1975; Lower part of "l'iunlingodden Formation" in eastern Svalbard: PEelina 1980. ORIGIN OF NAME: Svenskoya (transl. "The Swede Island"): The western island of Kong Karls Land TYPE SECTION (FIG. 3-57): Stratotype: Sjogrenfjellet W, Kongsaya DEPOSITIONAL AGE: ?Latest Triassic - Early Jurassic DATING METHOD: Fossils (foraminifera; palynology, etc.)

type section, but a greenish carbonate-cemented sandstone in the lower part, approximately 5 m above the uppermost exposure of the Flatsalen Formation is regarded as representing the basal bed. DESCRIPTION: The Svensksya Formation (Fig. 3-56) is subdivided into the Sjogrenfjellet and Mohdwgda members in Kong Karls Land. The Sjogrenfjellet Member extends to Hopen, Wilhelmsya and Olav V Land.

The formation is dominated by sandstone. The lower member consists of greenish, fine- to medium-grained sandstone in the lower part, grading into fine- to very fine- . grained, white sandstones with thin mudstone beds.

The upper member consists of yellow and white, fine- grained to very fine-grained sandstones that may occasionally be cemented by carbonate. A few mudstone horizons, siderite nodules and a few thin conglomerate beds are also present. The Mohdwgda Member displays a more pronounced bedding than the underlying member.

The formation grades laterally into the Teistberget member of the Knorringfjellet Formation. It is interpreted as representing tidal flat, tidal channel and coastal plain deposits (Sjogrenfjel- let Member) grading upward into a wave to tidal dominated shoreline or protected bay deposit (Mohnhnrgda Member).

Sjogrenfjellet Member (M-48)

STATUS OF UNIT: Formal FIRST USE OF NAME: Smith et al. 1976 CURRENT DEFINITION: Here, Olaussen et al., in prep. The stratigraphy of Kong Karls Land has been substantially revised according to recent understanding. The present definition of the Sjogrenfjellet Member corresponds to the ,:

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middle part of the "Sjogrenfjellet Sandstone Member" as originally defined, but geographically extended (see chapters 3.4.2,3.6.1). SYNONYM(S) AND REFERENCE(S): Lower part of "Tumling- odden Member" on Wilhelm0ya: Worsley 1973; "Lyngefjel- let Formation" on Hopen: Smith et al. 1975; Lower part of 'Tumlingodden Formation" in eastern Svalbard: PEelina 1980 OIUGIN OF NAME: Sjogrenfjellet: A mountain on Kongsarya, Kong Karls Land TYPE SECTION (FIG. 3-57): Stratotype: Sjogrenfjellet W, Kongssya DEPOSITIONAL AGE: ?Latest Triassic - Pliensbachian DATING METHOD: Fossils (foraminifera; palynology, etc.) REFERENCE(S) FOR AGE: Smith et al. 1975, 1976; Bjaxke 1977; PEelina 1980; Olaussen et al., in prep. OVERLYING UNIT(S): MohnhPlgda Member, Kongssya For- mation UNDERLY~G UNIT@): Flatsalen Formation SUPERIOR UNIT: Svensksya Formation O~EER USE OF NAME: "Sjogrenfjellet Sandstone Member" (Smith et al. 1976): See chapters 3.4.2,3.6.1 THICKNESS: 20-135 m (stratotype) MAIN LITHOLOGIES: Sandstone, mudstone LOWER BOUNDARY DEFINITION: See Svensksya Formation DESCRIPTION: The Sjogrenfjellet Member occurs on Kong Karls Land, Wilhelmraya and in Olav V Land, where it grades laterally into the Teistberget member of the Knorringfjellet Formation

It consists of greenish, fine- to medium-grained sandstone in the lower part, gradmg into fine- to very fine-grained, white sandstones with thin mudstone beds (Fig. 3-58).

The member is interpreted as representing tidal flat, tidal channel and coastal plain deposits.

Hellwaldfjellet Bed (M-49)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CUIIRENT DEFINITION: Here, following PEelina (1980) SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Hellwaldfjellet: A mountain in Olav V Land

Fig. 3-58: Trough cross-beds interpreted as tidal channels in the upper part of the Sjegrenfjel2et Member at Hhfagrehaugen, Kongswa. Photo: G.B. Larssen

TYPE SECTION (FIG. 3-47): Stratotype: Heuwaldfjellet, Olav V Land Hypostratotype: WiJhelmraya DEPOS~ONAL AGE: Pliensbachian DATING METHOD: Microfauna, foraminifera '

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REFERENCE(S) FORAGE: K ~ U ~ O V 1965; PEelina 1980 OVERLYING UNIT(S): Kongssya Formation '' ' L ' '

UNDERLYING UNIT(S): Unnamed SUPERIOR UNIT: Svensksya Formation -R USE OF NAME: None THICKNESS: Up to 6 m MAIN LITEOLOGIES: Shale LOWER BOUNDARY DEFINITION: In the type section, the base consists of a 0.6 m thick multicoloured siderite bed with pebbles of metamorphic basement origin. This bed is absent on Wilhelmarya. DESCRIPTION: The Hellwaldfjellet Bed, a prominent shale bed of Pliensbachian age, is observed on Wilhelmarya and eastern Spitsbergen southward to Kapp Miihry, with its type section (6 m thick) on the eastern slope of Hellwaldfjellet (PEelina 1980).

The main lithology of the bed is greenish-grey mudstone and clayey siltstone with phosphatic nodules and foraminifera, with orange-weathering sandstone intervals in the upper part.

Mohnhegda Member (M-50)

STATUS OF UNIT: Formal FIRST USE OF NAME: Smith et al. 1976 CURRENT DEFINITION: Here, Olaussen et al., in prep. The stratigraphy of Kong Karls Land has been substantially revised as a result of recent investigations. The present definition of the Mohnhergda Member corresponds to the middle part of the "Mohnhnrgda Sandstone Membel' as originally defined, but its use has been geographically extended (see chapters 3.4.2,3.6.1). SYNONYM(S) AND REFERENCE(S): Middle part of "Tumling- odden Member" on Wilhelmsya: Worsley 1973; Middle part of "Tumlingodden Formation" in eastern Svalbard: PEelina 1980 ORIGIN OF NAME: Mohnhragda: A mountain on Svensksya, Kong Karls Land ME SECTION (FIG. 3-57): Stratotype: Sjogrenfjellet W, Kongssya DEPOSITIONAL AGE: Pliensbachian - Toarcian DATING METHOD: Fossils (foraminifera; palynology, etc.) REFERENcE(s) FOR AGE: Smith et d. 1975, 1976; Bjaerke 1977; PEelina 1980; Olaussen et al., in prep.

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OVERLYING UNIT(S): Kongssya Formation UNDERLYING UNIT@): Sjogrenfjellet Member SUPERIOR UNIT: Svensksya Formation O n m ~ USE OF NAME: 'LMOhuh0gda ~andsbtoke ~ k b e r " (Smith et al. 1976): Originally assigned to the entire "Svensksya Formation" on Svenswa, Kong Karls Land. The stratigraphy of Kong Karls Land has been substantially revised as a result of recent investigations (see chapters 3.4.2, 3.6.1).

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DISTRIBUTION SHOWN ON FIG(s).: 3-1 1,3-12 Fig. 3-59: Laminated sandstone with tidal bundles and a truncation STATUS OF UNIT: F o ~

surface in the Mohnhragda Member at Hhfagrehaugen, Kongssya. FIRST USE OF NAME: Smith et d. 1976 photo: G.B. Larssen CURRENT DEFINITION: Here, Olaussen et al., in prep.

The formation was first defined on Kong Karls Land, but THICKNESS: 45-55 m, 51 m in the stratotype is here extended to WilhelmPrya and Olav V Land and used MAIN LITHOLOGIES: SllIldst~ne LOWER BOUNDARY DEFINITION: The lower boundary is defined at the onset of a pure sandstone succession with hummocky cross-beds a l t emhg with massive sandstones as described below. The conformably underlying succession shows m-scale alternations of sandstones and shales. D E S C ~ O N : The Mohnhnrgda Member occurs in Kong Karls Land. It is supposed to attenuate westward and to correlate with a hiatus on Spitsbergen.

The member consists of yellow and white, fine-grained to very fine-grained sandstones that may occasionally be cemented by carbonate. A few mudstone horizons, siderite nodules, and a few thin conglomerate beds are also present. An alternation between pure sandstone beds and heterolithic silt or mudstone and sandstone is typical. In contrast to the underlying unit, hummocky cross-bedded layers with wave ripples alternate with massive sandstones, and the sandstones are dominated by Ophiomoqha trace fossils. The member also displays a more pronounced bedding than the underlying Sjogrenfjellet Member (Fig. 3-59).

The MohnhQgda Member is interpreted as a wave to tidal dominated shoreline or protected bay deposit.

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Fig. 3-60: Hhfagrehaugen on Kongssya, Kong Karls Land, showing the Kongssya Formation (lower, light part), the Agardhfjellet For- mation (overlying dark shales) and the Helvetiafjellet Formation (uppermost cliff). Photo: E.&? Johannessen

Fig. 3-61: Stratigraphic section M-51/52 Stratotype for: Kongsoya Formation, Vrakbukta Bed Locality: Hhfagrehaugen 2 Reference: Larssen et al. 1995 (unpubl.)

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only for the part of the original succession which is lying beneath the marked unconformity between the Kapp Toscana and Advatdalen groups. The stratigraphy of Kong Karls Land has been substantially revised as a result of re- ,cent investigations (see chapters 3.4.2,3.6.1). SYNONYM(B) m REFERENCE(S): Upper part of "Tumling- odden Member: Worsley 1973; Upper part of ''lidingodden Formation": Ptielina 1980 ORIGIN^ OF NAME: Kongsqa (transl. "King's Island"): The middle island of Kong Karls Land TYPE SECTION @G. 3-61): Stratotype: Magrehaugen, Kongssya DEPOSITIONAL AGE: Toarcian - Bathonian DATING METHOD: Fossils (foraminifera; palynology, etc.) REFERENcE(S) FOR AGE: Smith et al. 1975, 1976; Bjaxke 1977; PEelina 1980; Doyle & Kelly 1988; Olaussen et al., in prep.; Lnrfaldli & Nagy 1980; Smelror 1988 OVERLYING UNIT(S): Agardhfjellet Formation UNDERLYING UNIT(S): Svenskraya Formation SUPERIOR UNIT: W~lhelmaya Subgroup OTHER USE OF NAME: "Kongssya Formation" (Smith et al. 1976): Not recognising the major stratigraphic break between the Kapp Toscana and Adventdaien groups, Smith et al. gathered all mid-Jurassic to Hauterivian deposits of Kong Karls Land in their "Kongssya Formation". THICKNESS: 22-24 m (stratotype) MAIN LITHOLOGIES: Sandstone, mudstone, conglomerate b W E R BOUNDARY DEFINITION: The lower boundary defined at the base of a pebbly, glauconite-bearing siderite bed which occurs above the white to yellow sandstones of the MoWgda Member. DESCRIPTION: The unit consists of alternating fine-grained, 'muddy sandstones and greyish-blue mudstones with siderite beds and siderite concretions (up to m-size), belemnite coquina beds and minor conglomerates with pebbles of quartz and siderite. Sedimentary structures are difficult to recognise because of bioturbation. The greyish-blue colour of rusty, large siderite nodules and the common belemnites exposed on the weathering surfaces make the unit appear quite distinctive. The top of the unit is the Brentskardhaugen Bed (see there) (Fig. 3-60).

The formation is interpreted as representing a shallow- marine, inner shelf succession.

Vrakbukta Bed @l-52)

STATUS OF UNIT: F o ~ FIRST USE OF NAME: Here, Olaussen et al., in prep. CURRENT DEFINITION: Here, Olaussen et al., in prep. SYNOM(S) AND REFERENCE(S): None ORIGIN OF NAME: Vrakbukta (transl. "The Wreck Bay"): A bay on the northern coast of Kongssya, Kong Karls Land TYPE SECTION (FIG. 3-61): Stratotype: Hilrfagrehaugen, Kongssya DEPOSITIONAL AGE: Middle Jurassic DATING METHOD: Indirect, stratigraphic relationships REFERENCE(S) FOR AGE: Olaussen et al., in prep. SUPERIOR UNIT: Kongssya Formation ~ E E R USE OF NAME: NON

THICKNESS: Ca. 2 m MAIN LITHOLOGIES: Calcareous sandstone LOWER BOUNDARY DEFINITION: The lower boundary is &all- sitional fiom underlying sandy mudstones. The base is defined at the onset of strongly bioturbated siltstone. DESCRIPTION: The Vrakbukta Bed is an easily recognised marker bed within the Kongssya Formation. It consists of considerably bioturbated carbonate-cemented siltstones to very-fine-grained sandstones in the middle part of the Kongssya Formation. It is rich in belemnites and contains abundant trace fossils of Teichichnus, Rhizocorallium, and Arenicolites. The upper boundary is sharp. The bed is interpreted as representing marine, condensed, inner shelf deposits.

Keisarkampen Member (M-53)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM@) AND REFERENCE@): Upper part of the "Tumlingodden Member" on Wilhelmsya: Worsley 1973; Upper part of the "Tumlingodden Formation" on Wilhelm- sya: PEelina 1980 ORIGIN OF NAME: Keisarkampen (transl. "The Emperor's Top"): A mountain on Wilhelmsya, near Tumlingodden TYPE SECTION (FIG. 3-47): Stratotype: Keisarkampen, Wilhelmarya DEPOSITIONAL AGE: Toarcian : Bathonian

'

DATING METHOD: Indirect, stratigraphic relationships REFERENCE(S) FORAGE: PEelina 1980; m k et d. 1982 OVERLYING UNIT(S): Agardhfjellet Forrhation UNDERLYING UNIT(S): Svenslwya Formation SUPERIOR UNIT: Kongsraya Formation OTHER USE OF NAME: None THICKNESS: 22.5 m (stratotype) MAIN LITHOLOGIES: Calcareous sandstone LOWER BOUNDARY DEFINITION: The base of the member and the overlying 10 m of the strata are not exposed. First recognised lithologies are the well consolidated sandstones described below. Underlying lithologies are greenish-grey mudstones intercalated with orange-weathering sandstones of the Hellwaldfjellet Bed. DESCRIPTION: The Keisarkampen Member represents the Kongsraya Formation on Wilhelmsya.

The member consists of very friable, fine-grained, yellowish-grey sandstones. A cliff 5 m above the supposed base consists of a better consolidated, prominent sandstone showing tabular cross-bedding. The sandstones above this cliff are again poorly consolidated. Several thin black shale beds with associated very thin coal lenses occur within the lower part of the member. Occasional more resistant beds of thin ferruginous sandstone occur, and several yellowish orange horizons with coarse to very coarse sand are seen; pockets of fine quartz and chert pebbles are often found within these coarse layers. Large tree remains are found in the sandstones.

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Brentskardhaugen Bed (M-54)

STATUS OF UNIT: Formal , FIRST USE OF NAME: Parker 1967 1 .

CURRENT DEFINITION: PEelina 1980 SYNONYM(S) AND REFERENCE(S): "Lias conglomerate": k i n 1940 ORIGIN OF NAME: Brentshdhaugen: A hill in the upper part of Adventdalen, central Spitsbergen TYPE SECTION (FIGS. 3-63,344): Stratotype: Drmbreen, eastern Nordenskiold Land Hypostratotype: Tilasberget, Van Keulenfjorden DEPOSITIONAL ACE: ?Bajocian - Bathonian DATING METHOD: Various fossils within reworked phosphatic nodules Fig. 3-62: The conglomeratic Brentskardhaugen Bed with phosphatic REFERENCE(S) FOR AGE: PEelina 1980; Backstr6m & nodules deposited on cross-bedded, grltty sandstones of the Nagy 1985 Knorringfjellet Formation. Type locality at Drnnbreen, central Spits- OVERLYING UNIT@): Marhsgda Bed, Agardhfjellet bergen. Photo: W.K. Dallmann Formation UNDERLYING UNIT@): Unnamed SUPERIOR UNIT: WilhelmPrya Subgroup group, taking into account that its lithology is reminiscent The stratigraphic affiliation of the Brentskardhaugen Bed to of that of the underlying units. either the underlying Wilhelmsya Subgroup (Kapp Toscana OTHER USE OF NAME: Brentskardhaugen Member (PEelina Group; original definition by Parker 1967) or the overlying 1980), rejected name (see Chapter 3.6.1) Janusfjellet Subgroup (Adventdalen Group) is disputed (see THICKNESS: 0.4-4.7 m, 1.4 m in the stratotype below). The bed is here placed in the WilhelmQya Sub- MAIN LITHOLOGIES: Nodular, pebbly calcareous sandstone

LOWER BOUNDARY DEFINITION: The lower boundary is defined at the base of the pebble conglomerate containing phosphatic nodules that occur on top of the sandstone suc-

. . age I lith. &at m

l units c~stvf f mcvcg pcbb

Fig. 3-63: Stratigraphic section M-54a. Stmtotype for: Brentskardhaugen Bed Locality: Drmbreen Reference: Backstrom & Nagy 1985

V ) :

21:

Fig. 3-64: Stratigraphic section M-54b Hypostmtotype for: Brentskardhaugen Bed Locality: Tilasberget Reference: Maher 1989

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cession of the Wilhelmarya Subgroup. Where absent (e.g. Kong Karls Land), the correlated base of other pebble or nodule horizons at the same stratigraphic level is used as the lower boundary. DESCRIPTION: The Brentskardhaugen Bed occurs throughout Svalbard and appears as a prominent marker bed. It is composed of conglomerates and calcareous sandstones with polyrnict pebbles and gravels, phosphate nodules with fossil inclusions, and stratiform ankeritelsiderite intercalations (Fig. 3-62). Toarcian to probably Bajocian fossils in the phosphate concretions of the Brentskardhaugen Bed document a major underlying hiatus, also expressed by the erosive base (Backstrom & Nagy 1985). In many localities, especially in southern and western Spitsbergen, one or several similar phosphatic conglomerates and some possible hiati occur within the upper part of the Wilhelmarya Subgroup which is shown at the herein defined hypostratotype at Tilasberget, Van Keulenfjorden (Worsley 1973; PEelina 1980; Mank et al. 1982; Maher 1989; Krajewski 1992). It must be noted that no age diagnostic fossils have been found in these beds, which makes the time range of hiati more uncertain there.

A different development occurs in Kong Karls Land, where an 80 cm thick silty horizon with siderite nodules occurs (HMargrehaugen; Llafaldli & Nagy 1980).

PEelina (1980) gave a description of the regional development of the Brentskardhaugen Be4 while Backstrom & Nagy (1985) discussed its origin in detail. Other authors described the unit in central Spitsbergen (Frebold 1929; Wienbowski et al. 1981; Maher 1989).

Many authors have regarded the Brentskardhaugen Bed as an integral part of the condensed sedimentary succession of the Wilhelmarya Subgroup (Parker 1967; Worsley 1973; Worsley & Mnnk 1978; PEelina 1980; Mark et al. 1982; Maher 1989; Krajewski 1992). Several authors, however, interpret it as the transgressive basal conglomerate leading to the development of the depositional basin of the Agardh- fjellet Formation, and have therefore formally placed it at the base of the latter within the Adventdalen Group (Birken- majer 1972a, 1975, 1980; Birkenmajer & Pugaczewska 1975; Birkenmajer et al. 1982; Backstrijm & Nagy 1985; Dypvik et al. 1985; Dypvik et al. 1991).

Marhngda Bed (M-55)

STATUS OF UNIT: Formal FIRST USE OF NAME: Backstrom & Nagy 1985 CURRENT DEFINITION: Bbkstriim & Nagy 1985 SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Marhragda: A hill on the southern coast of Isfjorden, central Nordenskiold Land TYPE SECTION (FIG. 3-66): Stratotype: Marbgda, central Nordenskiold Land DEPOSITIONAL AGE: Late Bathonian or early Callovian DATING METHOD: Indirect, stratigraphic relationships REFERENCE(S) FOR AGE: PEelina 1980 OVERLYING UNIT@): Agardhfjellet Formation UNDERLYING UNIT(S): Unnamed SUPERIOR UNIT: Wilhelmarya Subgroup

Fig. 3-65: The Brentskardhaugen Bed with large phosphatic nodules (below the metre stick) and the oolitic M&g& Bed (above the metre- stick), Marbgda, central Spits- bergen. Photo: J. Nagy

. . age I lith. strat. m 11111111111

I units clsivf f mcvcg pcbb

Fig. 3-66: Stratigraphic section M-55 Stmtotype for: Marbgda Bed Locality: Marbgda Reference: Backstrom & Nagy 1985

The Marhragda Bed is closely related to the Brentskard- haugen Bed and belongs to the same superior unit, regardless of the interpretation and formal grouping of the Brent- skardhaugen Bed (see M-54). OTHER USE OF NAME: None THICKNESS: 1.5 m in the stratotype MAIN LITHOLOGIES: Oolitic limestone

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LOWER BOUNDARY DEFINITION: The lower boundary is defined at the base of a mostly oolitic carbonate bed which overlies the Brentskardhaugen Bed. DESCRIPTION: The Marbgda Bed consists of a microsparitic limestone with ooids and glauconite as well as minor amounts of quartz and chert grains (Fig. 3-65). The bed weathers into white, light grey and reddish colours, but fresh surfaces are tight grey. Towards the east ooids may be lacking.

According to Backstrom L Nagy (1985) both the lower and upper boundaries of the Marbgda Bed are transitional. Based on the presence of phosphatic oolites, Kopik & Wierzbowski (1988), Krajewski (1992) and PEelina (1980) also advocate that the Marbgda Bed is genetically associated with the Brentskardhaugen Bed.

REALGRUWWN SUBGROUP (M-56)

STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): Realgrunnen "Group": Worsley et al. 1988. The rank is here revised to subgroup (under Kapp Toscana Group) in order to achieve a correlative group subdivision for Svalbard and the Barents Sea Shelf. ORIGIN OF NAME: Realgrunnen: A fishing bank NW of Smwa, northern Norway TYPE AREA: Block 712115, Hammerfest Basin. Base and top are defined in the cored exploration well 712 115-1. STRUCTURAL SETTING: Barents Sea Shelf (without Svalbard area) DEPOSITIONAL AGE: N~rian - Bajocian OVERLYING UNIT(S): Adventdalen Group UNDERLYING UNIT@): Storfiorden Subgroup SUPERIOR m: Kapp Toscana Group OTHER USE OF NAME: None TIIICKNESS: 400-500 m MAIN LITHOLOGIES: Sandstone, shale, coal DESCRIPTION: The Realgrunnen Subgroup ("Group") was defined in the Hammerfest Basin, but is now applied to all correlated deposits on the southern Barents Sea Shelf. It represents a more complete development than the condensed Wilhelmwa Subgroup of Svalbard.

Pale grey sandstones dominate the subgroup. Shale intervals are most common in the lower parts, where thin coals also occur. The lower boundary in the type area is defined by the basal shales of the Fruholmen Formation, which represent an important transgressive episode that can be traced over major areas of the Arctic. The subgroup is subdivided into four formations. A similar fourfold subdivision also occurs in eastern Svalbard in the Wilhelmsya Sub- group, which from there to the western Spitsbergen gradually becomes more condensed.

Following the initial transgression in the early Norian, deltaic systems developed over the southern parts of the Hammerfest Basin during the remainder of the late Triassic. Coastal marine environments developed during the early Jurassic, grading into a variety of shoreface, barrier and tidal inlet regimes from the Toarcian.

OCCURRENCE: Offshore unit, known from the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: F o ~ FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITLON: Worsley et al. 1988 SYNONYM(S) AND BEFERENCE(S): None O R I G ~ OF NAME: Fruholmen: A lighthouse on a skerry, north of Ingoya, northern Norway TYPE SECTION:

Stratotype: Exploration well 712115-1 Hypostratotype: Exploration well 7120112-1 DEPOSITIONAL AGE: N~r ian- Rhaetian DATING METHOD: Palynology REFERENCE(S) FOR AGE: Little detailed documentation available; first dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT@): Tubbn Formation UNDERLYING UNIT(S): Storfjorden Subgroup SUPERIOR m: Realgrunnen Subgroup OTHER USE OF NAME: None TIIICKNESS: 221 m (stratotype), 198 m (hypostratotype), thickest occurrence known 262 m (exploration well 71201 9-2)

LITHOLOGIES: Shale, sandstone, coal LOWER BOUNDARY D E F ~ O N : The base is defined by a marked increase in gamma ray and neutron porosity logs, but often a more moderate increase in interval transit time and bulk density readings occurs. DESCRIPTION: Basal grey to dark grey shales pass gradually upwards into interbedded mdstones, shales and coals. Sand dominates in the middle of the formation in several wells, while the upper part is more shaley, prompting a threefold subdivision into (in ascending order) the Akkar, Reke and Krabbe members.

There has not yet been observed significant lateral thickness variations. The formation is suggested to be represented by the shaley facies of the lowermost member (Akkar) passing into the sandstone facies of the overlying Tubilen Formation further north in the Hammerfest Basin.

Open marine shales of the Akkar Member pass into coastal and fluvial sandstone dominated successions of the Reke Member. These represent northward fluviodeltaic progradation with a depocentre to the south. As the main deltaic input shifted laierally, most of the central and southem parts of the basin became the site of flood-plain deposition, with more marine environments to the north (Krabbe Member).

Akkar Member (M-58)

STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Akkar: Norwegian for 'squid' TYPE SECTION:

Stratotype: Exploration well 7 12 115-1

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DEPOSTTIONAL AGE: Norim DATING METHOD: Palynology REFERENCE(S) FOR AGE: Little detailed documentation available; first dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT@): Reke Member UNDERLYING UNIT(S): Snadd Formation SUPERIOR UNIT: Realgrunnen Subgroup &'HER USE OF NAME: None THICKNESS: 55 m (stratotype) . MAIN LITHOLOGIES: Shale, sandstone, coal LOWER BOUNDARY DEFINITION: See Fruholmen Formation DESCRIPTION: See Fruholmen Formation

Reke Member (M-59)

STAWS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Reke: Norwegian for 'prawn' or 'shrimp' TYPE SECTION:

Stratotype: Exploration well 712115-1 DEPOSITIONAL AGE: Norian - 7Rhaetian DATING METHOD: Pdyn010gy REFERENCE(S) FOR AGE: Little detailed documentation available; first dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT(S): Krabbe Member UNDERLYING UNIT(S): Akkar Member SUPERIOR UNIT: Realgrunnen Subgroup OTHER USE OF NAME: None THICKNESS: 77 m (stratotype) MAIN LITHOLOGIES: Sandstone LOWER BOUNDARY DEFINITION: The lower boundary is defined by the base of a carbonate horizon, where the separation between density and porosity logs decreases markedly. See Fruholmen Formation. DESCRIPTION: The Reke Member is characterised by a lower, more funnel-shaped gamma ray response than the underlying Akkar Member. See Fruholmen Formation.

Krabbe Member (M-60)

STATUS OF UNIT: Formal FIRST USE OF NAME: W0l'Sley et d. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Krabbe: Norwegian for 'crab' TYPE SECTION: Stratotype: Exploration well 7 12115-1 DEPOSITIONAL AGE: Rhaetian DATING METHOD: PalyIl010gy REFERENCE(S) FOR AGE: Little detailed documentation available; first dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT(S): l b b h Formation UNDERLYING UNIT(S): Reke Member

SUPERIOR UNIT: Realgrunnen Subgroup OTHER USE OF NAME: None THICKNESS: 87 m (stratotype) MAIN LITHOLOGIES: Shale LOWER BOUNDARY DEFIMTION: The lower bounday of the Krabbe Member is characterised by an increasing separation between density and porosity logs. DESCRIPTION: The member shows funnel-shaped gamma ray responses. See Fruholmen Formation.

OCCURRENCE: Offshore unit, known from the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None O W G ~ OF NAME: lbbbn: A fishing bank off the northern point of Smoya, northern Norway TYPE SECTION: Stratotype: Exploration well 712115-1 Hypostratotype: Exploration well 7120112- 1 DEPOSITIONAL AGE: Late Rhaetian - early Hettangian, locally into Sinernurian DATING METHOD: PdJTl010g~ REFERENCE(S) FOR AGE: Little detailed documentation available; first dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT(S): Nordmela Formation UNDERLYING UNIT(S): Fruholmen Formation SUPEREOR UNIT: Real&nmnea Subgroup OTHER USE OF mm: None THICKNESS: 65 m (stratotype), 87 m (hypostratotype), thickest known OC(:urrrnce ea. 150 m (Askeladden area, blocks 7120/7 and 8) MAIN LITHOLOGIIES: Shale, sandstone, coal LOWER B O ~ Y D E ~ T I O N : The base is defined on gamma ray logs at the fmt sifl~cant sand bed with blocky to bell-shaped response patterns above the more irregular high responses of the underlying unit. There is also a marked change in the separation pattern between the neutron porosity and bulk density logs. DESCRIPTION: The formation is dominated by sandstones with subordinate shales and minor coals. Coals are most abundant near the southeastern basinal margins, and die out to the northwest. The formation has a general threefold development, with a lower and upper sand-rich unit separated by a more shaley interval.

The shale content increases towards the northwest where the TubHen Formation may interfinger with a lateral shale equivalent.

The sandstones of the lbbbn Formation are thought to represent a stacked series of high energy marginal marine deposits (tidal inlet and/or estuarine). Marine shales reflect more distal environments to the northwest, while coals and shales to the southeast were deposited in protected back- barrier lagoonal environments.

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OCCURRENCE: Offshore unit, known from the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: Formal FIRST USE OF NAME: Olaussen et al. 1984a CURRENT DEFINITION: W0r~ley et d. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Nordmela: A small community on the western coast of Andraya, northern Norway TYPE SECTION:

Stratotype: Exploration well 712115-1 Hypostratotype: Exploration well 71 19/12-2 DEPOSITIONAL AGE: Sinemurian - late Pliensbachian, the top possibly younging eastward into the Toarcian DATING METHOD: Palyn~logy REFERENCE(S) FOR AGE: Little detailed documentation available; first dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT(S): Sta Formation UNDERLYING UNIT(S): Thb&en Formation SUPERIOR UNIT: Realgrunnen Subgroup OTHER USE OF NAME: None THICKNESS: 62 m (stratotype), 202 m (hypostratotype) MAIN LITHOLOGLES: Siltstone, sandstone, shale LOWER BOUNDARY DEFINITION: The base is defined by a sharp increase in gamma ray response to high, irregular, patterns in contrast to the cylindrical, blocky to bell-shaped pattern of the underlying unit. This change is accompanied by an increase in bulk density values. DESCRIPTION: c e Nordmela Formation consists of interbedded siltstones, sandstones, shales and mudstones with minor coals. Sandstones become more common towards the top.

The formation seems to form a southwestward or westward thickening wedge, in marked contrast to the underlying Tubhen Formation. It may be diachronous, younging eastward.

The formation was deposited in tidal flat to flood-plain environments. Individual sandstone successions represent estuarine and tidal channels.

OCCURRENCE: Offshore unit, known fiom the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: Formal FIRST USE OF NAME: Olaussen et al. 1984a CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Sta: A small community on the northern coast of Langqa, northern Norway TYPE SECTION:

Stratotype: Exploration well 712115-1 Hypostratotype: Exploration well 71 19112-2 DEPOSITIONAL AGE: Late Pliensbachian to Bajocian DATING METHOD: Palyn~logy REFERENCE(S) FOR AGE: Little detailed documentation available; first dated by Worsley et al. (1988) on the basis of

proprietary oil company data. OVERLYING IJNIT(S): Fuglen Formation UNDERLYING UNIT(S): Nordmela Formation SUPERIOR umT: Realgrunnen Subgroup OTHER USE OF NAME: None THICKNESS: 77 m (stratotype), 145 m (hypostratotype) MAIN LITHOLOGIES: Sandstone, shale, siltstone LOWER BOUNDARY DEFINITION: The base is defined by the sharp transition fiom the regular and serrated gamma ray patterns of the underlying unit to the blocky to smooth cylindrical patterns of the St0 Formation. Density values decrease upwards over the boundary, but the change is gradual. DESCRIPTION: The Sts Formation consists particularly of moderately to well-sorted and mineralogically mature sandstones. Thin units of shale and siltstone are clear markers; phosphatic lag conglomerates occur in some wells, especially in the upper parts of the unit.

The formation thins generally eastwards in consistence with the underlying Nordmela Formation. The unit may be subdivided into three depositional units with bases defined by transgressive episodes. The basal unit is only present in the western parts of the Hammerfest Basin. The middle (late Toarcian - Aalenian) unit represents maximum transgression in the area. The uppermost (Bajocian) unit is highly variable owing to syndepositional uplift and winnowing and to later differential erosion.

The sands in the formation were deposited in prograding coastal regimes, and a variety of linear clastic coast lithofacies are represented. Marked shalelsiltstone intervals represent regional transgressive pulses in the late Toarcian and late Aalenian.

3.5.3 Adventdalen Group

ADVENTDALEN GROUP (M-64)

Group 1

STATUS OF UNIT: Formal FIRST USE OF NAME: Parker 1967 CURRENT DEFINITION: Parker 1967; extended to Kong Karls Land by Smith et al. 1976; here extended to comprise coeval deposits on the Barents Sea Shelf SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Adventdalen: A major valley in central Spitsbergen TYPE AREA: Central Spitsbergen STRUCTURAL SETTING: Barents Sea Shelf (including Sval- bard)

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DEPOSITIONAL AGE: Late Jurassic - Early Cretaceous OVERLYING UNIT@): Van Mijenfjorden Group (Svalbard), Nygrunnen Group (Barents Sea Shelf) UNDERLYING UNIT(S): Kapp Toscana Group SUPERIOR UNIT: None OTHER USE OF NAME: None THICKNESS: Thickness on Svalbard: ca. 750-1600 m, known thickness on Barents Sea Shelf ca. 1000-1750 m MAIN LITHOLOGIES: Shale, siltstone, sandstone DESCRIPTION: The Adventdalen Group comprises shales, siltstones and sandstones of Late ~ur&sic ~ a r l ~ Creta- ceous age in Svalbard and throughout the Barents Sea Shelf

3. MESOZOIC LITHOSTRATfc04PHY

.,? ..... =- m-. i . 1 5 / '.* G

(Figs. 3-67,3-68, 3-69). Fig. 3-67: JanwtJeh tral Spltsbergen, exposing the dark, shale- The group is widely exposed along the margins of the dominated lithologies of the Janusfjellet Subgroup in the lower part.

Central Tertiary Basin on Spitsbergen, as well as in eastern The Janusfjellet Subgroup is upwards succeeded by the Helvetia- Spitsbergen (Sabine Land) and on Kong Karls Land. It con- tjellet Formation (starting with the light band assigned to the Fest- tinues across the Barents Sea Shelf to the Bjanneland Plat- ningen sandstone member) and the Carolinefjellet Formation. The form, around the Loppa High and into the Hammerfest and cliff at the summit represents the basal Tertiary layers (Fikanten Nordkapp basins (Fig. 1-02). Formation). Photo: J. Nagy

The group is dominated by dark marine mudstones, but includes also deltaic and shelf sandstones as well as thin, condensed carbonate beds. Important hydrocarbon source OVERLYING m~(s)t -Helvetiafjellet and Klippfisk forma- rocks occur in the Upper Jurassic succession, both in Sval- tions bard and in the Barents Sea (Agardhfjellet, Fuglen and UNDERL.YING IJNIT(S): Kapp Toscana Group Hekkingen formations). A Barremian sandstone unit, SUPERIORUNIT: A d v M e n Group (Helvetiafjellet Formation) in Svalbard is the result of local OTHER USE OF NAME: None uplift and deltaic progradation, while a coeval, condensed THICKNE~ Ca. 750 m in Smbpp Land, 550-700 m on limestone interval in the Barents Sea (Klippfisk Formation) western S p i t s m 280420 m on eastern Spitsbergen grades into marls and calcareous mudstones in the basins. A (418 m in the stmtotype) hiatus occurs around the Jurassic - Cretaceous boundary. MAIN LITHOLOGIES: Shrtle, sirmme, sandaone

The Adventdalen Group was eroded down to varying lev- DESCRIPTION: The Jgnwdjellet Subpup is defmed in the els during the late Cretaceous uplift. On the southern Svalbard area, where it matiruty camist% of ~ o n s black Barents Sea Shelf, this hiatus comprises only the Cenoman- shales and silsstones that pess hito sar&tones uppermost in ian and part of the 'honian, while the entire Upper Creta- the unit (Fig. 3-67). ceous is lacking on Svalbard. The subgroup comprises the ellet et and Rurik-

fjellet formations. A common name for these two formations is appropriate, beoause; +he &sh&on is difficult or

JANUSFJELLET SUBGROUP (M-65) impossible in many tmtormised meas on western Spits- bergen, while the s u b ~ u p is an easily mappable unit. For this reason, it hm o h bean m m to as the Janusfjellet "Formationy' in pmvio~19 geolagieal literature. The subgroup is of marine shelf origin.

A G ~ R D ~ U B T PO-ON (Md6)

STATUS OF UNIT: Formal FIRST USE OF NAME: Parker 1967 CURRENT DEFINITION: wvik al. 1991 SYNONYM@) AND R E ~ C E ( S ) : None ORIGIN OF NAME: Jmusfjellet: A mountain in a d e m Nordenskiald Land TYPE SECTIUN (FIG, 3-70): Agardhfjellet, Sabine Land DISTRIBUTION SHOWN ON FIG@).: 3-06, 3-07, 3-08, 3-09, STRUCTURAL SETTING: Barents Sea Shelf (including Sval- 3-10, 3-11, 3-12 (partly within 'Janusfjellet Subgroup, un- bard) differentiate&) DEP~SITIONAL AGE: Late Jurassic - Early Barremian STATUS OF UNIT: Fcmnl

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-

Fig. 3-68: The Agardhfjellet Formation at Janusfjellet, central Spits- bergen, show~ng dark paper shales \nth intercalated sidenhc horizons and lenses. Photo: J. Nagy

FIRST USE OF NAME: Parker 1967 CURRENT DEFINITION: Parker 1967 SYNONYM(S) AND REFEWNCE(S): "Aucellenschichten": Nathorst 19 10 ORIGW OF NAME: Agardhijellet: A mountain in Sabine Land, Agardhbukta TYPE SECTION (FIGS. 3-7q3-71): Stratotype: AgardhtJellet, eastern Sabine Land Hypostratotype: Oppdalss&ta, western Sabine Land DEPOSITIONAL AGE: Late Jurassic DATING METEODS AND REFERENCE(S) FOR AGE: Macro- fossils (e.g. ammonites): Frebold 1928; Rbiycki 1959; Parker 1967; Birkenmajer & Pugaczewska 1975; PEelina 1980; Birkenmajer et al. 1982; Er Swa 1983; Birkenmajer & Wierzbowski 199 1. Foraminifera: Lsfaldli & Nagy 1980; Nagy et al. 1988,1990. Palynology: Lsfaldli & Thusu 1976; Bjaerke 1978 OVERLYING UNIT@): Rmlkfjellet Formation UNDERLYING UNIT(S): Wilhelm~lya Subgroup SUPERIOR UNIT: Janusfjellet Subgroup OTHER USE OF NAME: None THICKNESS: 90-350 m, 242 m in the stratotype

Fig. 3-70: Stratigraphic section M-65166a176a Strutotype for: Janusfjellet Subgroup, Agardhfjellet and Rurikfjellet

Fig. 369: Black paper shales of the Agardhfjellet Formation with a Formations huge carbonate concretion, Heimfjella, Wedel Jarlsberg Land. Locality: Agardhfjellet Photo: W.K. Dallmann Reference: Parker 1967, wth additional data from Nagy et al. 1990

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". MESOZOIC LITHOSTRATIGRAPHY

TMAIN LITHOLOGIES: Black shale, siltstone LOWER BOUNDARY DEFINITION: The lower boundary is defined at the boundary between the underlying oolitic Mar- bgda Bed or, where absent, the nodular Brentskardhaugen Be4 and an overlying fining-upward succession of poorly sorted sandstones and siltstones. DESCRIPTION: A fining upwards succession of poorly sorted, clay-rich fine-grained sandstone grades upward into the sand- and siltstone-dominated basal part of the Agardh- fjellet Formation. PEelina (1980) suggested a Bathonian hiatus at the forrnational base above the Marbgda Bed. The dominant lithology of the remaining part of the Agardh- fjellet Formation is dark grey or black shale with siltstone interbeds (Fig. 3-68, 3-76). Based on the alternation between siltstone and paper shale dominance, four members have been defined in central Spitsbergen (Oppdalen, Lardyijellet, Oppdalsstita and Slottsrmaya members; Dypvik et al. 1991). An earlier subdivision by R6iycki (1959; Inge- brigtsenbukta member and lower part of Tirolarpasset member) is only applicable in southwestern Spitsbergen.

Abundant faunas of belemnites, ammonites and bivalves are found throughout the Agardhfjellet Formation. The black shales are thought to represent alternating oxic and anoxic bottom conditions (Dypvik 1980, 1985); they commonly show red or white stained coating caused by secondary precipitation of jarosite and gypsum. Msrk & Bjorray (1984) indicate a vitrinite reflectance in the Agardhfjellet Formation at Myklegardfjellet between 0.6 % and 0.8 %.

Mainly because of the lack of a clear boundary relationships in tectonised areas in southern and southwestern Spitsbergen, the upper boundary is hard or impossible to recognise. The Agardhfjellet Formation commonly accom- modates major thrust faults of Tertiary age in western Spits- bergen, where stratigraphic control is therefore severely hampered. The formation was deposited in open marine shelf environments with periodic restricted water circulation.

Ingebrigtsenbukta member (M-67)

STATUS OF UNIT: Informal FIRST USE OF NAME: R6iycki 1959 CURRENT DEFINITION: R6iycki 1959 SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Ingebrigtsenbukta: A bay on the southern coast of Van Keulenfjorden TYPE SECTION:

Stratotype: Ingebrigtsenbukta, Van Keulenfjorden Hypostratotype: Jurakammen, Torell Land DEPOSITIONAL AGE: Callovian - Kimmeridgian DATING METHOD: Macrofossils (ammonites) REFERENCE(S) FOR AGE: R6iycki 1959; see also Agardh- fjellet Formation OVERLYING UNIT@): Tirolarpasset member UNDERLYING UNIT@): Wilhelmplya Subgroup SUPERIOR UNIT: Agardhfjellet Formation OFHER USE OF NAME: None THICKNESS: 110-150 m MAIN LITHOLOGIES: Black shale

LOWER BOUNDARY DEFINITION: See Agardhfjellet Forma- tion DESCRIPTION: The Ingebrigtsenbukta member is recognised in the area to the south of Van Keulenfjorden (R6iycki 1959). The unit is 150 m thick at Jurakammen and Polakk- fjellet, decreasing to 110 m at Homund (Birkenmajer 1975), however thickness estimates are uncertain due to tectonic deformation.

The member consists mainly of black argillaceous bituminous, oft+ silty shales (sometimes siltstones) with abundant fine muscovite flakes. Intercalations of black or black- blue clay-ironstone or siderite beds, 10-15 cm thick, occur in the shales at intervals from a few to a dozen or so metres. In the lowermost 10-15 m thick part of the member, the clay-ironstone intercalations are more frequent, rich in iron, and weather red or rusg red. Ferrigenous oolites may occur in the lowermost part of the member, just above the Brentskardhaugen Bed. At higher levels the amount of iron decreases and the clay-ironstone intercalations and lenses (up to several metres in diameter and up to 40 cm thlck) weather yellow. The member was deposited in marine shelf environments.

The unit is mostly disturbed by Tertiary deformation ham- pering good stratigraphic control, and its relations to areas outside Wedel Jarlsberg Land and Torell Land are thus not clear. The unit is, therefore, restricted to an informal status until further data permit a formal member subdivision of the Agardhfjellet Formation on western Spitsbergen.

Tirolarpasset member (M-68)

STATUS OF UNIT: Informal FIRST USE OF NAME: R6iycki 1959 , . . CURRENT DEFINITION: Rbiycki 1959 SYN0NYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Tirolarpasset: A mountain pass in Torell Land TYPE SECTION:

Stratotype: Tirolarpasset, Torell Land Hypostratotype: Jwakammen, Tore11 Land DEPOSITIONAL AGE: Volgian - Valanginian DATING METHOD: Macrofossils (ammonites) REFERENCE@) FOR AGE: R6iycki 1959; see also Agardh- fjellet Formation OVERLYING UNIT@): Ullaberget Member UNDERLYING UNIT@): Ingebrigtsenbukta member SUPERIOR UNIT: Janusfjellet Subgroup OTHER USE OF NAME: None THICKNESS: 28 (stratotype) - 60 m MAIN LITHOLOGIES: Shale LOWER BOUNDARY DEFINITION: In central Torell Land the Polakkfjellet Bed forms the base of the member. Not well- defined elsewhere. DESCRIPTION: The Tirolarpasset member was introduced by R6iycki (1959) in the area around Tirolarpasset, Torell Land, without a type section being designated. It constitutes the middle part of the Janusfjellet Subgroup, embracing parts of the Agardhfjellet and Runkfjellet formations. The unit was further applied by Birkenmajer (1975) in Torell

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Land. It is reported to be 28 m thick at Polakkfjellet and 60 m at Hornsund, but the thicknesses are uncertain because of the intensive deformation.

The member consists of black, argillaceous, often bituminous, sometimes silty shale, usually splitting into very thin plates (paper shales). Dark-grey or grey-bluish clay-ironstone or siderite-dolomite intercalations, 5-20 cm thick, red or yellow if weathered, occur at intervals of from a few to tens of metres in the lower part. In the upper part of the member 0.5-1 cm thick intercalations of black micaceous siltstones with worm trails, and scattered, black ovoidal and spheroidal clay-ironstones and phosphorite nodules, 1-3 cm in diameter, occur. The member was deposited in marine shelf environments.

The unit is commonly disturbed by Tertiary deformation obscuring the stratigraphic context, and the relations to areas outside Torell Land are not clear. The Jurassic-Creta- ceous boundary is widely recognised elsewhere on the Barents Sea Shelf, and the apparent lack of this boundary in Torell Land may be due to tectonism. The unit is restricted to an informal status until further data permit a formal member subdivision of the Agardhfjellet Formation in western Spitsbergen.

Polabkfjellet Bed (M-69)

STATUS OF UNIT: Formal FIRST USE OF NAME: Birkenmajer 1975 CURRENT D E ~ T I O N : Birkenmajer 1975 SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Tirolarpasset: A mountain pass in Torell Land TYPE SECTION:

Stratotype: Polakkfjellet NE, Torell Land Hypostratotype: Jurakam'men, Torell Land DEPOSITIONAL AGE: Early Volgian DATING METHOD: Macrofossils (ammonites) REFERENCE(S) FOR AGE: R6iycki 1959 UNDERLY~G UNIT@): Ingebrigtsenbukta member SUPERIOR UNIT: Agardhfjellet Formation, Tirolarpasset member, mrn~ USE OF NAME: None THICKNESS: 5 m at Polakkfjellet (stratotype), 47 m at Jura- kammen (hypostratotype) MAIN LITHOLOGTES: Sandstone LOWER BOUNDARY DEFINITION: The base is defined by the onset of orange-yellow weathering sandstones above a monotonous succession of black shales (Ingebrigtsenbukta member). DESCRIPTION: The Polakkfjellet Bed seems to be restricted to Torell Land and Wedel Jarlsberg Land. In the type section sideritic, medium- or coarse-grained sandstone, intensely yellow or orange-yellow if weathered, forms a marker horizon which is clearly visible h m a distance. The lower boundary in the type section is sharp against the underlying black arenaceous or argillaceous shales. Individual sandstone beds (0.3-0.5 m thick) are separated by thin black shales. Shaley clay-ironstone concretions (5-10 cm in diameter) are orange-yellow or reddish-yellow if weathered

and occur in the upper parts of some of these sandstones. A few pebble conglomerate intercalations occur within the sandstones, consisting of black, blue or whitish quartz pebbles and of bluish ?Permian chert. In the hypostratotype at Jurakammen the bed is developed as a conglomerate consisting of yellow-weathering femgenous sandstone with quartz pebbles.

The Polakkfjellet Bed should not be confused with other, more local, sandstone or siltstone horizons with a similar appearance in the Agardhfjellet Formation, e.g. the "Heim- fjella beds" with an older ammonite fauna (Dallmann et al. 1990).

Oppdalen Member (M-70) ,

STATUS OF UNIT: Formal FIRST USE OF NAME: Dypvik et al. 1991 CURRENT DEFINITION: Dypvik et al. 1991; here used excluding the Brentskardhaugen and Marhsgda beds (see these) SYNONYM@) AND REFERENCE(S): "Drsnbreen Bed" (Dypvik et al. 1991): The main part of the Oppdalen Member according to Dypvik et al. (1991), synonymous according to the present definition without the Brentskardhaugen and Marhagda beds. ORIGIN OF NAME: Oppdalen (uncertain origin, either "The Upward Leading Valley", the "High Valley", or from a synonymous place in middle Norway): A small valley in westem Sabine Land TYPE SECTION (FIG. 3-71): Stratotype: OppdalssAta, western Sabine Land DEPOSITIONAL AGE: ?Bathonian - Cd0vian DATING METHODS AM) REFERENCE@) FORAGE: See Agardh- fjellet Formation OVERLYING UNIT(S): Lardyfjellet Member UNDERLYING UNIT@): Wilhehqa Subgroup SUPERIOR UNIT: Agardhfjellet Formation OTHER USE OF NAME: None THICKNESS: 10-60 m, 13 m in the stratotype MAIN LITHOLOGIES: Shale, siltstone, sandstone LOWER BOUMIWY DEFIMTION: The lower boundary is defined at the boundary between the underlying oolitic Marhsgda Bed or, where absent, the nodular Brentskard- haugen Bed, and an overlying fining-upward succession of poorly sorted sandstones and siltstones. The boundary coincides with the lower boundary of the Agardhfjellet Forma- tion. DESCRIPTION: The Oppdalen Member is recognised on central and eastern Spitsbergen.

The member starts above the oolitic Marhergda Bed with a fining-upward succession of poorly sorted, clay-rich fine- grained sandstones and siltstones with up to 30 cm thick beds of siderite. Sedimentary structures are obliterated by bioturbation. In central Spitsbergen the unit thins eastwards. The sideritic beds of the Oppdalen Member are rich in arn- monites, belemnites and bivalves (Buchia). The member was deposited in shallow marine environments.

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". MESOZOIC LITHOSTRATIGRAPHY

Lardyfjellet Member (M-71) RurikfjeUet Formation

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STATUS OF UNIT: Formal FIRST USE OF NAME: Dypvik et al. 1991 CURRENT DEFINITION: Dypvik et al. 1991 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Lardyfjellet: A mountain in northern Heer Land TYPE SECTION (FIG. 3-72): Stratotype: Lardyfjellet, northern Heer Land DEPOSITIONAL AGE: Late Jurassic DATING METHODS AND REFERENCE@) FOR AGE: See Agardh- fjellet Formation OVERLYING IJNIT(S): OppdalssAta Member UNDERLYING UNIT@): Oppdalen Member SUPERIOR UNIT: Agardhfjellet Formation OTHER USE OF NAME: None THICKNESS: 35-80 m, 40 m in the stratotype MAIN LITHOLOGIES: Black shale LOWER BOUNDARY DEFINITION: The lower b0Ulldary is defined at the onset of black shales above the basal sand- and siltstones of the Agardhfjellet Formation. DESCRIPTION: The Lardyfjellet Member is recognised on central and eastern Spitsbergen.

It consists of dark-grey to black paper shales with common dolomitic concretionary beds. The member has a high content of organic material. The unit shows higher gamma activity and uranium enrichment compared with the overlying units. The Lardyfjellet Member is moderately rich in ammonites, belernnites and bivalves (Buch'ia). The member was deposited in open marine shelf environments.

OppdalssAta Member (M-72)

STATUS OF UNIT: Formal FIRST USE OF NAME: Dypvik et al. 1991 CURRENT DEFINITION: Dypvik et al. 1991 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: OppdalssAta (transl. "The Haystack of Oppdalen"): A mountain in western Sabine Land TYPE SECTION @G. 3-71): Stratotype: Oppdalssiita, western Sabine Land DEPOS~~ONAL AGE: Late Jurassic DATING METHODS AND REFERENCE(S) FOR AGE: See Agardh- fjellet Formation OVERLYING UNIT@): Slottsmya Member UNDERLYING UNIT(S): Lardyfjellet Member SUPERIOR UNIT: Agardhtjellet Formation OTKER USE OF NAME: None THICKNESS: 10-40 m, 28 m in the stratotype MAIN LITHOLOGIES: Siltstone, sandstone LOWER BOUNDARY DEFINITION: The lower boundary is defined at the first sandstone bed above the shaley Lardyfjellet Member. DESCRIPTION: The OppdalssAta Member is recognised on central and eastern Spitsbergen.

The member is characterised by silty and sandy lithologies showing a variable development. It consists of several minor coarsening-upward successions (a few metres to ca.

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Fig. 3-71: Stratigraphic section M-66bl70172 Shntotype for: Oppdalen and Oppdalsdta members Hyposhnto~e for: Agardhfjellet Formation Locality: Oppdalsdta Refirence: Dypvik et al. 1991

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h. B: Brentskardhaugen Bed Ma. B: Marhsgda Bed My. B: Myklegardfpllet Bed

RuMjl let Formation

Fig. 3-72: Stratigraphic section M-71 Strutotype for: Lardyfjellet Member Locality: Lardyfjellet Reference: Dypvik et al. 1991

10 m thick); their number and thickness vary throughout the exposure area. Three of these successions are present in the type section. The siltstones and sandstones are strongly bioturbated and contain rich assemblages of bivalves, ammonites and belemnites. The member was deposited in open marine shelf environments.

Slottsmaya Member (M-73)

STATUS OF UNIT: Formal FIRST USE OF NAME: Dypvik et d. 1991 CURRENT DEFINITION: Dypvik et al. 199 1 SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Slot t swa (transl. 'The Palace Maid" or "The Castle Maid"): A mountain top in western Sabine Land TYPE SECTION (FIG. 3-73): Stratotype: Slottsrmaya, western Sabine Land DEPOSITIONAL AGE: Late Jurassic DATING METHODS AND REFERENCE(S) FOR AGE: See Agardh- fjellet Formation OVERLYING UNIT(S): Wimanfjellet Member, Rurikfjellet Formation UNDERLYING UNIT@): OppdalssAta Member SUPERIOR UNIT: Agardhtjellet Formation OTHER USE OF NAME: None THICKNESS: 70-100 m, 84 m in the stratotype MAIN LITHOLOGIES: Black shale LOWER BOUNDARY DEFINITION: The lower boundary is defined at the renewed onset of black shales above the silt- and sandstones of the OppdalssAta Member. DESCRIPTION: The Slottsmaya Member is recognised on central and eastern Spitsbergen.

The member consists of dark grey shales with local occurrences of black paper shales containing red to yellowish siderite concretions as well as siderite and dolomite interbeds. The top of the member forms a coarsening-upward shale-silt-sandstone succession which is often rich in ammonites (Dorsoplanites) and bivalves, but also contains some belemnites and plesiosaurian bones. Fossils are mainly confined to the silty beds. The member was deposited in open marine shelf environments.

Biinsowbukta Member (M-74)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here, Olaussen et al., in prep. CURRENT DEFINITION: Here, Olaussen et al., in prep. SYNOM(S) AND REFERENCE(S): The Biinsowbukta and Hegsletta members form the middle parts of the "Kongsqa Formation" according to Smith et al. (1976). ORIGIN OF NAME: Biinsowbukta: A bay on the northern coast of Kongssya, Kong Karls Land TYPE SECTION (FIG. 3-74): Stratotype: Hiirfagrehaugen, Kongsqa DEPOSITIONAL AGE: Late Jurassic DATING METHOD: Ammonites, palynology

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a g e m lrlllll1l11 clsivf f mcvcg pcbb

Fig. 3-73: Stratigraphic section M-73 Shatotype for: Slottsmraya Member Locality: Slottsmraya Reference: Dypvik et al 1 0 0 1

(Barremian)

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Fig. 3-7rl: Stratigraphic section M-74/75 Shatotype for: Biinsowbukta and Hsgsletta members Locali~: HMagrehaugen 3 Reprace: Larssen et al. 1995 (uopubL)

REFERENCE(S) FOR AGE: Smith et al. 1976; Bjaerke 1977; Smelror 1988 OVERLYING UNIT(S): Hagsletta Member UNDERLYING UNIT(S): Kongssya Formation SUPERIOR UNIT: Agardhfjellet Formation OTHER USE OF NAME: None THICKNESS: 21 m in the stratotype MAIN LITHOLOGIES: Mudstone LOWER BOUNDARY DEFINITION: The lower boundary is defined at the onset of mudstones above the Brentskardhaugen Bed. DESCRIPTION: The Biinsowbukta Member is recognised in Kong Karls Land, where it reflects the lower, organic-lean part of a very thin development of the Janusfjellet Sub- group. It consists of grey to dark grey mudstones with siderite concretions. Ammonites, bivalves and belemnites are common. An inner shelf facies with variably oxygenated sea bottom conditions is suggested for this member.

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Hegsletta Member (M-75)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here, Olaussen et al., in prep. I

m CURRENT DEFINITION: Here, Olaussen et al., in prep. m

SYNONYM(S) AND RE~RENCE(S): The Biinsowbukta and 11 =

Hragsletta members form the middle parts of the "Kongssya I$+ m Formation" according to Smith et al. (1976). 116

ORIGIN OF NAME: Hragsletta (transl. "The Plateau"): A plateau on Kongssya, Kong Karls Land TYPE SECTION @G. 3-74): Stratotype: Hikfagrehaugen, Kongslaya DEPOSITIONAL AGE: Late Jurassic DATING METHOD: Ammonites, palynology REFERENCE(S) FOR AGE: Smith et al. 1976; Bjaerke 1977; Smelror 1988 O V E R L Y ~ G UNIT(S): Tordenskjoldberget Member, Klipp- fisk Formation UNDERLYING UNIT(S): Biinsowbukta Member SUPERIOR UNIT: Agardhfjellet Formation OTHER USE OF NAME: None THICKNESS: 20 m in the stratotype, variable MAIN LITHOLOGIES: Black mudstone LOWER BOUNDARY DEFINPTION: The lower boundary is defined by the transition from silly, grey to black, organic-rich mudstone, which correlates with the top of a limestone bed at HWagrehaugen. DESCRIPTION: The Hsgsletta Member is recognised in Kong Karls Land, where it reflects the upper, black mudstone part of a very thin development of the Janusfjellet Subgroup. The unit shows. variable thickness as the overlying fluvial sandstones are eroded down to varying levels.

The lower part of the member is organic-lean, while the upper part is rich in organic material and may form an ex- cellent hydrocarbon source rock. The member was deposited in restricted shelf environments.

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DISTRIBUTION SHOWN ON FIG@).: 3-06, 3-07, 3-08, 3-09, 3-10,3-11, 3-12 (partly within 'Janusfjellet Subgroup, undifferentiated') Fig. 3-75: Stratigraphic section M-76b/77 STATUS OF UMT: Formal Hypostmtofype for: Rurikfjellet Member FIRST USE OF NAME: Parker 1967 Shatofypefor: Wimantjellet Member CURRENT D E ~ T I O N : Parker 1967 Locality: Wimanfjellet SYN0NYM(S) AND REFERENCE(S): None Reference: Dypvik et al. 1991

ORIGIN OF NAME: Rurikfjellet: A mountain in Heer Land, Agardhbukta

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TYPE SECTION (FIGS. 3-70,3-75): Stratotype: Agardhfjellet, eastern Sabine Land Hypostratotype: Wimanfjellet, northern Nordenskiold Land DEPOSITIONAL AGE: Berriasian - early Barremian DATING METHODS AND REFERENcE(s) FOR AGE: Macro- fossils (e.g. ammonites): Frebold 1928; R6iycki 1959; Parker 1967; Birkenmajer & Pugaczewska 1975; PEelina 1980. Foraminifera: Nagy et al. 1988, 1990. Palynology: Lsfaldli & Thusu 1976; Bjrerke 1978; Gmsfjeld 1992. OVERLYING UNIT@): Helvetiafjellet Formation UNDERLYING um~(s): Agardhfjellet Formation SUPERIOR UNIT: Janusfjellet Subgroup OTHER USE OF NAME: None THICKNESS: 110-400 m, 176 m in the stratotype MAIN LITHOLOGIES: Dark shale, siltstone, sandstone LOWER BOUNDARY DEFINITION: The lower boundary is defined at a sharp contact between underlying shaleslsilt- stones and overlying shale with nodules. Where present, the boundary is defined by the base of the plastic clays of the Myklegardfjellet Bed. There is a distinct break in slope at the boundary, and exposures of the unit show different geo- morphologic features - e.g. guhes that have developed in the underlying Agardhfjellet Formation do not continue up into the Runkfjellet Formation.

Mainly because of the lack of a clear boundary relationship in tectonised areas of southern and southwestern Spits- bergen, the lower boundary is hard to recognise. DESCRIPTION: The dominant lithology is dark shale with clay-ironstone and siltstone nodules, coarsening upward to siltstones and sandstones. Dypvik et al. (1991) subdivided the formation into the Wmadjellet and Ullaberget members, the latter representing the upper coarsening-upwards part of the formation.

The Rurikfjellet Formation is an overall regressive succession deposited under oxic conditions (Dypvik 1980, 1985). It is overlain by the conspicuous coarse-grained sandstones of the Festningen Member (Helvetiafjellet For- mation). Bjorsy & Vigran (1979) reported the organic maturity in terms of vitrinite reflectance to be about 0.8 % in the Runkfjellet Formation at Myklegardfjellet. The member was deposited in open marine shelf environments.

W i a n f j e l l e t Member (M-77)

STATUS OF UNIT: Formal FIRST USE OF NAME: Dypvik et al. 1991 CURRENT DEFINITION: Dypvik et al. 199 1 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Wimanfjellet: A mountain in northern Nordenskiiild Land TYPE SECTION (FIG. 3-75): Stratotype: W i e l l e t , northern Nordenskiold Land DEPOSITIONAL AGE: Berriasian - Valanginian DATING METHODS AND REFERENCE(S) FOR AGE: See Rurik- fjellet Formation OVERLYING UNIT@): Ullaberget Member UNDERLYING UNIT(S): Slottsmciya Member SUPERIOR umT: R-ellet Formation OTHER USE OF NAME: None

THICKNESS: 180 m in the stratotype, variable MAIN LITHOLOGIES: Shale LOWER BOUNDARY DEFINITION: The lower boundary is defined at the base of the Myklegardfjellet Bed (see there). D E S C ~ O N : The Wimadjellet Member is recognised in central and eastern Spitsbergen.

The member starts with the plastic clay of the Myklegard- fjellet Bed. The dominant lithologies are grey shales and partly silty shales. The shales show prismatic fracturing and varying degrees of bioturbation. Reddish, sideritic lenticular concretions up to one metre in diameter are observed. The upper part of the member contains canonball-shaped and ovoidal nodules of siderite and calcite and thin limestone interbeds. The fossil content includes bivalves, belemnites and, rarely, ammonites. The member was deposited in open marine shelf enviroments.

Myklegardfjellet Bed (M-78)

STATUS OF UNIT: Formal FIRST USE OF NAME: Birkenmajer 1980 CURRENT DEFINITION: Birkenmajer 1980 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Myklegardfjellet: A mountain in southern Sabine Land, Agarclhbukta TYPE SECTION:

Stratotype: Myklegardfjellet, Sabine Land DEPOSITIONAL AGE: BerriaSian DATING METHODS AND REFERENCE(S) FOR AGE: See Rurik- fjellet Formation UNDERLYING UNIT@): Slottsmqa Member SUPERIOR UNIT: Wmadjellet Member OTHER USE OF NAME: None THICKNESS: 0.5-1 1 m MAIN LITHOLOGIES: Mudstone LOWER BOUNDARY DEFINITION: The base is defined by the onset of reddish-yellow or green plastic clay, overlying dark shales of the Slottsnwya Member.

Fig. 3-76: The Myklegard- fjellet Bed at Janus- fjellet, central Spitsbergen. These yellowish, glauconitic, plastic clays occur at the Jurassic-Cretaceous b o u n ~ in most parts of svalw where this i n t a d is exposed. Photo: J. Nagy

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DESCRIPTION: The Myklegardfjellet Bed is recognised throughout central and eastern Spitsbergen, including the outer Isfjorden area @ypvik et al. 1991; J. Nagy, unpubl. data) (Fig. 3-76).

The bed consists of reddish-yellow to green clays, usually very soft (plastic). Sometimes thin grey lenticular dolomite concretions with pyrite occur in the upper part.

The clay bed is an easily weathering marine deposit, rich in glauconite at some horizons. Its marine depositional environment is indicated by the foraminiferal content.

Ullaberget Member (M-79)

STATUS OF UNIT: Formal FIRST USE OF NAME: Rbiycki 1959 CURRENT DEFINITION: Birkenmajer 1975 SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Ullaberget: A mountain in Nathorst Land TYPE SECTION (FIG. 3-78): Stratotype: Ullaberget, Nathorst Land Hypostratotype: Kikutodden, Smkapp Land DEPOSITIONAL AGE: Valanginian - Early Barremian DATING METHODS AND REFERENCE(S) FOR AGE: See Rurik- fjellet Formation OVERLYING UNIT@): Helvetiafjellet Formation UNDERLYING UNIT@): Wimanfjellet Member, Tirolarpasset member SUPERIOR UNIT: Rutlldjellet Formation OTHER USE OF NAME: None THICKNESS: 10-160 m, 155 m in the stratotype MAIN LITHOLOGIES: Shale, siltstone, sandstone LOWER BOUNDARY DEFINITION: The lower boundary is defined at the first appearance of sandstones above grey shales of the Wimanijellet Member. DESCRIPTION: The Ullaberget Member is recognised in all sections of the Rurikfjellet Formation on Spitsbergen and constitutes the uppermost, generally coarsening-upward part of the Rurikfjellet Formation.

Fig. 3-77: The Ullaberget Keilhaufjellet, Smkapp L ening-upward successions sandstone just above the filgt OM is the m&&one member which defines the base ofthe RelxeWjellet Fopmation (to top of ridge). Photo: W.K. Dallmann

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Fig. 3-78: Stratigraphic section M-79 Hyposhruoype for: Ullaberget Member Locality: Kikutodden Reference: Edwards 1976

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The unit consists of shales, siltstones and sandstones forming a varying number of coarsening-upward minor successions developed in the upper part of the Janusfjellet Sub- group. The coarsest sandstone units occur in southern Spits- bergen where PEelina (1983) defined the "Kikutodden Member" (Fig. 3-77). This thick, coarse-grained development is here introduced as a reference section (hypostratotype) (Edwards 1976).

The section on Jurakarnmen in Torell Land (R6iycki 1959) consists of black and brownish black shales, often laminated and with worm trails (Taenidium) intercalated with thin siltstones. Several intercalations of fie-grained conglomerates are present.

The great variability in thickness reported along the westem Tertiary fold belt may partly reflect the Tertiary tectonic overprint. The member represents prodelta to shallow marine shelf deposits.

OCCURRENCE: Offshore unit, known fkom the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: F o ~ FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFJNITION: W0rsley et d. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF ~ m : Fuglen (transl. "The Bird"): A lighthouse on the western tip of Smoya, northern Norway TYPE SECTION:

Stratotype: Exploration well 7120112-1 Hypostratotype: Exploration well 71 19112-1 DEPOSITIONAL AGE: Late Bathonian - middle Oxfordian DATING METHOD: Ammonites, pal)JllologJ' ~FERENcE(s) FOR AGE: Smehr 1994, and ~ n p ~ b l . IKU data OVERLYING UNIT@): Hekkingen Formation UNDERLYING UNIT(S): St0 Formation, Realgrunnen Sub- group SUPERIOR UNIT: Adventdalen Group OTHER USE OF NAME: None THICKNESS: 28 m (stratotype), 48 m (hypostratotype) MAIN LITHOLOGIES: Mudstone, limestone LOWER BOUND'ARY DEFINITION: The lower boundary is marked by sharp increases in gamma ray and density responses and by an accompanying decrease in interval transit time. DESCRIPTION: The unit consists of pyritic mudstones with interbedded thin limestones which give characteristic gamma, sonic and density log responses. The mudstones are dark brown and the limestones white to brownish grey.

The formation is thickest in southwestem parts of the Ham- merfest Basin, thinning to less than 10 m on the central highs in the basin, these areas are characterised by rare, thin limestones and by pyritic shales.

In the Troms III area, a more silty development of 120 m is fully recorded in shallow cores (7018105-U-06 and 02). Silty developments also occurs north of the Hammerfest Basin.

The formation was deposited in marine shelf environments. Coarse clastic souroes were not emergent, but local structures were the sites of low sedimentation rates.

OCCURRENCE: OffShore unit, known from the Hammerfest Basin and the Bjanneland Platform (Fig. 1-02) STATUS OF UNIT: F 0 d h R s ~ USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: W~rsley et d. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Hekkingen: A lighthouse on the northern tip of Senja, northern Norway TYPE SECTION:

Stratotype: Exploration well 7 120112-1 Hypostratotype: Exploration well 7 1 19112- 1 DEPOSITIONAL AGE: Late Oxfordian - Volgian DATING METHOD: Ammonites, palynology REFERENcE(s) FOR AGE: Wierzbowski & h h ~ s 1990; Wierzbowski & Smelror 1993 and unpubl. IKU data OVERLYING UNIT(S): Knurr and Klippfisk formations UNDERLYING m@): Fuglen Formation SUPERIOR UNIT: Adventdalen Group OTHER USE OF NAME: None THICKNESS: 359 m (stratotype), 113 m (hypostratotype) MAIN LITHOLOGIES: Mudstone, limestone, shale, siltstone, sandstone LOWER BOUNDARY DEFINITION: The base is defined by the transition from carbonate-cemented, pyritic mudstone to poorly consolidated shales, producing a sudden increase in interval transit time and an abrupt decrease in bulk density values. DESCRIPTION: The Hekkingen or mat ion consists of brownish-grey to very dark grey shales and mudstones with occasional thin interbeds of limestone, dolomite, siltstone and sandstone. The minor clastic components are most common towards the basin margins.

The lower parts of the formation show especially high gamma ray values. This is used to differentiate the Alge Member from the overlying Krill Member.

The formation is thickest in its type well. It thins northwards to less than l00 m towards the axis of the Hammer- fest Basin. This pattern reflects the development of semi- grabens along basin margins while doming was active along the basin-axis.

The depositional environment was deep shelf with anoxic to dysaerobic conditions resdting fkom the formation of local barriers to circulation by Kimmerian movements. It is a correlative of the Agardhfjellet Formation in Svalbard.

Alge Member (M-82)

STATUS OF m: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: WorSley et d. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Alge: Norwegian for 'algae' TYPE SECTION:

Stratotype: Exploration well 7 1 1911 2-1 Hypostratotype: Exploration well 7 120112-1 DEPOS~I'IONAL AGE: Late Oxfordian - Kimmeridgian DATING METHOD: See Hekkingen Formation

195

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REFERENCE(S) FOR AGE: See Hekkingen Formation OVERLYING UNIT@): Krill Member UNDERLYING UNIT@): Fuglen Formation SUPERIOR UNIT: Hekkingen Formation OTHER USE OF NAME: None THICKNESS: 35 m (stratotype), 50 m (hypostratotype) MAIN LITHOLOGIES: Shale LOWER BOUNDARY DEFINITION: See F~glen Formation DESCRIPTION: The Alge Member forms the lower high gamma intensity part of the Hekkingen Formation and consists of black paper shales rich in organic material. The member was deposited in restricted shelf environments. See also Hekkingen Formation.

KrW Member (M-83)

STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Krik 'Krill' in English and Norwegian is a small, marine shrimp-like crustacean, the main food source of many marine mammals and bird species. TYPE SECTION:

Stratotype: Exploration well 7120112-1 Hypostratotype: Exploration well 7 1 1911 2- 1 DEPOSITIONAL AGE: Kimmeridgian -Volgian DATING METHOD: See Hekkingen Formation REFERENCE(S) FOR AGE: See Hekkingen Formation OVERLYING UNIT@): Knurr and Klippfisk formations UNDERLYING UNIT@): Alge Member SUPERIOR UNIT: Hekkingen Formation OTHER USE OF NAME: None THICKNESS: 80 m (stratotype), 3 10 m (hypostratotype) MAIN LITHOLOGIES: Mudstone, limestone, shale, siltstone, sandstone LOWER BOUNDARY DEFINITION: The base is defined at the abrupt reduction in gamma ray intensity. DESCRIPTION: The Krill Member is dominated by brownish- grey to very dark grey shale and mudstone with occasional thin interbeds of limestone, dolomite, siltstone and sandstone. The unit was deposited in open to restricted shelf environments. See also Hekkingen Formation.

OCCURRENCE: Offshore unit, known fiom the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None Omcm OF NAME: Knurr: Norwegian for the fish species 'grey gurnard' (EutngIa gumardus) TYPE SECTION:

Stratotype: Exploration well 71 19112-1 Hypostratotype: Exploration well 7120112-1 DEPOSITIONAL AGE: (?Volgian) Nalanginian - early Bar- remian

DATING METHOD: Dinoflagellates, foraminifera REFERENCE(S) FOR AGE: NO published data available; dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT@): Kolje Formation UNDERLYING UNIT@): Hekkingen Formation SUPERIOR UNIT: Adventdalen Group OTHER USE OF NAME: None THICKNESS: 56 m (htotype), 285 m (hypostratotype) MAIN LITHOLOGIES: Mudstone, limestone, sandstohe LOWER BOUNDARY DEFINITION: The base is defined by decreasing gamma ray response and by the sonic log showing decreasing interval transit time. In the reference well, the base is marked by a thin sandy limestone. DESCRIPTION: The Knurr Formation consists of dark grey to greyish-brown mudstone with thin limestone and dolomite interbeds in the type section. Sandstones are also seen in the lower part of the unit, but these disappear laterally into the Hammerfest Basin. Red to yellow brown mudstones generally occur in the upper part of the formation.

Present data suggest similar lithologies in all wells which penetrate the formation. The sand content is somewhat higher close to the Troms-Finnmark Fault Complex (e.g. well 7120112-1). Most complete developments are seen along basin margins.

The Knurr Formation was deposited in open and generally distal marine shelf environments with local restricted bottom conditions and represent the basinal development to the coeval platform carbonates of the Klippfisk Formation on the Bjarmeland Plaform. Both formations are lateral equivalents of the Rurikfjellet Formation in Svalbard.

OCCURRENCE: Offshore unit, known fiom the Bjarmeland Platform (Fig. 1-02) and Kong Karls Land (Fig. 3-1 1) STATUS OF UNIT: Formal FIRST USE OF NAME: Smelror et al. 1998 CURRENT DEFINITION: SmelrOr et al. 1998 SYNONYM@) AND REFERENCE(S): None ORIGIN OF NAME: Klippfisk: Norwegian for 'stockfish, dried cod' TYPE SECTION:

Stratotype: Exploration well 743011 0-U-0 1 Hypostratotype: Exploration well 723 1101-U-01 DEPOSITIONAL AGE: Late Berriasian - Hauterivian DATING METHOD: Palynology, nannofossils, bivalves REFERENCE(S) FORAGE: khus et al. 1990; Smelror et al. 1998 OVERLYING UNIT(S): Kolje Formation UNDERLYING UNIT@): Hekkingen Formation SUPERIOR UNIT: Adventdalen Group OTHER USE OF NAME: None THICKNESS: 8.9 m (stratotype), 4.5 m (hypostratotype), 15 m in Kong Karls Land MAIN LITHOLOGIES: Limestone, marl, calcareous sandstone LOWER BOUNDARY DEFINITION: The base is defined at the abrupt decrease in gamma ray intensity, where the dark mudstones of the underlying formation are replaced by marls.

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DESCRIPTION: The Klippfisk Formation represents a condensed carbonate succession occurring in platform areas (Kutling Member), where it consists of limestones and mark, and is often glauconitic. The limestones may have a nodular appearance. Fossil debris, dominated by Znocem- mus prisms may be abundant. The formation is strongly bioturbated.

In Kong Karls Land the coeval Tordenskjoldberget Mem- b e r h a similar lithology and is here assigned to the Klipp- fisk Formation.

The Klippfisk Formation is the carbonate platform time- equivalent of the Knurr Formation (Hammerfest Basin) and the Runkfjellet Formation (Svalbard). The unit has also been penetrated by shallow drilling and sampling in Hopendjupet and in the Olga Basin as well as farther south in the Barents Sea.

Kutling Member (M-86)

STATUS OF UNIT: Formal FIRST USE OF NAME: Smelror et al. 1998 CURRENT DEFINITION: Smelror et al. 1998 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Kutling: Norwegian for the fish family 'goby' (Gobiidae) TYPE SECTION: Stratotype: Exploration well 7430/10-U-01 Hypostratotype: Exploration well 723 1101-U-0 1 DEPOSITIONAL AGE: Late B e w i a n - &uterivian DATING METHOD: Palynology, nannofossils, bivalves REFERENCE(S) FOR AGE: h h u s et al. 1990; Sme'tror et al. 1998 OVS,RLYING UNIT@): Kolje Formation UNDERLYING UNIT(S): Hekkingen Formation SUPERIOR UNIT: Klippfisk Formation OTHER USE OF NAME: None THICKNESS: 8.9 m (stratotype), 4.5 m (hypostratotype) MAIN LITIXOLOGIES: Limestone, mar1 LOWER BOUNDARY DEFINITION: See Klippfisk Formation DESCRIPTION: The Kutling Member is a condensed carbonate succession and represents the entire Klippfisk Forma- tion on the Bjanneland Platform. See also Klippfisk For- mation.

Tordenskjoldberget Member (M-87)

STATUS OF m: Formal FIRST USE OF NAME: Smith et al. 1976

CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): The "Tordenskjoldberget Limestone Member" (Smith et al. 1976) includes 15 m of overlying shale which is now included in the Kolje Forma- tion (Smelror et al. 1998). ORIGIN OF NAME: Tordenskjoldberget: A mountain on Kongsplya, Kong Karls Land TYPE SECTION:

Stratotype: Tordenskjoldberget DEPOSITIONAL AGE: Late Berriasian - Hauterivian DATING METHOD: Palynology, nannofossils REFERENCE(S) FOR AGE: Bj~erke 1977; Verdenius 1978; Smelror et al. 1998 OVERLYING UNIT(S): Kolje Formation UNDERLYING UNIT(S): Hngsletta Member, Agardhfjellet Formation SUPERIOR UNIT: Klippfisk Formation OTHER USE OF NAME: None THICKNESS: 15 m in the stratotype MAIN LITHOLOGIES: Calcareous sandstone, limestone LOWER BOUNDARY DEFINITION: The lower boundary is covered in the entire exposure area. DESCRIPTION: The Tordenskjoldberget Member is a limestone unit representing the entire Klippfisk Formation on Kong Karls Land. It has been found only along one mountain side of Tordenskjoldberget for a distance of little more than 1 km.

The member consists of 15 m of white and light yellow, loosely cemented, coarse to medium-grained calcareous sandstone. The sandstone consists almost entirely of prismatic bivalve shell fragments (Znocemmw prisms). The member represents shallow marine carbonate platform sediment~. See also Klippfisk Formation.

OCCURRENCE: Offshore unit, known from the Hammerfest Basin (Fig. 1-02), Fig. 3-1 1 STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Kolje: Norwegian for 'haddock' (Melanogmmmus aegleflnus) TYPE SECTION:

Stratotype: Exploration well 71 19/12-1 Hypostratotype: Exploration well 7 120112-1 DEPOSITIONAL AGE: Barremian - ?early Aptian DATING METHOD: Palynology REFERENCE(S) FOR AGE: NO published &h available; &tea

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by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT(S): Kolmule Formation UNDERLYING UNIT(S): Knurr and Klippfisk formations SUPERIOR UNIT: Adventdalen Group OTHER USE OF NAME: None THICKNESS: 437 m (stratotype), 103 m (hypostratotype), 15 m in Kong Karls Land MAIN LITHOLOGIES: Shale, mudstone, limestone, dolomite LOWER BOUNDARY DEFINITION: The base is marked by gradually decreasing gamma ray, decreasing interval transit time and increasing density log responses in the type well. How- ever, in central parts of the Hammerfest Basin, the density log response shows a decreasing trend at the base. DESCRIPTION: The Kolje Formation consists of dark brown Fig. 3-79: Helvetiafjellet Formation at Fotografryggen, Torell Land. to grey shale and mudstone, with minor interbeds of pale The two light-coloured sandstone beds are lobes of the Festningen limestone and dolomite. The upper part of the formation sandstone member. Photo: WK. Dallmann also has thin interbeds of light grey-brown siltstone and sandstone.

The Kolje Formation thickens westwards but thins to- I wards the central part of the Hammerfest Basin. A 15 m thick wedge of the formation occurs locally in Kong Karls Land and consists of shales and siltstones with dark brown weathering ironstone nodules, including a calcareous horizon 4 m above the base. There are no marked regional vaxi- ations in lithology across the Barents Sea Shelf.

The formation was deposited in distal, open marine conditions, with good water circulation, but also with periodically restricted environments.

I HELVETIAFJELLET FORMATION (M-89)

Fig. 3-80: Growth faults in a delta front environment at the base of the

DISTRIBUTION SHOWN ON RG(S).: 3-06, 3-07, 3-08, 3-09, 3-10,3-l1 S T ~ S OF UNIT: Formal F ' T USE OF NAME: Parker 1967 C ~ R E N T DEFJNITION: Parker 1967 SYNONYM(S) AND RE~RENCE(S): "Sandsteinreihe": Nat- horst 1910; " C o ~ ~ h t a l Series": R6iycki 1959; "Shore Fig. 3-81: Foot imprints of a carnivorous dinosaur at KvalvHgen, east- sandstone": Hagennstn 1925. em Spitsbergen, in the Helvetiafjellet Formation. Photo: A. Mmk ORIGIN OF NW: Ha1t&@ellet: A mountain in eastern Nordenskiold Land TYPE SECTION (FIG. 3-82): Stratatype: Helvetiafjellet, eastern Nordenskiold Land OVERLYING UNIT(S): Carolinefjellet Formation DEPOSITIONAL AGE: Ban- UNDERLMNG UNIT(S): Runkfjellet, Agardhfjellet and Kolje DATING METHOD: Plant fossits; hdbxt, stratigraphic rela- formatiohs tionships SUPERIOR UNIT: Adventdalen Group REFERENCE(S) FOR AGE: Parker 1967; Vasilevskaja 1980 OTEER USE OF NAME: None

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Fig. 3-82: Stratigraphic section M-89 Stmtotype for: Helvetiafjellet Formation Locality: Helvetiafjellet Reference: Gjelberg & Steel 1 9 F

THICKNESS: 40-155 m (measured sections, no geographical trend), probably thicker at Keilhadjellet (Smkapp Land); 45 m in the stratotype MAIN LITHOLOGIES: Sandstone, shale, coal, congiommte LOWER BOUNDARY DEFINITION: The bwer boundary is defined as the erosional base of a massive, fluvio-h1taic m d - stone on top of the marine coarsening-upward successions of the Ullaberget Member or the shales and mudstones of the Kolje Formation. DESCRIPTION: The Helvetiafjellet Formation consists of coarse sandstones with subordinate carbonaceous shales and thin coal seams. The basal part of varying thickness is made up of the massive Festningen Sandstone member, which actually consists of several laterally intdigering lobes, with interbedded siltstones, shales and local coals (Figs. 3-79,3-80). The upper part of the formation consists of coarse, grey sandstones, cross-bedded and ripple-laminated, with abundant plant remains and carbonaceous streaks, together with carbonaceous shales, clay-ironstone horizons and thin seams of coal. Material of volcanic origin is present in several thin beds. Dinosaur footprints are found at several places (Fig. 3-81).

The Helvetiafjellet Formation is interpreted as the result of interacting fluvial, delta plain, mouth-bar, barrier-bar, tidal estuary and transgressive sheet sandstone facies formed after a period of relative fall in sea level followed by sea level rise and transgression (Gjelberg & Steel 1995).

Festningen (sandstone) member (M-90)

STATUS OF UNIT: Informal FIRST USE OF NAME: Nathorst 19 10 CURRENT DEFINITION: Parker 1967 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Festningen (transl. "The Fort"): A skerry off the southern coast of outer Isfjorden consisting of this unit. TYPE SECTION (FIG. 3-84): Stratotype: Festningen, outer Isfjorden DEPOS~TIONAL AGE: Barremian DATING METHOD: Indirect, stratigraphic relationships REFERENCE(S) FOR AGE: Parker 1967 OVERLYING =(S): Unnamed UNDERLYING UNIT(S): Rurrkfjellet Formation SUPERIOR UNIT: Helvetiafjellet Formation O T ~ R USE OF NAME: The 'Festningen' skerry has given its name to a large stratigraphic reference section through the Upper Palaeozoic and entire Mesozoic, the Festningen section. THICKNESS: Metres to a few tens of metres, not defined in many places; 15.5 m in the stratotype MAIN LITHOLOGIES: Sandstone, conglomerate LOWER BOUNDARY DEFINITION: See Helvetiafjellet Forma- tion. DESCRIPTION: The Festningen sandstone member is well- established and a useful descriptive name, but kept informal. The reason is that a clear definition and delimitation against other parts of the Helvetiafjellet Formation is impossible

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Fig. 3-83: Cross-bedded sandstone, Festningen sandstone member, Kikutodden, S~rkapp Land. Photo: W.K. Dallmann

The unit represents prominent, cliff-forming, hard, light grey sandstones in the. lower part of the Helvetiafjellet For- mation. It weathers grey, but also yellowish and orange, with variable grain size, normally from medium-grained sandstone to a coarse conglomerate. Cross-bedding is typical and conglomeratic beds and lenses occur frequently.

As shown by Steel (1977) and Gjelberg & Steel (1995), the Festningen sandstone member consists of several interfingering sandstone lobes. The facies is interpreted as mainly fluvial, although interacting with fluvial-dominated mouth bar and interdistributary bay environments.

~girfagrehaugeu Member (M-91)

STATUS OF UNIT: Formal FIRST USE OF NAME: Smith et al. 1976 CURRENT DEFINITION: Here, Olaussen et al., in prep. SYNONYM(S) AND REFERENCE(S): "HArfagrehaugen Sand- stone Member" (Smith et al. 1976): Only applied to western Kongssya; ''Johnsenberget Sandstone Member" (Smith et al. 1976): Correlative of the HArfagrehaugen Member, but only applied to eastern Kongssya; "Kiikenthalfjellet Sand- stone Member" (Smith et al. 1976): Correlative of the HArfagrehaugen Member, but only applied to Svenskqa. ORIGIN OF NAME: Hkfagrehaugen: A mountain on Kongssya, Kong Karls Land TYPE SECTION VIGS. 3-87,3-88,3-89): Boundary stratotype: HMagrehaugen, Kongslaya Unit Stratotype: Sjegrenfjellet W, Kongssya Hypostratotype: Kiikenthalfjellet, Svenskrqya DEPOSITIONAL AGE: Barremian DATING METHOD: Indirect, stratigraphic relationships REFERENCE(S) FOR AGE: Smith et al. 1976; Bjzerke 1977 OVERLYING UNIT(S): KOng Karls Land Flows v,,, UNDERLYING UNIT@): AgardhfjeUet and Kolje formations -

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SUPERIOR UNIT: Helvetiafjellet Formation OTHER USE OF NAME: None THICKNESS: Up to 70 m, including intercalated lava flows Fig. 3-84: Stratigraphic section M-90 MAIN LITHOLOGIES: sandstone, conglomerate, mudstone Stmtotypefor: Festningen sandstone member LOWER BOUNDARY DEFINITION: See Helvetiafjellet Forma- Locality: Festningen 3 tion. Reference: Steel et al. 1978

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Fig. 3-85: Dolerite dikes transsecting sandstones of the HMagre- haugen Member, Kongsraya. Photo: E.P. Johamessen

Fig. 3-86: A fwil tree trunk in ohe FElrhgrehaugen ember at Tordenskjoldberget, Kongssya. Photo: G.B. Larssen

DESCRIPTION: The HMagrehaugen Member represents the Helvetiafjellet Formation in Kong Karls Land.

TRe member rests with a probable erosional boundary on top of the Agardhfjellet Formation and, locally, the Kolje Fo-on. The unit consists of sedimentary rocks domi- - nated by sandstones in the lower part (Fig. 3-85), and by interbedded coal (elm), mudstones and sandstones in the upper part. Silicified wood occurs ab.mdantly (Fig. 3-86).

On Kongsraya the member shows a twofold appearance by colour. The lower part consists of yellow and white sandstones and conglomerates with quartzitic pebbles, mudstones and coal clasts. Separated by a sharp boundary, the upper part contains green sandstones with volcanoclastic and quartzitic pebbles, mudstones and coal-fragments. This boundary represents the onset of volcanic activity. The member was mainly deposited in fluvial channels, probably braided streams, in incised vdleys/creeks and passes upwards into flood plaintdelta plain deposits.

Kong Karls Land Flows (M-92)

STATUS OF UNIT: Formal FIRST USE OF NAME: Smith et d . 1976 CURRENT DEFINITION: Here, Olaussen et al., in prep. SYNONYM(S) AND REFERENCE(S): “brig Karl~ Land Forma-

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tion" (Smith et al. 1976): Synonym of Helvetiafjellet For- mation in Kong Karls Land. The stratigraphy of Kong Karls Land has been substantially revised according to recent understanding (see chapters 3.4.2,3.6.1). O m ~ m OF NAME: KOng Karls Land: A small archipelago in the eastern reaches of the Svalbard island group TYPE S E ~ O N (FIG. 3-91): Stratotype: Sjsgrenfjellet S, Kongsnrya DEPOSITIONAL AGE: Barremian and ?Aptian DATING METHOD: Indirect, stratigraphic relationships REFERENCE(S) FOR AGE: Smith et al. 1976 OVERLYING UNIT@): None UNDERLYING UNIT(S): Hiirfagrehaugen Member SUPERIOR UNIT: Helvetiafjellet Formation Chmm USE OF NAME: fing Karls Land Platfonn ("Kong Karl platform" of Gabrielsen et al. 1990): A structural element on the northern Barents Shelf, on which the archipelago of Kong Karls Land is situated THICKNESS: Up to 25 m, top eroded MAIN LITBOLOGIES: Basalt DESCRIPTION: The Kong Karls Land Flows represent two basaltic lava flows and associated pyroclastic rocks which interfinger with the sediments of the HMagrehaugen Mem- ber. The lower basalt flow varies considerably in thickness, and is locally overlain by grey-green pyroclastic rocks with large lava fragments. The upper basalt flow rests on sand-

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Fig. 3-90: Columnar basalt of the Kong Karls Land Flows at Retzius- fjellet, Kongserya. Photo: G.B. Larssen

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DISTRIBUTION SHOWN ON FIG(s).: 3-06,3-07,3-08,3-09,3-10 STATUS OF UNIT: Formal FIRST USE OF NAME: Parker 1967 CURRENT DEFINITION: Nagy 1970 SYNONYM(S) AND REFERENCE(S): "Dentalienschichten": Nathorst 19 10; "Ditrupa Shale Series": R6iycki 1959 ORIGIN OF NAME: Carolinefjellet: A mountain in northern Nordenskiold Land TYPE SECTION FIG. 3-93): Stratotype: Langstakken, eastern Nordenskiold Land DEPOSITIONAL AGE: Aptian - Albian *

DATING METHODS AND REFERENCE(S) FOR AGE: Macro- fossils: Parker 1967; PEelina 1967; Nagy 1970. Dinoflagel- lates: Thusu 1978; h h u s 199 1 OVERLYING UNIT(S): Firkanten Formation UNDERLYING m(s ) : Helvetiafjellet Formation SUPERIOR UNIT: Adventdalen Group OTHER USE OF NAME: None THICKNESS: 190-11200 m; increasing to the southeast; 770 m in the stratotype

Fig 3-92: Cretaceous succession at Zillerberget, Torell Land, starting with the light-coloured Festningen sandstone member. The top of the Helvetiafjellet Formation is at the first bend in the slope profile. The Carolinefjelet Formation constitutes most of the overlying succession (Dalkjegla member), succeeded by the slightly darker Innkjegla Member, the thin Langstakken Member at the bend at two thirds of the slope, and the Zillerberget member. The top plateau of the mountain in front represents the Tertiary Firkanten Formation. Photo: V.K. Dallrnann

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DESCRIPTION: The Carolinefjellet Formation is subdivided into five members according to the predominance of sandstones or shales. In most areas with outcrops of the formation, three members are defined: Dalkjegla Member (sandstone-dominated), Innkjegla Member (shale-dominated), Langstakken Member (sandstone-dominated alternation of sandstones and shales) (Fig. 3-94). In the southern parts of Spitsbergen the Zillerberget member occurs consisting of shales iind siltstones. The uppermost Schonrockfjellet member, again of alternating shales and sandstones (dominated by the latter) occurs very locally on southeastern Spits- bergen. (Fig. 3-92)

The formation was deposited in prodelta to distal marine shelf conditions following the fluvial and delta-related facies of the underlying Helvetiafjellet Formation. It correlates with the Kolmule Formation of the Barents Shelf.

Dalkjegla Member (M-94)

STATUS OF UNIT: Formal FIRST USE OF NAME: Parker 1967

I CURRENT DEFINITION: Parker 1967 SYNONYM(S) AND REFERENCE(S): "Dalkjegla Formation": PEelina 1983; "Lower lamina sandstone": Hagerman 1925 ORIGIN OF NAME: Dalkjegla (transl. "The Valley Cone"): A mountain in eastern Nordenskiold Land TYPE SECTION (FIG. 3-93): Stratotype: Langstakken, eastern Nordenskiold Land DEPOSITIONAL AGE: Aptian DATING METHODS AND REFERENCE(S) FOR AGE: Macro- fossils: Parker 1967; PEelina 1967. Dinoflagellates: k h u s 1991 OVERLYING UNIT@): Innkjegla Member UNDERLYING UNIT(@: Helvetiafjellet Formation SUPERIOR UNIT: Carolinefjellet Formation OTHER USE OF NAME: None THICKNESS: Ca. 50-180 m, thickening southeastwards; 130 m in the stratotype MAIN LITHOLOGIES: Sandstone, shale LOWER BOUNDARY DEFINITION: See Carolinefjellet Fonna- tion DESCRIPTION: The Dalkjegla Member is a cliff-forming unit. It consists of fine- to medium-grained, flaggy, thin- bedded, greenish-grey sandstones with intercalated grey siltstones and shales. The sandstones may contain minor amounts of carbonate. Mud flakes, cross-bedding, ripple lamination, ripple marks (in great variety) and load casts occur, though undisturbed parallel laminations dominate. Bivalve shells and imprints, and Ditrupa tubes are common. Yellow, carbonate-bearing sand interbeds of a few cm to dm thickness, locally with gravel, show hummocky cross-stratification and may be storm deposits. The member was deposited in shallow marine prodelta environments.

The DalEcJegla Member rests conformably and with a transitional contact on the Helvetiafjellet Formation. Its upper boundary shows a similar transition. The member is locally absent in the Hornsund area, west of Storbreen. It attains a maximum exposed thickness of 180 m at KvalvAgen.

Innkjegla Member (M-95)

STATUS OF UNIT: Formal FIRST USE OF NAME: Parker 1967 CURRENT DEFINITION: Parker 1967 SYNONYM(S) AND REFERENCE(S): "Singerfjella Formation" in eastern and southern Spitsbergen: PEelina 1983; "Ymer- bukta Formation" in western Spitsbergen: PEelina 1983; "Cretaceous shale": Hagerman 1925 ORIGIN OF NAME: Innkjegla (transl. "The Inner Cone"): A mountain in eastern Nordenskiold Land TYPE SECTION (FIG. 3-93): Stratotype: Langstakken, eastern Nordenskiold Land DEPOSITIONAL AGE: Aptian - Albian DATING METHODS AND REFERENCE@) FOR AGE: Macro- fossils: Parker 1967; PEelina 1967; Nagy 1970. Dinoflagel- lates: k h u s 1991 OVERLMNG UNIT(S): Langstakken Member, Firkanten For- mation UNDERLMNG UNIT@): Dalkjegla Member SUPERIOR UNIT: Carolinefjellet Formation OTHER USE OF NAME: None THICKNESS: Ca. 160-?S00 m, southeastward increasing; 430 m in the stratotype MAIN LITHOLOGIES: Shale, siltstone, sandstone LOWER BOUNDARY DEFINITION: The lower boundary is defined by the sudden predominance of monotonous, grey to dark-grey shales above the sandstone-dominated Dalkjegla Member. DESCRIPTION: The Innkjegla Member is 'a succession of grey shales, weathering grey, with interbeds of yellow weathering grey siltstone in the lower part and with intercalations of grey, flaggy, fine- to medium-grained sandstone, weathering orange and buff.

A large number- of red-orange or yellow carbonate (siderite and/or dolomite) layers occur in the lower part of the member in southeastern Spitsbergen. Higher up in the member, only a f m similar, most yeliowish beds occur spo- radically.

Clay-ironstone and other types of carbonate concretions frequently occur, mostly stratabound and concentrated in certain stratigraphic intervals. Small glendonites (Kemper 1983) form characteristic nodular aggeregates a few centimetres in diametre, while other concretions often are between 20 and 30 cm across, and among Svalbard geologists known as distinctive features for the Innkjegla Member by the descriptive name 'cannon balls' (Fig. 3-95). They often contain fossil remains.

Fossil fauna is scarce in the lower, but increasingly rich in the upper part, consisting mainly of bivalve shells and Dihupa tubes, but subordinately also ammonites occur. The member was deposited in moderately deep marine shelf environments.

The upper boundary towards the Langstakken Member is gradational due to upward increasing amounts of inter-, calated sandstone layers.

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Langstakken Member (M-96)

STATUS OF UNIT: Formal FIRST USE OF NAME: Parker 1967 CURRENT DEFINITION: Parker 1967 SYNONYM(S) AND REFERENCE(S): Lower part of "Kvalvigen Formationy': PEelina 1983; Lower part of "Upper lamina sandstone": Hagerman 1925 ORIGIN OF NAME: Langstakken (transl. "The Long Skirt", possibly "long stack"): A mountain in eastern Nordenskiold Land I . I ,

TYPE SECTION (FIG. 3-93): - Stratotype: Langstakken, eastern Nordensiiild Land DEPOSITIONAL AGE: Albian Fig. 3-96: The upper members of the Carolinefjellet Formation with DATING METHODS AND REFF,RENCE(S) FOR AGE: Macro- monotonous prodelta sediments at Kostinskifjellet, Torell Land. The fossils: Parker 1967; PEelina 1967; Nagy 1970. Dinoflagel- member subdivision is not clear in th~s area. Photo: W.K. DalImann lates: k h u s 1991 OVERLYING UNIT(S): Zillerberget member and Firkanten Formation DESCRIPTION: The Langstakken Member consists of alter- UNDERWING UNIT(S): Innkjegla Member nating shales, siltstones and flaggy, thin-bedded grey sand- SUPERIOR UNIT: Carolinefjellet Formation stones, weathering grey-green (Fig. 3-94). Both the lower -R USE OF NAME: None and upper boundaries are transitional. At the base of the unit THICKNESS: 208 m in the stratotype in the type section, there is an equal alternation of shales MAIN LITEOLOGIES: Sandstone, siltstone, shale and sandstones in units about 10-15 m thick, although LOWER BOUNDARY DEFINITION: The lower boundary is de- higher up in the succession sandstones predominate, and fined at the onset of equal sandstone - shale alternations ripple marks are common. The fossil content is similar to above the shale-dominated Innkjegla Member. . that of the Innkjegla Member, but is more scarce. The mem-

ber was deposited in moderately deep marine shelf environ-

I ments.

Fig. 3-94: Prodelta sandstone-shale facies of the Langstakken Mem- ber, Longyearbyen. Photo: J. Nag

Fig. 3-95: "Canon balls" (clay-ironstone concretions) in the Innkjegla Member of the Carolinefjellet Formation, here at Utnibba near Kvalvtigen, Heer Land. Photo: W.K. Dallmann

Zillerberget member (M-97)

STATUS OF UNIT: Informal FIRST USE OF NAME: Nagy 1970 CURRENT DEFINITION: Nagy 1970 SYNONYM(S) AND REFERENCE(S): Middle part of "Kval- vAgen Formation": PEelina 1983; Middle part of "Upper lamina sandstone": Hagerman 1925 ORIGIN OF NAME: Zillerberget: A mountain in northeastern Wedel Jarlsberg Land TYPE SECTION @G. 3-97): Stratotype: Zillerberget, northeastern Wedel Jarlsberg Land Hypostratotype: SchiinrockfJellet, eastern Torell Land DEPOSITIONAL AGE: Albian DATING METHOD: Ammonites REFERENCE(S) FOR AGE: Nagy 1970 OVERLYING UNIT(S): Schonrockfjellet member and Fir- kanten Formation UNDERLYING UNIT(S): Langstakken Member SUPERIOR UNIT: Carolinefjellet Formation OTHER USE OF NAME: None THICKNESS: Up to 334 m (Heer Land) MAIN LITHOLOGLES: Sandstone, siltstone, shale LOWER BOUNDARY DEFINITION: The lower boundary is not sufficiently defined, but is in general characterised by the onset of alternating clastic lithologies above the sandstone- dominated Langstakken Member. The uppermost shale- prone part assigned to the Langstakken Member in Fig. 3- 93 may belong to the Zillerberget Member, but this member

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was not recognised as an individual unit by Parker (1967). DESCRIPTION: The Zillerberget member consists of grey shales and siltstones with beds of grey-green, fine-grained sandstone (Fig. 3-96), The sandstones occur in more or less laterally persistent beds (5-20 cm thick) interbedded with the finer-grained sediment. The member was deposited in moderately deep marine shelf environments.

Both the lower and upper boundaries of the member are transitional.

The member, as defined and illustrated by Nagy (1970), was not accompanied by a type section log. Later work in southern Spitsbergen has shown difficulties in recognising member boundaries above the Langstakken Member, and the unit should be regarded as informal until further investigations have been carried out.

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SchonrockQellet member (M-98)

STATUS OF UNIT: IIlfoIlllal FIRST USE OF NAME: Nagy 1970 CURRENT DEFINITION: Nagy 1970 SYNONYM(S) AND REFERENCE(S): Upper part of "Kvalv8gen Formationy': PEelina 1983; Upper art of "Upper lamina sandstone": Hagerman 1925 P ORIGIN OF NAME: Schiinrockfjellet: A mountain in Heer Land TYPE SECTION (FIG. 3-97): Stratotype: Schiinrockfjellet, eastern Torell Land Hypostratotype: Schonrockfjellet, eastern Torell Land The hypostratotype is defined because the originally described section (Nagy 1970) was not accompanied by a log. The logged section is not located in the same place. DEPOSITIONAL AGE: Albian

Fig. 3-97: Stratigraphic section M-97b/98 Hypostmtotype for: Zillerberget and Schonrockfjellet members Locality: Schonrockfjellet Reference: Knarud & Msrk, in khus 199 1

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DATING METHOD: Ammonites REFERENCE(S) FOR AGE: Nagy 1970 OVERLYING UNIT(S): Firkanten Formation UNDERLYING LINIT(S): ZiUerberget member SUPERIOR UNIT: Carolinefjellet Formation OTHER USE OF NAME: None THICKNESS: 83 m in the stratotype MAIN LITHOLOGIES: Sandstone, siltstone, shale LOWER BOUNDARY DEFINITION: The lower boundary is defined where sandstones start to dominate above the shale- dominated Zillerberget member. It is not recognised in the hypostratotype. DESCRIPTION: The Schonrockfjellet member is locally preserved in Heer Land. It consists of grey-green, fine-grained sandstones interbedded with dark grey shales and siltstones (Fig. 3-96). The lower boundary of the member is transitional. Sandstones dominate and usually show a distinct stratification, expressed by weathering into thin flakes by splitting along shale partings. The member was deposited in moderately deep marine shelf environments.

The member as defined by Nagy (1970) was not accompanied by a type section. Later work in southern Spitsbergen has shown mculties in recognising member boundaries above the Langstakken Member, and the unit should be regarded as informal until further investigations have been carried out.

OCCURRENCE: Offshore unit, known from the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: Formal FIRST USE OF NAME: W0rsky et d. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Kolmule: Norwegian for the fish species 'blue whiting' (Micmmesistius poutassou) TYPE SECTION:

Stratotype: Exploration well 71 19112- 1 Hypostratotype: Exploration well 7120112-1 DEPOSITIONAL AGE: Aptian - Middle Cenomanian DATING METHOD: Palynology RE~RENCE(S) FOR AGE: NO published data available; dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVF,RLMNG =(S): Nygrunnen Group UNDERLYING UNIT(S): Kolje Formation SUPERIOR UNIT: Adventdalen group^ OTHER USE OF NAME: None THICKNESS: 945 m (stratotype), 530 m Olypostratotype), thickens westwards towards and into the Tromse Basin and slightly eastwards in-the Hammerfest Basin MAIN LITHOLOGIES: Shale, mudstone, siltstone LOWER BOUNDARY D E F ~ O N : The base is defined by sharply increasing intervd transit time aad neutron porosity values and a slight decrease in gamma log response. The reference well shows a similar sonic and neutron log trend, although with a gradually increasing gamma ray log response.

DESCRIPTION: The Kolrnule Formation consists of dark- grey to green mudstone and shale, partly with minor thin siltstone interbeds and limestone and dolomite stringers. Traces of glauconite and pyrite occur.

Open marine environments are indicated. The lower parts of the formation correlate to the

prodeltaic to open shelf deposits of the Carolinefjellet For- mation on the Svalbard Platform. The base of the unit mks a regionally sigmficant transgressive pulse; its top is eroded by the Late Cretaceous uplift, most significant on the northem shelf margins.

3.5.4 Nygrunnen Group

NYGRUNNEN GROUP (M-100)

STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Nygrunnen: A fishing bank NW of Smsya, northern Norway TYPE AREA: Block 7121112, Hamrnerfest Basin. Blocks 712115 and 7120112 show a thinner development typical of central and southeastern basin areas STRUCTURAL SETTING: Tromse and Hammerfest basins, Bjarmeland Platform (Southern Barents Sea Shelf) DEPOSITIONAL AGE: Late Cenomanian - Maastrichtian OVERLYING UNIT(S): Sotbakken Group (Palaeogene) UNDERLYING UNIT(S): Adventdalen Group SUPERIOR UNIT: None OTHER USE OF NAME: None THICKNESS: 50-250 m in the Hammerfest Basin, 1200 m in the Tromser Basin MAIN LITHOLOGIES: Sandstone, claystone, limestone DESCRIPTION: The Nygrunnen Group shows a distinctly twofold development. The Tromser Basin was the depositional centre throughout most of the period. Areas farther east were either only transgressed at times of maximum sea level andor display only condensed sections.

Greenish grey to grey claystones with thin limestone intervals in the Tromse Basin (Kveite Formation) pass,eastwards and southwards into a more calcareous, or sandy, I

condensed succession (Kviting Formation). Open marine, deep shelf environments in the west passed

into shallower, starved regimes (uplifted at times) in the east. The unit has no correlatives in Svalbard, where the entire Upper Cretaceous is represented by a major hiatus.

OCCURRENCE: Offshore unit, known from the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None

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ORIGIN OF NAME: Kveite: Norwegian for the fish species 'halibut' (Hippoglosssus hippoglossus) TYPE SECTION:

Stratotype: Exploration well 7 119112-1 Hypostratotype: Exploration well 71 1917-1 DEPOSITIONAL AGE: Late Cenomanian - Early Maastrichtian DATING METHOD: Palynology

I REFERENCE(S) FOR AGE: NO published data available; dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT(S): Tomk Formation (Palaeogene) UNDERLYING UNIT(S): KOlmule Formation SUPERIOR UNIT: Nygrunnen Group OTHER USE OF NAME: None THICKNESS: 249 m (stratotype), 1200 m (hypostratotype) MAIN LITHOLOGIES: Shale, mudstone, limestone LOWER BOUNDARY DEFINITION: The formation is characterised by a lower gamma response and higher i n t e~a l transit time than the underlying unit. A basal sand in the type well gives a marked break in both these logs. The boundary in these wells is also marked by a sudden increase in bulk density values above a generally decreasing trend, but the formation as a whole shows a highly variable and irregular density response. DESCRIPTION: The Kveite Formation consists of greenish- grey to grey shales and mudstones with thin interbeds of limestone and siltstone. A tuffaceous andtor glauconitiic component is present in several wells.

The formation appears to be characteristically developed in the Tromss Basin and across the Ringvassarya - Loppa Fault Complex into the Hammerfest Basin, thinning eastwards and passing into the sandstones and carbonates of the Kviting Formation.

The deposits indicate deep, open shelf environments with normal water circulation.

OCCURRENCE: Offshore unit, known from the Hammerfest Basin (Fig. 1-02) STATUS OF UNIT: Formal FIRST USE OF NAME: Worsley et al. 1988 CURRENT DEFINITION: Worsley et al. 1988 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Kviting: Norwegian for the fish species 'whiting' (Merlangius merlangus) TYPE SECTION:

Stratotype: Exploration well 7 120112- 1 Hypostratotype: Exploration well 7 12 115-1 DEPOSITIONAL AGE: CWIlpdan DATING METHOD: PalJ"ll010gy REFERENCE(S) FOR AGE: NO published data available; dated by Worsley et al. (1988) on the basis of proprietary oil company data. OVERLYING UNIT(S): Torsk Formation (Palaeogene) UNDERLYING UNIT(S): Kolmule Formation SUPERIOR m. Nygrunnen Group -R USE OF NAME: None THICKNESS: 17 m (stratotype), 3 1 m (hypostratotype)

MAIN LITEOLOGIES: Sandstone, mudstone LOWER BOUNDARY DEFINITION: The base is defined in the type well by log breaks showing a sharp decrease in gamma response and internal transit time, and increasing density. DESCRIPTION: Thsj Kviting Formation consists of calcareous sandstones with interbedded sandy and glauconitic mudstones. Limestones in the reference well are interbedded with, and grade up into sandy mudstones.

The formation is apparently restricted to the central and eastern parts of the Hammerfest Basin.

Deep to shallow shelf environments are indicated.

3.5.5 Intrusive rocks

DIABASODDEN SUITE (M-103)

Diabasodden I

DISTRIBUTION SHOWN ON FIG@).: 3-09, 3-10, 3-1 1, 3-12 (The suite occurs also on western Spitsbergen, but dikes there are too thin to be indicated on the respective maps.) STATUS OR UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE@): The suite has been referred to as "Mesozoic dolerite sills and dikes" on published maps. ORIGIN OF NAME: Diabasodden (transl. "The Diabase Point"): A point on the southern coast of Sassenfjorden TYPE AREA: Diabasodden, northern Nordenskiold Land INTRUSIVE AGE: Late Jurassic - Early Cretaceous DATING METHOD: Radiometric age determination, K-Ar method REFERENCE(S) FOR AGE: BUOV et d. 1977 HOST ROCKS: Precambrian through to Lower Cretaceous OTFKER USE OF NAME: None MAIN LITHOLOGIES: Dolerite DESCRIPTION: Dolerite dikes and sills cut strata of all ages up to early Cretaceous in most areas of Svalbard. In central and eastern Svalbard, where sediments of these ages are flat-lying, they cover major areas and often form top plateaus of table mountains or islands. The dolerite intrusions are generally considered to be of Cretaceous age, with one age distribution maximum at the JurassiclCretaceous boundary, and another one in the late Early Cretaceous (Burov et al. 1977). The minimum age of the host rocks decreases eastwards.

The thickness of sills normally varies from a few metres to more than 50 m. The observed lateral extent of individual sills attains 10-1 5 km. They are oriented parallel with the bedding of the host rocks or slightly cut them, mostly at low

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angles. Forking of sills occurs frequently. Subvertical dikes occur, but are not observed frequently.

The mineral composition of dolerites is: Plagioclase (An 40-80) 40-60%, clinopyroxene 30-50%, opaques (mag- netite, pyrite) 5-20%. Secondary minerals are carbonate, chlorite and saussuritised plagioclase. A small amount (up to 2-3%) of quartz is recorded close to margins of intrusive bodies. Dolerites containing up to 10% olivine are reported from the Agardhbukta area (Panov et al. 1968, unpubl.). The central parts of intrusive bodies are mainly medium- to coarse-grained and show doleritic an4 less commonly, ophitic textures. The peripheral parts are fine-grained and have a microdoleritic texture. In calcified marginal zones of the intrusive bodies, porphyritic and relic-doleritic matrix textures occur.

The chemical composition is tholeiitic, partly oversatu- rated, and their REE patterns reflect a continental intraplate setting with a hot-spot affinity (Murosko 1981, unpubl.; Hauser 1982, unpubl.).

Thermal effects around intrusions are essentially developed in shales and siltstones, where hornfelsing and calcifi- cation of the host rocks are observed. The thickness of these altered zones attains 2 m or, less commonly, up to 4 m, de- pendant on the thickness of the dolerites.

3.6 Abandoned lithostratigraphic unit names

3.6.1 Names with aplace name segment

Names listed in this section are not recommended for future use. They are either synonyms of other, preferred names, or describe units that overlap, or are incompatible, with another, preferred stratigrapbic subdivision. Preferences are discussed in sections 3.2 and 3.4.

Some names describe local facies variations that SKS does not consider to deserve lithostratigraphic names in order to avoid unnecessary proliferation. Some names are defined in a chronostratigraphic context and without lithostratigraphic merit, or are replaced by a preferred, conven- tional, lithostratigraphic grouping.

Many of the listed units and their correlations are schematically shown in Figs 3-02 to 3-04. Units that have changed their rank or category, but not their place name segment, and that still refer to the same lithostratigraphic section, are not listed here. See section 3.5.


Arnesenodden Shale Bed (Smith et al. 1976): Correlative of the Flatsalen Formation (M-46) on Svensksya and replaced by the latter name.

Austjekelen Formation et al. 1982): Correlative of the Tscherma@ellet Formation (M-33) in $mkapp Land and replaced by the latter name. Correct spelling of the place name: Austjerhlen.

Barentseya Formation (Lock et al. 1978, redefined by Mmk et al. 1982): The subdivision into two distinct for-

mations (Vikinghagda Formation, M-13 and Botneheia Formation, M-24) is preferred. These formations are easily distinguished, also on the eastern islands.

Bjernbogen Formation (PEelina 1980): Correlative of the Flatsalen Formation (M-46) on Hopen, Kong Karls Land and eastern Spitsbergen and - together with the "Basal" and "Transitional members" replaced by the latter formation name. The new grouping is proposed for the purpose of correlation between eastern Spitsbergen, Hopen and Kong Karls Land.

Bjernbogen Horizon (PEelina 1983): A chronostratigraphic "group" of Norian age corresponding to the "Keilhau- fjellet", "Tvillingodden", "Bjmbogen" and "Isfjorden formations" (acc. to PEelina), or the lower, Triassic part of the FF?lhelm~ya Subgroup (M-38) according to present definition.

Bjernbogen Member (Worsley 1973): Correlative of the Flatsalen Formation on Wilhelrmaya and replaced by the latter name. PEelina (1980) applied the name to the Trias- sic part of the Wilhelm0ya Subgroup (M-38) in eastern Svalbard. The name is superfluous in connection with the present lithostratigraphic nomenclature.

Bogen bed (Larssen et al. 1995, unpubl.): Synonym of Vmk- bukta Bed (M-52). The name 'Bogen' is used for a member of the Proterozoic Kingbreen Formation (Harland et al. 1966) and has priority there.

Botneheia Horizon (PEelina 1983): A chronostratigraphic "group" of Anisian to Ladinian age corresponding to the Botneheia, Bravaisberget, "Hyrnefjellet" and "Van Keulenfjorden formations" (acc. to PEelina), or the Botne- heia (M-24) and Bmvaisberget (M-19) formations according to present definition.

Brentskardhaugen Member (PEelina 1980): Corresponds to the uppermost part of the condensed succession of the Teistberget member (34-45) as defined herein, including the Brentskardhaugen Bed (M-54). It is preferred to re- serve the place name to the Brentskardhaugen Bed, due to priority and wide use.

Brevassfjellet Myalina Bed (Birkenmajer 1977): The name was used for both the basal conglomerate directly resting on the Pre-Old Red on the S~rkapp-Hornsund High (Brevassfjllet Bed, M-08 in the present defmition) and for the bivalve-rich beds in the middle part of the Varde- bukta Formation (M-02) east of the High.

Drevbreen Formation (Birkenmajer 1977): The name was used for the Bmvaisberget (M-19) and Tscherma@ellet (M-33) formations in southern Spitsbergen. According to the established group subdivision, this unit does not provide an appropriate grouping.

Drenbreen Bed (Dypvik et al. 1991): Corresponds to the Oppdalen Member (M-70) of the Agarwellet Formation (acc. to Dypvik et al.) excluding the Marhnrgda Bed. The present nomenclature does not include the Marbgda Bed in the Oppdalen Member, thus making the member and the "Drmbreen Bed" synonymous. The name is also considered to be superfluous, because the naming of a bed within a member does not necessarily require naming df the remainder of the member.

Dunerfjellet Shale Member (Smith et al. 1976): Not recognising the major stratigraphic break between the Kapp

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Toscana and Adventdalen groups, Smith et al. let their i '

"Kongssya Formation" reach into the late Jurassic. The "Dunhfjellet Shale Member", together with its lateral equivalents, the "Retziusfjellet" and "Nordaustpynten membersyy, form the Late Jurassic part of the formation, now correlated with the AgardhJellet Formation (M-66). In the present nomenclature proposal, the lateral member subdivision of the upper Jurassic is replaced by a stratigraphic member subdivision, Bunswbukta Member (M- 74) and H~gsletta Member (M- 75).

Edgesya Formation (Lock et al. 1978): Correlative of the Tscherma&iellet Formation (24-33) and refhaced by the latter name.

Glitrefjellet Member (Parker 1967): Upper part of the HelvetiaBellet Formation (M-89), overlying the Festnin- gen sandstone member (34-90). The base of this unit cannot be defined properly due to the multiple sandstone lobes developed in many exposure areas of the Festningen sandstone member. The name is proposed to be dropped.

Hahnfjella Formation (PEelina 1983): A name for the Cam- ian deposits of Svalbard. It corresponds to the Tscher- maMellet Formation (M-33) and the part of the De Geerdalen Formation (34-34) below the IsJorden Member (M-35).

Hahnfjella Horizon (PEelina 1983): A chronostratigraphic grouping of Carnian age corresponding to the "Hahnfiella Formationyy (acc. to PEelina), or the Tscherma~ellet For- mation (34-33) and the De Geerdalen Formation (M-34) without the Is$orden Member (34-35) according to present definition.

Hirfagrehaugen Sandstone Member (Smith et al. 1976): Originally restricted to the western part of Kongsnrya, the name is now applied to the HelvetiaJellet Formation (M- 89) on Kong Karls Land. See Hdrjagrehaugen Member (34-91).

HeimfjelIa beds (Dallmann et al. 1990): Yellowish weathering, ammonite-bearing siltstone beds within the Agardh- Jellet Formation (M-66) south of Van Keulenfjorden. The unit is indicated on the geological map to illustrate Ter- tiary folding and thrusting of the black shale-dominated formation, but is probably not stratigraphically significant.

Hyrnefjellet Formation (PEelina 1983): A correlative of the Bravaisberget Formation (M-19) excluding the Van IGulenJorden Member (M-23), but restricted to the Smkapp - Homund area. The name is also used for a Car- boniferous formation in southern Spitsbergen (CP-41; Birkenmajer 1959,1964). The latter usage has priority.

Iversenfjellet Formation (Smith et al. 1975): Correlative of the De Geerdalen Formation (34-34) on Hopen and replaced by the latter name.

Johnsenberget Sandstone Member (Smith et al. 1976): Correlative of the Hddagrehaugen Member (M-91) on Svenskraya and replaced by the latter name.

Kapp Kobnrg Formation (Worsley & Heintz 1977): Cor- relative of the Flatsalen Formation (34-46) and replaced by the laiter name.

Kikntodden Member (PEelina 1983): Correlative of the Ullaberget Member (M-79) in Smkapp Land and replaced by the latter name, although the member here is coarser-

grained than in other areas. Kong Karls Land Formation (Smith et al. 1976): The Bar-

re& and possibly younger strata of Kong Karls Land correlated with the Helvetiafiellet Formation (M-89). The stratigraphy of Kong Karls Land has been substantially revised according to recent understanding (Olaussen et al. in prep.). The sedimentary part is referred to as Hdrjagre- haugen Member (M-91). The name Kong Karls Land Flows (M-92) is reserved for the basalt flows in the upper part of the succession.

Kongressfjellet Subgroup (Buchan et al. 1965), Kongressf- jellet Formation (Flood et al. 1971): Corresponds to the two upper members (Lusitaniadalen Membec M-15, and Yendomdalen Membe M-16) of the ViRingh0gda Forma- tion (M-13) and the Botneheia Formation (U-24). The unit name is obsolete.

Kongseya Formation (Smith et al. 1976): Not recognising the major stratigraphic break between the Kapp Toscana and Adventdalen groups, Smith et al. gathered all Mid- Jurassic to early Barremian deposits of Kong Karls ~ & d in their "Kongsraya Formation'". The stratigraphy of Kong Karls Land has been substantially revised according to recent understanding (Olaussen et al. in prep.). The deposits are now assigned to the (revised) Kongswa Formation (M-51), Agardhfiellet Formation (34-66; Bunsowbukta Member, M-74, and Hpgsletta Membet; M-75), Klippfisk Formation (34-86; Tordensljoldberget Member, M-87) and Kolje Formation (34-88).

Konussen Formation (PEelina 1983): Valanginian-Berri- asian part of the RuriHellet Formation W-76) in southern and central western Spitsbergen, where it approximately corresponds to the Ingebngtsenbukta (M-67) and Timlarpasset (U-68) members.

Kiikenthalfjellet Sandstone Member (Smith et al. 1976): Correlative of Hdrfagrehaugen Member (M-91) on Svensksya and replaced by the latter name.

Kvahrigen Formation (PEelina 1983): Corresponds to the upper three members of the CamlineJellet Formation (M-93), the Langstakken (M-96), Zillerberget (M-97) and Schonm~ellet (34-98) members, mainly in southern and eastern Spitsbergen.

Lyngefjellet (Shale) Formation (Smith et al. 1975): Correl- ative of the Sj~grenJellet Member (M-48) of the Svensk- 0ya Formation (M-46) on Hopen and replaced by the latter name.

Mohnhegda Sandstone Member (Smith et al. 1976): Ori- ginally the representative of the "Svensksya Formation" on Svensksya, Kong Karls Land. The stratigraphy of Kong Karls Land has been substantially revised according to recent understanding (Olaussen et al. in prep.). The Mohnh~gda Member (24-50) is now assigned to the upper part of the SvensKBya Formation (M-47) on Kong Karls Land.

Negerfjellet Formation (Lock et al. 1978): Correlative of the De Geerdalen Formation (M-34) on the eastern islands and replaced by the latter name.

Nordaustpynten Shale Member (Smith et al. 1976): Not recognising the major stratigraphic break between the Kapp Toscana and Adventdalen groups, Smith et al. let their "Kongsnrya Formation" extend into the upper Juras-

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sic. The 'Wordaustpynten Shale Member", together with its lateral equivalents, the "Retziusfjellet" and "DunBr- fjellet Shale members", form the Upper Jurassic part of the formation, now correlated with the AgardhJellet For- mation (M-66). In the present nomenclatorial proposal, the lateral member subdivision of the upper Jurassic is replaced by a stratigraphic member subdivision (Bunsow- bukta Member, M-74, and Hogsletta Membec M-75).

Nordvestbanken Group (Worsley et al. 1988): Cretaceous group in the southern Barents Sea, comprising the Knurr (M-84), Kolje (M-88) and Kolmule (M-99) formations. These formations are correlated with and included in the Adventdalen Group (M-64), and the group name is abandoned. Authors wishing to apply the name should give it subgroup rank.

Passet Clay Member (Smith et al. 1976): The main, Early- Middle Jurassic part of the Kongsoya Formation according to Smith et al. on the island of Kongssya. It corresponds to the present definition of the Kongsoya Formation (M-51).

Pitnerodden Formation (PEelina 1983): Equivalent of the Tvillingodden Formation (M-09) (Mnrrk et al. 1982). The latter name is preferred because the name-giving locality is made up of rocks of this formation, while the place called Pitnerodden is not. Furthermore, the name 'Tvillingodden' has been used on all published geological maps.

Retzfusfjellet Shale Member (Smith et al. 1976): Not recognising the major stratigraphic break between the Kapp Toscana and Adventdalen groups, Smith et al. let their "Kongsaya Formation" extend into the Upper Juras- sic. The "Retziusfjellet Shale Member", together with its lateral equivalents, the "DunBrfjellet" and 'Wordaustpyn- ten shale members", form the Upper Jurassic part of the formation, now correlated with the AgardhJellet Forma- tion (M-66). In the present nomenclature proposal, the lateral member subdivision of the upper Jurassic is replaced by a vertical member subdivision (Bunsowbukta Member, M-74, and Hogsletta Member: M-75).

Rnrikfjellet Horizon (PEelina 1983): A chronostratigraphic "group" of Berriasian to Hauterivian age comprising the Rurikjellet, "Sylodden", and "Konussen formations" (acc. to PEelina). It corresponds to the Rurikjellet Forma- tion (M-76) according to the present defition.

Singerfjella Formation (PEelina 1983): Corresponds to the Innkjegla Member (M-95) of the CarolineJellet Forma- tion (M-93) in southern and eastern Spitsbergen.

Singerfjella Horizon (PEelina 1983): A chronostratigraphic grouping of Aptian-Albian age comprising the "Singer- fjella" and "Ymerbukta formations" (acc. to PEelina). It corresponds roughly to Innkjegla Member (M-95) of the Carolinejjellet Formation (34-93) according to the present definition.

Sjegrentjellet Sandstone Member (Smith et al. 1976): Orig- inally the representative of the "Svenslaya Formation" on Kongssya, Kong Karls Land. The stratigraphy of Kong Karls Land has been substantially revised according to recent understanding (Olaussen et al. in prep.). The Sjogren- Jellet Member (M-48) is now assigned to the lower part of the Svensbya Formation (M-47) across eastern Svalbard.

Srrrkapp Formation (PEelina 1980): Original name and synonym of the Mathiasbreen member, a subunit of the Smalegga Formation (M-40) in Ssrkapp Land. The name "Ssrkapp Formation" (PEelina 1980) does not seem to be appropriate: The locality 'Ssrkapp' on Ssrkappciya comprises Permian and Sassendalen Group strata. The similar name 'Smkapp Land' is used for an Ordovician Group (Birkenmajer 1978).

Sticky Keep Formation (Buchan et al. 1965), Sticky Keep Member (Marrk et al. 1982): There are difficulties in recognising the boundary between the Deltadalen and "Sticky Keep" units because there is also another similar but distinct .lithological boundary within the "Sticky Keep" unit. To avoid redefmitions of established names, and to facilitate the recognition of boundaries in the field, a threefold subdivision of the Mkinghogda Formation (M- 13) (Mnrrk et al. 1998) into Deltadalen Member (M-14) (unchanged definition, but adjusted levels on maps and published sections), Lusitaniadalen Member (M-15) and Vendomdalen Member (34-16) is proposed herein, the two latter replacing the "Sticky Keep Member".

Storbreen Subgroup (Birkenmajer 1977): A grouping of units containing bituminous shales in southern Spits- bergen, part of the "Torell Land Group". The subgroup comprises the Tvillingodden (M-09), Bmvaisberget (M- 19) and Tschermakjellet (M-33) formations. The unit is controversial, because its constituents belong to two groups according to the nomenclature of Buchan et al. (1965) which is preferred, both for priority reasons and from the recent understanding of the facies development.

Svensbya Formation (Smith et al. 1976): The stratigraphy of Kong Karls Land has been substantially revised according to recent understanding (Olaussen et al. in prep.). The lower part of the succession is now correlated with the Flatsalen Formation (M-46), while the upper part is referred to the (revised) Svenskoya Formation (M-47).

Sylodden Formation (PEelina 1983): Hauterivian part of the Rurikjellet Formation (M-76) in southern and western central Spitsbergen, where it approximately corresponds to the Ullaberget Member (34-79).

Teistengrnnnen Group (Worsley et al. 1988): Late Jurassic group in the southern Barents Sea, comprising the Fuglen (34-80) and Hekkingen (34-81) formations. These formations are correlated with and included in the Adventdalen Group, and the group name is abandoned. Authors wishing to apply the name should give it subgroup rank.

Tordenskjoldberget Limestone Member (Smith et al. 1976): Originally defined for the stratigraphic interval between the "Retziusfjellet Shale Member" and the '<H&: fagrehaugp Sandstone Member" on Kongsciya. The unit has recently been recognised as a twofold succession, the lower limestone interval, Tordenskjoldberget Member (M- 87) correlated with the Klippfisk Formation (M-86), and the overlying shale interval correlated with the Kolje For- mation (34-88) of the Barents Sea Shelf (Smelror et al. 1998; Olaussen et al. in prep.).

Torell Land Group (Birkenmajer 1977): Correlative of the Sassendalen (M-01) and Kapp Toscana (M-31) groups in southern Spitsbergen and replaced by the latter names. The name overlaps with the nomenclature of Buchan et al.

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(1965) which is preferred, both for priority reasons and from the recent understanding of the facies development.

'hmlingodden Member (Worsley 1973): Upper part of the Wilhelmqa c'Fonaation" of Worsley (1973). It corresponds to the Sjogrenjjelellet Member (M-48; Svensbya Formation) and the Keisarkampen Member (M-53; Kongsqw Formation) on Wilhebyz?. The change in subdivision is proposed for the purpose of correlation between eastern Spitsbergen and Kong Karls Land.

lhmlingodden Formation (PEelina 1980): Correlative of the Svensbya (34-47) and Kongs~ya (M-51) formation on Kong Karls Land and replaced by the latter names. The new subdivision is proposed for the purpose of correlation between eastern Spitsbergen and Kong Karls Land.

lbmlingodden Horizon (PEelina 1983): A chronostratigraphic grouping of Hettangian to Bathonian age comprising the "Tumlingodden". "Teistberget" and "Smkapp formations" (acc. to PEelina). It corresponds to the upper part (Jurassic) of the E?lhelmnya Subgroup (M-38) according to the present defition.

Tvillingodden Formation (PEelina 1980): "Tvillingodden Formation" was used by PEelina (1980) for the unit herein defined as the Tverrbekken member (M-44). Although the definition of PEelina should have priority due to first publication, the name-giving locality "Tvillingodden'' refers to the unit herein defined as Tvillingodden Formation (Marrk et al. 1982). The latter meaning of the name has been used more widely in the literature and on published geological maps.

Uleneset Member (SI13ith 1975): Correlative of the De Geerdalen Formation (M-34) on WIlhelmqa and replaced by the latter name.

Vardebukta Horizon (PEelina 1983): A chronostratigraphic grouping of Induan age corresponding to the "Vardebukta Formation" (acc. to PEelina), or the Vardebukta Formation (M-02) and Deltadalen Member (24-14) according to the present definition.

WichebnMa Formation (PEelina 1983): Correlative of the "Pitnerodden Formation" in eastern Svalbard. The unit corresponds to the two upper members of the V i g - bgda Formation, the Lusitaniadalen Member (M-15) and Vendomdalen Member (M-16), or the abandoned name "Sticky Keep Member".

Wichebnkta, Horizon (PEelina 1983): A chronostratigraphic grouping of Olenekian age corresponding to the "W~chebukta" and "Pitnerodden formations" (acc. to PEelina), or the Tvillingodden Formation (M-09) and the Lusitaniadalen (M-15) and Vendomdalen (M-16) members according to present definition.

Ymerbnista Formation (PEelina 1983): Corresponds to the Znnkjegla Member (34-95) of the Camlinejjellet Forma- tion (M-93) in western central Spitsbergen.

3.62 Names without aplace name segment

Names without a place indicative segment are in general old, informal names that meanwhile have been substituted by formal names. For a number of names, the grouping of strata does not correspond to the more recent lithostratigraphic subdivision. All of these names are today out of use.

They are listed here with their reference (first published) and indication of stratigraphic range for the purpose of understanding older geological literature in a modern context. Many of the old units and their correlations are schematically shown in Figs 3-03 and 3-04.


Anasiberites horizon (Spath 1921): Basal part of the Lusi- taniadaLen Member (M-1 5)

Arctoceras-Schichten, A. Horizont (Stolley 19 1 1 ; Frebold 193 1): Part of Ekinghngda Formation (M-1 3)

Argillite unit (Klubov 1965): Lower part of Tschermak- Jellet Formation (M-33) on the eastern islands of Sval- bard

Aucellenschichten, A. Shale (Nathorst 19 10; Hagerman 1925): Synonym of Janus$ellet Subgroup (M-65)

Basal Bed (Smith 1975): Lower part of Flatsalen Forma- tion (M-46)

Basal member (Worsley 1973): Lower part of Flatsalen Formation (M-46)

Black shales and yellow flags (Gregory 1921): Large section of the Ekinghflgda Formation (M-13)

Blue and purple shales (Falcon 1928): Synonym of Tscher- mueellet Formation (M-33)

Bottom shale (Orvin 1934): A thin section of Triassic between the Permian and Tertiary strata of Brsggerhalvraya correlated with the Vardebuha Formation (M-02) (Mid- bnre 1985, unpubl.)

Claraia Zone (Frebold 1936): Otocems boreab Zone in the Vardebuka Formsrt$on (M-02)

Continental series ( ~ 6 h c k i 1959): Synonym of Helvetia- jjellet Formation (34-89)

Cretaceous shale (Hagerman 1925): Synonym of the Innkjegla Member (3495)

Daonellenkalk, D. schichten, D.-Niveau (MojsisoviEs 1886; Nathorst 1910; Wiman 1910): Upper part of the Botneheia Formation (M-24)

Dentalienschichten (Nathorst 1910): Synonym of Cam- 1ineJellet Formation (M-93)

Ditmpa-Schichten, D. shale series (Stolley 191 1; ~ b h c k i 1959): Synonym of Camlinejjellet Formation (34-93). equivalent of "Dentalienschichten"

Elatides-Schichten, E. Niveau (Nathorst 1910; Hoel & O ~ i n 1937): Thin horizon within the Helvetiajjellet For- mation (M-89) at Festningen, between Festningen sandstone member (M-90) and "Lioplaxschichten"

Escarpment shales (Oregory 1921): Lower and middle shales of the Botneheia Formation (M-24)

Eutomoceras-Teilzone (Frebold 193 1): Part of Botneheia Formation (M-24)

Fisch-Nivean (Wiman 1910): Lower part of Vikinghngda Formation (M-13)

Fossesandstein (Hoel & O ~ i n 1937): Upper part of Van Keulenjjorden Member (M-23)

Ginkgo-Schichten, G. Niveau (Nathorst 1910; Hoel & Orvin 1937): Correlates with the upper part of Helvetia- Jellet Formation (M-89), between "Pityophyllum- Schichten" and "Dentalienschichten"

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Grippia-Niveau (Wiman 1928): Part of Vikinghegda For- mation (M-I3), between "Fisch-Niveau" and "Unteres Saurierniveau"

Gymnotoceras-Teilzone (Frebold 193 1): Shale part of Botneheia Formation (M-24), overlying "Unteres Saurier- niveau"

Halobia limestone (Frech 1903): Synonym of Tschermak- Jellet Formation (34-33)

Halobia shales (Stolley 1911): Lower part of Tschermak- Jellet Formation (M-33)

Halobia zitteli bed (MojsisoviEs 1886): Base of the "Halo- bia limestone", Tscherma&ellet Formation (34-33)

Hieroglyphic series (R6iycki 1959): Probably a synonym of the Vardebukta Formation (34-02)

Hustediakalk (Nathorst 1910): A synonym of the Skilisen Bed (M-12) or "Retziakalk", Tvillingodden Formation (M-09), above "Pseudomonotisskifer 1 Pkalk"

Lias conglomerate (Orvin 1940): Synonym of Brentskard- haugen Bed (34-54)

Lindstroemi-Horizont (Frebold 193 1): A limestone-sandstone succession within the "Nathorstites-Niveau", part of the Van KeulenJorden Member (34-23) according to PEelina (1983)

Lingula Sandstein (Stolley 191 1): Part of "Nathorstites- Niveau", De Geerdalen Formation (3434)

Lioplaxschichten, Siisswasserschichten mit Lioplax (Nathorst 1897, 19 10): Thin horizon within the Helvetia- Jellet Formation (34-89)

Lower Continental Series (Birkenmajer 1975): Lower part of HelvetiaJellet Formation (M-89), Festningen sandstone member. (M-90)

Lower lamina sandstones (Hagerman 1925): Synonym of Dalkjegla Member (M-94)

Lower Posidonia (Posidonomya) shales (Spath 1921): Arc- tocems blomstrandi Zone of Lusitaniadalen Member (M- I5), Vikinghegda Formation (34-13)

Lowest nodule beds (Gregory 1921): Part of Arctocerm blomstrandi Zone, Lusitaniadalen Member ( W 5 of Vikinghegda Formation (24-13)

Myalinaskifer, M. Niveau, M. beds (Lundgren 1887; Fre- bold 1930; Tozer & Parker 1968): Section in the Varde- bukta Formation (M-02) and Deltadalen Member (M-14) of the Vikinghegda Formation (M-13)

Myophoria-Sandstein (Andersson 1900): Top of Skuld Formation (M-366 Bjsnuaya

Nathorstites-Nivean (Stolley 19 1 1): Part of Tschermak- Jellet (34-33) and De Geerdalen (34-34) formations

Oberes Saurierniveau (Wiman 1910): Upper part of the "Daonella Niveau", corresponding to upper part of Botne- heia (M-24) and lowest part of Tscherma&ellet (M-33) formations

Oil shale member, Oil shale series (Lock et al. 1978; Falcon 1928): Correlative of Botneheia Formation (M-24) on the eastern islands

Oozy mound beds (Gregory 1921): Upper part of Botne- heia Formation (M-24), overlying "Escarpment shales"

Passage unit (Klubov 1965): Upper part of Tschermak$ellet Formation (M-33) on the eastern islands, between "Argilite" and "Sandstone units"

Pityophyllum-Schichten, P. Niveau (Nathorst 19 10; Hoe1 & Orvin 1937): A thin horizon within the HelvetiaJellet Formation (M-89), between "Lioplaxschichten" and "Ginkgoschichten"

Plateau flags (Gregory 1921): Corresponds to the De Geer- dalen (34-34) and Knorrindellet (M-43) formations in central Spitsbergen

Posidonomyenkalk, Posidonomyenschichten (MojsisoviEs 1886; Nathorst 1910): Corresponds roughly to the middle part of the Vikinghegda Formation (M-13)

Pseudomonotisskifer, P.kalk (Lundgren 1887): Section in the upper part of Vardebukta Formation (M-02), 130 m above "Myalinaskifer"

Ptychites beds (Spath 1921): Lower part of Botneheia For- mation (M-2.4)

Retziakalk (Lundgren 1887): Synonym of Skilisen Bed (M-12)

Sandsteinreihe (Nathorst 1910): Synonym of Helvetia- Jellet Formation (M-89)

Sandstone and shale series (Falcon 1928): Corresponds to the De Geerdalen Formation (M-34) and E3lhelmqva Sub- p u p (M-38) on the eastern islands

Sandstone unit (Klubov 1965): Synonym of De Geerdalen Formation (M-34) on the eastern islands

Saurian bed (Spath 1921): A section within the Viking- hegda Formation (M-I3). between "Lower" and "Upper Posidonomya shales7'

Shore sandstone (Hagerman 1925): Synonym of "Glitre- fjellet Member", or the part of HelvetiaJellet Formation (34-89) overlying the Festningen sandstone member (M- 90)

Transitional beds (Smith 1975): Corresponds roughly to the Svenslwya Formation (M-47) on Wilhelmraya and eastern Spitsbergen ("Transitional member" of Worsley 1973)

Transitional member (Worsley 1973): Corresponds roughly to the upper part of the Flatsalen Formation (34-46) on Wilhelm~ya and eastern Spitsbergen

Unteres Saurierniveau (Wiman 1910): Upper part of Endomdalen Member (M-16), Vikinghegda Formation (34-13)

Upper Continental Series (Birkenmajer 1975): Upper part of Helvetia$ellet Formation (M-89), roughly corresponding to the "Glitrefjellet Member"

Upper lamina sandstones (Hagerman 1925): Upper three members of CarolineJellet Formation (M-93), the Langstakken (M-96), Zillerberget (M-97) and Schonrock- Jellet (M-98) members

Upper nodule beds (Gregory 1921): Synonym of Tscher- ma&ellet Formation (M-33)

Upper Posidonia (Posi'donomya) shales (Spath 192 1): Part of the Keyserlingite subrobustus Zone of Vardebukta (M- 02) and Vikinghegda (M-13) formations

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4. TERTIARY LITHOSTRATIGRAPHY

WINFRLED K. DALLMANN, PETER S. MDBOE, ARVID NDTTVEDT & RON J. STEEL


The Tertiary rocks of Svalbard are confined to several individual, probably isolated basins. The 18 formations and two additional, informal units are traditionally grouped according to their association with these basins (Figs. 1-05,4-01, 4-03). This grouping is maintained herein and extended to comprise all of the Tertiary formations of Svalbard.

The Central Tertiary Basin is the largest and most prominent of the Tertiary basins. Although the name refers to the present structural depression, it indicates also the remainder of the syn-orogenic foreland basin of a Tertiary fold-thrust belt. Its sedimentary rock formations of Paleocene to Eocene age cover large areas of southern and central Spits- bergen (Figs. 1-04,4-04,4-05). The seven formations constituting the Tertiary clastic infill of this basin are grouped under the name Van MijenBorden Group (Harland 1969).

The minor occurrence of Tertiary rocks in the Tertiary fold-bust belt in the Kongsfjorden area (northwestern Spitsbergen) is now with great probability correlated with strata of the Central Tertiary Basin. The rocks there are grouped as the Ny-,+!lesund Subgroup (from "Ny-aesund Formation", Challinor 1967) and included in the Van Mijen- jorden Group.

A separate depositional basin containing Eocene to Oligocene strata is preserved on western Spitsbergen and Prim Karls Forland in the Forlandsundet Graben (Figs. 1- 05, 4-06). The graben is a younger overprint of an older, syn-depositional structure, possibly a pull-apart basin, situated in the hinterland of the main Tertiary fold-thrust belt. The former group name "Forlandsundet Group" (Harland 1969) for the eight clastic formations and informal stratigraphic units of the basin reflects an inconvenient double use of the place name 'Forlandsundet'. This name has been established m the geological Literature for the post-sedimentary graben structure, and a new name for the stratigraphic group is introduced here: Buchananisen Gmp, named from

jor glacier developed between the various outcrops of L sedimentary succession. A third sttatigraphic group is &fined to embrace the two

Tertiary formations of the Renardodden area at Bellsund,

southwestern Spitsbergen: Ca2ypsostranda Group (Figs. 1- 05,4-M), named from the marine terrace south of Bellsund covering most of the onland occurrences of the group. An original connection of their depositional basin with that of the Buchananisen Group is possible, but speculative.

Miocene-Pliocene volcanic flows occur on mountain tops on northern Spitsbergen (Fig. 4-07). These are assigned to a single formation, the Seid!ellet Formation, and are not in-, cluded in any stratigraphic group.

A conglomerate on northwestern Prins Karls Forland (Fig. 4-06), the Sutorjella conglomerate, has been proposed to have Precambrian, Devonian or Tertiary age. The age question is still open, and the conglomerate is preliminarily not included in any superior lithostratigraphic unit.

4.2 Previous stratigraphic schemes

The stratigraphic schemes of the individual basins or stratigraphic groups have developed independently. For the Cen- tral Tertiary Basin, the first six-fold subdivision by Nathorst (1910) and the first seven-fold subdivision by LjutkeviE (1937a) have remained valid through this century for all subsequent work in Norway and the Soviet Union, respectively (Fig. 4-02). The presently proposed nomenclature is a synthesis of the Norwegian and Russian schemes, modified according to the present stratigraphic understanding.

The twofold subdivision of the Tertiary of the Kongs- fjorden area was established by Orvin (1934) and has been used by all subsequent authors (Fig. 4-02) with a gradually developing, additional member subdivision. The contradict- ing use of the place name '~y-hesund' is now decided in favour of its first application by Challinor (1967) for the entire succession.

The subdivision of the Tertiary strata of Forlandsundet has gradually been developing fiom three (Atkinson 1963) to eight (Rye Larsen 1982, unpubl.) formations (Fig. 4-02). A revision pyoposed here is the informal rank of the poorly understood conglomerates east of Forlandsundet.

Fig. 4-01: Group and subgroup subdivision of the Tertiary rocks

--=J LALYPSO- BUCHAN- VAN MIJENFJORDEN -- lavas

STRANDA ANISEN GROUP GROUP affiliation

Nykesund undifferentiated Subgroup

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Famat@ 1 Formation l Formation I Gbnry~gsn Mb.

I

I I . .

McVitie(pynten) Formation

I Reinhardpynten I Rein hardpynten Formation Formation

I Sesshegda I Sesshqda Formation Formation

Fig. 4-02: Previous and proposed stratigraphic schemes for the Ter- tiary showing the formation and member levels. The tables are sorted according to area and present the general development of the lithostratigraphic nomenclature. The references do not necessarily indicate that the author@) introduced the individual names. In each table, the column to the right shows the presently recommended scheme.

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Paleocene

QRQUP:

Formation

-7 elvagen Fm. -3-

Kongsfjorde

4 Bocwrden Volcanic Complex

Fig. 4-03: Proposed lithostratigraphic scheme for the Tertiary of Svalbard. The diagram contains all names recommended by SKS at group, subgroup, formation, member and bed levels. Member and bed names in italics represent informal units. The ages and age boundaries of the units are indicated in accordance with existing data, but are admittedly schematic (see age discussions in section 4.4). Possible diachronous boundaries are drawn straight unless reliable data can document the diachronism. The age of the Buchananisen Group is not well-established, but is here applied h m Livgic' (1967, 1974) interpretations. The indicated major hiati are also drawn schematically and do not claim any precision concerning their age range. Minor hiati are omitted.

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4.3 Regional descriptions and major revisions 03). Relations are clarified by an appropriate subdivision into members.

4.3.1 Central Tertiary Basin The 0yrlandet area shows Tertiary strata preserved within a southerly dipping halfgraben. Lithostratigraphic correla-

The Central Tertiary Basin (Fig. 1-05) forms a NNW-SSE tion with the Firkanten Formation in the southern termina- trending synclinorium in southern and central parts of the tion of the Central Tertiary Basin outcrops seems obvious island of Spitsbergen, infilled with clastic rocks. The basin (Dallmann et al. 1993). axis is asymmetrical and lies close to the western margin of the preserved part of the basin. The eastern basin limb dips gently (0-6Y), the western limb more steeply (5-30Y), to- 4.3.2 KongsJjorden area wards the basin axis. The original sedimentary basin must have covered a considerably larger area. The Tertiary sedi- On the southwestern shore of Kongsfjorden, clastic Tertiary ments overlie strata of progressively younger Early Creta- strata occur in a tectonic block within the Tertiary fold-and- ceous age towards the southeast. The Tertiary sedirnents are thrust belt (Fig. 4-06). These unconformably overly Triassic clastic, mostly sandstones and shales, coal-bearing in the and Permian rocks and are assigned to the ~~-.t!lesund Sub- lowermost and uppermost parts, representing delta-related p u p . These strata are mostly considered to be correlatives shelf sedimentation of Paleocene to Eocene age. The upper of the lower part of the Van Mijenfjorden Group in the Cen- part of the succession shows transport directions from the tral Tertiary Basin (Midb~le 1985), although LivSic (1967, SSW and is thought to indicate the uplift of the Western 1973, 1974, 1992) regards the Tertiary of Kongsfjorden as Basement High. Six of the seven formations are traced the remainder of a separate basin of younger age. Because throughout the area; all seven are collected within one of the disagreements about the correlation, it is suggested group (Van MijenBorden Group, Harland 1969), overlying use of separate formation names for these two areas, but Early Cretaceous strata with a stratigraphic unconformity of include the strata in the Van Mijenfjorden Group. 0.5-1Y. Challinor (1967) introduced the name "Ny-Besund For-

The two almost equivalent stratigraphic subdivisions of mation" for the entire Tertiary of the Kongsfjorden area. No the Van Mijenfjorden Group by Major & Nagy (1964,1972) proper definition was given, although he referred to the de- and Livlic (1967, 1974) (Fig. 4-02) should be considered as tailed description of Orvin (1934), redefining only the base contemporanously published. There was a significant delay of the succession by excluding the "Bottom Shale'" that he in the publication process of the first mentioned work, found to be of Triassic age. which - in spite of its listed year of publication (1964) - ac- Recent work (LivSic 1973, 1974; Midbse 1985, unpubl.; tually was not p@nted before 1967. Furthermore, communi- and several subsequent theses) has shown that a twofold cation between geologists of the western countries and the subdivision of the Kongsfjorden succession is convenient Soviet Union was difficult at that time. Both stratigraphic and consistent with the criteria used for the subdivision of subdivisions are well established in the western and eastern the Central Tertiary Basin (LivSic 1973: Kongsfiorden For- literature, respectively. The principle of priority through mation and 'Wy-kesund Formation"; Fig. 4-02). LivSic first publication is therefore disregarded. The present re- (1973) made a formal mistake when he used the name "Ny- commendation is based on establishment of names in the kesund" for only half of the succession that the name was geological literature and on maps, completeness of name- introduced for. The name should be reserved for the entire giving sections and - where no other distinguishing criteria Tertiary succession of the Kongsfjorden area an4 conse- exist - better accessibility to the name-giving localities. The quently, must have subgroup rank. recommended use of formation names is thus based on the The need for a new formation name for the upper part of Norwegian scheme in the lower (Firkanten Formation, Basi- the succession met the lack of suitable place names that lika Formation) and upper levels (BatFtjellet Formation, have not already been used for the members of the forma- Aspelintoppen Formation) of the Central Tertiary Basin, but tion. Type sections, however, are boreholes in the moraines on the Russian scheme in the middle part (Grumantbyen and fluvial fans developed at the fronts of the glaciers Formation, Hollendardalen Formation, Frysjaodden For- 'Austre' and 'Vestre Brsggerbreen'. Broggerbreen Forma- mation). The formational subdivision reflects in general the tion is therefore proposed herein as a new name for the altemaing sandstone and shale dominance in the succession. upper unit of the Ny-Alesund Subgroup.

A redefinition of some of the middle part of the succes- The names 'Kongsfjorden' and 'Brsggerbreen' for the two sion is suggested due to newly acquired data on the rela- Tertiary formations fit well, using relatively major geo- tionships between the sandstone wedge of the Hollendar- graphical features for this important (though poorly ex- dalen Formation and the shales of the Frysjaodden posed) coal-bearing unit, the fiord name describing the Formation. The name Hollendardalen Formation is recom- lower, and the glacier name describing the upper formation. mended to be used for the sandstone body only. This involves a slight redefinition of the base of the Hollendar- dalen Formation which originally (LivSic 1967) included 4.3.3 Forlandsundet Graben shales underlying the sandstone wedge. Later mapping showed that these shales are part of the Frysjaodden Forma- Tertiary clastic strata are exposed within the Forlandsundet tion, divided from the main part of this formation by the Graben on the western coast of north-central Spitsbergen sandstone wedges of the Hollendardalen Formation (Fig. 4- and, particularly, on northeastern PMS Karls Forland (Figs.

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1-05,4-06). The Forlandssundet Graben shows only part of 4.3.4 Renardodden area the strata that were deposited within a larger sedimentary basin of possible partly pull-apart origin (Gabrielsen et al. A fault block southwest of Bellsund, at Renardodden, con- 1992). These are clearly different from the Central Tertiary sists of clastic, coal-bearing Tertiary strata unconformably Basin strata in facies and age (Eocene-Oligocene). They overlying Precambrian basement, and representing the Ca- form an individual group which consists of seven forma- lypsostmnda Group (Fig. 4-04). A structural connection tions of unknown continuity, laterally replacing each other with the depositional area of the Forlandsundet Graben is &the surface sections. They unconformably overlie Pre- possible, though the strata of both areas cannot be corre- cambrim basement. Most of the formations display incom- lated. LivBic (1967) defined the underlying Skilvika Forma- plete stratigraphic sections. The stratigraphic nomenclature tion and the overlying Renardodden Formation, both in this area was first established by Atkinson (1962, 1963) forming clastic fining-upward sequences, and mainly dis- who defined the basal conglomeratic Selvdgen Formation tinguished by the high number of coal seams in the lower and the sandstone-shale dominated "McVitie Formation". formation. The exposed area is situated close to a long-lived LivBic (1967) subdivided the "McVitie Formation" into the fault zone that may have been active since Caledonian times Sesshtagda, Reinhardpynten, Krokodillen and Marchaisla- (Dallmann 1989). guna formations, and Rye Larsen (1982, unpublished) added the uppermost sandstone-shale unit, the Aberdeenj7ya Formation (Fig. 4-02). 4.3.5 Plateau b a s e

The name "McVitie Formation", later changed according to the correct place name "McVitiepynten Formation" Within the Devonian graben of northern Spitsbergen, Ter- (Birkenmajer 1981), is redundant, because there is no rea- tiary plateau basalts (Seid8ellet Formation) unconformably son to summarise the three constituent units while exclud- overlie Devonian and Precambrian rocks (Fig. 4-07). A cor- ing the underlying SelvAgen Formation. relation with the isolated basalt exposure at Manbreen in Ny

In contrast to Livgic (1967, and subsequent publications), Friesland, outside the graben, is tentative. we suggest keeping the stratigraphic nomenclature of the The name SeidBellet Formation (defined here) is pre- poorly exposed Tertiary to the east of Forlandsundet sepa- ferred instead of the better known place name and type lo- rate from that of Prim Karls Forland. Correlations between cality 'Tavlefjellet' which has been used for a Devonian for- the two areas are not established with any certainty. Docu- mation (MuraSov & Mokin 1976). mentation is poor and the base of the succession is not known. An informal name, Balsnuspten conglomemtes, is here proposed to replace the incorrect earlier name "Sars Formation" (AtStinson 1963). These conglomerates actually belong to two sedimentary successions differing considerably in texture, limcation and probable age (Sarsbukta and Sarstangen conglomerates).

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4. TERTIARY LLTHOSTRATIGRAPHY

rl

i-

\

Frysjaodden Frn. ;;b$]orden

Grurnantbyen Fm.

Baslllka Formation

Late Palaeozoic cover rocks

Fig. 4-04: Distribution map T-I: Tertiary of the Central Tertiary Basin, southern part, and the Renardodden area

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4. TERTIARY LITHOSTm^"GRAPHY

Fig. 4-05: Distribution map T-11: Tertiary of the Central Tertiary Basin, northern part

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4. TERTIARY LITHPCTDAriCDADUv

Fig. 4-06: Distribution map T-IIL Tertiary of the Forlandsundet and Kongsfjorden areas

U 1 Relnhardpynten Fm.

~~esshegda~annatlon

' deb3OZdC c0vW rocks l

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Fig. 4-07: Distribution map T-IV Tertiary and Quaternary volcanic rocks, northern Spitsbergen

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4.4.1 Van Mijenflorden Group

VAN MIJENFJORDEN GROUP (T-01)

STATUS OF UNIT: Formal FIRST USE OF NAME: Harland 1969 CURRENT DEFINITION: Harland 1969; extended here to include the ~y -kesund Subgroup SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Van Mijenfjorden: A fiord in south- central Spitsbergen TYPE AREA (FIG. 4-10): Southern coastal areas of Van Mijentjorden, south-central Spitsbagen STRUCTURAL SETTING: Preserved mainly in the post-depositionally formed Central T d a y Basin, and in a tectonic block within the West spitsbefgen Fold-thrust Belt on Br0ggerhalv~ya (Kongsfjorden area) DEPO~ITIONAL AGE: Paleocene- Eocene (? to Oligocene)

Earlier interpretations of Miocene age of the Tertiary of Spitsbergen (Heer 1868, 1870) have been questioned since the bivalve work of Ravn (1922) and are directly negated by the results of modern palynological and micropalaeontolog- ical studies (Manum k Throndsen 1986; Nagy, pen. comm. 1998). LivSicYs (1973, 1974) age determinations based on invertebrates, plant remains and palynology, are in general slightly younger than those suggested by the Norwegian workers for the middle and upper parts of the Van Mijen- fjorden Group. OVERLYING UNIT(S): None UNDERLYING UNIT(S): Adventdalen Group; in Kongsfjorden area: Sassendalen or Tempelfjorden Group SUPERIOR UNIT: None -R USE OF NAME: None THICKNESS: Up to 1900 m preserved MAIN LITHOLOGIES: Sandstone, siltstone, shale DESCRIPTION: The Van Mijenfjorden Group is a clastic sedimentary succession consisting of sandstones, siltstones, shales and subordinate coals and conglomerates. It comprises all Tertiary sedirnents in the Central Tertiary Basin of Spitsbergen (Figs. 4-08,4-09), including Tertiary exposures on Byrlandet and Erdmannflya, and the Ny-aesund Sub- group of the Kongsfjorden area. For descriptions see Firkan- ten, Basilika, Grumantbyen, Frysjaodden, Hollendardalen, Battfjellet, Aspelintoppen, Kongsfjorden and Brarggerbreen formations.

Fig. 4-08: Liljevalchfjellet and the coal mine Sveagruva, showing the lower part of the Van Mjenfjorden Group. The mine entrance to the right is close to the base of the Firkanten Formation which termi- nates above the sandstone of the Endalen Member (lowermost exposures). It is overlain by the dark shales of the Basilika Formation and the monotonous sandstones of the Grumantbyen Formation (ridge). Photo: J. Nagy

Fig. 4-09: Krokryggen at Van Mjenfjorden, showing the upper part of the Van Mijenfjorden Group. The foreground consists of Gilson- ryggen shales, grading into the sandstone-bearing Battfjellet Forma- tion. Above (ridge below and behind the long snow field), the sandstones and shales of the very thick Aspelintoppen Formation are visible in the background. Photo: W.K. Dallmann

The basal Firkanten Formation of the Van Mijenfjorden Group contains the most important coal deposits of Sval- bard (Longyearbyen, Barentsburg and Sveagruva; Fig. 4- 08).

The upper part of the Van Mijenfjorden Group is a pre- sumable time equivalent to the lower part of the Buchanan- isen Group of the Forlandsundet Graben. The overlap includes the Battfjellet and Aspelintoppen formations (Steel et al. 1985) and possibly also the Frysjaodden Formation (Gilsonryggen Member; LivSic 1967, 1974). The Firkanten and Basilika formations are thought to be correlative with the Kongsfjorden and Brsggerbreen formations (Midbse 1985.

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ag6llith.shPt m unk


Fig. 4-10: Stratigraphic section T-01 Composite section for: Van Mijenfjorden Group Locality: Central Tertiary Basin Reference: Ohta et al. 1992, modified from Spielhagen 1985

DISTRIBUTION SHOWN ON FIG(s).: 4-m,4-05 STATUS OF UNIT: Formal FIRST USE OF NAME: Major & Nagy 1964 CURRENT DEFINITION: Major & Nagy 1972 SYNONYM(S) AND REFERENCE@): "Lower light sandstone series": Nathorst 1910; "Lower coal-bearing sandstone h.": LjutkeviE 1937a; "Barentsburg Formation": Livgic 1967. The contemporaneously published name Firkanten Formation (Major & Nagy 1964,1972) is preferred because of its more extensive use in the published literature on this unit (see Section 4.3.1). ORIGIN OF NAME: Firkanten (transl.: "The Rectangle"): A mountain in Nathorst Land, south-central Spitsbergen TYPE SECTION (FIGS. 4-14,615,4-17,4-19): Stratotype: Karl Brryfjellet (composite section) DEPOSITIONAL AGE: P d e ~ ~ e n e DATING METHOD: Bivalves; plant remains; palynology RERERENCE(S) FOR AOE: h 1922; Li~gic 1973, 1974; Manum & Throndsen 1986 (m Van Mijenfjorden Group) OVERLYING UNIT(S)S P)itsilika Formation w l ': r ' , . . UNDERLYING UNIT(S): Carolinefjellet Formation SUPERIOR UNIT: Van Mijenfjorden Grouy) -R USE OF NAME: None THICKNESS: 100-170 m, ca. 125 m in the stratotype MAIN LITHOLOGIES: Sandstone, shale, coal LOWER BOUNDARY DEFINITION: The base of the Firkanten Formation is marked by the low-angle unconformity above the Lower Cretaceous Carolinefjellet Formation. Where no basal conglomerate or palaeo-weathering surface is developed, the base may be hfficult to recognise, although the basal sandstones are softer or more massive than the underlying Cretaceous platy and well-laminated sandstones. DESCRIPTION: The Firkanten Formation is 170 m thick in type area, thinning northeastwards to less than 100 m thick. A basal conglomerate often defines the base (Fig. 4-11). The lower part of the formation is characteristically coal- bearing (less marked in the south), with interbedded marine and non-marine sandstones, siltstones and shales. The upper part is sand-prone in the north and northeast, consisting of light, well-bioturbated or laminated marine sandstones interbedded with minor conglomerates, siltstones and clay ironstones. In western and southern regions the same interval contains southwesterly thickening wedges of shales and siltstones, especially in its lower and middle portions.

The Firkanten Formation contains the most important pro- ductive coal deposits of Svalbard (Longyearbyen, Barents- burg and Sveagruva; Fig. 4-12).

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4. TERTIARY LITHOSTRATIGRAPHY -

Fig. 4-11: Cretaceous-Tertiary boundary at Grsnijorden, across the Fig. 4-13: Coal seam in the Todalen Member (Firkanten Formation), fiord from Barentsburg. The basal Tertiary strata, the Grsnfjorden Longyearbyen. Photo: J. Nagy conglomerate, begins to the left of the hammer. Photo: A. Msrk

Stratotype: Bayfjellnosa, Todalen N, close to Longyearbyen, -1 Nordenskiold Land

Fig. 4-12: The abandoned coal mine "nye gruve 1" at Longyearbyen. The mine entrance is in the Todalen Member (Fikanten Formation), while the photograph shows the section upward to the massive sand-

stones of the Endalen Member and the base of the overlying dark shales of the Basilika Formation. Photo: W.K. Dallmann

The unit shows a systematic thickening and deepening of facies from the north and northeast to the south and west. The lower, coal-bearing part is deltaic in origin and represents a stacked series of units interpreted as deltaic lobes. The upper part is more thoroughly marine and apparently represents a series of barrier shoreline developments. The overall transgressive trend in the unit, with coastline retreat towards the east and northeast, is typical for the earliest infill of foreland basins.

rodalen Member (T-03)

STATUS OF UNIT: Formal FIRST USE OF NAME: Steel et al. 1981, after Kalgraff 1978 (unpubl.) CURRENT DEFINITION: Steel et d . 1981 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Todalen (transl. "The No. 2 Valley"): A tributary valley to Adventdalen, close to Longyearbyen

Hypostratotype: Rqsklumpen, Kjellstrrmdalen, Heer Land DEPOSITIONAL AGE: Paleocene DATING METHOD: Palynology REFERENCE(S) FOR AGE: Manum & Throndsen 1986 OVERLYING UNIT(S): Endalen and Kolthoflberget members UNDERLYING UNIT(S): Carolinefjellet Formation SUPERIOR UNIT: Firkanten Formation OTHER USE OF NAME: None THICKNESS: 53 m in the stratotype MAIN LITHOLOGIES: Sandstone, shale, coal LOWER BOUNDARY DEFINITION: See Firkanten Formation DESCRIPTION: The unit consists of some 3-5 rhythrmc successions of shale-siltstone-sandstone-coal in the northeastern part of the Central Basin. Coals and shales can dominate north of Adventdalen, whereas bioturbated marine sandstones and shales are common south of Van Mijenijorden. The base of the unit is defined either by basal conglomerates and conglomeratic sandstones (Grmijorden conglom-. erate), or, where these are absent, the depositional contact with the underlying Cretaceous strata.

The Todalen Member contains the most important pro- ductive coal deposits of Svalbard (Longyearbyen, Barents- burg and Sveagruva; Figs. 4-08,4-12,4-13).

The unit thickens and shows a slight deepening of depositional environment to the west. Rhythrmc successions represent repeated progradation and retrogradation of deltaic systems which built out mainly from the northeast and east of the basin. A marked structural horst separated subbasins north and south of Van Mijenfjorden.

Granfjorden Bed (T-04)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE@): None ORIGIN OF NAME: Grsnfjorden (transl. "The Green Fiord"): A fiord in northwestern Nordenskiold Land

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4:TERTIARY LITHOSTRATIGRAPHY

Endalen

m - dsivf f mcvcg pcbb

K , & ; ; a m o e - " & 2 l - 0 2

,',-Ha

l - n < e

Carollnefpllet Fonnatlon

(Cretaceous)

Fig. 4-14: Stratigraphic section T-03a Stmtotypefor: Todalen Member Locality: Bayijeilnosa Refrence: Steel, R. (unpubl.), modified h m Kalgraff 1978 (unpubl.)

Endalen Member

-xcp ix r unlts

Member (Paleocent

2 0 Y

m Z "

ec & Cf

C4

< k

z :

IIIIIIIIIII clslvf f rncvcg pcbb

Fig. 4-15: Stratigraphic section T-03b Hypstmtotypefbr: Todalen Member Locality: Rprysklumpen Refireme: Nemec, in Steel et al. 1989

>

l- K

7 units

K " G ( m 0 - " F 4 2

" , - H *

' - n * t I

Carolinefprllet Fonnat~on

(Cretaceous)

(Palaoceng)

z 0

H

= M

0 2 m p l 2

= R :

M

E

-

a

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Kolthoftberget Member (T-05)

Z 0 CI

H

i-

5 P,

Ilth. clsivf f rncvcg pcbb

Fig. 4-16: Stratigraphic section T-04 Strutotype for: Grcsnfjorden Bed Localiry: Grmfjorden NW Refemnce: Steel, ip Ohta et al. 1992

u n k

C , 2: g : P,z: ; % S Z : : < b G '

strat

TYPE SECTION (FIG. 4-16): Stratotype: Grsnfjorden NW, northwestern Nordenskiold Land DEPOSITIONAL AGE: Paleocene DATING METHOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: See Firkanten Formation OVERLYING UNIT@): Not named UNDERLYING UNIT(S): Carolinefjellet Formation SUPERIOR UNIT: Todalen Member OTHER USE OF NAME: None THICKNESS: 0-5 m, 4 m in the stratotype MAIN LITHOLOGIES: Conglomerate LOWER BOUNDARY DEFINITION: The base of the unit is defined by the development of conglomerate above platy Cretaceous sandstones. DESCRIPTION: The Grmfjorden Bed is only irregularly developed as a basal conglomerate interval across the basin, reaching a maximum of more than 4.5 m at the northwestern corner of Grmfjorden in the type area (Fig. 4-1 1). The bed consists of clast-supported and matrix-supported conglomerates, conglomeratic sandstones and associated sandstones and has been recorded up to 2 m thick in the northeast (Bassen, Konussen) as well as along the western edge of the basin as far south as Van Mijenfjorden (Kolfjellet).

The basal conglomerates and associated sandstones probably represent an incised valley within the underlying Cre- taceous land surface, infilled by alluvial processes.

228

-

P3

9 G

-

STATUS OF UNIT: Formal FIRST USE OF NAME:

Steel et al. 1981, after Kalgraff 1978 (unpubl.) CURRENT DEFINITION: Steel et al. 1981 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Kolthoffberget: A mountain on the northern coast of Van Keulenfjorden, Nathorst Land TYPE SECTION (FIG. 4-17): Stratotype: Kolthoffberget, Nathorst Land DEPOSITIONAL AGE: Late Paleocene DATING METHOD: Agglutinated foraminifera REFERENCE(S) FOR AGE: J. Nagy @ers. comm. 1998) OVERLYING UNIT(S): Endalen Member, Basilika Formation UNDERLYING UNIT(S): Todalen Member SUPERIOR UNIT: Firkanten Formation OTHER USE OF NAME: None THICKNESS: Up to 120 m, 98 m in the stratotype MAIN LITHOLOGIES: Shale, sandstone LOWER BOUNDARY DEFINITION: The lower boundary is defined by the base of a shale-dominated succession overlying the upper sandstones of the Todalen Member. DESCRIPTION: The unit is developed only in the western and southern parts of the basin and reaches a thickness of about 120 m on Kolthoffberget. It is a fine-grained lateral equivalent to the Endalen Member and consists of repeated rhythmic successions of shales. Organic rich, very fine sandstones also occur in the type area on Kolthofierget. The sandstones are always extremely bioturbated and individual successions are less than 10 m thick. Where present, the unit overlies the coal-bearing Todalen Member and underlies the youngest sandstone tongues of the Endalen Member (if present) or interfingers with the Basilika Formation.

The member represents repeated shoaling-upward conditions on the pro-deltaic or shelf areas of the Central Tertiary Basin.

Endalen Member (T-06)

STATUS OF UNIT: Formal FIRST USE OF NAME: Steel et al. 1981, after KalgraR 1978 (unpubl.) CURRENT DEFINITION: Steel et al. 198 1 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Endalen (transl. "The No. 1 Valley"): A tributary valley of Adventdalen, close to Longyearbyen TYPE SECTION (FIG. 4-19): Stratotype: Bayljellnosa, Todalen N, close to Longyearbyen, Nordenskiald Land DEPOSITIONAL AGE: Paleocene DATING METHOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: See Firkanten Formation OVERLYING UNIT(S): Basilika Formation UNDERLYING UNIT($): TOdalen or Kolthomerget members SUPERIOR UNIT: Firkanten Formation OTHER USE OF NAME: None THICKNESS: 40-100 m, 72 m in the stratotype MAIN LITHOLOGIES: Sandstone

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4. TERTIARY LlTHOSTRATlGRAPHY

Fig. 4-17: Stratigraphic section T-05 Strutotype for: Kolthoffberget Member Locality: Kolthoffberget Reference: Steel, R (unpubl.), modified fiom Kalgraff 1978 (unpubl.)

Fig. 4-18: Sandstone of the Endalen Member (Firkanten Formation) with typical convolute bedding. Kapp Hesselman, Van Keulen- fjorden. Photo: W.K. Dallmann

LOWER BOUNDARY DEFINITION: The base of the member is marked by the first thick, medium-grained, cliff-forming sandstone above the coals and shales of the underlying To- dalen or Kolthoffberget members. DESCRIPTION: The Endalen Member is some 70 m thick in its type area, but otherwise varies from 40 m (northeast) to 100 m (south and southwest). It consists of a stacked series of 4-5 sandstone intervals which oRen show an upward- coarsening trend in the northeastern part of the area. The sandstones form prominent cliffs (Fig. 4-12,4-18) and are well bioturbated or cross-stratified, with interbedded thin conglomerates, clay ironstones and minor shales. In the west of the basin and south of Van Mijenfjorden the unit becomes thicker and interfingers with the shale-prone Kolthoffberget Member.

The Endalen Member thickens considerably and shows a deepening of facies to the west and south in the basin. Component sandstone intervals represent transgression and regression of a deltaic or barrier shoreline which built out repeatedly from the northeast.

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Basilika Fonnation

(Paleown*

0 0

B 0

Z n U 4

e?J U @ ia

a E H

)c J4

a:: 4 e a - e h + O X a w @ - h

0 6- P -4-

M z R

I

0

d B 0

z d 0 4

m a 0

F

clsivf f mcvcg pcbb

DISTRIB~ON SHOWN ON FIG(s).: 4-04,4-05 STATUS OF UNIT: F o ~ FIRST USE OF NAME: Major & Nagy 1964 CURRENT DEFINITION: Major & Nagy 1972 SYNONYM(S) AND REFERENCE(S): "Lower , black shale series": Nathorst 1910; 'Zower black shale formation": LjutkeviE 1937a; "Colesbukta Formation": LivBic 1967. The contemporaneously published name Basilika Fonna- tion (Major & Nagy 1964, 1972) is preferred because of its more extensive use in the published literature; it is also more completely exposed at the mountain Basilika (see Sec- tion 4.3.1). ORIGIN OF NAME: Basiliha (tr-ansl.: "Basilica"): A mountain in northeastern Wedel Jarlsberg Land, Van Keulenfjorden, south-central Spitsbergen TYPE SECTION (FIG. 4-20): Stratotype: Akselvarden, Nordenskiold Land DEPOSITIONAL AGE: Late Paleocene DATING METHOD: Palynology, agglutin. for-era REFERENCE(S) FOR AGE: Manum & Throndsen 1986; J. Nagy (pers. comm. 1998) OVERLYING UNIT(S): Grumantbyen Formation UNDERLYING UNIT(S): Firkanten Formation SUPERIOR m: Van Mijenfjorden Group O ~ R USE OF NAME: None THICKNESS: 10-350 m, 270 m m the stratotype MAIN LITHOLOGIES: Shale, mudstone, siltstone LOWER BOUNDARY DEFINITION: The base of the unit is well defined by thick shales which overlie the uppermost sandstone beds of the Endalen Member. DESCIUPTION: The Basilika Fonnation thickens from about 10 m in the northeastern region to more than 300 m in westem Nordenskiold Land and more than 350 m in western Torell Land. It consists primarily of shales, mudstones and siltstones, usually organised in repeatd, thin upward-coarsening successions. Rounded dropstones of metamorphic basement and dolerite lithologies are common, as well as bentonitic interbeds.

The unit represents muddy shelf conditions, with repeated influx of silty sediments from the east and northeast, the lat-

- ter caused by repeated shoaling in the northeasterly reaches of the basin.

Fig. 4-19: Stratigraphic section T-06 Stmtotype for: Endalen Member Locality: Endalen, Karl Bayfjellet Reference: Steel et al. 1981

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(Palmne)

z 2 i+

* m 4 K c z sod - 0 0 + o h

W - , +: 7n

4 m

- Firkanten Formetion

(Paleocene)

age I lii. StRlt l units

Fig. 4-20: Stratigraphic section T-07 Stmtofype for: ,Basilika Formation Localify: Akselvarclen Refemnce: Nagy, J. (unpubl.)

cldvf f mcvcg pcbb

DISTRIBUTION SHOWN ON h*).: 4-04,4-05 STATUS OF UNIT: Formal FIRST USE OF NAME: Livgic 1967 CURRENT DEFINITION: Steel et al. 1981 SYNONYM(S) AND REFERENCE(S): " h e n sandstone formation": LjutkeviE 1937a; "Grumant Formation": Livgic 1967 The place segment of the name was first completed by Steel et al. 1981. The Grumautbyen Fonnation is equivalent to the lower part of both the "Green sandstone series" (Nathorst 1910) and of the ''Smkofagen Formation" (Major & Nagy 1964, 1972). ORIGIN OF NAME: Grumantbyen: An abandoned Soviet coal mine on the coast of Isfjorden, Nordenskiold Land, central Spitsbergen TYPE SECTION:

Stratotype: Grumantbyen, Nordenskiold Land DEPOSITIONAL AGE: ?Paleocene - ?Eocene DATING METBOD: Indirect, stratigraphic rehtionship REFERENCE(S) FOR ACE: L-C 1973, 1974; M m & Throndsen 1986 (W Van Mij@aden Group) OVERCYING mm(@$ E r y s j ~ n F o m t i o n UNDERLYING UNIT@): B d h Formation SUPERIOR UNIT: Vm Mjedjorden Group -R USE OF NAME: None THICKNESS: 0-450 m lMAIN LITHOLOGIES: Sandstone LOWER BOUNDARY DEFINITION: The base of the unit is gradational from the shales and siltstones of the Basilika For- mation, but is defined by the incoming of greenish, bioturbated, silty sandstones. DESCRIPTION: The unit is some 450 m thick in the northeast and east of the Central Tertiary Basin, but thins to less than 200 m to the west and southwest. Relations in the southemmost reaches of the basin are not quite clear yet, but the formation possibly pinches out completely to the south to be replaced by an upward coarsenipg trend in the underlying siltstones of the Basilika Formation. The Grumant- byen Formation consists of a greenish, massive and highly bioturbated sandstone. The upper part of the unit becomes finer grained, with a rhythrmc development of siltstone to silty sandstone motifs.

The origin of the Grumantbyen Formation is still problematic. It has been little studied but its glauconitic, bioturbated and massive character, together with lack of evidence of any subaerial facies, suggests an entirely submarine, shelfal origin.

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DISTRIBUTION SHOWN ON FIG(s).: 4-04,4-05 STATUS OF UNIT: Formal FIRST USE OF NAME: LivBic 1967 CURRENT DEFINITION: Here The present redefiition changes the original base of the formation, but only m western areas of the Central Tertiary Basin, to include the shaley Marstranderbreen Member. The latter is included because of its lateral correlation with the southern and eastern exposures of the Frysjaodden Forma- tion which remain unchanged fiom its original definition. SYNONYM(S) AND REFERENCE(S): "Upper black shale series": Nathorst 1910; ''Upper black shale formation": L j u W E 1937a; "Upper argillite formation": Livgic 1965; "Gilsonryggen Formation": Major & Nagy 1964, 1972. These names are equivalents of the original defiition of the Frysjaodden Formation, i.e. without the Marstranderbreen Member. ORIGIN OF NAME: Frysjaodden: A cape on the southern coast of Van Mij-enfjorden. TYPE SECTION (FIG. 4-21): Stratotype: Lindstromijellet-Nordenskioldfjellet, Norden- skiold Land DEPOS~ONAL AGE: ?Paleocene - ?Eocene DATING METHOD: Bivalves; palynology REFERENCE(S) FOR AGE: R ~ M 1922; Livgic 1973, 1974; Manum & Throndsen 1986 (see Van Mijenfjorden Group) OVERLYING UNIT(S): Battfjellet Formation UNDERLYING UNIT(S): Grummtbyen Formation INTERCALATED UNIT(S): Hollendardalen Formation SUPERIOR UNIT: Van Mijenfjorden Group OTHER USE OF NAME: None THICKNESS: 200-400 m, 250 m in the stratotype MAIN LFFBOLOGIES: Shale, sandstone LOWER BOUNDARY DEFINITION: The basal part of the formation consists of shale with thin and irregularly shaped conglomerate lenses. The shales rest sharply on the siltstones and silty sandstones of the Grumantbyen Formation. DESCRIPTION: The unit is about 200 m thick in the northern and northeastern parts of the Central Tertiary Basin, but thickens to more than 400 m south- and southwestwards. These thickness values include the up to 150 m thick intercalated sandstone lobes of the Hollendardalen Formation. The Frysjaodden Formation is essentially shale-prone, but is interbedded with a major laminated sandstone wedge (Hol- lendardalen Formation) near its base and several thinner sandstone wedges (Bjsmsonfjellet Member) in its middle Part.

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Together with the sandstone lobes of the Hollendardalen - Formation, the Frysjaodden Formation represents a major change in drainage direction and pattern compared to the earlier history of the basin. The unit is thought to be contemporaneous with major uplift and overthrusting of the West Spitsbergen Fold-thrust Belt, and shows clear evidence of sediment input from west and of eastwards migration of the basin depocentre.

Marstranderbreen Member (T-10)

STATUS OF UNIT: Formal MT USE OF NAME: Here CURRENT D E ~ T I O N : Here SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Marstranderbreen: A glacier in western Nordenskiold Land TYPE SECTION (FIGS. 4-21,4-22): Stratotype: Marstranderbreen, Nordenskiold Land Hypostratotype: Lindstromfjellet - Nordenskioldfjellet DEPOSITIONAL AGE: ?Pdeocene - ?Eocene DATING METHOD: Indirect, stratigraphic relationship F&FERENCE(S) FOR AGE: See Frysjaodden Formation OVERLYING UNIT(S): Hollendardalen Formation UNDERLYING UNIT@): Grumantbyen Formation SUPERIOR UNIT: Frysjaodden Formation OTHER USE OF NAME: None THICKNESS: 10-60 m, 38 m in the stratotype MAIN LITHOLOGIES: Shale LOWER BOUNDARY DEFINITION: See Frysjaodden Formation DESCRIPTION: b e unit consists of dark shales with occasional siltstone layers. It interfiigers laterally with the sandstones of the Hollendardalen Formation.

Currently the Marstranderbreen Member is only defined in localities where the Hollendardalen Formation is developed, but it may well be feasible to apply the name to equivalent strata in other areas, if acceptable distinctive criteria can be defined.

The Marstranderbreen Member represents the deeper water deposits of the foreland basin adjacent to the growing West Spitsbergen Fold-thrust Belt.

Gilsonryggen Member (T-11)

STATUS OF UNIT: Formal Fms~ USE OF NAME: Major & Nagy 1964,1972 CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): Gilsonryggen "Formation": Major & Nagy 1964, 1972 ORIGIN OF NAME: Gilsonryggen: A mountain south of Adventdalen, Nordenskiold Land TYPE SECTION (FIG. 4-21): Stratotype: Nordenskioldfjellet, Nordenskiold Land DEPOSITIONAL AGE: ?Paleocene - Eocene DATING METHOD: Plant remains, foraminifera; palynology REFERENCE(S) FOR AGE: Livgic 1973, 1974; Manum & Throndsen 1986 (see Van Mijenfjorden Group) OVERLYING UNIT(S): Battfjellet Formation

Fig. 4-23: Gilsonryggen shales (Frysjaodden Formation, grading upwards into the sandstones of the Battfjellet Formation at Liljevalch- fiellet, near Sveagruva. Photo: J. Nagy

UNDERLYING UNIT@): Hollendardalen Formation SUPERIOR UNIT: Frysjaodden Formation OTHER USE OF NAME: None THICKNESS: 190 (stratotype) - 250 m MAIN LITHOLOGIES: Shale LOWER BOUNDARY DEFINITION: The base of the Gilson- ryggen Member is defined where shales and siltstone become dominating above the sandstones of the Hollendard- den Formation. DESCRIPTION: The Gilsonryggen Member consists of black shales with occasional siltstone layers and bentonites (Fig. 4-24). It varies in thickness from about 200 m in the north and northeast of the Central Tertiary Basin to more than 250 m in the south and southwest. The unit interfingers laterally northwestwards with the sandstones of the Bjmmonfjellet Member. The base of the unit is gradational from the sandstones of the Hollendardalen Formation, the top is also gradational to the sandstones of the Battfjellet Formation (Fig. 4-23).

The member is only defined where the Hollendardalen Formation occurs as an underlying development. It is a time and facies equivalent of the upper, undivided parts of the Frysjaodden Formation developed farther east.

The shales of the Gilsonryggen Member represent the deeper water deposits of the foreland basin adjacent to the growing West Spitsbergen Fold-thrust Belt.

Bjnrnsontjellet Member (T-12)

STATUS OF UNIT: Formal ~ S T USE OF NAME: Steel et al. 198 1 CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): None ONGIN OF NAME: Bjmonfjellet: A mountain in western Nordenskiold Land TYPE SECTION (FIG. 4-25): Stratotype: Bjmonfjellet, Nordenskiold Land DEPOSITIONAL AGE: ?Paleocene - Eocene DATING METHOD: Indirect, stratigraphic relationship

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Fig. 4-24: Bentonite horizon in the Gilsonryggen Member (Frysja- odden Formation), Nordenskioldfjellet, central Spitsbergen. Similar bentonites are typical for the shale sequences of the Basilika and Frysjaodden formations. Photo: J. Nagy

REFERENCE(S) FOR AGE: See Frysjaodden Formation OVERLYING UNIT(S): Gilsonryggen Member UNDERLYING UNIT(S): Gilsonryggen Member SUPERIOR UNIT: Frysjaodden Formation HER USE OF NAME: None THICKNESS: C100 m, 90 m in the stratotype MAIN LITHOLOGIES: &3lldStone, Shale LOWER BOUNDARY DEFINITION: The base of the Bjermson- fjellet Member is transitional and defined at the first thick (several metra) sandstone wedge in middle levels of the Gilsonryggen Member. D~scru~no~: The Bjm-nsonfjellet Member consists of several thin sandstone wedges, each up to 15-20 m thick, in the western areas of the basin, both north and south of Van Mijenfjorden. They thin out in the centre of the basin, passing into Gilsonryggen Member shales. The sandstone units consist of beds which are massive, nonnally graded or soft- sediment deformed, and have fluted or grooved soles. The unit occurs in the middle or just below the middle levels of the shales of the Gilsonryggen Member.

As with the Hollendardalen Formation on a larger scale, the Bjm-nsonfjellet Member represents clastic input to the basin from the west, as a result of uplift and growth of the West Spitsbergen Fold-Thrust Belt. The Bjmonfjellet Member represents high density turbidite and slump deposits in the foreland basin.

Though having a similar origin as the Hollendardalen For- mation, the comparatively thin sandstone intercalations of the Bjmnsonfjellet Member between shales of the Gilson- ryggen Member do not satisfy demands for distinguishing the two latter units on a formational level.

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Fig. 4-25: Stratigraphic section T-12 Stratotype for: Bjmonfjellet Member Locality: Bjernsonfjellet Reference: Steel, in Ohta et al. 1992

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'Hollendardale PR\&% b

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DISTRIBUTION SHOWN ON FIG(s).: 4-05 STATUS OF u r n Formal a FIRST USE OF NAME: LivSic 1967 CURRENT DEFINITION: Here. Although the base of the for- e'

mation is redefined to exclude the very thin shales of the Marstranderbreen Member, the basic idea that the Hollen- P dardalen Formation essentially dessignates a thick sandstone succession below the main shale body of the Frysja- odden Formation, is kept. The formation name fiom LivBic P (1967) is therefore not changed. SYNONYM(S) AND REFERENCE(S): "Shaley green sandstone P

P- formation": LjutkeviE 1937a; "Lower transitional fonnation": LivSic 1965. These names are equivalents of the Hol- a lendardalen Formation as originally defined, i.e. including P the Marstranderbreen Member. This unit also equals the upper part of the "Green sandstone series" (Nathorst 19 10) P and the "Sarkofagen Formation" (Major & Nagy 1964, P

1972). P ORIGIN OF NW: Hollendardalen (transl.: "The Valley of the Dutch"): A valley in western Nordenskiold Land TYPE SECTION (FIGS. 4-22,426): Stratotype: Marstranderbreen, western Nordenskiold Land P (development with two sandstone lobes) P Hypostratotype: Bnrdalen, central Nordenskiold Land (development with one sandstone lobe) P

P S DEPOSITIONAL AGE: ?Paleocene - ?Eocene DATING METHOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: LivSic 1973, 1974; Manum & P

Throndsen 1986 (see Van Mijenfjorden Group) P S OVERLYING UNIT(S): Gilsonryggen Member (Frysjaodden Formation) P UNDERLYING UNIT(S): Marstranderbreen Member (Frysja- P odden Formation) P SUPERIOR UNIT: Van Mijenfjorden Group OTHER USE OF NAME: None TmcmuEss: 450 m, 82 m (cumulative) in the stratotype, 18 m in the hypostratotype MAIN LITEIOLOGIES: Sandstone LOWER BOUNDARY DEFINITION: The formation boundary grain size

approximate occurs within a coarsening-upward succession and is de- Trn - - fined, where sandstone beds begin to form a distinct ele- un~ts clsivf f ~ C V C ~ pcbb

ment. The sandstones of the Hollendardalen Formation rest with a fairly sharp contact on the shales of the Marstrander- Fig. 4-26: Stratigraphic section 1'-'13b breen Member. Hypostmtotype for: Hollendardalen Formation ,DESCRIPTION: The Hollendardalen Formation consists of Locality: B d e n several wedges of well-laminated sandstone which collec- Reference: Dalland, A. (unpubl.) tively reach a thickness of up to 150 m in the western parts of the basin. They thin out eastwards to the basin centre,

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where they are replaced by the shales of the Frysjaodden Formation. 'Ifipical features of the sandstones are plant fragments, rootlets and ripple lamination.

The Holkndardalen Formation represents initial coarser clastic input from the uplifting West Spitsbergen Fold- Thrust Belt. The sandstones are shallow marine deposits originating on tidally-influenced deltas.

DISTRIBUTION SHOWN ON RG(s).: 4-04,4-05 STATUS OF UNIT: Formal FIRST USE OF NAME: Major & Nagy 1964 CURRENT DEFINITION: Major & Nagy 1972 SYNONYM(S) AND REFERENCE(S): "Fissile sandstone series": Nathorst 19 10; "Upper shaley sandstone formation": Ljutkevie 1937a; "Flaggy sandstone series": Orvin 1940; "Collinderodden Formation": LivSic 1967. The contemporaneously published name Batt$ellet Formation (Major & Nagy 1964,1972) is preferred because of its more extensive use in the published literature (see Section 4.3.1). ORIGIN OF NAME: Battfjellet: A mountain in central Nordenskiold Land TYPE SECTION (FIG. 4-27): Stratotype: Battfjellet SW, central Nordenskiold Land DEPOSITIONAL AGE: ?Paleocene - Eocene DATING METHOD: Bivalves; indirect REFERENCE(S) FOR AGE: Ram 1922; LivSic 1973, 1974; Manum & Throndsen 1986 (see Van Mijenfjorden Group) OVERLYING UNIT@): Aspelintoppen Formation UNDERLYING UNIT@): Frysjaodden Formation SUPERIOR UNIT: Van Mijenfjorden Group ~ I I E R USE OF NAME: None THICKNESS: >300 m, 71 m in the stratotype Mm LITHOLOGIES: Sandstone, siltstone, shale Fig. 4-27: Stratigraphic section T-14 LOWER BOUNDARY DEFINITION: The formation boundary Stratotypefor: Battfjellet Formation occurs within a coarsening-upward succession. The base of Locality: Battfjellet the Battfjellet Formation is defined by the first occurrence Reference: Steel et al. 1981 of thick sandstone beds above the dark shales of the Frysja- odden Formation (Fig. 4-23). DESCRIPTION: The Battfjellet Formation varies in thickness from less than 60 m in the northeast of the basin (type area) to more than 300 m south of Van Mijenfjorden. It consists of well-laminated and cross-stratified, cliff-forming, The formation represents a late stage of coastal prograda: whitish sandstones interbedded with minor shales and silt- tion and infill of the fold-belt-flanked foreland basin, when stones. The formation has a gradational contact with the un- sediment input f i y outpaced subsidence and the basin derlying shales of the Gilsonryggen Member. was filled to sea level.

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DISTRIBUTION SHOWN ON FIG@).: 4-04,4-05 STATUS OF UNIT: Formal FIRST USE OF NAME: Major & Nagy 1964 CURRENT DEFINITION: Major & Nagy 1972 SYNONYM(S) AND REF'ERENCE(S): ''Uppe~ coal-bearing series": Nathorst 1910; "Upper coal-bearing sandstone fin.": LjutkeviE 1937a; "Upper plant-bearing sandstone seriesyy: Orvin 1940; "Storvola Formation": LivSic 1967. The contemporaneously published name Aspelintoppen Formation (Major & Nagy 1964,1972) is preferred because of its more extensive use in the published literature (see Section 4.3.1). ORIGIN OF NAME: Aspelintoppen: A mountain in Nathorst Land on the southern coast of Van Mijenfjorden, east of the type section TYPE SECTION (RG. 4-29): Stratotype: Rhekampen, Nathorst Land DEPOSITIONAL AGE: ?Eocene - ?Oligocene DATING METHOD: Plant remains; palynology REFERENCE(S) FOR AGE: L~vS~C 1973, 1974; man^ & Throndsen 1986 (see Van Mijenfjorden Group) OVERLYING UNIT(S): None UNDERLYING UNIT@): Battfjellet Formation SUPERIOR UNIT: Van Mijenfjorden Group OTHER USE OF NAME: None THICKNESS: >l 000 m MAXN LITHOLOGIES: Sandstone, siltstone, mudstone LOWER BOUNDARY DEFINITION: The base of the Aspelin- toppen Formation is defined at the base of the first coals or thicker shaley intervals above the thick, sand-prone intervals at the top of Battfjellet Formation. DESCRIPTION: The Aspelintoppen Formation reaches a

I- Fig. 4-28: Fossil leaves in the Aspelintoppen Formation on Urdkollen,

Van Mijenfjorden. Photo: W.K. Dallmam

thickness of more than 1000 m south of Van Mijenfjorden. It consists of alternations of sandstones with siltstones, mudstones and thin coals. Sandstone intervals, which are cross-stratifled and commonly soft-sediment deformed, are rarely thicker than 3-5 metres. The formation contains abundant plant remains. Especially abundant and well preserved are leaves of trees (Fig. 4-28).

The formation represents the culmination in growth of the foreland basin, with its final infill of deposits with distinct terrestrial influence. Sediments represent various shallow- water deposits like distributary channels, crevasse splays and swamp deposits.

M - ~ E s S U N D SUBGROUP (T-16)

~y-Alesund 1 Subgroup

STATUS OF UNIT: Formal FIRST USE OF NAME: Challinor 1967 CURRENT DEFINITION: Chalhor 1967 SYNONYM(S) AND REFERENCE(S): Ny-hesund "Formation": Challinor 1967 ORIGIN OF NAME: Ny-hesund: A former coal mining settlement on Br~ggerhalvsya, now a research centre (Fig. 4-30), named after hesund, a town in western mainland Norway TYPE AREA / TYPE SECTIONS: Ny hesund coal mining area ("Kongsfjordfeltet"), Brarggerhalvsya. The stratigraphy of the area is only sufficiently known from borehole data, and type sections are mostly confined to boreholes. STRUCTURAL SETTING: Occurs in the West Spitsbergen Fold-thrust belt. Deposits are most probably related to the succession of the Central Tertiary Basin. DEPOSITIONAL AGE: Paleocene (or ?Oligocene). Earlier interpretations of Miocene age of the entire Tertiary of Spits- bergen (Heer 1868, 1870) have been questioned since 1922 (Ravn) and are oumed by modern palynology (Manum & Throndsen 1986). Most authors favour a Paleocene age of the subgroup based on lithostratigraphic correlations and comparative studies of plant remains. Livlic's (1973, 1974) age interpretation (Oligocene) is considerably younger. Ac- cording to Manum & Throndsen (1986) the flora is not con- clusive, hence the age preferred by the various authors depends on the lithostratigraphic correlations preferred by them. OVERLYING UNIT(S): None UNDERLYING UNIT(S): Vardebukta Formation (Sassendalen Group) or Kapp Starostin Formation (Tempelfjorden Group) SUPERIOR UNIT: Van Mijenfjorden Group OTHER USE OF NAME: "Ny-hesund Formationyy (LivSic

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Barnjellet Formation (Erne)

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1973) for the upper formation of the subgroup (see Brag- gerbreen Formation); ~y-Alesund coal field (LivSic 1973) for the coal mining area developed in this unit THICKNESS: ca. 270 m preserved MAIN LITHOLOGIES: Sandstone, shale, coal DESCRIPTION: The ~ ~ - & e s u n d Subgroup comprises all Tertiary deposits present in the Kongsfjorden (Ny-hesund) area which are preserved in minor fault blocks of altogether 6 X 3 lun lateral extension. It overlies Triassic and Permian deposits with a low-angle unconfonnity and is overlain by Carboniferous and Perrnian strata thrust over along a high- angle reverse fault. It consists of the clastic, coal-bearing Kongsfjorden and Braggerbreen formations (see these formational descriptions).

The ~y-&esund unit has been raised to subgroup rank, because unpublished work (mainly Midbee 1985) has shown that the definition of the two formations is most appropriate with regard to comparison to the Central Tertiary Basin succession of the Van Mijenfjorden Group.

DISTRIBUTION SHOWN ON FIG(s).: 4-06 STATUS OF UNIT: Formal FIRST USE OF NAME: LivSic 1973 CURRENT DEFINITION: LivSic 1973 SYNONYM(S) AND REFERENCE(S): ''Grey sandstone": Orvin 1934; "Grey Sandstone Member": Challinor 1967. ORIGIN OF NAME: Kongsfjorden (transl. fiom "King's Bay"): A fiord in northeastern Spitsbergen TYPE SECTION @GS. 4-32,434,435): Stratotype: Boreholes 4-1928 and 5-1928 (composite) DEPOSITIONAL AGE: Paleocene (*alternatively Oligocene; see Ny-aesund Subgroup) DATING METHOD: Plant fossils; lithostratigraphic correlation -RENCE(S) FOR AGE: Orvin 1934; Schloemer-Jager 1958; Schweitzer 1974; *LivSic 1973, 1974; Midbae 1985 (unpubl.) OVERLYING UNIT@): Brffggerbreen Formation UNDERLYING UNIT(S): Vardebukta Formation (Sassendalen Group) or Kapp Starostin Formation (Tempelfjorden Group) SUPERIOR UNIT: Ny-kesund Subgroup OTHER USE OF NAME: Kongsfiordfeltet (Norwegian for Kongsfiorden Field = Kings Bay coal miningfield) is used for the coal mining area related to this and the overlying formation

The place name is also used based on another fiord with

Fig. 4-30: The f o r m mining community (now research station) of Ny-&esund, the coal field in the background. Mining was given up in 1962. Photo: P. Midbse (1990)

the same name in Finnmark, mainland Norway (Kongs- Bord[en] Formation: Siedlecka 197213; Kongsfiorden Anti- cline: Roberts 1972; Kongsfiordgangkomplehet: registered by NSK). THICKNESS: 110 m (cumulative) in the stratotypes MAIN LITHOLOGIES: Sandstone, shale, coal LOWER BOUNDARY DEFINITION: The lower boundary is marked by the first appearance of Tertiary sediments (clastic rocks or coal) on the angular unconforrnity above Trias- sic and Permian folded sediments. The Tertiary succession starts normally with the Ester coal seam. DESCRIPTION: The Kongsfjorden Formation consists of clastic sediments (sandstones, shales and conglomerates) with coal seams representing alluvial to foreshore depositional environments. For more detailed descriptions see its subunits: the Kolhaugen and Tvillingvatnet members.

Fig. 4-31: Drilling of borehole 24 in the western coal field of Ny-hesund; Scheteligfjellet with thrusted Carboniferous and Permian strata in the background. Photo: F'. Midbse (1976)

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Kolhaugen Member (T-18)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here, following Midbnre 1985 (unpubl.) SYNONYM(S) AND REFERENCE(S): "Lower coal horizon": Orvin 1934 ORIGIN OF NAME: Kolhaugen (transl.: "The Coal Hill"): A hill SW of the settlement Ny-aesund TYPE SECTION (FIG. 4-32): Stratotype: Borehole 5-1928 Hypostratotype (prehmry): Borehole 25-1976 Borehole 5-1928 represents the most complete section through the Kolhaugen Member. The cores from this borehole do not exist any more, but the lower part of the member was penetrated in borehole 25-1976 (preliminary hypostratotype). A log of the stratotype (Fig. 4-32) has been reconstructed by Midbnre (1985, unpubl.) from the detailed core descriptions of Orvin (1934). DEPOSITIONAL AGE: Paleocene (alternatively Oligocene; see Ny-Alesund Subgroup) DATING METHOD: Plant fossils and lithostratigraphic correlation REFERENCE(S) FOR AGE: See Ny-ae~und Subgroup OVERLYING UNIT@): Tvillingvatnet Member UNDERLYING UNIT(S): Vardebukta Formation (Sassendalen Group) SUPERIOR UNIT: Kongsfjorden Formation OTHER USE OF NAME: None THICKNESS: <45 m, 40 m in the stratotype MAIN LITHOLOGIES: Sandstone, shale, coal LOWER BOUNDARY D E ~ T I O N : See Kongsfjorden Forma- tion DESCRIPTION: The Kolhaugen Member consists of rapidly alternating fine-grained sandstones, shales, coaly shales and coal with several well-developed coal seams, named (fkom below) the Ester, Sofie and Advokaten seams. The unit rests with a slightly angular unconformity on the lower Triassic Vardebukta Formation in the east; it thins towards the west and is missing in the westernmost parts of the Kongsfjorden area. The member is interpreted to represent alluvial plain deposits.

Tvillingvatnet Member (T-19)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here, following Midbae 1985 (unpubl.) SYNONYM(S) AND REFERENCE(S): "Light sandstone": Orvin 1934; "Tvillingvann Member": Midbe 1985 (unpubl.). The name is here changed according to the correct modem spelling of the place name. ORIGIN OF NAME: Tvillingvatnet (transl.: "The Twin Lake"): A small lake SW of the settlement ~ y - a e s u n d TYPE SECTION (FIGS. 4-344-35): Stratotype: Borehole 4-1928 Hypostratotype: Borehole 21 -1 97f5

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2. Hypostratotype: Scheteligfjellet Q (L) -

Borehole 4-1928 is the most complete section through the G H a 4 2 Tvillhgvatnet Member (70 meter). The cores from this : E $ borehole do not exist any more and the log has been drawn * E, Q

"1 T from k i n ' s (1934) descriptions. a o DEPOSITIONAL AGE: Paleocene (alternatively Oligocene; see - 2

NY-kesund subgroup) + r g ; & L DATING METHOD: Plant fossils and lithostratigraphic cone- : :, g lation z z : REFERENCE(S) FOR AGE: See ~y-kesund Subgroup O a H

O~ERL,YING UNIT(S): Brsggerbreen Formation 2 m z 0 UNDERLYLNG UNIT(S): Kolhaugen Member, Vardebukta For- a # mation, locally. Kapp Starostin Formation (Tempelfjorden Group) SUPERIOR UNIT: Kongsfjorden Formation OTHER USE OF NAME: None THICKNESS: 15-70 m, 70 m in the stratotype MAIN LITFIOLOGIES: Sandstone, conglomerate LOWER BOUNDARY DEFINITION: The base of the member is defined by marine sandstone and conglomerate which overlie the eroded continental deposits of the Kolhaugen Mem- ber or older formations (Vardebukta Formation, Kapp Starostin Formation); The contact is an angular unconformity. DESCRIPTION: The Tvillingvatnet Member consists mainly of coarse- and medium-grained sandstones, pebbly sandstones and conglomerates, unconforrnably resting on older - 116 m below units. Most of the marine sandstones of the Tvillingvatnet ~ohau~e-n surface Member were deposited below normal wave base and are gEziel grain size intensively bioturbated. Well-presewed primary structures m approximate - are only seen in the upper regressive part of the unit, where u n b dsivff mcvcg pcbb

upper shoreface and foreshore deposits are directly overlain by the Agnes-Otelie coal seam of the Braggerbreeen For- Fig. 4-34: Stratigraphic section T-19a mation (Fig. 4-33). Smrotype for: Tvillingvatnet Member

Where the member directly overlies the Permian Kapp Locality: Borehole 4-1928 Starostin Fonnation, a thick, local conglomerate is devel- Reference: Midb~le 1985 (unpubl.), redrawn from Orvin 1934 oped (see Mmebekken Bed).

The current interpretation of the unit as a shallow marine sandstone succession is based on data from boreholes 21- 1976 and 25-1976 which penetrate the upper and lower part of the Kongsfjorden area. The mountain top of Schetelig- of the unit, respectively. A thin (16.5 m) development of the fjellet shows the lower 60 m of the Tvillingvatnet Member, unit is found in borehole 38-1976 in the northwestern part 20 m of which belong to the Mmebekken Bed.

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m - clsivf f mcvcg I:

Fig. 4-35 : Stratigraphic section T- 19b

below

-m L__rrr_rrrrrm, dsivff mcvcg pcbb

Wypostratotype for: Tvilliugvatnet Member Localiiy: Borehole 21-1976 Reference: MiMidbrlle 1985 (uapubl.)

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4. TERTIARY LITHOSTRATICRAPHY

Marebekken Bed (T-20)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here, following Midbere 1985 (unpubl.) SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Msrebekken (after the Norwegian area Mare, where also the town Alesund is situated): A creek joining the river Bayelva NW of the settlement Ny-&esund TYPE SECTION (FIG. 4-37): Stratotype: Borehole 38-1976 Hypostratotype: Scheteligfjellet DEPOSITIONAL AGE: Paleocene (alternatively Oligocene; see Ny Aesund Subgroup) DATING METEOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: See ~y-Aesund Subgroup OVERLYING UNIT@): Unnamed UNDERLYING UNIT(S): Kolhaugen Member, Kapp Starostin Formation (Tempelfjorden Group) SUPERIOR UNIT: Tvillingvatnet Member OTHER USE OF NAME: None THICKNESS: <20 m, possibly locally thicker, 10 m in the stratotype MAIN LITHOLOGIES: Conglomerate, sandstone LOWER BOUNDARY DEFINITION: The base of the unit is defined by the appearance of conglomerates erosively overlying the glauconitic sandstones and cherts of the Perrnian Kapp Starostin Formation. DESCRIPTION: Known thicknesses of the Mmebekken Bed are 10 m in borehole 38-1976 and 20 m on Scheteligfjellet. The unit consists mainly of coarse conglomerates with thin beds of coarse-grained sandstone. It is only locally represented in ''Lagunefeltet" (a northwestern subarea of the coal mining area) and on Scheteligfjellet. The upper part of the bed is exposed along Merrebekken in "Lagunefeltet". The conglomerate is moderate to poorly sorted with well- rounded pebbles of chert and glauconitic sandstone and is interpreted to have been deposited in a marine beach to shoreface environment (Fig. 4-36).

lih, strat u n b

-85.5 m below surface grain size approximate -

dstvf f m c v c g pcbb

Fig. 4-36: Conglomerates of the Menebekken Bed at Mmebekken, Ny- Fig. 4-37: Stratigraphic section T-20 Alesund. Photo: P. Midbrae Stmtotype for: Mmbekken Bed

Locality: Borehole 38-1976 Rejei-ence: Midbare 1985 (unpubl.)

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DISTRIBUTION SHOWN ON FIG@).: 4-06 STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: LivSic 1973 SYNONYM(S) m REFERENCE(S): "Green sandstone": Orvin 1934; "Green Sandstone Member": Challinor 1967; "Ny- Alesund Formation": Livgic 1967. ORIGIN OF NAIWE: Br~ggerbresn: A glacier system (Austre and Vestre Brrggerbreen) with tongues ending into the outcrop area of the formation, Brwerhalvsya TYPE SECTION (FICS. 4-3&4-39): Stratotype: Boreholes 21-1976,24-1976 and 38-1976 (composite) (Fig. 4-3 l) DEPOSITCONAL AGE: Paleocene (*alternatively Oligocene; see NY-kemd Subgroup) DATING METAOD: Plant fossils; lithostratigraphic correlation REFERENCE(S) FOR AGE: Orvin 1934; Schloemer-Jager 1958; Schweitzer 1974; *LivSic 1973, 1974; Midbnre 1985 (@l.) O V E ~ Y I N G UNIT@): None UNDERLYMG UNIT@): Kongsfjorden Formation SUPERIOR UNIT: Ny-hesund Subgroup -R USE OF NAME: None WCI(NESS: > 180 m MAIN LFTHOLOGIES: Sandstone, shale, conglomerate LOWER BOUNDAWI DEFINITION: The base of the formation is defined at the base of the Agnes-Otelie coal seam or of laterally correlative coaly shales which overlie the marine sadstones and conglomerates of the Kongsfjorden Forma- tion. DESCRIPTION: The Br~ggerbreen Formation comprises a sedimentary succession of conglomerates, sandstones, shales, coaly shales and coals with a transition Born marginal marine to continental depositional environments. For more detailed descriptions see its submits: the Leirhaugen and Bayelva members.

Member

z

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m 0 0

a'"% - z ~ a + " ' W P ,

- W W @ & '

c m " W m P ? & + U W Z

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a

4 -- Tvillingvatnet Member

(Paleocene)

55 m below -h surface

grain size approximate 1

Fig. 4-38: Stratigraphic section T-22 Stratotype for: Leirhaugen Member Locality: Borehole 21-1976 Reference: Midbee 1985 (-L)

Leirhaugen Member (T-22) A hill SW of the settlement ~y-Alesund

STATUS OF UNIT: Formal TYPE SECTION (FIG. 4-38): FIRST USE OF NAME: Here Stratotype: Borehole 21 -1 976 CURRENT D E ~ T I O N : Here, following Midbnre 1985 (un- DEPOSITIONAL AGE: Paleocene (alternatively Oligocene; see

Ny-&esund Subgroup) publ.) SYNONYM(S) AND REFERENCE(S): None DATING METHOD: Plant fossils and lithostratigraphic corre- ORIGIN OF NAME: Leirhaugen (transl.: "The Mud Hill"): lation

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4. TERTIARY LITHOSTRATICRAPHY

REFERENCE(S) FOR AGE: See Ny-kesund Subgroup OVERLYING UNIT(S): Bayelva Member UNDERLYING UNIT(S): Kongsfjorden Formation SUPERIOR UNIT: Brsggerbreen Formation HER USE OF NAME: None THICKNESS: 5-20 m, 15 m in the stratotype MAIN LITHOLOGIES: Sandstone, conglomerate, coal LOWER BOUNDARY DEFINITION: See Brsggerbreen Forma- tion DESCRIPTION: The Leirhaugen Member consists of alternating conglomerates, sandstones, shales, coaly shales and coal deposits deposited in back-barrier marshes, tidal flats and lagoons. The unit is defined because of its transitional depositional environment between the marine Tvillingvatnet Member and the continental Bayelva Member.

Bayelva Member (T-23)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here, following Midbe 1985 (W- publ.) SYNONYM(S) AND REFERENcE(s): None ORIGIN OF NAME: Bayelva: A river running into Kongs- fjorden west of the settlement Ny-kemnd TYPE SECTION @G. 8-39): Boundary s-type: Barehole 38-1976 Unit stratotype: Borehole 24-1976 (Fig. 4-31) The most complete section through the Bayelva Member is seen in borehole. 24-1976, though the bsrse was not penetrated. Less complete sections including the boundary with the underlying Leirhaugen Member are seen in boreholes 21-1976 and 38-1976, of which the latter is defined as the boundary stratotype. DEPOSITIONAL AGE: Paleocene (alternatively Oligocene; see Ny-kesund Subgroup) DATING METHOD: Plant f0SSilS and lithostratigraphic corn- lation REFERENCE(S) FOR AGE: See ~ y - & e ~ W d Subgroup OVERLYING m(s ) : None UNDERLYING -(S): Leirhaugen Member, Kongsfjorden Formation SUPERIOR m: Broggerbreen Formation

USE OF NAME: None THIcxmss: >l60 m Bhm ~ o L O O I E S : Sandstone, shale, cod Lowlm BO- DEFINITION: The base of the unit is defied at h base of the Josejlne coal seam or correlative sandstones rich in coal $hgments. Where the Leirhaugen Member is not Wqd, the boundary is defined at the lithological change h m the pebbly sandstones of the Tvillingvatnet Member to the greenish sandstones of the present unit.

Fig. 4-39: Stratigraphic section T-23 Boundary stratotype for: Bayelva Member Locality: Borehole 38-1976 Reference: Midbee 1985 (unpubl.)

z El 2 2

> - M *

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o d - w m P 3 0 + ; H X

0 hl p4 C9

- Leirhaugen Mb.

(Paleocene)

IIJ

m I

m m - 53 m below surface

77 cb b

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DESCRIPTION: The member consists of alternating conglomerates, sandstones, shales, coaly shales and coals representing fluvial channel and interchannel to interdistributary bay sediments deposited on a subsiding coastal plain. The sandstones have a characteristic greenish colour reminiscent of the possibly correlative Grumantbyen Formation of he Central Tertiary Basin. Coal seams (from below): Josefine seam, Ragnhild seam, Kings Bay 1 seam and Kings Bay seam (the same as Kings Bay I?). The upper part of the unit is cut by a thrust plane, but at least 160 m are preserved in the western part of the Kongsfjorden area.

4.4.2 Buchananisen Group

BUCHANANISEN GROUP (T-24)

/T

. Buchananise

STATUS OF UNIT: Formal FIRST USE OR NAME: Here CURRENT DEFINITION: Harland 1969 SYNONYM(S) AND REFERENCE(S): "Forlandsundet Group": Harland 1969. The name is changed to Buchananisen Group to avoid confusion with the Forlandszrndet Gmben. The graben is a younger and narrower structure than the original sedimentary basin where the group was deposited. ORIGIN OF NAME: Buchananisen: A glacier on Prins Karls Forland TYPE AREA: Central eastern coast of Prins Karls Forland STRUCTURAL SETTING: Preserved in the post-depositionally formed Forlandsundet Graben DEPOSITIONAL AGE: ?Late Paleocene - Eocene - ?Early Oligocene The age of the Buchananisen Group is poorly defined. Re- liable fossil age determinations have only been reported from the Sarstangen conglomerate, which is not stratigraph- i d l y correlated with the other formations with certainty. The age is mainly interpreted from the general tectonic development of the Tertiary basins of Svalbard (LivSic 1967, 1973, 1974; Steel & Worsley 1984; Steel et al. 1985; Gabrielsen et al. 1992). OVERLYING UNIT(S): None UNDERLYING UNIT(S): Pre-Old Red SUPERIOR UNIT: None OTHER USE OF NAME: None THICKNESS: >4000 m ? MAIN LITHOLOGIES: Sandstone, conglomerate, shale D E S C ~ O N : The Buchananisen Group is a clastic sedimentary succession consisting of conglomerates, sandstones, siltstones and shales occurring within the Forland- sundet Graben, on both sides of Forlandsundet. For

descriptions see individual formations (SelvAgen, Sess- hsgda, Reinhardpynten, Krokodillen, Marchaislaguna, Aberdeenflya formations and Balanuspynten conglomerates). The individual formations are local and in parts laterally interfingering (LivSic 1967, 1973, 1974; Rye Larsen 1982, unpubl.).

The Forlandsundet Graben (Harland 1969) is a younger (and probably partly coeval) Tertiary structure containing preserved deposits of an originally larger sedimentary basin (Gabrielsen 1992; Kleinspehn & Teyssier 1992).

DISTRIBUTION SHOWN ON ~ G ( S ) . : 4-06 STATUS OF UNIT: Formal FIRST USE OF NAME: Atkinson 1962 CURRENT DEFINITION: LivSic 1967 SYNONYM(S) AND REFERENCE(S): "SelvAgen conglomerate": Atkinson 1962 ORIGIN OF NAME: SelvAgen (transl.: "The Seal Bay"): A bay on the eastern coast of Prins Karls Forland TYPE SECTION (FIG. 4-40): Stratotype: SelvAgen N, Thomsonfjella h. 431 m, Prins Karls Forland DEPOSITIONAL AGE: Late Paleocene - Eocene (?) DATING METHOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: See Buchananisen Group OVERLYING UNIT(S): Sessbgda, Krokodillen and Aber- deenflya formations UNDERLYING UNIT(S): Pre-Old Red SUPERIOR UNIT: Buchananisen Group OTHER USE OF NAME: None THICKNESS: 40-170 m, 170 m in the stratotype (top not exposed) MAIN LITHOLOGIES: Conglomerate LOWER BOUNDARY D E m I O N : The base is defined by conglomerates on the angular unconformity above folded metamorphic basement. DESCRIPTION: The Selvagen Formation has been defined around the type area of Sessbgda, Geddesfjellet and Krokodillen. Similar, lithostratigraphically correlatable, immature conglomerates are, however, preserved also to the north along the western Forlandsundet Graben margin on Buchananryggen and Aberdeenflya.

The SelvAgen Formation consists of polymict, pebbly to boulder-size greenish-grey to yellow and red conglomerates, often transitional to breccias, especially close to the western boundary faults of the Forlandsundet Graben. Rare

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z 0 I

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= c 2 u ' = o - = h

+ @ z = O W w o o + W 4 *

cl W V1

Pmmrnbrkrn basement

ments and grades upwards into conglomeratic saudstones of the Sessbgda Formation in the SelvAgen - Krokodillen area.

The Selvilgen Formation represents mainly alluvial fan- glomerate and talus deposits, deposited close to a tectonically active basin margin.

DISTRLBUTION SHOWN ON FIG@).: 4-06 STATUS OF UNIT: Formal FIRST USE OF NAME: LivSic 1967 CURRENT DEFINITION: LivSic 1967 SYNONYM(S) AND REFERENCE(S): None. Part of the former "McVitie Formation" (Atkinson 1962) or "McVitiepynten Formation" (Birkenmajer 1972b). ORIGIN OF NAME: Sessbgda (transl.: "The Seat Hill"): A mountain on central eastern Prins Karls Forland TYPE SECTION (FIG. 4-41): Stratotype: SelvAgen N, Prins Karls Forland DEPOSITIONAL AGE: ECMXlle (?) DATING METHOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: See Buchananisen Group

- OVERLYING UNIT@): Reinhardpynten Formation UNDERLYING UNIT(S): Selvilgen Formation SUPERIOR UNIT: Buchananisen Group OTHER USE OF NAME: None THICKNESS: 59 (stratotype) - 120 m MAIN LITHOLOGIES: Sandstone, siltstone, shale, conglomerate LOWER BOUNDARY DEFINITION: This boundary between conglomerates of the underlying SelvAgen Formation and finer-grained clastics of the Sessbgda Formation is relatively sharp in the type section. The boundary is defined, where mdstones, siltstones and shales start to dominate over conglomerates. DESCRIPTION: The Sessbgda Formation comprises a large- scale fining-upward succession. It consists of light grey, medium- to coarse-grained, conglomeratic, stratified sandstones alternating with siltstones and claystones in the lower part, grading upwards into fine-grained, more homogenous sandstones in the upper part. The sandstones in the lower part show mostly fining-upwards motifs and contain siderite concretions, whereas in the upper part they tend to be coarsening upward and contain pyrite concretions. The formation

intercalations of thin sandstones and siltstones occur. The contains abundant plant remains. thickness of the formation varies between 170 m and 40 m, The Sesshnrgda Formation has an apparently transitional thinning from west to east. The SelvAgen Formation rests boundary to the underlying conglomerates of the SelvAgen with an angular unconformity on Pre-Old Red metasedi- Formation. The upper boundary is also gradational and is

IIIIIIIIIII clsivf f mcvcg pcbb

Fig. 4-40: Stratigraphic section T-25 S m t o ~ f o r : Selvdgen Formation Locality: Thomsonfjella, Selvilgen N Reference: Rye Larsen 1982 (unpubl.)

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- l units dsivff mcwp pcbb

Fig. 4-41: Stratigraphic section T-26 Stmtotype for: Sesshragda Formation Locality: Selvigen N Reference: Rye Larsen 1982 (unpubl.)

defined at the uppermost conglomerate bed under the more homogeneous siltstones of the Reinhardpynten Formation.

The Sessbgda Formation represents a large-scale transgressive succession, passing from alluvial and fan-delta plain facies in the lower part to fan-delta front and nearshore marine facies in the upper part.

l

.? Rein hardpynter Formation

f "ORTHWESTERN

SVALBARD - DISTRIBUTION SHOWN ON FIG(s).: 4-06 STATUS OF UNIT: Formal FIRST USE OF NAME: L~vS~C 1967 CURRENT DEFINITION: LivSic 1967 SYNONYM(S) m REFERENCE(S): None. Part of the former "McVitie Formation" (Atkinson 1962) or "McVitiepynten Formation" (Birkenmajer 1972b). ORIGIN OF NAME: Reinhardpynten: A cape on central eastern Prim Karls Forland TYPE SECTION (FIG. 4-42): Stratotype: Reinhardpynten, Prim Karls Forland DEPOSITIONAL AGE: Eocene (?) DATING METEIOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: See Buchananisen Group OVERLVING UNIT(S): Krokodillen Formation UNDERLYING UNIT(S): Sessbgda Formation SUPERIOR UNIT: Buchananisen Group OTHER USE OF NAME: None THICKNESS: 32 10 m in the stratotype MAIN LITEOLOGIES: Siltstone, shale, fine-grained sandstone LOWER BOUNDARY DEFINITION: The lower boundary is defined at the first appearance of homogeneous siltstones above the uppermost conglomerate bed of the Sessbgda Formation. The basal 10 m of the Reinhardpynten Forma- tion in the type section form a distinct fining-upward succession. DESCRIPTION: The Reinhardpynten Formation consists of dark grey, very fine sandstones and siltstones with pyrite and siderite concretions in the lower part, fining upwards into dark silty claystones with abundant carbonate concretions and floating quartzite pebbles. Some quartzitic sandstones with rare conglomerate bands occur at the top of the formation on northern Sessflya. The boundary to the overlying Krokodillen Formation is not exposed. The Reinhard- pynten Formation contains a scattered marine bivalve fauna.

The Reinhardpynten Formation -has an overall transgressive character, passing upwards from nearshore to mostly distal marine facies. However, the uppermost sandstones probably represent nearshore, marine fan-delta deposits similar to the underlying Sessbgda Formation.

If these sandstones prove to have a significant thickness and can be mapped laterally, they should be considered for member status. However, the area is structurally complex and more work is needed in order to resolve the stratigraphy in more detail.

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- , V m -rrrrrmTn dsivf f rncvcg pcbb

Fig. 4-42: Stratigraphic section T-27 Strumtype for Reinhardpynten Fomtion Loculi@: Rehhydpynten Refmnce: Pagels 1986 (unpubl.)

DISTRIBUTION SHOWN ON hqs).: 4-06 STATUS OF UNIT: Formal h R s T USE OF NAME: L~vN~c 1967 CURRENT DEFINITION: LivNic 1967 Smom(s) AND REFERENCE(S): None, Part of the former "McVitie Formation" (Atkinson 1962) or "McVitiepynten Formation" (Birkenmajer 1972b). ORIGIN OF NAME: Krokodillen (transl.: "The Crocodile"): A mountain on central eastern Prim Karls Forland TYPE SECTION (FIG. 4-43): Stratotype: Krokodillen N, Prins Karls Forland DEPOSITIONAL AGE: (?) DATING m m ~ : Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: see B~~hanani~en &OUP

OV~RLYING UNIT@): Marchaislaguna Formation U N D E R L . . m(s ) : Selvagen and Reinhardpynten(?) formations SUPERIOR mm Buchananisen Group O ~ R USE OF NAME: None T I E I C ~ S S : 400 m (?), l l0 m exposed in the stratotype MAIN LITHOLOGIES: Shale, sandstone LOWER BOUNDARY DEFINITION: The lower boundary is sharp and defined by shales overlying the conglomerates of the SelvELgen Formation. Where the Reinhardpynten Forma- tion occurs below the Krokodillen Formation, the boundary is not exposed well enough to give any precise definition. DESCRIPTION: The Krokodillen Formation consists of predominantly dark, silty claystones interbedded with 2-40 m thick light, fine-grained, almost quartzitic sandstones, sometimes coarsening upward. The type section at Kroko- dillen is highly faulted and the total thickness of the fonnation is estimated to 400 m. The Krokodillen Formation rests directly on the conglomerates of the Selvagen Formation at western Krokodillen. The boundary with the thick silty claystones and sandstones of the Reinhardpynten Formation to the south is not well exposed and therefore not well understood. It has been suggested, however, that the Krokodillen Formation conformably overlies the Reinhardpynten For- mation. Upwards, the Krokodillen Formation is overlain, possibly erosively, by heterolithic sandstones and siltstones of the Marchaislaguna Formation.

The Krokodillen Formation represents a mainly shallow marine facies. The massive, unstructw:ed appearance of the sandstones and also the incipient cleavage in the claystones are attributed to deep burial with high heat and pressure al- teration.

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MPS -- 6 M P S = 3 v

MPS= 7 U

DISTRIBUTION SHOWN ON RG(s).: 4-06 STATUS OF UNIT: Formal FIRST USE OF NAME: LivSic 1967 CURRENT DEFINITION: LivSic 1967 SYNONYM(S) AND REFERENCE(S): bbMar~haise Formation": LivSic 1967. The place name segment is incomplete. Part of the former "McVitie Formation" (Atkinson 1962) or "McVitiepynten Formation" (Birkenmajer 1972b). ORIGIN OF NAME: Marchaislaguna: A small lagoon at the coast of central eastern Prins Karls Forland TYPE SECTION (FIG. 4-44): Stratotype: Peter Winterbukta, Prins Karls Forland DEPOSITIONAL AGE: Eocene - Oligocene (?) DATING METHOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: See Buchananisen Group OVERLMVG UNIT(S): None in outcrop UNDERLYING UNIT(S): Krokodillen Formation SUPERIOR UNIT: BuchaDdni~eIl Group -R USE OF NAME: None THICKNESS: >600 m (?), 290 m exposed in the stratotype MAIN LITHOLOGIES: Sandstone, shale, conglomerate LOWER BOUNDARY DEFINITION: The b0Wldv with the W- derlying Krokodillen Formation is defined at the onset of sandstones above the upper shales of the Krokodillen For- mation. It is abrupt, possibly slightly erosive. DESCRIPTION: The Marchaislaguna Formation consists of alternating polymict, stratified, grey to yellowish, pebble- size conglomerates and medium-grained sandstones, interbedded with dark grey, sandy siltstones and claystones. Vertical tubular and U-shaped burrows, e.g. Skolithos, Arenicolites and Diplocmterion are common. The formation is dominated by sandstones and conglomerates in the lower and uppermost parts, whereas thicker units of sandy siltstones and claystones are common in middle and upper parts. The Marchaislaguna Formation is upwards truncated by the Recent erosion surface.

The Marchaislaguna Formation represents a mainly shallow marine and fan-delta front facies. The large-scale variations between sandstone and conglomerate units as well as sandy siltstone and claystone units could possibly justlfy a further subdivision of the formation into members.

PPS = 1-8

M P S = M

MPS = 2-4

U

Vm - un~ts dsld f movcg pcbb

Fig. 4-44: Stratigraphic section T-29 Stmto@pe for: Mttrchaislaguna Formation Locality: Peter Winterbukta Reference: Rye Larsen 1982 (unpnbl.)

232

Formation - 1 k i; W ' NORTHWESTERN

SVALBARD

DISTRIBUTION SHOWN ON FIG(s).: 4-06 STATUS OF UNIT: Formal FIRST USE OF NAME: Here, following Rye Larsen 1982 (unpubl.)

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Fig. 4-45b: Stratigraphic section T-30.3, T-30.4 Stmtovpe for: Aberdeenflya Formation (continued) Locality: Aberdeenflya Reference: Rye Larsen 1982 (unpubl.)


Aberdeenflya 3

CURRENT DEFINITION: Here, following Rye Larsen 1982 (unpubl.) SYNONYM(S) AND REFERENCE(S): None ONGIN OF NAME: Aberdeenflya: A coastal plain on northeastern Prim Karls Forland TYPE SECTION PIG. 4-&a-C): Stratotype: Aberdeenflya coast, Prins Karls Forland DEPOSITIONAL AGE: Eocene - Oligocene (?) DAT~NC WTHOD: Indirect, stratigraphic relationship

age I~ii.sbat m - l u n b clsivf f mcvcg pobb

Aberdeenflya 4

REFERENCE(S) FOR AGE: See Buchananisen Group OVERLYING UNIT(S): None UNDERLYING UNIT(S): Selvhgen Fonnation SUPERIOR m: Buchananisen Group OTHER USE OF N A ~ : None THICKNESS: >2800 m (?) MAIN LITHOLOGIES: Conglomerate, sandstone, shale LOWER BOUNDARY DEFINITION: The lower boundary is poorly exposed, but lithologies of the Aberdeenflya Forma-

http://jurassic.ru


MPS=20 v

MPS=8 MPS-S MPS4 7 v

tion are underlain by immature conglomerates probably belonging to the SelvAgen Formation, along the western boundary fault of the Forlandsundet Graben. The relationship with the probably older Marchaislaguna Formation is not known. DESCRIPTION: The Aberdeenflya Formation consists of alternating polymict, stratified, grey to yellowish, pebble-size conglomerates and fine- to medium-grained sandstones, interbedded with dark grey, sandy siltstones and claystones. Horizontal burrows are common. There is an overall coarsening-upward trend within the Aberdeenflya section, with thicker sandstone and conglomerate units and thinner sandy siltstone and claystone units upward. The formation is truncated by Recent erosion.

The Aberdeenflya Formation represents mainly submarine fan and basin-floor facies. The large-scale variations between sandstone/conglomerate units and sandy siltstone/claystone units could argue for a W e r subdivision of the formation into members. The Aberdeenflya Forma- tion is distinguished from the Marchaislaguna Formation as a separate unit because of uncertain stratigraphic relations across unexposed areas and because of slightly different lithological characteristics.

Fig. 44%: Stratigraphic section T-30.5 Stmtotype for: Aberdeenflya Formation (continued) Locality: Aberdeenflya Reference: Rye Larsen 1982 (unpubl.)

a p s m - ddvf f m c w g pcbb

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Balanuspynten conglomerates Q'-31)

STATUS OF UNIT: Informal FIRST USE OF NAME: Here CURRENT DEFINITION: Here, following Atkinson 1963 SYNONYM(S) AND REFERENCE(S): "Sars Formation": Atkin- son 1963. The place name segment is incomplete, referring either to Sarsrayra, Sarstangen or Sarsbukta. All these names are used for other stratigraphic units, the two latter for the two subunits of this one. ORIGIN OF NAME: Balanuspynten: A point on the eastern coast of Forlandsundet TYPE SECTION (FIGS. 4-46,447): See Sarsbukta and Sarstangen conglomerates D E P O ~ I ~ ~ N A L AGE: Eocene - Oligocene (?) DATING METHOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: See Buchananisen Group; Sars- bukta and Sarstangen conglomerates OVERLYING UNIT(S): None UNDERLYING UNIT@): Pre-Old Red SUPERIOR UNIT: Buchananisen Group OTHER USE OF NAME: None THICKNESS: >l600 m (?) MAIN LITHOLOGIES: Conglomerate LOWER BOUNDARY DEFINITION: The base is not exposed, but the unit's conglomerates must rest unconformably on folded metamorphic basement. DESCRIPTION: The name Balanus~nten conglomerates is assigned to Tertiary conglomerates and intercalated sandstones and shales which occur on the eastern shore of For- landsundet. .

The Balanuspynten conglomerates represent the only outcrop of Tertiary strata on the eastern side of Forlandsundet. No continuous stratigraphic section is exposed, and relations between the two subunits (Sarsbukta and Sarstangen conglomerates are not known). The correlation with strata on the western side of Forlandsundet is not known. Docu- mentation of the unit is poor.

Sarsbukta conglomerate (T-32)

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STATUS OF UNIT: Informal FIRST USE OF NAME: Here, following Rye Larsen 1982 (un- Fig. 4-46: Stratigraphic section F32 publ.) Unit stmtotjpe for: Sarsbukta conglomerate CURRENT DEFINITION: Here, following Rye Larsen 1982 Locality: Sars0ya (unpubl.) Reference: Rye Larsen 1982 (unpubl.) SYNONYM(S) AND REFERENCE(S): None

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ORIGIN OF NAME: Sarsbukta: A bay on the eastern coast of Forlandsundet TYPE SECTION (FIG. 4-46): Unit stratotype: Sarsaryra DEPOSITIONAL AGE: Eocene DATLNG METHOD: Indirect, stratigraphic relationship REFERENCE(S) FOR AGE: See Buchananisen Group OVERLYING UNIT(S): Sarstangen conglomerate UNDERLYING UNIT(S): Pre-Old Red SUPERIOR UNIT: Buchananisen Group, (Balanuspynten conglomerates)

USE OF NAME: None THICKNESS: ca. 600 m (?) MAIN LITHOLOGIES: Conglomerate LOWER BOUNDARY DEFINITION: See Balanuspynten con-

/ glomerates DESCRIPTION: The Sarsbukta conglomerate consists of polymict, pebbly to boulder size, grey to yellow-red, partly stratified conglomerates, with interbeds of medium- to coarse-grained sandstones and rare thin siltstones. The Sars- bukta member occurs from Sarsbukta southwards on -- qra , and a minimum total thickness of 600 m can be estimated. The Sarsbukta conglomerate contains scattered plant debris.

The conglomerate has a faulted contact with the Pre-Old Red to the east. The lower boundary is not exposed. The boundary with the Sarstangen conglomerate is not clear, but the latter is likely to unconformably overlie the Sarsbukta conglomerate.

Sarstangen conglomerate ('I-33)

NORTHWESTERN

DISTRIBUTION SHOWN ON RG(s).: 4-06 STATUS OF UNIT: Informal FIRST USE OF NAME: Here, following Rye Larsen 1982 (unpubl.) CURRENT DEFINITION: Here, following Rye Larsen 1982 (unpubl.) SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Sarstangen: A cape on the eastern coast of Forlandsundet TYPE SECTION @G. 4-47): Stratotype: Sarsbukta. The borehole at Sarstangen is probably more suitable, but the log data have not been released by the owners (Norsk Polar Navigasjon 1974). DEPOSITIONAL AGE: Latest Eocene - (?Early) Oligocene DATING METHOD: Foraminifera, dinoflagellates, palynology REFERENCE(S) FOR AGE: Manum 1960, 1962; Feyling-

age l lith. strat - l units dsivf f m c v c g pcbb

Fig. 4-47: Stratigraphic section T-33 Hypostratotype for: Sarstangen conglomerate Locality: Balanuspynten Reference: Feyling-Hanssen & Ulleberg 1984

Hanssen & Ulleberg 1984; Manum & Throndsen 1986; Livsic 1992; unpubl. data, Norsk Hydro 1996 OVERLY~VC UNIT(S): None UNDERLYING UNIT(S): Pre-Old Red, Sarsbukta conglomerate (?) SUPERIOR UNIT: Buchananisen Group, (Balanuspynten conglomerates) OTHER USE OF NAME: None THICKNESS: >l050 m (?) MAIN LITHOLOGIES: Conglomerate LOWER BOUNDARY DEFINITION: The lower boundary is defined by conglomerates resting on an angular unconformity above folded metamorphic basement (borehole data). The boundary with the Sarsbukta conglomerates to the east is presently unclear, but another, low-angle unconformity is suggested (K. Kleinspehn, written comm. 1997). DESCRIPTION: The Sarstangen member consists of interbedded, commonly stratified conglomerates, fine- to coarse- grained sandstones or conglomerates and siltstones. The formation is present along the coast from Sarsoyra to Kaffi- BYI;~, but the exact thickness is not known. The borehole at Srrrstangen (Norsk Polar Navigasjon 1974) shows 1050 m of probable Sarstangen conglomerate strata unconfonnably overlying folded and metamorphic basement. The unit contains abundant plant remains.

The Sarstangen member represents mixed alluvial fan toe and alluvial plain facies. The main difference from the Sars- bukta member is the presence of alluvial plain sandstones and siltstones, as well as a distinctly less consolidated texture and lack of deformation.

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4.4.3 Calyasostranda Group

CALYPSOSTRANDA GROUP (T-34)

STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Here SYNONYM(S) AND REFERENCE(S): None The unit has been called '"Tertiary of Kapp Lyell" and "Ter- tiary of Renardodden" in various publications. ORIGIN OF NAME: Calypsostranda: A strandflat south of Bellsund TYPE AREA: Skilvika - Renardodden STRUCTURAL SETTING: West Spitsbergen Fold-thrust belt; probably a remainder of a Tertiary sedimentary basin, whose main record is suggested to to lie offshore west of Spitsbergen DEPOSITIONAL AGE: Late Eocene - Early Oligocene OVERLYING UNIT@): None UNDERLYING UNIT(S): Re-Old Red SUPERIOR UNIT: None OTHER USE OF NAME: None THICKNESS: 265 m in the stratotype MAIN LITHOLOGIES: Sandstone, siltstone, shale, coal DESCRIPTION: The group comprises a sedimentary succession consisting of sandstones, siltstones, shales, coal seams and subordinate conglomerates, comprising the Tertiary rocks of the Bellsund area. It unconformably overlies the Precambrian basement, but is - in outcrop - mostly separated from the basement by a fault. The strata probably belong to a larger basin extending into the western offshore area. For descriptions see the two individual Skilvika and Renardodden formations.

1 SOUTHERN SPlTSBERGE

DISTRIBUTION SHOWN ON FIG@).: 4-04 STATUS OF UNIT: Formal FIRST USE OF NAME: LivBic 1967 CURRENT DEFINITION: LivBic 1967 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Skilvika (transl.: "The Divide Bay"): A bay south of Bellsund, in the type area TYPE SECTION (FIG. 4-49): Stratotype: Skilvika DEPOSITIONAL AGE: Late Eocene - Early Oligocene DATING METHOD: Palynology REFERENCE(S) FOR AGE: Head 1984 OVERLYING UNIT(S): Renardodden Formation UNDERLYING UNIT(S): Re-Old Red SUPERIOR UNIT: Calypsostranda Group

USE OF NAME: None THICKNESS: 103 m in the stratotype MAIN LITHOLOGIES: Sandstone, shale, coal, breccia LOWER BOUNDARY DEFINITION: The formation rests with an angular unconformity on Precambrian metasediments. A 4.3 m thick breccia occurs at the base of the formation. DESCRIPTION: There may be a slight unconformity between the basal breccia and the overlying strata. The Skilvika For- mation otherwise consists of interbedded, often fining- upwards, grey, fine-grained sandstones and dark siltstones/claystones, with calcareous horizons in the middle part adabundant thin coal seams in the upper part (Fig. 4- 48). The formation is abruptly, possibly erosively, overlain by conglomerates and sandstones of the Renardodden For- mation. The rocks contain abundant plant remains. (Atkin- son 1963; LivSic 1967,1974; Lehrnann et al. 1978; Thiedig et al. 1979.)

The Skilvika Formation represents a mainly fluvio-deltaic facies. The fine-grained nature of the formation suggests low depositional gradients and prolonged stability accompanied by gradual basin subsidence.

Fig. 4-48: Sandstone and coal seam in the Skilvika Formation. Photo: E.P. Johannessen

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mations Locality: Skilvika - Renardodden Refwnce: Kleinspehn, K. (unpubl.)

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4. TERTIARY LITHOSTRATIGRAr""

RENARDODDEN FORMATION (T-36) 4.4.4 Other units

D I ~ ~ U T I O N SHOWN ON RG(s).: 4-04 STATUS OF UNLT: Formal FIRST USE OF NAME: Livgic 1967 C ~ N T DEFINITION: Livgic 1967 SYNONYM(S) AND REFERENcE(S): None ORIGIN OF NAME: Renardodden: A cape south of Bellsuncl, type area TYPE SECTION (FIG. 4-49): Stratotype: Skilvika - Renardodden DEPOSITIONAL AM: Late Eocene - Early Oligocene DATING METHOD: PalJ'n010gy REFERENCE(S) FOR AGE: Head 1984 OVERLYING UNIT@): None UNDERLYING UNIT(S): SUYika Fonwion SUPERIOR m: -R USE OF NAME: NOlIe

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Trm~~~~sars >l6Q m (apmd prtrt of type section) MAIN LSL'H~LOGM: Sandstone LAWER BOUNDA~;(Y DEFINITION: A 2.6 thick conglomerate defines the base of the formation, ass iated with a possible

Skilvika Formation.

2 unconformable (erosive) boundary with the underlying

DESCRIPTION: The Renardodden Formation consists of relatively monotonous, grey, fine to medium-grained sandstones, with some interbeds of dark grey siltstones and claystones, as well as streaks and thin seams of coal. The sandstones are loosely cemented and contain numerous siderite concretions and Ophiomo7pha burrows. The top of the formation is truncated by the Quaternary unconformity. (Atkinson 1963; LivSic 1967, 1974; Lehmam et al. 1978; Thiedig et al. 1979.)

The Renardodden Formation represents a mostly shallow marine facies, and the homogeneous nature of the formation suggests that sediment equal or close to the rate of b i n t3hsi&m for p a i d .

. L ..

DISTRIBUTION SHOWN ON FIG@).: 4-07 STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Prestvik 1978 SYNONYM(S) AND RE~RENCE(S): None ORIGIN OF NAME: Seidfjellet: A mountain with a basalt plateau in eastern Andreie Land adjacent to Tavlefjellet. TkPE SECTION: Stratotype: Sddfjellet ("Tav1efjellet" according to Muragov & Mokin 1976) STRU- SET~NG: ~ ~ - P l b c e n e plateau of northern Swsllkd, still r e q p h i d by a northward inclined

of the momaai& taps ia Andr6e Land DEPOSITIONAL AGE: EMiocene-Pliwene DATING METHOD: Isotopic age determination, K-Ar and 40Arl39Ar methods REFERENCE(S) FOR AGE: BWOV &. -0 1976; Pre~tvik 1978 OVERLYING UNIT(S): None U N D E R L ~ G UNIT(S): Andreie Land Group (Devonian) and Pre-Old Red SUPERIOR UNIT: None OTHER USE OF NAME: None THICKNESS: < ca. 400 m (275 m in type section) MAIN LITHOLOGIES: B d t LOWER BOUNDARY DEFINITION: The lower boundary is marked by the base of Tertiary basalt flows or associated pyroclastic rocks above Devonian or older rocks. DESCRIPTION: The SeidfjeIlet Formation consists of plateau lavas unconformably overlying Devonian (occasionally Pre- cambrian) rocks in the area a r d Woodqorden (NW Spitsbergen). They are only preserved within the limits of the Devonian Graben. Their thickness is 275 m in the trpe section (Burav L Zagruzh 1976), where up to 15 lava flows (Hoel 1914) are reported, with interbeds of scoriaceous material. The l a w are transitional olivine basalts (both ne- and hy-normative types). A prominent pre-basalt palamrelief is observed in the area around Scott-Keltiefjel- let and Loyndfjellet, where the thickness of the lava flows locally reaches up to ca. 400 m above the valley bottoms in the underlying incised relief (Fig. 4-50).

Fig. 4-50: Basalt flows of the Seidtjellet Formation filing in a palam- . relief, Lnyndfjellet, Andrbe Land. Photo: W.K. DaUmann.

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The lavas are thought to represent different degrees of par- known, but it certainly attains several hundred meters. t i a l melting of a mantle source where clinopyroxene was a The Sutorfjella conglomerate represents mostly alluvial

residual phase. Trace element data suggest that some of the fan facies, deposited close to a tectonically active basin basalt magmas were contaminated by crustal material margin (Rye Larsen 1982, unpubl.). (Prestvik 1978). WAr age determinations yielded ages of 6W25 and 2U10 Ma (Burov & Zagruzina 1976), 11.5*1.2 and 10.4*l.l Ma (Prestvik 1978). 40ArJ39Ar age detenninations yielded 8.7 Ma for the Manbreen exposure in Ny Friesland (Prestvlk, Ohta pers. comm. 1994).

4.5 Abandoned lithostratigraphic unit names

4.5.1 Names with aplace name segment

Sutorfjella conglomerate (T-38)

DISTRIBUTION SHOWN ON FIG(s).: 4-06 STATUS OF UNIT: Informal FIRST USE OF NAME: Hoe1 19 12 CURRENT DEFINITION: Craig 19 16 SYNONYM(S) AND REFERENCE(S): "Sutor" conglomerate: Hoe1 1912; Sutorfjella conglomerate member: Harland et al. 1979 ORIGIN OF NAME: Sutorfjella: A mountain area on northwestern Prins Karls Forland TYPE AREA: S~toIfJella STRUCTURAL SETTING: Occurs locally on the Western basement province DEPOSITIONAL AGE: The conglomerate has not been dated conclusively. All published interpretations are based on "re- semblance" when compared with Svalbard's deposits of the respective ages. Geologist of the Norwegian Polar Institute presently mapping the area favour Atkinson's Late Protero- zoic age interpretation (A. Hjelle, Y. Ohta, pers. comm. 1997). The unit is included here, because the Tertiary option has been favoured repeatedly, e.g. by Rye Larsen (1982, unpubl.). REFERENCE(S) FOR AGE: Late Proterozoic (Atkinson 1956); Devonian (Craig 191 6); Tertiary (Tpell 1924) OVERLYING UNIT(S): None UNDERLYING UNIT(S): Pre-Old Red SUPERIOR UNIT: None OTHER USE OF NAME: None THICKNESS: Several hundred metres MAIN LITHOLOGIES: Conglomerate LOWER BOUNDARY DEFINITION: Unconfonnable boundary with underlying metapelitic and metapsammitic rocks of the metamorphic basement. DESCRIPTION: The Sutorfjella conglomerate occurs locally in a fault block of ca. 4 km exposed length on northwestern Prim Karls Forland. It consists of polymict, pebble to boulder size, greenish-grey to yellow-brown conglomerates with a weak slaty cleavage. The total thickness of the unit is not

- -p p p

Names listed in this section are not recommended for future use. They are either synonyms of other, preferred names, or describe units that overlap, or are incompatible, with another, preferred stratigraphic subdivision. Some names are defined in a sequence stratigraphic context and have no lithostratigraphic merit. Preferences are discussed in sections 4.2 and 4.3.

For most entries, the synonym or superior unit name which should be consulted in the lexicon (section 4.4) is indicated with its ID number.

Advenffjorden Beds (A. Schichten; Vonderbank 1970): The name refers to a genetically defined unit and is applicable in sequence stratigraphy. It has no value for lithostratigraphic subdivision, because its boundaries are not mappable by normal/common field methods.

Askeladden Delta Sequence (N0ttvedt 1982 [unpubl.], 1985): The name refers to a genetically defined unit and is applicable id sequence stratigraphy. It lias no value for lithostratigraphic subdivision, because its boundaries are not mappable by normaYcommon field methods.

Barentsburg Formation (LivSic 1967): The contemporaneously published synonym "Firkanten Formation" (Major & Nagy 1964, 1972) is preferred because of its more extensive use in the published literature.

Berzeliusdalen Member (Ytreland 1980, unpubl.): The member is locally observed in western Nordenskiold Land, but has not been discussed in a regional context. It is suspected to overlap with the already defined member subdivison of the Firkanten Formation (T-2 to T-6) (Kalgraff 1978, unpubl.; Steel et al. 1981).

Camp Morton Member (Ytreland 1980, unpubl.): The member is locally observed in western Nordenskiijld Land, but has not been discussed in a regional context. It is thought to overlap with the previously defined member subdivison of the Firkanten Formation (T-2 to T-6) (Kalgraff 1978, unpubl.; Steel et al. 1981).

Colesbukta Formation (Livlic 1967): Synonym of the contemporaneously published term Basilika Formation (T-7) (Major & Nagy 1964, 1972); the latter is preferred because of the more complete section at the mountain Basi- lika and the more extensive use in the published literature (see section 43.1). At Colesbukta, the lower part of the formation is not exposed.

Collinderodden Formation (LivSic 1967): Synonym of the contemporaneously published term Battfjellet Formation (T-14) (Major & Nagy 1964, 1972); the latter is preferred because of its more extensive use in the literature on this unit (see section 4.3.1).

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Fardalen Beds (E Schichten; Vonderbank 1970): The name refers to a genetically defined unit and is applicable in sequence stratigraphy. It has no value for lithostratigraphic subdivision, because its boundaries are not mappable by normal/common field methods.

Forlandsundet Group (Harland 1969): The name is also used for a structural feature (Forlandsundet Graben; Har- land 1969). This is an inconvenient double use of the name, especially because the depositional area of the Ter- tiary strata was not restricted to the present graben (IUein- spehn & Teyssier 1992). The name 'Forlandsundet' is better established for the structure than for the stratigraphic group. The group is proposed to be renamed Buchanan- isen Group (T-24) (see section 4.3.3).

Gramant Formation (LivBic 1967): Incomplete place name, see Grumantbyen Formation (T-8).

Grnmantdalen Beds (G. Schichten; Vonderbank 1970): The name refers to a genetically defined unit and is applicable in sequence stratigraphy. It has no value for lithostratigraphic subdivision, because its boundaries are not mappable by normal/common field methods.

Kolfjellet Member (Ytreland 1980, unpubl.): The member is locally observed in western Nordenskiold Land, but has not been discussed in a regional context. It is thought to overlap with the previously defined member subdivison of the Firhnten Formation (T-2 to T-6) (Kalgraff 1978, unpubl.; Steel et al. 1981).

Marchaise Formation (LivSic 1967): Incomplete place name, see Marchaislaguna Formation (T-29).

McVitie Formation (Atkinson 1963): Incomplete place name, see McYitiepynten Formation (below).

McVitiepynten Formation (Birkenmajer 1972, following Atkinson 1963): Within this unit, LivSic (1967) and Rye Larsen (1982, unpubl.) have distinguished five formations (Sesshagda, Reinhardpynten, Krokodillen, Marchais- laguna and Aberdeenflya formations). The latter subdivision uses formational rank in a way consistent with the earlier published subdivision of the Van Mijenfjorden Group. The name 'McVitiepynten', comprising arbitrarily five of the eight formations of the Buchananisen Group, or five of six formations on the Prins Karls Forland side of the Forlandsundet Graben, is superfluous (see section 4.3.3). Authors wishing to use the name because of its chronological priority, should apply a subgroup rank.

Mendelejevbreen Member (Ytreland 1980, unpubl.): The member is locally observed in western Nordenskiold Land, but has not been discussed in a regional context. It is thought to overlap with the previously defined member subdivison of the Firkanten Formation (T-2 to T-6) (Kalgraff 1978, unpubl.; Steel et al. 1981) and possibly also with the Basilika Formation (T- 7).

Nordenskiiildfjellet Beds (N. Schichten; Vonderbank 1970): The name refers to a genetically defined unit and is applicable in sequence s'tratigraphy. It has no value for lithostratigraphic subdivision, because its boundaries are not mappable by normal/comm.on field methods.

Sarkofagen Formation (Major & Nagy 1964, 1972): The name comprises two different sandstone sheets, the Grumantbyen Formation (T-8), Hollendardalen Forma- tion (T-13) and the intercalated Marstmnderbreen Mem-

ber P O ) . The contemporaneously published alternative subdivision by LivSic (1967) is preferred, although revised (see section' 4.3.1). The upper boundary of the "Sarkofagen Formation" cannot be defined in northeastern areas because of the lack of the Hollendardalen For- mation.

Sars Formation (Atkinson 1963): Incomplete place name, comprising the conglomeratic Sarstangen (Rye Larsen 1982, unpubl.) and Sarsbukta (Birkenmajer 1972) conglomerates (T-32,33). See synonym Balamqvnten conglomerates (T-31).

Storvola Formation (LivBic 1967): Synonym of the contemporanously published name Aspelintoppen Formation (T-15) (Major & Nagy 1964, 1972); the latter is preferred because of easier access to the locality and its more extensive use in the literature (see section 4.3.1). Both sections are equally well developed.

Sutor conglomerate (Hoe1 1912): Incomplete place name, see Sutorjjella conglomemte (T-38).

Tvillingvann Member: See Tvillingvatnet Member.

4.5.2 Names without aplace name segment

Names without a place indicative segment are in general old, informal names that meanwhile have been substituted by formal names. For a number of names, the grouping of strata does not correspond to the more recent lithostratigraphic subdivision. All of these names are today out of use. They are listed here with their reference (first published) and indication of stratigraphic range for the purpose of understanding older geological literature in a modern context.

For each entry, the synonym or superior unit name which should be consulted in the lexicon (section 4.4) is indicated with its ID number.

Fissile sandstone series (Nathorst 1910): Synonym of Batt- dellet Formation (T-14)

Flaggy Sandstone Series (Orvin 1940): Synonym of Batt- jellet Formation (T-14)

Green Sandstone (Orvin 1934): Synonym of Brsggerbreen Formation (T-21)

Green sandstone formation (LjutkeviE 1937a): Synonym of Grumantbyen Formation (T-8)

Green Sandstone Member (Challinor 1967): Synonym of Br~ggerbreen Formation (T-21)

Green sandstone series (Nathorst 1910): Corresponds to "Sarkofagen Formation", or Grumantbyen Formation (T- 8), Marstmnderbreen Member (T-10) and Hollendardalen Formation (T-13)

Grey Sandstone (Orvin 1934): Synonym of Kongsfiorden Formation (T-17)

Grey Sandstone Member (Challinor 1967): Synonym of Kongsjorden Formation (T-17)

Light Sandstone (Orvin 1934): Synonym of Tvillingvatnet Member (T-19)

Lower argiIlite formation (LivBic 1965): Synonym of Basilika Formation (T-7)

Lower black shale formation (LjutkeviE 1937a): Synonym of Basilika Formation (T-7)

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Lower black shale series (Nathorst 1910): Synonym of Basilika Formation (T-7)

Lower Coal Horizon (Orvin 1934): Synonym of Kol- haugen Member (T-18)

Lower coal-bearing sandstone formation (LjutkeviE 1937a): Synonym of Firkanten Formation (T-2)

Lower Dark Shale Series (Orvin 1940): Synonym of Basi- lika Formation (T-7)

Lower light sandstone series (Orvin 1940): Synonym of Filtkanten Formation (T-2)

Lower sandstone series (Hoel 1925): Corresponds to the lower part of the Van Keulenfjorden Group, comprising the Firkanten (T-2), Basilika (T-7) Grumantbyen (T-10) and Hollendardalen (T-13) firmations

Lower transitional formation (LivSic 1965): Corresponds to Marstmnderbreen Member (T-10) and Hollendardalen Formation (T-13)

Middle shale series (Hoel 1925): Synonym of Gilson- w e n Member (T-I I)

Shaley green sandstone formation (LjutkeviE 1937a): Corresponds to Marstmnderbreen Member (T-10) and Hollendardalen Formation (T-13)

Taxodium shale (Heer 1870): The Taxodium shale unit consists of less than 1 m thick, dark grey to black, laminated paper shales with abundant plant fossils. They occur in the lower part of the Todalen Member (T-3) at Gmm-

fjorden. They contain ca. 20% (of dry rock) bituminous matter. Characteristic plant fossils are Taxodium dis- tichum miocenum HEER, Sequoia nordenskioldi HEER and Libocedrus subiniana HEER.

Upper argillite formation (LivSic 1965): Synonym of Gilsonryggen Member (T-11)

Upper black shale formation (LjutkeviE 1937a): Synonym of Gilsonryggen Member (T-11)

Upper black shale series (Nathorst 1910): Synonym of Gilsonryggen Member (T-1 I)

Upper coal-bearing sandstone formation (LjutkeviE 1937a): Synonym of Aspelintoppen Formation (T-15)

Upper coal-bearing series (Nathorst 1910): Synonym of Aspelintoppen Formation (T-15)

Upper Plant-Bearing Sandstone Series ( k i n 1940): Synonym of Aspelintoppen Formation (T-15)

Upper sandstone formation (LivBic 1965): C~rresponds to upper part of Battjjellet Formation (T-14) and Aspelin- toppen Formation (T-15)

Upper sandstone series (Hoel 1925): Corresponds to upper part of Battjjellet Formation (T-14) and Aspelintoppen Formation (T-15)

Upper shaley sandstone formation (LjutkeviE 1937a): Synonym of Bat@ellet Formation (T-14)

Upper transitional formation (LivBic 1965): Lower part of Bawellet Formation (T-I4)

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WINFRIED K. DALLMANN

5.1 General remarks

Volcanic activity of Quaternary age occurred in northwestern Spitsbergen. Remains of three volcanic features are preserved on, or in the vicinity of, the Breibogen Fault (Fig. 1- OS), a major north-south directed fault separating Devonian sediments from metamorphic Caledonian basement rocks. Movements along this fault date back to at least the Devon- ian.

One of the features, Sverrefjellet, still is reminiscent of a volcano, although it has been reshaped by glacial activity. It consists mainly of pyroclastics. Halvdanpiggen is the remains of a volcanic pipe and forms a prominent basalt neck rising above red Devonian sandstones. Sigurdfjellet shows a prominent ridge composed of basaltic pyroclastics (Fig. 4- 07).

The volcanic and subvolcanic rocks are classified as off- ridge alkali basalts, with a considerable amount of xenoliths derived from deep crustal and upper mantle regimes. The age of the two first cehtres is probably between 100,000 and 250,000 years, while the third may be older (Skjelkville et al. 1989). Thermal springs situated close to Sverrefjellet (Trolkjeldane, .Jotunkjeldane), with water temperatures reaching 14-28°C witness to the continuously high geothermal gradient in the area, which is related to the Yermak h a spot north of Spitsbergen (Fig. 1-02).

No stratigraphic nomenclature for these rocks has been published. A collective name, Bocworden Volcanic Com- plex, is proposed here, while the individual occurrences should conveniently be addressed by their geographical names Sverrejellet, Halvdanpiggen and Sigurdjellet.


BOCKFJORDEN VOLCANIC COMPLEX (Q-01)

NOR

~)ISTRIBUTION SHOWN ON FIG@).: 4-07 STATUS OF UNIT: Formal FIRST USE OF NAME: Here CURRENT DEFINITION: Skjelkviile et al. 1989 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Bockfjorden: A fiord in northwestern Spitsbergen, a bifurcation of Woodfjorden TYPE AREA: Bockfjorden and its environments, northwest- em Spitsbergen STRUCTURAL SETTING: Breibogen Fault and ass0ciate.d structures VOLCANIC AGE: Pleistocene (see individual eruptive centres) OVERLYING UNIT(S): None HOST UNIT@): AndrBe Land Group (Devonian), Pre-Old Red SUPERIOR UNIT: None OTHER USE OF NAME: Bockfjorden anticline (Gee 1972): A basement anticline paralleling Bockfjorden, west of the Breibogen Fault. The name is informal and little used. MAIN LITHOLOGIES: Basaltic pyroclastics and lava DESCRIPTION: The complex consists of three separate eruptive centres (Sverrefjellet, Halvdanpiggen and Sigurdfjellet) within a distance of 20 km. The centres show varying volcanic and subvolcanic features and are preserved at different erosional levels, all from the eroded remains of stratovolcano to subvolcanic vents.

A wide variety of upper mantle and lower crustal xenoliths comprise about 15-20 vol.% of the volcanic centres (Arnundsen 1987; Arnundsen et al. 1987, 1988).

The petrographic composition of the basalts is alkaline, with phenocrysts of olivine, titanaugite and rare plagioclase together with xenocrysts, embedded in a fine-grained matrix of euhedral olivine, titanaugite, plagioclase laths, ti- tanomagnetite and basaltic glass.

The chemical composition indicates that magmas were primitive and that some may be primary. The magmas as-

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5. QUATERNARY VOLCANIC AND SUEVOLCANIC ROCKS

cended rapidly after the entrainment of the xenoliths, and no low lavas and pahoehoe flows indicates that the volcano magma chamber developed. The magmas are typical of in- grew concurrently with the rise of the surrounding glaciers. traplate, alkaline volcanism. Geothermobarometry calcula- Glacial debris occurs on its flanks. Reworked material from tions on xenoliths fiom the three eruptive centres define a the volcano forms marine terraces below the eastern slope very high geotherm consistent with their location near the at Bockfjorden at 5-60 m above sea level. Yermak hot spot (Fig. 1-02). The crust-mantle boundary is Though reminiscent of a primary volcanic shape, the pre- calculated to be at a depth of 27 km. (SkjelkvIle et al. 1989) sent outline of the mountain is the result of erosion. The sur-

face is 80% covered with frost-weathered material, while 20% is made up of lava surfaces. Lava flows are 1-3 m thick

SVERREFJELLET VOLCANO (Q-02) and may form successions of up to 15 flows. Most seem to be derived from flank eruptions. A dike is exposed in an

DISTRIBUTION SHOWN ON FIG@).: 4-07 eroded valley side on the southeastern flank. STATUS OF UNIT: Formal At an elevation of 350-450 m,-the main volcanic vent is FIRST USE OF NAME: Hoe1 & Holtedahl 191 1: Le volcan de exposed with a diameter of ca. 200 m. Its pyroclastic mate- la Baie Bock [Mt. Sverre] rid is hydrothermally altered and shows up to 10 m high CURRENT DESCRIPTION: SkjelkvAle et al. 1989 erosional pillars consisting of lava, outwardly grading into SYNONYM(S) AND REFERENCE(S): None scoriaceous material. Some of the pillars contain hollow ORIGIN OF NAME: Sverrefjellet: The ruin of a volcano west tubes interpreted as magma conduits. (SkjelkvUe et al. of Bockfjorden, northwestern Spitsbergen, named after an 1989) Old Norse king VOLCANIC AGE, REFERENCES AND DATING METHODS: Hoe1 & Holtedahl 191 1: Post-glacial; morphological (mis)interpre- H~LMANPIGGEN ERUPTIVE CENTRE (4-03) tation Gjelsvik 1963: Partly subglacial; fiom the existence of pil- DISTRJBUTION SHOWN ON FIG@).: 4-07 low lavas STATUS OF UNIT: Formal Burov & MuraSov 1964 (unpubl.): 0.01-0.2 Ma; geomor- FIRST USE OF NAME: SkjelkvAle et al. 1989 phological analysis CURRENT DESCRIPTION: SkjelkvIle et al. 1989 Halvorsen 1972: <0.7 Ma; palaeomagnetology SYNONYM(S) AND REFERENCE@): None Burov & Zagruzina 1976: < 1 Ma; K-Ar radiometric age de- ORIGIN OF NAME: Halvdanpiggen (transl. "The Peak of termination Halvdan"): A volcanic pipe in Riisefjella east of Bock- SkjelkviUe et al. 1989: 0.1-0.25 Ma, comparative studies of fjorden, northwestern Spitsbergen, named after an Old glaciation episodes, erosion and morphology Norse king. The associated volcanic features Olavst&rnet HOST UNIT@): Pre-Old Red (transl. "The Tower -of Olav") and Haraldknattane (transl. SUPERIOR UNIT: Bockfjorden Volcanic Complex "The Humps of Harald") are also named after ancient kings. OTHER USE OF NAME: None VOLCANIC AGE, REFERENCES AND DATING METHODS:

DIMENSIONS: Elevation above sea level: 20-506 m. Area: Halvorsen 1972: >0.7 Ma; palaeomagnetology Subcircular, ca. 7 km2 (3 km across) SkjelkvIle et al. 1989: Older than Sverrefjellet; concluded MAIN LITHOLOGIES: Basaltic pyroclastics and lavas from its deeper erosion and greater degree of weathering DESCRIPTION: The Sverrefjellet Volcano (F@. 5-01) is the HOST UNIT(S): Andrbe Land Group (Devonian) ruin of a stratovolcano constructed of primitive alkali SUPERIOR UNIT: BockfjordenVolcanic Complex basaltic pyroclastics (scoria, lapilli, bombs) with subordi- OTHER USE OF NAME: None nate pahoehoe lavas rich in xenoliths derived from the upper DIMENSIONS: Elevation above sea level: 580-834 m. Area: mantle and lower crust. The occurrence of interbedded pil- Subcircular, 0.012 kmZ (400 m across)

MAIN LITHOLOGIES: Basaltic pyroclastic breccia DESCRIPTION: The Halvdanpiggen Eruptive Centre (Fig. 5- 02) is a complex of vents and high-level intrusives in Halv- dandalen (Riisefjella). The largest body is Halvdanpiggen itself, a volcanic neck 200 m across, consisting of a pyroclastic breccia of basaltic blocks and 60-70 % angular high-

+- - --:{h * F T .C pressure xenoliths. The central section of Halvdanpiggen is

h , , intruded by aphanitic, non-vesicular basalts weathering with '?U .

.I* a fanning columnar jointing. Small outcrops of pyroclastics and basalt around the neck

suggest that the actual diameter of the vent is ca. 400 m. Halvdanpiggen is interpreted to be a complex, deeply eroded diatreme or volcanic conduit.

Numerous associated satellite vents occur within a 2-km Fig. 5-01: Svmefjellet at Bockfjorden, part of the volcanic structure radius. Olavst4met is a small neck, 5 m across and 5 m

is preserved, although the present shape is a result of glacial erosion. high, ca. 1 km southwest of Halvdanpiggen. It consists of Photo: K. Hsgvard basalt with radial, columnar jointing. Two dikes strike from

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Fig. 5-02: Halvdanpiggen at'woodfjorden; erosion of the volcanic complex is deep and only part of the volcanic pipe and some veins fonn morphological features. Photo: W.K. Dallmann

the neck towards Halvdanpiggen. Haraldknattane occur 1.5-2 km east of Halvdanpiggen and comprise three small tuff-breccia vents at 485 m, 520 m and 700 m elevations. They consist of loosely consolidated breccia containing lava fragments, high-pressure xenoliths and Devonian host rock. The breccia is cut by two dikes, 10 m and 50 m long, and 0.2 m and 0.5 m thick, the longer terminating in a small volcanic neck. (Skjelkv8le et al. 1989)

DISTRIBUTION SHOWN ON FIG@).: 4-07 STATUS OF UNIT: Formal FIRST USE OF NAME: Skjelkvkle et al. 1989 CURRENT DESCRIPTION: Skjelkvkle et al. 1989 SYNONYM(S) AND REFERENCE(S): None ORIGIN OF NAME: Sigurdfjellet: A mountain ridge consisting of volcanic rocks at Vonbreen, northwestern Spits- bergen, named after an Old Norse king VOLCANIC AGE, REFERENCES AND DATING METHODS:

Skjelkvdle et al. 1989: 0.1-0.25 Ma; indirectly from of morphology and degree of weathering in comparison with Sverrefjellet HOST UNIT(S): Andrte Land Group (Devonian), Pre-Old Red SUPERIOR UNIT: Bockfjorden Volcanic Complex OTHER USE OF NAME: None DIMENSIONS: Elevation above sea level: 910-1,162 m Area: Elongate, 4.5 km long, 200-250 m wide MAIN LITHOLOGIES: Basaltic pyroclastics DESCRIPTION: The Sigurdfjellet Eruptive Centre is an elongate ridge on - although normal to - the Breibogen Fault. It cuts across the fault and overlies Devonian rocks to the east, and Proterozoic basement rocks to the west of it.

The ridge consists of coarsely bedded pyroclastics (breccias, lapillistones, tuffs, bombs) penetrated by several smaller (5-10 m in diameter) explosion vents. One basalt neck, 2 m across, occurs on the top of the ridge on the eastern side. Pahoehoe lava flows occur locally at the southeastern end overlying Devonian. The occurrence is interpreted as a partially eroded diatreme or magma conduit. (SkjelkvAle et al. 1989)

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6. TABLES

6.1 Recommended stratigraphic unit names

The table below contains all 234 stratigraphic unit names which form part of the Upper Palaeozoic to Tertiary schemes recommended herein. The names are listed in al- phabetical order according to their English form. The Nor- wegian spelling follows modern Nynorsk orthography and has been approved by the Norwegian Language Council.

The ID numbers help identifying the respective units in the lexicon text, stratigraphic type sections, maps and other tables. The table further indicates the formal or informal status of the units (see Appendix). The right column shows the superior stratigraphic unit to allow a quick check where a respective name belongs.

CP-71 formal Kapp U e Formation Botneheia Formation Botneheiformasjonen M-24 formal Sassendalen Group Brattberget member Brattbergleddet CP-43 informal Hyrnefjellet Formation Bravaisberget Formation Bravaisbergformasjonen M- 19 formal Sassendalen Group Brentskardhaugen Bed Brentskardhauglaget M-54 formal Wilhelmraya Subgroup

Brevassfjellaget (Brev.fjel1-laget) M-08 formal Kistefjellet Member Brarggerbreen Formation Brarggerbreformasjonen T-2 1 formal Ny-hesund Subgroup Braggertinden Formation Braggertindformasjonen CP-35 formal Charlesbreen Subgroup

CP-56 formal Tyrrellfjellet Member Buchananisen Group Buchananisgruppa T-24 formal none Biinsowbukta Member Biinsowbuktleddet M-74 formal Agardhfjellet Formation Cadellfjellet Member Cadellfjelleddet (Cadellfjell-leddet) CP-50 formal Wordiekammen Formation Calypsostranda Group Calypsostrandgruppa T-34 formal none Campbellryggen Subgroup Campbellryggundergruppa CP-24 formal Gipsdalen Group Carolinefjellet Formation Carolinefjellformasjonen M-93 formal Adventdalen Group Carronelva member Carronelvleddet CP-3 1 informal Minkinfjellet Formation Charlesbreen Subgroup Charlesbreundergruppa CP-34 formal Gipsdalen Group Dalkjegla Member Dalkjegleleddet M-94 formal Carolinefjellet Formation De Geerdalen Formation De Geerdals-formasjonen M-34 formal Storfjorden Subgroup Deltadalen Member Deltadalsleddet M- 14 formal Vikinghargda Formation

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6. TABLES

Helvetiafjellformasjonen M-89 formal Advcmtdalen Group Hjelmleddet CP-42 informal Hyrnetjellet Formation Hoelbreleddet CP-04 formal bbyebreen Formation Hsgsletteleddet M-75 formal Agardhfjellet Formation

Hollendardalen Formation Hollendardalsformasjonen T-13 formal Van Mijenfjorden Group v ' $ "

I Hmbyebreen Formation m~ ~ Hmbyebreformasjonen - . -". . CP-02 formal Billefjorden Group Hornsundneset Formatioq ' : Hornsundnesformasjonen - - "

CP-14 formal Billefjorden Group Hovtindleddet , , -

. . ~ , - CP-82 informal Kapp Starostin Formation : : Hultbergformasjonen A . -. - CP-25 formal Campbellryggen Subgroup

Hyrnefjellformasjonen CP-41 formal GipsdalenGroup Idunfjellet Member

M-67 informal Janustjellet Subgroup M-27 formal Sassendalen Group

- -- - M-95 formal Carolinefjellet Formation

. . M-35 formal De Geerdalen Formation ' M- 10 formal Tvillingodden Formation

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;TATUS SUPERIOR UNIT 1 3 L ormd lngeydjupet Subgroup

H-a5 . . ,to@,. Adventdalen Group 3-6J . , informal Gipshuken Formation

l

- -

M43 formal Wilhelmsya Subgroup ,. . l

Knurrfonnasj one formal, Adventdalen Groy ' : ~ ' .

Reke Member Rekeleddet :: : .M-59 formal Fruholmen Formation Renardodden Formation Renardoddfonnasjonen ' ' ' T-36.,'!;' .. . is: L,.!:r - hrmd Calypsostranda Group

m&-- Revtannleddet :-a woml Kappm--"I Formae - - m m I

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I STRATIGRAPHIC UNIT NORWEGLAN SPELLING ID

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6. TABLES

STRATIGRAPHIC UNIT NORWEGIAN SPELLING ID STATUS SUPERIOR UNIT

Urnetoppen member Urnetoppleddet M-05 informal Vardebukta Formation Van Keulentjorden Member Van Keulenfj ord-leddet M-23 formal Bravaisberget Formation Van Mijenfjorden Group Van Mijenfjord-gruppa T-0 1 formal none Vardebukta Formation Vardebuktfomjonen M-02 formal Sassendalen Group Vegardfjella Formation Vegardfjellformasjonen CP-09 formal Billefjorden Group Vendomdalen Member Vendomdalsleddet M-16 f o m l %kinghragda Formation Vengeberget member Vengebergleddet CP-61 informal Gipshulten Formation Verdande Bed Verdandelaget M-18 formal Urd Formation Vesalstranda Member Vesalstrandleddet CP- 17 formal Raedvika Formation Vikinghsgda Formation Vikinghragdformasjonen M-13 formal Sassendalen Group Vmhgen Member Veringleddet CP-80 formal Kapp Starostin Formation Vrakbukta Bed Vrakbuktlaget M-S2 formal Kongssya Formation Wibebreen member Wibebreleddet M-06 informal Vardebukta Formation Wilhelmarya Subgroup Wilhelmqmdergruppa M-38 formal Kapp Toscana Group Wimanfjellet Member Wimanfjelleddet (W.fjell-leddet) M-77 formal Ruriktjellet Formation Wordiekammen Formation Wordiekamformasjonen CP-47 formal Dickson Land Subgroup Zeipelodden member Zeipeloddleddet CP-62 informal Gipshuken Formation

Zillerbergleddet

6.2 Type sections and type localities

The table below contains all 234 stratigraphic units which form part of the Upper Palaeozoic, Mesozoic and Tertiary schemes, respectively, recommended herein. The names are listed in the order of their ID numbers used to identify the units in the lexicon text, stratigraphic type sections, maps and other tables. In the type sectionlarea column, type areas without a definite type section are written in italics. Type sections are indexed according to their nature as explained here:

Stratotype (S): The main type locality and section which presently defines the unit.

Hypostmtome (H): The second or third type locality of a unit that documents major regional variations.

Boundary stratotype (B): If a unit does not have a documented locality where both: its base and its main body are dicient ly represented, the type locality for the lower boundary is defined by the boundary stratotype.

Unit stmtotype (U): I f a unit does not have a documented locality where both its base and its main body are sufficiently represented, the type locality for the main body is defined by the unit stratotype.

UTM coordinates are given for all type sections with the accuracy of 100 m, using the ED50 system which is also used on Norsk Polarinstitutt's geological inaps. For small type areas, UTM coordinates are indicated for the approximate centre of the area. For larger type areas, no coordinates are provided.

References are given to the author(s) responsible for the presented stratigraphic log (if not available, for the presently valid description) of the respective type section. This is not necessarily the first stratigraphic log or description of the respective unit. See lexicon text in Chapters 2 ,3 and 4 for further references. For type sections with unpublished references, the present volume should be referred to as the first published source.

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UTM POSITION REFERENCES 1

- -- (composite) -- , , .* to 6263 82695

CP-20 Nordkapp Formation U ~ a n d n m d i n ~ s v i k a ~ 33X XC 6195 82587 Gjelberg 1981

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ID STRATIGRAPHfC UNlT TYPE SECTION /AREA UTM POSITION REE"]ERENCES I M-04 Shaken member S Iskletten 33X WH 4757 87107 Buchan et al. l965 M-05 Urnetoppen m&r S Urnetoppen SW 33X WF 5281 85524 Birkenrnajer 1977 M-06 Wibebreen member S Urnetoppen SW 33X WF 5281 85524 Birkenmajer 1977 M-07 Kistefjellet Member S Kistefjellet 33X WF 5452 85029 Mmk et al. l982 M-08 Brevassfjellet Bed S Kistefjellet 33X WF 5452 85029 Mmk et al. 1982 M-09 Tvillingodden Formation S Festningen l 33X VG 4741 86697 Mmk et al. 1982 M- 10 Iskletten Member S Metten 33X WH 4757 87107 Buchan et al. 1965 M-l l Kaosfjellet Member S Iskletten 33X 'WH 4757 87107 Buohan et al. 1965 M-12 Skilisen Bed

M- 14 Deltadalen Member S Deltailden 33X WG 5424 86891 Mmk et al. 1999 M-15 Lusitaniadalen Member S Deltailden-Vtkingbgda 33X WG 5424 86891 M k et al. 1999 I

33X WG 5421 86902 Mnrrk et al. 1999 l

M-1 7 Urd Formation M-I% Verdande Bed .M-19 Bravaisberget Fomati011 S Bravaisberget 2 " : 33X VG 4994 86165 Mmk et al. 1982 M-20 P Member S Treskelen - Y : : il -, 33X WF 5309 85485 Mark et al. 1982

N.-= S m h M * S Treskelen ~

M-24 Botneheia Formation S Sticky Keep 33X WG 5439 86890 Mark et al. 1982 M-25, Blanknuten Member S Blanknuten 35X LG 3662 86621 Mnrrk et al. 1982 U-26 Steinkobbe Formation S block/b.hde 7%$M-%03 3%: 3734 81357 Mgsk & Elvebakk 1"""

block/b.hole 7323/07-U44 block/b.hole 7323197-U41 blockhhole 7323/07-U-07

M-27 Ingarydjupet Subgroup , ,-" block 7120/12 Worsley et al. 1988 U-28 Havwt Formation S J V . S ^b2ocklb.hole 7120/12-2 MW 4930 78916 Womley et al. 1988

g : . l

1. _ ~ .,H block/b.hole 712019-2 34W 4894 79328 Worsley et al. 1988 ~ p p r n y w ~ o n a a ' ~ ^ l ":S blockm.hole 7120112-2 34W 4930 78916 ,Worsley et al. l988

.. : .C.. H block/b.hole 712019-2 34W 4894 79328 Worsl~y et al. 1988 1 M.30 KubbFormatim ~

"~ " ' 1 S b1ocWb.hole 7120112-2 34W 4930 78916 Worsley et al. 1988 1

M35 kfjorden Membe . , r

34W 4930 78916 Worsley et al. 1988

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6. TAP' "

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6. TABLES

ID STRATIGRAPHIC UNIT TYPE SECTION /AREA UTM POSITION REE'ERENCES I M-84 Knurr Formation S block/b.hole 7 1 19/12- 1 34W 4564 78894 Worsley et al. 1988

H block/b.hole 7 120112-1 34W 4912 78903 Worsley et al. 1988 M-85 Klippfisk Formation S block/b.hole 7430110-U-01 35X 5985 82387 Smelror et al. l998

H block/b.hole 723 1101-U-0 1 35X 6364 80779 Smelror et al. l998 M-86 Kutling Member S block/b.hole 743011 0-U41 35X 5985 82387 Smelror et al. l998

H, blockh.hole 7231101-U-01 35X 6364 80779 Smelror et al. l998 M-87 Tordenskjoldberget Member S Tordenskjoldberget 35X NH 5250 87540 Smith et al. 1976 M-88 Kolje Formation S blockfb.hole 71 19112-1 34W 4564 78894 Worsley et al. 1988

H block/b.hole 7 120112-1 34W 4912 78903 Worsley et al. l988 M-89 Helvetiafjellet Formation S HelvetiafjeUet 33X WG 5298 86852 Gjelberg & Steel l995 M-90 Festningen member S Festningen 3 33X VG 4758 86699 Steel et al, 1978 M-9 1 Hhrfagrehaugen Member B Hasfagrehaugen 4 35X NH 5254 87604 Collinson & Rad l984

(unpubl.1 U SjBgrenfjellet W 2 35X NH 5191 87535 Olaussenetal.,inprep. H Ktikenthalfjellet S 35X MH 4984 87327 Olaussen etal., in prep.

M-92 Kong Karls Itand Flows S Sjogrdellet S 35X NH 5217 87533 Collinson & b d 1984 (unpubl.)

M-93 Carolinetjellet Formation S Langstakken 33X WG 5513, 86565 Parker 1967 M-94 Dalkjegla Member S Langstakken 33X WG 5513 86565 Parker 1967 M-95 Innlcjegla Member S Langstakken 33X WG 5513 86565 Parker 1967 M-96 Langstaklcen Member S Langstakken 33X WG 5513 86565 Parker 1967 M-97 Zillerberget member S SchBnrockfjellet 2 33X WF 5148 85966 Nagy 1970

H Zillerberget 33X WF 5618 85893 Knarud & W in h u 9 1991

M-98 Schtinrockfjellet member S Sch6nroclUjelle.t l 33X WF 5618 85893 Nagy 1970 Y V ' b .:V) , H Schhmddjellet 2 33X WF 5618 85893 Knamd &MPrrkin

' I 8 . h I n # bus 1991

M-99 Kolrnule Formation S block/b.hole 71 191121 34W 5464 78894 Worsley et al. 1988 H Mock/b.hole 7120112-1 34W 4912 78903 Worsley et al. l988

M-100 Nygrunnen Group block 7119/12 Worsley et al. 1988 M- 10 1 Kveite Fonqatio blockhhole 71 19112- 1 34W 5464 78894 Worsley et al. 1988

M-102 Kviting Formation S block/b.hole 7120f 12-1 34W 4912 78903 Worsley et al. 1988 H block/b.hole 712115-1 34W 5 143 79444 Worsley et aL 1988

M- 103 Diabasodden Suite Diabasodden 33X WG 5255 86991

KalgrafF 1978 (unpubl.) w ' 3 3 ~ WC 5500 86497 Nemec in Steel et al. a4 .

l T-04 Gmnfjox&n Bed S Gronfjorden NW$?$t , 33X VG 4767 86691 Steel in Ohta et al. 1992 T-05 Kolthoffberget Membm 33X WG 5102 86132 Steel 1995 (unpubl.);

cvnd 5076 86776 (composite)

T-1 0 Marstranderbreen Member S Marstranderbreen . H LindstrBmfjeUet 33X WG 5016 86752 Nagy 1987 (unpubl.)

T-l l Gilsonryggen Member S Nordenskiiildfjellet 33X WG 5076 86776 Nagy 1987 (unpubl.) T-12 Bjnrmsonfjellet Member S Bjamonfjellet 33X VG 4984 86576 Steel in Ohta et al. 1992 T-13 Hollendardalen Formatioa S Marstranderbreen 33X V(? 4955 86497 Dalland (unpubl.)

H BBdalen 33X WG 5104 86692 D a h d (unpubl.) 4 Battfjellet Formation S Battfjellc 33X WG 5261 86629 Steel e ' 198'

- I- -

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LD STRATIGRAPHIC UNIT UTM POSITION REFERENCES

T-15 ABpe1intoppe.n Formation S Ikkhgqm 33X W 5281 86306 SBd et al. l981 T-16 Ny-hesund Subgroup N ~ ~ ~ I W T-17 Kongsfjorden Formation S bmhob 4-1928 + 5.1921 m F@ @dW9 Midbe 1985 (Impubl.);

(c-, . , ONin 1934 T-18 ~ 0 n M e m b e s r 5, tj~r&b S-I.%et Jsle QH 4348 87621 Midbe 1985 (unpubl.);

Orvia 1934

OMin 1934 h borehole 21-1976 33X VH 4323 87626 Midbe 1985 CmpubL); H ScheteligtjelIet . ,33X VH" 4288 87641,,, , , ,

T-20 Msrebekken Bed S borehole 38-1976 33X W 4317 87652 Wdbm 1985 (wpubl.) H Scheteligfjellet ~ , 33X 4288 87641 , , ,,, ~ , ,

T-21 Brmrggerbm Formation S boreholes 2 1-1 975;,24- me 2r22 and F23 Midbm 1985 Cunpubl.) 1976 + 38-1976 (compa.1

T-22 Leirhaugen Member S borehole 21-1976 33X W 4323 87626 Mldbere"l9$5)85,(pp&l.) T-23 Bayelva Membet B borehole 38-1976 33X VW 4317 87652 W e 3985 ~qxht . )

4-01 Bocldjorden Volcanic Complex Bocworden - 4-02 Sverrefjellet Volcano Svewe&ellet 33X VJ 4653 88188 ,

4-03 Halvdanpiggen Eruptive Centre Halvdanpiggen 33X VJ 4720 88238 4-04 Sigurdfjellet Eruptive Centre Sigurdfiellei - 33X ?'H 4705 87990

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7. BIBLIOGRAPHY

1 SVALBARD, REGIONAL STRATIGRAPEY 1.1 Svalbard, regional, entire succession 1.2 Svalbard, regional: Upper Palaeozoic successwn 1.3 Svalbard, regional: Mesozoic succession 1.4 Svalbard, regional: Mesozoic dolerites 1.5 Svslbard, regional: Tertiary succession 1.6 Correlation Svalbard - Barents Shelf (with emphasis

on Mesozoic succession)

2 BJORN~YA 2.1 Bjnrney~, entire succession 2.2 Bjerneya: Upper Palaeozoic succession 2.3 Bjmneya: Ih'assic succession

3 SOUTHERN SPITSBERGEN 3.1 Southern Spitsbergen, entire succession

(without Central Teriirny Basin) 3.2 Southern Spitsbergen: Upper Palaeozoic succession 3.3 Southern Spitsbergen: Mesozoic succession

4 CENTRAL AND WESTERN SPITSBERGEN (wITR ENTIRE CENTRAL

TERTIARY BASIN) 4.1 CenW and western Spitsbtrgen, entire succession

(with entire Central Terthy Basin) 4.2 Central and western Spitsbergen: Upper Palaeozoic

succession 4.3 Cenfral and western Spitsbergen: M~sozoic succession 4.4 Central and western Spitsbergen: Tertiary succession

of Central Tertiary Basin 4.5 Central and western Spitsbergen: Tertiary succession

of Renardodden

1 Svalbard, regional stratigraphy

1.1 Svalbard, regional, entire succession

Aga, 0.J.L Worsley, D. 1986: The geological history of Svalbard. Evo- lution of an Arctic archipelago. Den norske stats oljeselskap a.s, Stavanger, 121 pp.

Allan, D.A. 1942: The geology of Spitsbergen. Liverpool Geological Society, Proceedings 18 (2 and 3). 3748.

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Dallmann, W.K. & Mmk, A. (eds.) 1991: Stratigraphical dictionary of Svalbard. Translation from the Russian title: Stratigrafiteskij slovar' Spicbergena (Gramberg, I.S., Krasil'SEikov, AA.. & Semevskij, D.Y,

5 NORTEWESTERN SPITSBERGEN 5.1 Northwestern Spitsbergen, entire succession 5.2 Northwestern Spitsbergen: Upper Palaeozoic succession 5.3 Northwestern Spiisbergen: Tertiary succession of

Forlandsundet Graben 5.4 Northwestern Spitsbergen: Tertiary succession of

Kongsfioorden area 5.5 Northwestern Spitsberge: Tertiary lavas

6 EASTERN SPITSBERGEN AND EASTERN ISLANDS . 6.1 Eastern Spitsbergen and eastern islands, entire succession 6.2 Eastern Spiisbergen and eastern islands, Upper Palaeozoic

succession 6.3 Eastern Spitsbergen and eastern islands, Mesozoic

succession

8 MAPS (FIG. 7-01) 8. 1 NP 0vernMew map 1:l million 8.2 NP Re&ional maps 1:500,000 8.3 NP Dhiled maps I:lOO,OOO to 1:50,000 8.4 Mapspublislred by others than the Norwegian Polar Znslilute

eds., 1990). Norsk Polarinstitutt Rapportserie 74. 1-189. Dallmann, W.K., Ohta, Y. & Andresen, A. (eds.) 1988: Tertiary tecton-

ics of Svalbard. Extended abstracts from Symposium held in Oslo 26 and 27 April 1988. Norsk Pol~~mti tut t Rapportserie 46, 1-1 10.

Edwards, M.B. 1975: Preliminary report. Upper Paleozoic and Meso- zoic sandstones of Svalbard. A reconnaissance. Ni'7VF"U Publ. 87.

Eiken, 0. (d.) 1994: Seismic atlas of -tern Svalbard. Norsk Polar- institutt Meddelelser 130, 1-73, 13 planches.

Eiken, 0. 1985: Seismic mapping of the post-Caledonian strata in Svalbard. Polar Research 3,167-1 76.

Elverbi, A. & G d i e , G. 1981: Diagenetic and sedimentology explanation for high seismic velocity and low porosity in Mesozoic and Tertiary sediments, Svalbard region. American Association of Petroleum Geologists Bulletin 65, 145-153.

Evdokimova, N.K. 1984: VeEestvennyj sostav i kdestvo uglej ostrova Zapadnyj Spicbergen. (Composition and quality of coals of Spits- bergen.) Unpublished report, PG0 "Sevmorgeologija ", Leningrad. Project report, 1981-1984. 144 pp.

reb bold, H.-1930: Neuere ~orschun~en iiber die Geologie Wnlands, Suitzbemens und der Bh-Insel . Die Naturwissenschafien. 18. ~ l h r ~ . , 5. 576-585.

Frebold, H. 1932: Parallele Ziige im geologischen Bau Ostgronlands, Spitzbqens, der Bhnimel sowie Norwegens und ihre Bedeutung. Die Naturwissenschaften, 20. Jahrg., 44.799-806.

Gramberg, I.S., Krasil'SEikov, A.A. & Semevskij, D.X (eds.) 1990: Stratigmfiteskij sl0yar'~picbergena (Simtigmphical dictionary of Svalbard). Nedra, Leningrad. 1-203.

Gripp, K. 1927: Beitriige zur Geologie von Spitzbergen. Abhandlungen des Naturwi'ssenschaftlichen Vereins zu Hamburg 21, 1-38.

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1.2 Svalbard, regional: Upper Palaeozoic succession

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1.3 SvatBard, regional: Mimozoic succession

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, 1.4 Svalbard, regional: Mesozoic dolerites

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1.5 Svalbard, regional: Tertiary succession

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LivSic, Ju.Ja. 1992: Tectonic history of Tertiary sedimentation of Sval- bard. Discussion. In Dallmann, W.K., Andresen, A. & Krill, A. (d.): Post-Caledonian tectonic evolution of Svalbard. Norsk Geologisk Tidcrskrii 72/1.

Manurn, S.B. & Throndsen, T. 1986: Age of Tertiary formations on Spitsbergen. Polar Research 4, 103-131.

Manum, S.B. 1962: Studies in the Tertiary flora of Spitsbergen, with notes on Tertiary floras of Ellesmere Island, W a n d and Iceland. A palynological investigation. Norsk Polarinstitutt Skrijter 125, 1-127.

Manum, S.B., Bjterke, T., Throndsen, T. & Eien, M. 1977: Preservation and abundance of palynomorphs, and obsewations on thermal alter- ation in Svalbard. Norsk Polarinstitutt Arbok 1976, 121-130.

Nathorst, A.G. 1896: Marine Conchylien im Tertiar Spitzbergens und Ostgr6nlands. Zeitschni der Deuschen Geologischen Gesellschaft, Jahrg. 1896.983-986.

Nathorst, A.G. 1919: Ginkgo adiantoides (UNGER) HFER im Tertiir Spitzbergens nebst einer h e n fibenicht der iibrigen fossilen Ginkgophyten desselben Landes. Geologiska Fiireningens i Stock- holm Forhandlingac Mars 1919,233-248.

Nmedt , A., Berglund, L.T., Rasmussen, E. & Steel, R.J. 1988: Some aspects of Tertiary tectonics and sedimentation along the western Barents Shelf. Geological Society of America, Special Publication 39,421-425.

Schweitzer, H.J. 1980: Environment and climate in the Early Tertiary of Spitsbergen. Paleogeogmphy, Paleoclimatology, Paleoecology 30, 297-31 1.

Steel, R.J., Gjelberg, J., Helland-Hansen, W., Kleinspehn, K., Nmedt , A. & Rye Larsen, M. 1985: The Tertiary strike-slip basins and orogenic belt of Spitsbergen. Society of Economic Paleontologists and Minemlogists, Special Publication 37, 339-360.

Vakulenko, A.S. & LivSic, Ju.Ja. 1971: PalinologiEeskaja charakteris- tica paleogenaych otloZenij Spicbergena. (Palynological characteristics of Paleogene deposits of Spitsbergen). NZIGA UEenye zapiski. Paleontologija i Bioshatigmfija 31,39-50.

Wolfe, J.A. 1980: Tertiary climates and floristic relationships at high latitudes in the northern hemisphere. Palaeogeogmphy, Palaeoclima- tology, Palaeoecology 30,313-323.

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7. BIBLIOGRAPHY

1.6 Correlation SvaIbard - Barents Shelf (with emphasls on Mesozoic succession)

Antonsen, P., Elverhei, A., Dypvik, H. & Solheim, A. 1991: Shallow bedrock geology of the Olga Basin area, northwestern Barents Sea. American Association of Petroleum Geologists Bulletin 75, 1178- 1194.

Arhus, N. 1991: Dinoflagellate cyst stratigraphy of some Aptian and Albian sections from Northern Greenland, Southeast Spitsbergen and Barents Sea. Cretaceous Research 12,209-225.

khus, N., Kelly, S.R.A., Collins, J.S.H. & Sandy, M. R. 1990: Sys- tematic palaeontoloy and biostratigraphy of two Lower Cretaceous condensed sections from the Barents Sea. Polar Research 8 (2), 165- 194.

Berglund, L.T., Augustson, J., Faerseth, R.B., Gjelberg, J. & Rarnberg- Moe, H. 1986: The evolution of the Hammerfest Basin. In: Spencer, A.M. (ed.), Habitat of Hydrocarbons on the Norwegian Continental Shelj; Graham & Trotman Ltd., 319-338.

Bjazke, T. & Thusu, B. 1976: Cretaceous palynomorphs from Spits- bergenbanken, NW Barents Shelf. Norsk Polarinstitutt Arbok 1974. 258-260.

Bjrerke, T. 1979: Geology of the Barents Sea Shelf: Evidence from palynological studies of drift material. Norwegian Sea Symposium, Norsk Petroleumsforening 17, 1-15.

Bjmlykke, K., Bue, B. & Elverhei, A. 1978: Quaternary sediments in the northwestern part of the Barents Sea and their relation to the underlying Mesozoic bedrock. Sedimentology 25,227-246.

Bjorw, M., Bue, B. & Elvsborg, A. 1983: Organic geochemical analysis of the first two wells in the Troms 1 area (Barents Sea). In: Bjomy, M. et al. (eds.), Advances in Organic Geochemistry 1981, Pergamon Press, 16-27.

Bro, Y.G., Pchelina, T.M., Preobrazhenskaya, E.N., Ronkina, Z.Z., Voytsekhovskaya, A.G., Krasnwa, V.L. & Mozhayeva, 0.V 1991: Sedimentary cover of the Barents Sea shelf from drilling data on islands. Petroleum Geology 25, 7/8,239-243.

Bugge, T. & Fanavoll, S. 1995: The Svalis Dome, Barents Sea - a geological playground for shallow stratigraphic drilling. FTrst Break 13 (6), 237-251.

Edwards, M.B. 1975: Gravel fraction on the Spitsbergen Bank, NW Barents Shelf. Noees geologiiske undem~kelse Bulletin 316, 205- 217.

Eiken, 0. & Austegard, A. 1987: The Tertiary orogenic belt of West Spitsbergen: Seismic expressions of the offshore sedimentary basins. Nomk Geologisk Tidsskri$67,383-394.

Elverhei, A. & Lauritzen, 0. 1984: Bedrock geology of the northern Barents Sea (west of 35" E) as inferred from the overlying Quater- nary deposits. NorskPolarinstitutt Skn$er 180, 5-16.

Embry, A.F. 1989: Correlation of Upper Palaeozoic and Mesozoic sequences between Svalbard, Canadian Arctic Archipelago, and northem Alaska. In: Collinson, J.D. (ed.), Correlation in Hydrocarbon Exploration, Norwegian Petroleum Society, Graham & Trotman, 89- 98.

Harland, W.B. & Dowdeswell, E.K. (eds.) 1988: Geological evolution of the Barents ShelfRegion. Graham & Trotman, London.

Heafford, A.P. 1984: The Carboniferous to Triassic evolution of the Barents Sea region. CASP Report 346. Regional Tectonic Series, Barents ShelfSubseries. 1-36.

Heafford, A.P. 1988: Carboniferous through Triassic stratigraphy of the Barents Shelf. 4. 19-32 in W.B. Harland & E.K. Dowdeswell (eds.): Geological evolution of the Barents Shelf region. Graham & Trot- man, London.

Jacobsen, VW. & Veen, F! van 1984: The Triassic offihore Norway north of 62" N. In: Spencer, A.M. et al.( eds.), Petroleum Geology of the North European Margin. Norwegian Petroleum Society, Graham & Trotman Ltd., 317-328.

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Kelly, S.R. A. 1988: Jurassic through Cretaceous stratigraphy of the Barents Shelf. In: W.B. Harland & E.K. Dowdeswell (eds.), Geolog- ical evolution of the Barents SherfRegion, Graham & Trotman Ltd., London, 109-130.

Kristoffersen, Y., Milliman, J.D. & Ellis, J.P. 1984: Unconsolidated sed-

iments and shallow structure of the northern Barents Sea. Norsk Polarinstitutt Skrifter 180,2539.

Lundstr~m, R. 1987: A compamtive sedimentological study of two coal-bearing deltaic successions: The Nordmela Fm. (early Jumssic) of Hammerfart Basin and the Todalen h4b. (early Paleocene) of Cen- tral Spitsbergen Basin. Unpublished cand. scient, thesis, University of Bergen, Volume 1 (text) 149 pp. and volume 2 (illustrations) 124pp.

Mangemd, G. 1994: Palynostmtigmphy of thepennian - lowermost Tri- assic succession, Barents Sea area. Unpublished Dr. scient. thesis, University of Bergen.

Msrk, A. & Elvebakk, G. 1999: Lithological description of subcrop- ping Lower and Middle Triassic rocks from the Svalis Dome, Bar& Sea. Polar Research 18 (I), 83-104.

Msrk,A., Vigran, J.O., KolEinskaja, M.V, Relina, T.M., Fefilwa, L.A., Vavilov, M.N. & Weitschat, W. 1993 (reprints dated 1992): Triassic rocks in Svalbard, the Arctic Soviet Islands and the Barents Shelf: bearing on their correlations. Pp. 455477 in: Vorren, T.O. et al.: Arc- tic Geology and Petroleum Potential. Norwegian Petroleum Socieiy Special Publication 2, Elsevier, Amstersdam.

Nagy, J. 1973: Fossilfmende blokker av Mesozoisk alder fra Svalbard- banken. IKUPublication 42,26 pp.

Nmedt , A., Cecchi, M., Gjelberg, J.G., Kristensen, S.E., Lsnsy, A., Rasmussen, A., Rasmussen, E., Skott, P.H. & Veen, P.M. van 1992: Svalbard-Barents Sea correlation: a short review. Pp. 363-375 in Vorren, T.O. et al. (eds.) Arctic Geology and Petroleum Potential, Norwegian Petroleum Society Special Publication No. 2, Elsevier Sci.Publ.

Nmedt , A., Livbjerg, F., Midbe, P.S. & Rasmussen, E. 1992: Hydro- carbon potential of the Central Spitsbergen Basin. 4. 333-361 in Vorren, T.O. et al. (eds.) Arctic Geology and Petroleum Potential, Norwegian Petroleum Society Special Publication No. 2.

Olaussen, S., Dalland, A, Gloppen; T.G. and Johannessen, E. 1984. De- positional environment and diagenesis of Jurassic reservoir sandstones in the eastern part of the Troms I area. In Spencer, A.M. et al (eds.): Petroleum Geology of the North European Margin, Norwe- gian Petroleum Society, Graham L Trotman, London. 61-79.

Pavlenkin, A.P, L i i c , Ju.Ja., Matveev, J.I. & Toporskaja, L.P. 1977: StratigrafiCeskaya priuroEemost' opornych seismiEeskich gorisontov na akvatorii Barentseva i PeEorskogo rnorej. (Stratigraphic confine- ment of seismic key horizons of the aquatory of the Barents and Pe- chora seas). In: Problems ofgeophysical investigations ofpolar areas of the earth. Sbornik naufnych trudov (Collecfion of Scienttpc Papers), NUGA, Leningrad.

Pavlov, VV, Fefilova, L.A., Lodkina, L.B. 1985: PalinologiEeskaja charakteristika mezozojskich otloZeny joZnoj Easti Belfa Barentseva moja (Palyn010gical characterization of the Mesozoic deposits of the southern Barents Sea Shelfl. In: Vasilevskaia. N.D. (ed.). Stmti- . , . ,, gmjija i paleontologiia Mezozojskich osaddnych bass@nov sevem SSSR, 88-103. PGO"Sevmorgeologija", Leningrad.

Prestholm, E. 1985: Barentshavets-krittassbke Sedimentasjonsbas- seng. Et studie av geologiske data fm k m s - l blokken (Barents- havet) samt en sammenligning med kqgmkkene fm andre Artiske sed- imentasjonsbasseng basert prf littemturstudieer og feltarbeid. Unpublished cand. real. thesis, University of Bergen, 241pp.

Riis, F., Vollset, J. & Sand, M. 1986: Tectonic development of the western part of the Barents Sea and adjacent areas. American Association of Petroleum Geologists Memoir 40,661-675.

RPInnevik, H.C. 1981: Geology of the Barents Sea. In: Illing, L.\! & Hobson, G.D. (eds.), Petroleum geology of the continental shelf of northwest Europe. Heyden & Son Ltd., 395406.

Roufosse, M.C. 1987: The formation and evolution of sedimentary basins in the Western Barents Sea. In: Petroleum Geology of North West Europe. Brooks, J. & Glennie, K. (eds.), Graham & Trotman, 1149-1161.

Smelror, M. 1994: Jurassic stratigraphy of the Western Barents Sea region: a review. Geobios 17,441 4 5 1.

Smelror, M., -&,A., Monteil, E., Rutledge, D. & leereveld, H. 1998: The Klippfisk Formation - a new lithostratigraphic unit of Lower Cretaceous platform carbonates on the Western Barents Shelf. Polar Research 17 (2), 1 8 1-202.

Steel, RJ., Felt, V.L., Johannessen, E.P. & Mathieu, C. (eds.) 1995: Se- quence stratigraphy on the northwest European Margin. NPF Special Publication No. 5, Elsevier. 608 pp.

Throndsen, T. & Bjrerke, T. 1983: Palynodebris analysis of a shallow core from the Barents Sea. Polar Research 1,43-47.

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Vorren, T.O., Bergsager, E., Dahl-Stamnes, @.A., Holter, E., Johansen, B., Lie, E. & Lund, T.B. 1993: Arctic Geology and Petroleum Poten- tial. NPF Special Publication No. 2, Elsevier. 75 1 pp.

Wiembowski, A & Smelror, M., 1993: Ammonite succession in the Kimmeridgian of southwestern Barents Sea, and the Amoebocems zonation of the Boreal Kimmeridgian. Acta Geologica Polonica 43, 229-249.

Wierzbowski, A. & khus, N. 1990: Ammonite and dinoflagellate cyst succession of an Upper Oxfordian - Kimmeridgian black shale core from the Nordkapp Basin, southern Barents Sea. Newsletters on Stmtigmphy 22 (I), 7-19.

Worsley, D., Johansen, R. & Kristensen, S.E. 1988: The Mesozoic and Cenozoic succession of Tromseflaket. NPD Bulletin 4,42-65.

2 Bjerneya

2.1 Bjerneya, entire successwn '

Andersson, J.G. 1900: iiber die Stratigraphie und Tektonik der Bkeninsel. Bull. Geol. Inst. University of Uppsala 4,243-280.

Bjonay, M., MBrk, A. & Vigran, J.O. 1983: Organic geochemical studies of the Devonian to Triassic succession on Bjemeya and the implications for the Barents Shelf. 4.49-59 in M. Bjorq et al. (eds.) 1983, Advances in organic geochemistry, John Wiey & Sons Ltd., London.

Buch, L.v. 1849: Die Baereninsel nach B.M. Keilhau: geognostisch beschrieben; iiber Cemtiten. G. Reimer, Berlin. 49 pp.

Craig, L.E. 1984: The geology of Bjmmya. Parts 1 and 2. CASP Report 325/326. Area1 Series, Svalbard Subseries. 1-120.

Frebold, H. 1935: Geologie von Spitzbergen, der Biireninsel, des Konig Karl- und Fmnz-Joseph-Landes. Verlag von Geb~der Borntriiger, Berlin. 1-195.

Heer, 0. 187 1: Fossile Flora der Bhninsel. Kungl. Svenska Vet.-Akad. Handlingar 9 (5). 5 1 pp.

Holtedahl, 0. 1920: Spitsbergens og Bjrmomrens geologi Naturen 44 (9- 10). 288-307.

Holtedahl, 0. 1929: Die geologischen Verhiiltnisse der Bieninsel. Petermanns Geographische Mitteilungen 3/4, 1929. 1 p.

Horn, G. & Orvin, A.K. 1928: Geology of Bear Island. S h i e r om Svalbard og Ishavet 15, 1-152.

Krasil'SEikov, A.A. & LivSic, Ju.Ja. 1974: Tektonika ostrova Medvdij. (Tectonics of Bjsmraya.) Geotektonika, 4,39-5 1.

Krasil'SEikw. A.A.. LivSic. Ju.Ja.. Mokin. Ju.1.. & Peelina T.M. 1971 : ~ e o l o ~ i ~ e ~ k o e sioenie ostrova'~edv&j. (Outline of th;: geology of Bjsmraya.) Unpublished report, PW"Sevmorgeologija", Lenin- - - grad. Report on fieldwork in 1969-1970. 192 pp.

Malecki, J. 1977: Permian bryozoans from Southern Spitsbergen and Bjsmraya (Svalbard). Sfudia Geologica Polonica 51, 75-88.

Ritter, U., Duddy, I., Mnrrk,A., Johamen, H. & Arne, D. 1996: Temper- ature and uplift history of Bjernqa (Bear Island), Barents Sea. Petroleum Geoscience 2, 133-1 44.

Worsley, D. & Gjelberg, J. 1980: Excursion Guide to Bjsmeya, Sval- bard. Contributions h r n the Paleontological Museum, Oslo, Nor- way, No. 258, 1-33.

2.2 Bjerneya: Upper Palaeozoic succession

Agdestein, T. 1980: En stmtigmf~k,sedimentologisk og diagenetisk undersnkelse av karbon-penn sedimenter (Kapp Hanna og Kapp Dun& fonnasjonene) pd Bjamaya, Svalbard. Unpublished cand. real. thesis, University of Oslo, 1-144.

Andrews-Speed, C.P. 1980: The Carboniferous and Permian geology of the Barents Shelf. CASP Report 204, Barents Shelf Stmtigmphic Series. 1-50.

Folk, RL. & Siedlecka, A. 1974: The "schizohaline" environment: its sedimentary and diagenetic fabrics as examplified by Late Paleozoic rocks of Bear Island, Svalbard. Sedimentary Geology I I, 1-15.

Gjelberg, J. & Steel, R.J. 1983: Middle Carboniferous marine transgression, Bjsmsya, Svalbard: facies sequence from an interplay of sea. level changes and tectonics. Geological Journal 18, 1-19.

Gjelberg, J. 1978: Facia analysis of the coal-bearing Vesalstranda Member (upper Devonian) of Bjarmeya. Norsk Polarinstitutt ldrbok 1977,71-100.

7. BIBLIOGRAPHY

Gjelberg, J.G. 1978: The Upper Devonian (Famennian) to Middle Car- boniferous (?Moscovian) strata on Bjarneya (Svalbard) - A study in alluvial and coastal marine sedimentation. Unpublished cand. real. thesis, University of Bergen, 1-265.

Gjelberg, J.G. 1981: Upper Devonian (Famennian) - Middle Carbonif- erous succession of B j m q a . A study of ancient alluvial and coastal marine sedimentation. Norsk Polarinstitutt Skrifter 174, 1-67.

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Holtedahl, 0. 1925: A 'pipe-rock' in the Upper Carboniferous of Bear Island. Norsk Geologisk lFdssknfl 8 (4), 270-280.

Kaiser, H. 1970: Die Oberdevon-Flora der Btireninsel3. Mikoflora des hoheren Oberdevons und des Unterkarbons. Palaeontogmphica Abt. B 129, 71-124.

Kaiser, H. 1971 : Die Oberdevon-Flora der Btireninsel4. Mikroflora der Misery-Serie und der flozleeren Sandstein-Serie. Palaeontogmphica Abt. B 135, 127-164.

Kirkerno, K. 1979: En sedimentologisk undersakelse i Kapp Kdre formasjonen (Moscov), Bjernaya. Unpublished cand. real. thesis, Uni- versity of Oslo.

Lsnray, A. 1988: Environmental setting and diagenesis of Lower Per- mian palaeoaplysinic build-ups and associated sediments from Bjsmsya: Implications for the exploration of the Barents Sea. Jour- nalofPetroleum Geology 11, 141-156.

Malecki, J. 1968: Permian bryozoans from Tokrossraya beds, Smkapp Land, Vestspitsbergen. Studia Geolonica Polonica 21,7-29.

Nakrem, H.A. 1988: Permian bryozoans from southern Spitsbergen and Bjemeya. A review of bryozoans described by J. Malecki (1968, 1977). Polar Research 6, 113-121.

Nakrem, H.A. 1991: Conodonts from the Pennian succession of Bjmnraya (Svalbard). Norsk geologisk lFclsskrij7 71 (4). 235-248.

Nowii~ski, A. 1982: Some new species of Tabulata from the Lower Per- mian of Hornsund, Spitsbergen. Palaeontologia Polonica 43,83-96.

Pavla: A.V, Evdokimaa, N.K. & Witina, N.V 1983: Uglenosnost' i kaCestvo uglej o. Medvhj. (Coal potential and quality on Bjsmsya) Pp. 102-109 in A.A. Krasil'SEikov & VA. Basov (eds.): Geolo- g~a$picbergma. PG0 "Sevmorgeologija" 1983, Leningrad.

Schweitzer, H.J. 1967: Die Oberdevon-Flora der Biireninsel. 1. Pseudobornia ursha Nathorst. Palaeontogmphica Abt. B 120, 116- 137.

Schweitzer, H.J. 1969: Die Oberdevon-Flora der B-el. 2. Ly- copodinae. PalaeontograpMca Abt. B 126, 10 1-137.

Siedlecka, A. 1972: Length-slow chalcedony and relicts of sulphates - evidences of evaporitic environments in the Upper Carboniferous and Permian beds of Bear Island, Svalbard. Journal of Sedimentary Peirolog~ 42 (4), 812-816.

Siedlecka, A. 1975: The petrology of some Carboniferous and Permian rocks from Bjsmraya Norsk Polarinstitutt ldrbok I973,53-72.

Simonsen, B.T. 1988: Upper Palaeozoic fusulinids of Bjsmraya. IKU Report 23.1252.06/02/88. 1-90.

Stemmenk, L. & Larssen, G.B. 1994: Diagenesis and porosity evolution of Lower Permian Palaeoaplysina buildups, Bjemeya, Barents Sea: An example of diagenetic response to high-frequency sea level fluctuations in an arid climate. In Horbury, A.D. & Robinson, A.G. (eds.): Diagenesis and basin development. American Association of Petroleum Geologists, Studies in Geology 36, 199-21 1.

Stemmerik, L., Larson, P.A., Larssen, G.B., Merk, A. & Simonson, B.T. 1994: Depositional evolution of Lower Permian Palaeoaplysina build-ups, Kapp Dunk Formation, Bjeuruaya, Arctic Norway. Sedi- mentary Geology 92, 161-174.

Stepanov, D.L. 1924: Short article on the bryozoan fauna of Bear Island. ZZK Geol. Kom. (Bull. Com. Geol.). 40,2-6.

Vigran, J.O. 199 1 : Palynologiske dateringer av Bjemeyas paleo- zoikum, Palyno nytt 16, (abstr.), Nordiske Palynologiske mate, Roskilde, p. 191.

W i a n , C. 1914: &er die Karbonbrachiopoden Spitzbergens und Beeren Eilands. Nova Acta Soc.Sci. Uppsala ser. 4, 3 (8).

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Wright, N.J.R 1975: The Billefjorden Group of Bjmmya. CASP Re- port 10, Svalbard Stratigraphic Series, Carboniferous and Permian Subseries. 1-5 1.

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7. BIBLIOGRAPHY

2.3 Bjerneya: Triassic succession

Bohm, J. 1899: &r Tnasfossilien von der Blireninsel. Zeitschrift der Deutschen Geologischen Gesellschaft 51,325-326.

Bohm, J. 1903: &r die obertriadische Fauna der Bhninsel. Konge- liga Svenska Vetenshps Akademiens Handlingar 37 (3).

Msrk, A. (ed.) 1987: Geological Excursion Guide to B j n n ~ a . Un- published IKUISintef Report, Tmndheim.

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PEelina, T.M. 1972: Triassovye otlo2enija ostrova MedveZij. (Triassic deposits of Bjmmya). In. Mezozoiskie otlotenija Sval'barda. NIIGA, Leningrad. 5-20.

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3 Southern Spitsbergen

3.1 Southern Spitsbergen, entire succession (without Central Tertiary Basin)

Birkenmajer, K. 1959: Report on the geological investigations of the Homsund area, Vestspitsbergen, in 1958. Pt. 1. Hecla Hoek Forma- tion. Bulletin of the Polish Academy of Sciences, Earth Sciences VII (2), 129-136.

Birkenmajer, K. 1959: Report on the geological investigations of the Hornsund area, Vestspitsbergen, in 1958. Pt. 2: Post-Caledonian succession. Bulletin of the Polish Academy of Sciences, Earth Sciences VII Q), 191-196.

Birkenmajer, K. 1960: Course of the geological investigations of the Hornsund area, Vestspitsbergen, in 1957-1958. Stadia Geologica Polonica 4,7-36.

Birkenmajer, K. 1960: Geological sketch of the Horsund area. Int. Geol. Congx, Rep. 2lst Ses. Supplement to Guide for Excursion A.16, Krmbenhavn. 1-12.

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Kellogg, H.E. 1978: The geology of Southern Spitsbergen and thepe- troleum potential of the GrimJellet claims block. Report to Den Norske Stats Oljeselskap (Statoil), unpublished.

Malecki, J. 1977: Permian bryozoans from Southern Spitsbergen and Bjerruaya (Svalbard). Studia Geologica Polonica 51,75-88.

Nagy, J. 1966: Preliminary report on the geology of eastern Torell Land, Vestspitsbergen. Norsk Polarinstitutt h b o k 1964, 69-72.

Osm6lska, H. 1968: Two new trilobites fkom the Treskelodden Beds of Hornsund. Acta Palaeontologica Polonica 13,605-613.

R e c k i , S.Z. 1959: Geology of the northwest part of Torell Land, Vest- spitsbergen. Studia Geologica Polonica 2, 1-98.

3.2 Southern Spitsbergen: Upper Palaeozoic succession

Biernat, G. & Birkenmajer, K. 1981: Permian brachiopods from the base of the Kapp Starostin Formation at Polakkfjellet, Spitsbergen. Studia Geologica Polonica 73,7-24.

Birkenmajer, K. & Czamiecki, S. 1960: Stratigraphy of marine Car- boniferous and Permian deposits in Honwnd (Vestspitsbergen), based on brachiopods. Bulletin of the Polish Academy of Sciences, Earth Sciences 8 (3), 203-209.

Birkenmajer, K. & Logan, A. 1969: On the fauna and age of the Can- crinella Limestone (Permian) at Kopernikusfjellet, Vestspitsbergen. Norsk Polarinstitutt Arbok 1967,2845.

Birkenmajer, K. 1964: Devonian, Carboniferous and Permian formations of Hornsund, Vestspitsbergen. Studia Geologica Polonica 11, 47-123.

Birkenmajer, K. 1979: Channelling and orientation of Rugose corals in shallow-marine Lower Permian of south Spitsbergen. Studia Geolog- ica Polonica 60,45-56.

Birkenmajer, K 1979: Paleotransport and source of Early Carbonifer- ous hsh-water clastics of south Spitsbergen. Studia Geologica Polonica 60, 3943.

Birkenmajer, K 1984: Cyclic sedimentation in mixed alluvial to marginal-marine conditions: The Treskelodden Formation (?Upper Car- boniferous and Lower Permian) at Hornsund, south Spitsbergen. Stu- dia Geologica Polonica 80,2546,

Birkenmajer, K. 1984: Mid-Carboniferous red beds at Homund, south Spitsbergen: Their sedimentary environment and source area. Studia Geologica Polonica 80,7-23.

Birkenmajer, K. 1994: Proterozoic and Palaeozoic formations in Cen- tral Ssrkapp Land, South Spitsbergen. Bulletin of the PolishAcademy of Sciences, Earth Sciences 42 (4), 265-283.

Birkenmajer, K. and Fedorowski, J. 1980: Corals of the Treskelodden Formation (Lower Permian) at Triasnuten, Hornsund, South Spits- bergen. Studia Geologica Polonica 66,7-34.

Bjmerud, M. 1992: Evidence for extensive post-Caledonian karst development in southwestern Spitsbergen. Geological ,Magazine 129, 465469.

Czamiecki, S. 1964. Occurrence of genus Archimedes (Hall) in Horn- sund, Vestspitsbergen. Studia Geologica Polonica 11, 147-153.

Czarniecki, S. 1966: Upper Paleozoic deposits of the north-eastern coast of Hornsund (Vestspitsbergen). Bulletin Polish Academy of Sciences, Series Geological and Geographical Sciences 14, 1.

Czarniecki, S. 1969: Sedimentary environment and stratigraphical position of the Treskelodden beds (west Spitsbergen). Pmce Muz. Ziemi 16,201-236.

Fedorowski, J. 1964: On late Paleozoic rugosa from Hornsund, Vest- spitsbergen (preliminary communication). Studia Geologica Polo- nica 11, 139-146.

Fedorowski, J. 1965: Lower Permian Tetracoralla of Honwnd, Vest- spitsbergen. Studia Geologica Poionica 17, 1-173.

Fedorowski, J. 1967: The Lower Permian Tetracoralla and Tabulata from Treskelodden, Vestspitsbergen. Norsk Polarinstitun Skriper 142, 1-61.

Fedorowski, J. 1982: Coral thanatocoenoses and depositional environment in the upper Treskelodden beds of the Hornsund area, Spits- bergen. Palaeontologica Polonica 43, 17-68.

Gavrilw, B.P. 1965: Sredne- i verchnepaleozojskie otlozenija zapadnogo pobereZtja ostrova Zapadnyj Spicbergen (poluostrov B*gger, Sent-DZons-fiord, Chomsunn). (Middle and Upper Paleozoic deposits of the west coast of Spitsbergen preggerhalvoya, St.Jons- fjorden, Hornsund].) Unpublished report, PG0 "Sevmorgeologija ", Leningrad. Report on fieldwork in 1964. 148 pp.

Gavrilov, B.P., Pavlov, A.\! & Fedina, LP. 1964: GeologiEeskie issledovanija v rajonach Bille-fiorda i Chornsunna, Zapadnyj Spicbergen. (Geological studies in the Billefjorden and Hornsund areas.) Unpub- lished report, PG0"Sevmorgeologija ", Leningrad. Report on field- workin 1963. 196 pp.

Haczewski, G. 1984: Lower Carboniferous alluvial sandy deposits (Homsundneset Formation) of South Spitsbergen. Studia Gwlogica Polonica 80,91-98.

Hellem, T. &. Worsley, D. 1978: An outcrop of the Kapp Starostin For- mation at Austjekultinden, Smkapplandet. Norsk Polarinstitutt ldrbok 1977,340-342.

Karczewski, L. 1982: Some gastropods and bivalves from the Treske- lodden and Kapp Starostin formations, Hornsund region, Spits- bergen. Pal~eontoiogica Polonica 43,83-96.

Liparski, L & Crniel, S. 1984: The geological conditions of the occurrence of Carboniferous coal in the northwestern part of Smkapp Land in West Spitsbergen. Polish Polar Research 5,255-266.

Liszka, S. 1964: Occurrence of Lower Permian foraminifers in the Treskelodden beds of Honwnd, Vestspitsbergen. Studia Geologica ' Polonica 11, 169-172.

Nakrem, H.A. 1988: Permian bryozoans from southern Spitsbergen and Bjerneya. A review of bryozoans described by J. Malecki (1968, 1977). Polar Research 6, 113-121.

Nysiether, E. 1977: Investigations in the Carboniferous and Permian stratigraphy of the Torell Land area, Spitsbergen. NorskPolarinstitutt ldrbok 1976,2141.

Siedlecka, A. 1968: Lithology and sedimentary environment of the Hymefjellet Beds and the Treskelodden Beds (Late Paleozoic) at ~ieskelen, pomsund, Vestspitsbergen. Studia ~ e o l o ~ i c a ~olohica 21, 53-96. C

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Siedlecka, A. 1970: Investigations of Permian cherts and associated rocks in southern Spitsbergen. Norsk Polarinstitutt ShFer 147, 1- 70.

Siedlecki, S. & 'hnau, E. 1964: Palynological investigations of the Culm in the area southwest of Homsund, Vestpitsbergen. Studia Geologica Polonica 11, 125-138.

Siedlecki, S. 1960: Culm Beds of the SW coast of Hornsund, Vest- spitsbergen. (Preliminary communication). Studia Geologica Polonica 4,93-102.

Siedlecki, S. 1964: Permian succession on Tokrossleya, S~rkapplandet, Vestspitsbergen. Studia Geologica Polonica 11, 155-168.

Wendorff, M. 1985: Geology of the Palffyodden area (NW Smkapp Land, Spitsbergen): Course and some results of investigations. Zeszyty Naukaoe Uniwersytetu Jagiellonskiego Pmce Geogmficzne Z. 63,33-55.

Wright, N.J.R. 1975: The Billefjorden Group, Southern Spitsbergen. CASP Report 7, Svalbani Stmtigraphic Series, Carboniferous and Permian Subseries. 1-46.

3.3 Southern Spitsbergen: Mesozoic succession

Birkenmajer, K. & Jerzmanska, A. 1979: Lower Triassic shark and other fish teeth from Hornsund, South Spitsbergen. Studia Geologica Polonica 60,7-38.

Birkenmajer, K. & Pugaczewska, H. 1975: Jurassic and Lower Creta- ceous marine fauna of SW Torell Land, West Spitsbergen. Studia Geolagica Polonica 44,45-92.

Birkenmajer, K. & Trammer, J. 1975: Lower Triassic conodonts from Hornsund, south Spitsbergen. Acta Geologica Polonica 25,299-308.

Birkenmajer, K. & Turnau, E. 1962: Lower Carboniferous age of the so-called Wijde Bay Series in Hornsund, Vestspitsbergen. Norsk Polarinstitutf h b o k 1961,4 1-61.

Birk-jer, K 1975: Jurassic and Lower Cretaceous sedimentary formations of SW Torell Land, Spitsbergen. Studia Geologku Polonica 44,7-43.

Birkenmajer, K. 1977: Triassic sedimentary formations of the Horn- sund area, Spitsbergen. Studia Geologica Polonica 51, 1-74.

Birkenmajer, K. 1984: Facies variation in the Helvetiafjellet Formation (Barremian) of Torell Land, Spitsbergen. Studia Geologica Polonica 80,7 1-90.

Bohm, J. 1913-1914: %er Triasversteinerungen vom Bellsunde auf Spitzbergen. Archivfir Zoologi. 8 (2), 1-15.

Edwards, M.B. 1976: Depositional environments in Lower Cretaceous regressive sediments, Kikutodden, Smkapp Land, Svalbard. Norsk Polarinstitutt ldrbok 1974,35-50.

Elverhai, A. & Bjmlykke, K. 1978: Sandstone diagenesis of Mesozoic rocks from southern Spitsbergen. Norsk Polarinstitutt Arbok 1977, 145-157.

Frebold, H. 1929: Die Schichtfolge des Jura und der Unterkreide an der Kiiste Siidwest-Spitzbergens. Abhandlungen des Naturwissenxhaft- lichen Yereins zu Hamburg 22,250-292.

Krajewski, K. 1992: Phosphorite-bearing succession of the Wilhelm- 8ya Formation at Hornsund and along the western coast of Sarkapp Land, Spitsbergen. 98,201-233.

Mmk, A. 1978:. Observations on the stratigraphy and structure of the inner Hornsund area. Norsk Polarinstihtt ldrbok 1977,61-70.

Sokolav, XN. & PEelina, T.M. 1967: On the lower and middle Triassic of Smkappland, Vestspitsbergen. Akad. Nauk SSSR Dokl. 176 (6), 1374-1377.

Worsley, D. & Mark, A. 1978: The Triassic stratigraphy of southern Spitsbergen. Norsk Polarinstitutt ldrbok 1977,43-60.

4 Central and western Spitsbergen (with entire Central Tertiary Basin)

4.1 Central and western Spitsbergen, entire succession (with entire Central Tertiary Barin)

Bergvik, A. 1990: StruRhrrgeologiske og stmtigrafiske undersflkelser i mesozoiske og tertkre bergarter pd EnimannJlya, vest Spitsbergen. Unpublished cand. scient. thesis, University of Tromsa.

Bro, E.G., PEelina, T.M., PreobraZenskaja, E.M. & Desjatkov, XM. 1993: Parametric drilling wells in the kssdalen area of Spitsbergen. Unpublished report, VNIIOkeangeologija, St. Peterburg (in Russian).

De Geer, G. 1910: A geological excursion to central Spitzbergen. Guide de 1'Excursion au Spizberg. Congris Gkologique International, Stockholm 1910.23 pp.

Gee, E.R, Harland, W.B. & McWhae, J.RH. 1952: Geology of central Vestspitsbergen. Part I: Review of the geology of Spitsbergen with special reference to central Vestspitsbergen. Transactions Royal Society ofEdinburgh 52 (g), 299-356.

Gregory, J.W. 1921: Note on the sequence across central Spitsbergen from Advent Bay to Agardhs Bay. Geological Magazine 58,295-296.

Haremo, I?, Andresen, A., Dypvik, H, Nagy, J., Elverhei, A., Eikeland, T.A. & Johansen, H. 1990: Structural development along the Bille- fjorden Fault Zone in the area between Kjellstr~mdalen and Advent- dalenfSassendalen, central Spitsbergen. Polar Research 8, 195-2 16.

Harland, W.B., Cutbill, J,L., Friend, RF., Gobbett, D.J., Holliday, D.W., Maton, PI., Parker, J.R. & Wallis, R.H. 1974: The Billefjorden Fault Zone, Spitsbergen - the long history of a major tectonic lineament. Norsk Polarinstitutt S h y e r 161, 1-72.

Major, H. &. Nagy, J. 1972: Geology of the Adventdalen map area. NorskPolarinstitutt Sk@er 138,l-58. (with map, published in 1964)

Nordenskiold, A.E. 1875: Utkast till Isfjordens och Belsounds geologi. Geologiska Fiireningens i Stockholm Forhandlingar Bd. 2 (8), 243- 260,301-322,356-373.

Nordenskiold, A.E. 1876: Sketch of the geology of Ice Sound and Bell Sound. Geological Magazine, dec. 5, 10,393-401.

Panov A.I. & Nepomiluev, V.F. 1967: OtEet o &rutno-poiskovych i struktumych issledovaniyach, provedennych otrjadom No. 1 Spic- bergenskoj ekspedicii letom 1966 g. na 0. Zap. Spicbergen: "Ge- ologieeskoe stroenie uEastka Agard-buchta - Sassendalen". (Report on map drafting, prospecting and structural studies, carried out by Party no. 1 of the Spitsbergen Expedition, summer 1966, on Spits- bergen: "Geological structure of the Agardhbukta - Sassendalen area"). Unpublished report, PG0 "Sevmorgeologija '*, Leningmd.

Panov, A.I. & Nepomiluev, XF. 1969: GeologiEeskie issledovanija v vostoEnoj Easti Zemli Nordensel'da i zapadnoj Easti Zemli Cheera (verchav'ja Adventdalen - Rinders-buchta). (Geological study in eastern Nordenskiold Land and western Heer Land [upper reaches of Adventdalen-Rindembukta].) Unpublished report, P W "Sevmorge- ologgn ", Leahgrad. Report on fieldwork in 1968.95 pp.

P m , AI. et al. 1968: GeoiogiWkie issledovanija v vosMnoj Easti Zemli NordenBelh (rajon K'ell'-en, Dancigdalen i Agard- dalen). Wt o poiskovo-m&mtnych stdchmych i litologo-strati- gd~tkskich issl-jach, p " ootrjadom No. 1 Spicber- genskoj ekspedicii letom 1%7=picbrgene. (Tkological studies in the eastern part of Nordenskiold Land (Kjellstrmdalen, Danzigdalen and Agardhdalen areas). Report of map drafting, prospecting and structural studies, Ganied out by party no. 1 of the Spitsbergen expedition, summer 1967, on Spitsbergen.) Unpublished report, PG0 "Sevmorgeologija ", Leningrad.

Panov, A.I., LivSic, Ju.Ja. & Urtinskaja, M.\! 1966: GeologiEeskoe stroenie ucastkov tundra Bochemana i mys Lajla - Gren-fiord (Is- fiord, o. Zapaduyj Spicbergen). (Outline of the geology of the Bohe- manflya and Kapp Laila-Grenfjorden areas [Isfjorden, Spitsbergen].) Unpublished report, PG0"Sevmorgeologija ", Leningrad. Report on reconnaissance and structural studies in 1965. 136 pp.

Panov, A.I., LivSic, Ju.Ja., Mokm, Ju.1. & MuraSa: L.G. 1970: Ge- ologiEeskie issledovanija v severnoj Easti Zemli Nordeael'da i zapadnoj Easti Zemli Sabine (j&nye pobereZ'ja Sassen-fiorda i Tempe1'-fiorda). (Geological study in northern Nordenskiold Land and western Sabine Land [south coast of Sassenfjorden and Tempel- fjorden].) Unpublished report, PGO"Sevmorgeologija", Leningrad. Report on reconnaissance and structural studies in 1969.99 pp.

$kola, I.V., Relina, T.M., Mazur, XB. & Alter, S.M. 1980: Novye dannye o sostave i stroenil osadoEnogo Eechla po materialam burenija grumantskoj parametriEeskoj s W y (New data on the composition and structure of the sedimentary platform cover on the basis of material from the drilling of a parametric hole at Grumantbyen). In: Geology of the sedimentary platform cover of the archipelago of Svalbard). Sborniknatienych trudov (Collection of Scientific Papers), NIIGA, Leningrad, 13-24.

Sun, A. Y. 1980: Structure and stmtigmphy of the Beneliustinden area, Wedel Jarlsberg Land and Torell Land, Spitsbergen. Unpublished M.S. thesis, University of Wisconsin-Madison. 1-1 16.

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4.2 Central and western Spihbergen: Upper Palaeozoic succession

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Baker, B.H., Forbes, C.L. & Holland, M.E.W. 1952: Fossiliferous strata at Kapp Scania, Daudrnannsqm, Vestspitsbergen. Geological Mag- azine 89 (4), 303-304.

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Cutbill, J.L., Henderson, W.G. & Wright, N.J.R. 1976: The Billefjorden Group (Early Carboniferous) of central Spitsbergen. Norsk Polar- institutt Sknfer 164,57-89.

Cutler, M.A. 1981: The Middle Carbonifrous-Permian stmtigmphy of Midterhuken Peninsula, Spitsbergen. Unpublished M.S. thesis, Uni- versity of Wisconsin-Madison. 1-100.

Dallmann, W.K. 1993: Notes on the stratigraphy, extent and tectonic implications of the Minkidjellet Basin, Middle Carboniferous of central Spitsbergen. Research Note. PoIar Research 12 (2). 153-160.

Dons, C.E. 1983: Fasies og paleostr0manalyse av Nordenskioldbreen Formasjonen (overkarbon-undeyenn), sentmle Spiisbergen. Unpub- lished cand. real. thesis, University of Oslo, 1-335.

Ezaki, Y. & Kawamura, T. 1992: Carboniferous-Permian corals from Skansen and Festningen, Central Spitsbergen: their fauna1 characteristics. 4. 59-75 in Nakamwa, K. (ed.) 1992: Investigations on the Upper Carboniferous - Upper Permian Succession of West Spits- bergen 1989-1991. Japanese-Norwegian Research Group, Hokkaido University, Sapporo.

Forbes, C.L., Harland, W.B. & Hughes, N.E. 1958: Paleontological evidence for the age of the Carboniferous and Permian rocks of central Vestspitsbergen. Geological Magazine 95,463-490.

Frebold, H. 1937: Das kstuqpprofil auf Spitzbergen. IV: Die Bra- chiopoden- und Lamellibrauchiatenfauna und die Stratigraphie des Oberkarbons und Unterperms. S h i e r om Svalbard og Ishavet 69, 1-94.

Frebold, H. 1939: Das Festungsprofil auf Spitzbergen. X Stratigraphie und Invertebratenfauna der ateren Eotrias. Sknfer om Svalbard og Ishavet 77, 1-58,7 figs, 3 tbl.

Fredriksen, K.R. 1988: Sedimentologiske og diagenetiske unders0kel- ser av Kapp Starostinfomjonen p i Akselaya og Mariaholmen, Svalbard. Unpublished cand. scient. thesis, University of Tromss. 1-303.

Gavrilov, B.P. & Bijukov,A.S. 1986: Informacionnyj 06% oprovedenii rekognoscirovoEnych rabot Wastka "Gora Ferdinanda" mesto&de- nija "Piramida" v 1985 g. (Prelimhq report on reconnaissance work in the "Ferdinand Mountain" area of the Pyramiden coal deposit in 1985.) Unpublished report, PGO"Sevmorgeologija", Leningrad. 3 1 pp.

Gavrilw, B.P., Bijukov, A.S. & Evdokimova, N.K. 1988: Sopostavle- nie razrezov kamennougol'nych i permskich otloZenij v rajone Bille- fiorda i projavlenija v nih uglja, gipsa i bituma. (Correlation of Car- boniferous and Permian successions in the Billefjorden area and coal, gypsum and bitumen occurrences in them.) Unpublished report, PGO"Sevmorgeologija", Leningrad. Report on the thematic project h m 1986-1988. 131 pp.

Gavrila: B.P., Pavlw, A.V. & Fedina, LP. 1964: GeologiEeskie issledovanija v rajonach Bille-fiorda i Chornsunna, Zapadnyj Spicbergen. (Geological studies in the Billefjorden and Hornsund areas.) Unpub- lished report, PGO"Sevmorgeolog~ija ", Leningrad. Report on fieldwork in 1963. 196 pp.

Hellem, T. 1980: En sedimentologisk og diagenetisk unders0kelse av utvalgte profiler fm Tempewordgruppen berm) i Isjordomrddet, Spitsbergen. Unpublished cand. real. thesis, University of Oslo. 1- 214.

Henriksen, L.B. 1988: En sedimentologisk og diagenetisk unders0kelse av Kapp Starostinformasjonen pd Akselaya og Mariaholmen, Sval- bard. Unpublished cand. scient. thesis, University of Tromse.

Holliday, D.W. & Cutbill, J.L. 1972: The Ebbadalen Formation (Car- boniferous), Spitsbergen. Proceedings Yorkshire Geological Society 39, 1-32, 3 plates.

Holliday, G.W. 1966: Nodular gypsum and anhydrite rocks in the Bille- fjorden region, Spitsbergen. NorskPolarinstitutt Arbok 1965,65-73.

Holliday, G.W. 1968: Early diagenesis in Middle Carboniferous nodular anhydrite of Spitsbergen. Proceedings Yorkshire Geological Soci- ety 36,277-292.

Holtedahl, 0. 1911: ZUI Kenntnis der Karbonablagerungen des westlichen Spitzbergens. I: Eine Fauna der Moskauer Stufe. SRn'fter Vifenskapssel~kupet i Kristiania, 191 1, no. 10, 1-46.

Holtedahl, 0. 1913: Zur Kenntnis der Karbonablagerungen des westlichen Spitsbergens. II: Allgemeine stratigraphische und tektonische Beobachtungen. Yidenskapsselskapets Sknf er Matematisk-Natur- vitenskapelig Masse, 1912. 23. Kristiania. 1 -9 1.

Igo, H. & Okimura, Y. 1992: Carboniferous-Permian foraminifers of west Spitsbergen. Pp. 97-1 17 in Nakamura, K. (ed.) 1992: Investiga- tions on the Upper Carboniferous - Upper Permian Succession of West Spitsbergen 1989-1991. Japanese-Norwegian Research Group, Hokkaido University, Sapporo.

Johannessen, E.P. & Steel, RJ. 1992: Mid-Carboniferous extension and rift-infill sequences in the Billefjorden Trough, Svalbard. In Dall- mann, W.K., Andresen, A. & Krill, A. (eds.): Post-Caledonian tectonic evolution of Svalbard. Norsk Geologisk Ifdssknji 72 (l), 35-48.

Johannessen, E.P. & Steel. RJ. 1990: Carboniferous sequences, Bille- fjorden Trough. Pp. 1-26 in Mmk, A. (ed.): Sequence stmtigmphy jkld workshop, Svalbard 1990. IKU, Trondheim.

Johannessen, E.P. 1980: Fasies analyse av Ebbadalen formasjonen (mellomhrbon), Billejorden trau, Spitsbergen: studier av alluviale og kystsedimenter i et forkastningsbasseng. Unpublished cand. real. thesis, University of Bergen. 1-314.

Johansen, T. 1994: Sedimentology and diagenesis of Tjrrelljellet Mem- bel: Biinsow Land, Centml Spitsbergen. Unpublished cand. scient. thesis, University of Tromss. 1-230,2 app.

Kano, A. 1992: Paleoecology of palaeoaplysinid bioherms of the Lower Permian in central Spitsbergen. 4. 119-125 in Nakamura, K. (ed.) 1992: Investigations on the Upper Carboniferous - Upper P e d a n Succession of West Spitsbergen 1989-1991. Japanese-Norwegian Research Group, Hokkaido University, Sapporo.

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Kleinspehq K.L., Steel, R.J., Johannesen, E. & Netland, A. 1984: Con- glomeratic fan-delta sequences, Late Carboniferous-Early Pemian, western Spitsbergen. Canadian Society of Petroleum Geologists M m i r 10,279-294.

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Lauritzen, 0. 1 98 1 : Investigations of Carboniferous and Permian sediments in Svalbard: I. The development of the Gipshuken Fomation (Lower Permian) at Trollfuglfjella in central Spitsbergen, Svalbard. Norsk Polarinstitutt Sknfer 176, 1-22.

Lauritzen, 0. 1983: Karstic surface in the Lower Permian Sabkha sequence of the Gipshuken Fomation, central Spitsbergen, Svalbard. Polar Research I n.s., 157-160.

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LW, A. 1981: Fasies analyse av undre permiske karbonater i Tjrrelwellet Ledd av Nordenswldbreen Formasjonen, Billejord- omrddet, Spitsbergen. Unpublished cand. scient. thesis, University of Bergen, 1-2 18.

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Netland, A. 1982: Fasies analyse av Drevbreen be& og Nordenski5ld- breen Formasjonen, m karbon til undre penn, BeNsund omrddet, Svalbard. Unpublished cand. real. thesis, University of Bergen, 1-204.

Nilsson, I. 1988: Carboniferous - Permian fusulinids on the Nord- jorden Block, Spitsbergen (Svalbard). Unpubl. cand. scient. thesis, University of Oslo, 1-106.

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Skaug, M. 1982: BentisRe fossile assosiasjoner og faciemariasjoner I Nordenskiiildbreen Formasjonen (overkarbon-underpenn), sentmle Spitsbergen. Unpublished cand. scient. thesis, University of Oslo, 1-220.

Skaug, M., Dons, C., Lauritzen, 0. & Worsley, D. 1982: Lower Permian palaeoaplysinid bioherms and associated sediments from central Spitsbergen. Polar Research 2,57-75.

Stensio, E.A. 1918: Zur Kenntnis des Devons und des Kulms an der Klaas Billenbay, Spitzbergen. Bulletin Geologiska Institutionen Uni- versitet Uppsala 16, 115-124.

Sundsbee, G. 1982: Facies analysis of Lute C a r b o n i f m and Early Permian carbonates in the Billejorden area, Spitsbergen. Unpub- lished cand real, thesis, University of Bergen, 1-161.

Svindland, T. 1983: Studim av Kmbonater og evaporitter i mellomkarbon, Billejorden tmu, Spitsbergen. Unpublished cand. scient. thesis, University of Bergen. 1-179.

Tidten, G. 1972: Morphogenetisch-otogenische Untersuchungen an Pterocorallia aus dem Penno-Karbon von Spitzbergen. Palaeonto- gmphica, Abt. A. 139 (1-3), 1-63.

Toula, E & Drasche, R.v. 1875: Penno-Carbon-Fossilien von der West- kiiste von Spitzbergen (Belsund, Cap Stamtschin, Nordjord)). E. Schweizerbart'sche Buchdruckerei, Stuttgart. 37 pp.

Ustrickij, VI. & Sosipatrava, G.P. 1969: Detal'naja stratigrafija moskovskich, verchnekamemougol'nych i niZn-ch otloZenij rajona Is-fiorda. (Detailed stratigraphy of Moscovian, Upper Car- boniferous and Lower Permian deposits in the Isfjorden area.) Un- published report, PG0 "Sevmorgeologija ", Leningrad Report on fieldwork in 1967.41 pp.

Wines , T.S. 1966: Observations on the Carboniferous and Permian rocks of Vestspitsbergen. Norsk Polarinstitutt ldrbok 1964,7-29.

Wordie, J.M. L919: Report on the Carboniferous exposures north of Adolf Bay (Spitsbergen). Scottish Spitsbergen Syndicate Papers.

Wright, N.J.R. 1975: The Billefjorden Group of Western Spitsbergen. CASP Report 9, Svalbard Stratigmphic Series, Carbonifrow and Permian Subseries. 1-37.

Wright, N.J.R. 1975: The Billefjorden Group, Central and Eastern Spitsbergen. CASP Report 6, Svalbard Stmtigmphic Series, Car- boniferous and Permian Subseries. 1-79.

4.3 Central and western SpWergen: Mesozoic successZon

Biickstriim, S.A. & Nagy, J. 1985: Depositional history and fauna of a Jurassic phosphorite conglomerate (the Brenthrdhaugen Bed) in Spitsbergen. Norsk Polarinstitutt Skrifter 183, 1-61.

BBckstriim, T. 1980: Paleontologisk og sedimentologisk unders0klse av Brentskarhaugen-laget (h) pd Spitsbergen. Unpublished thesis, University of Oslo. 1-139.

Birkenmajer, K. 1966: Lower Cretaceous tidal deposits of Central Vest- spitsbergen. Norsk Polarinstitutt ldrbok 1964, 73-85.

Birkenmajer, K. 1972: Megaripples and phosphorite pebbles in the

Rhaeto-Liassic beds south of Van Keulenfjorden, Spitsbergen. Norsk Polarinstitutt ldrbok 1970, 1 17-127.

Bjaerke, T. & Dypvik, H. 1977: Sedimentological and palynological studies of Upper Triassic - Lower Jurassic sediments in Sassen- fjorden, Spitsbergen. Norsk Polarinstituttldrbok 1976,131-150.

Bjorey, M. & Vigran, J.O. 1980: Geochemical study the organic matter inoutcrop samples from Agardhijellet, Spitsbergen. In: Douglas, A.G. and Maxwell, J.R. (eds.). Advances in Organic Geochemisfry 1979, Pergamon Press, 141-147.

Chlebowski, R & Wierzbowski, A. 1983: Pyroclastic material from the Upper Triassic deposits of Sassenfjorden, Spitsbeeen. Polar Re- search I n.s., 75.

Dypvik, H. 1980: The sedirnentology of the Janusfjellet Formation, Central Spitsbergen (Sassenfjorden and Agardhijellet areas). Norsk Polarinstitutt Sknfier 172, 97- 134.

Dypvik, H. et al. 1987: Study of the sedimentological and structural evolution of the area between Kjellstmdalen and Adventdalenl Sassendalen, central Spitsbergen. I987-Report. B e R&D project 1068.

Dypvlk, H., Hvoslef, S., Bjaerke, T & Finnerud, E. 1985: The Wilhelm- aya Formation (Upper Triassic-Lower Jurassic) at Bohemanflya, Spitsbergen. Polar Research 3 (2), 155-1 65.

Dypvik, H., Nagy, J., Eikeland, T.A., Backer-Owe, K., Andresen, A., Haremo, l?, Bjaxke, T., Johansen, H. & Elv&i,A. 1991: The Janus- fjellet Subgroup (Bathonian to Hauterivian) on central Spitsbergen: a revised lithostratigraphy. Polar Research 9,2 1-43.

Endresen, T. 1985: Sedimentologi og diagenese i nedre-kritt, Caroline- jellet Fonnasjon, Svalbard. Unpublished cand. scient. thesis, Uni- versity of Oslo. 1-258.

F ie rud , E. 1982: Sammensetning, sedimentasjon og termisk omdan- ning av klastisk organsk materiale i jumssiske og krittassiske svart- shfi., Svalbard. Unpublished cand. scient. thesis, University of Oslo. 1-165.

Frebold, H. & Stoll, E. 1937: Das Festungsprofil auf Spitzbergen. 111: Stratigraphie und Fauna des Jura und der Unterkreide. Sknfier om Svalbard og Ishavet 68, 1-85.

Frebold, H. 1928: Das Festungsprofil auf Spitzbergen. Jura und Kreide. 11: Die Stmtipphie. Sknfier om Svalbard og Ishavet 19, 1-39.

Frebold, H. 1928: Stratigraphie und Paliiogeographie des Jura und der Kreide Spitzbegens. Zentmlblatt fir Minemlogie, Geo1w.e und Paliiontologi'e, Jdkrg 19281, Abt. b. 12,625-629.

Frebold, N. 1931: Faziellc Verh&iwe des M e s o z o ~ s im Eis- tjorden-Gebiet Spitzbegem. &@er m Svalbard og Ishavet 37, 1-94.

Haremo, E, ,Andmsen, A. & Dypvik, H. 1993: Mesozoic extension ver- sus Tertiary compression along the Billefjorden Fault Zone south of Isfjorden, central Spitsbagen. G e o l ~ ' m 1 Magazine 130 (6), 783- 795.

Hatleberg, E.W. 1982: Conodont biostmtipphy of the Lower Triassic at Van KeulenBonien, Spitsbergen and the ThakRhoIa Valley, Nepal. M.S. thesis, University of Wisconsin-Madison.

Ishibashi, T. & Nakazawa, K. 1989: Triassic ammonites from West Spitsbergen. Mem. Fac. Sci., Kyurhu Univ., S m D, GeoL, 26 (3), 21 5- 241.

Jacobsen, K.D. 1983: En sedimentologisk unders0kelse av Kapp Toscana Gruppen (0. Dias - M. Jum) ved Yan Keulenjorden pd Svalbard. Unpublished cand real. thesis, University of Bergen, 158 PP.

Johnsen, S. 1980: A sedimentological, palaeontological and palaeoe- cological investigation of Lower Ih'assic outcrops on the west coast of Spitsbergen. Unpublished cand. real. thesis, University of Oslo, 206 PP.

Kopik, J. & W~erzbowski, A. 1988: Ammonites and stratigraphy of the Bathonian and Callovian at Janusfjellet and Wimadjellet, Sassen- fjorden, Spitsbergen. Palaeontologica 33 (2), 145-1 68.

Krajewski, Kl? 1992: Phosphorite-bearing sequence of the Wilhelm- aya Formation in Van Keulenfjorden, Spitsbergen. Studia Geologica Polonica 98,171-200.

Moe, H.R 1980: Sedimentologiske og diagenetiske undersakelser i kn'ttlagrekken pd Svalbard. Unpublished cand. real. thesis, Univer- sity of Oslo. 1-140.

Mmk, A., Elvebakk, G., Forsberg, A.W., Hounslow, M.W., Nakrem, H.A., Vigran, J.O. & Weitschat, W. 1999: The type section of the Vikinghagda Formation - a new Lower Triassic unit in Central and Eastern Svalbard. Polar Research 18 (l), 5 1-82.

Nagy, J., Lefaldli, M., Biickstriim, S. & Johmen, H. 1990: Aggluti-

http://jurassic.ru

7. BIBLIOGRAPHY --

nated foraminiferal stratigrsphy of Middle Jurassic to basal Creta- ceous shales. central S~itsbemen. PD. 969-1015 in Hemlebea C. et " . al. (eds.): Paleoecology, biostratignaphy, paleoceanogmphy and taxonomy of agglutinated firaminifera. Kluwer Academic Publishers, Netherlands.

Nymther, E. 1966: Petrogmfisk undersekelse av sedimentam bergarter& tidsmmmet kritt-ternemer i Nathorst Land, Vest Spitsbergen. Unpublished cand. real. thesis, University of Bergen. 1-168.

Panov, A.I., Nepomiluev, VF., KoEinskaja, M.X & Mokin, Ju.1. 1968: GeologiEeskie issledovanija v vostoEnoj Casti Zemli Norden%lYda (rajony K'ellstxtbmMen, ~ & i ~ d a l e n i ~~arddalen). (Geological study in eastern Nordemkicild Land Kiellstromdalea Danzigdalen and Agardhdalen areas].) ~npublishid-report, PGO O"~evmo~eo1ogzga l',

Leningrad. Report on reconnaissance, structural and lithostratigraphical studies in 1967. 170 pp.

Parker, J.R 1966: Folding, faulting and dolerite intrusions in the Meso- zoic r& of the fault zone of central Spitsbergen. Norsk Polarinsti- tutt Arbok 1964,47-55.

Pavlov, A.V, Relina, T.M., Gavrilov, B.P., Petrenko VM., DanjuSev- skaja, A.I. & Fedina, I.P. 1963: GeologiEeskie issledovanija v central'noj Easti ostrova Zapadnyj $icbergen (v S jaZi S problemoj neftegazonosnosti). (Geological study in central Spitsbergen [in the context of oil and gas problems].) Unpublished report, PG0"Sev- morgeologija", Leningrad. Report on fieldwork in 1962.478 pp.

PEelina, T.M. & Sokolov, YN. 1964: LitostratigrafiEeskaja i bitwni- nologiCeskaja charakferistika rnezozojskich otl&enij rajonov Van- ~ejlin-fiorda i mysa Sel'maneset ~sifiorda. (The li&o&atigraphy and bitumen content of Mesozoic dewsits in the Van Keulenfiorden and Isfjordem [Selmaneset] areas.) kpublished report, PGO"S~V- morgeolog~a ", Leningrad. Report on fieldwork in 1963. 162 pp.

PEelina, T.M. 1965: Mezozojskie otloZenija rajona Van-Kejlenf'orda, Zapadnyj Spicbergen (Mesozoic deposits around Van Keulentjorden, Vestern Spitsbergen). In Maferialy po geolog'iSpicbergena. Lenin- grad 1965.

Schenk, A. 1890: Jurasische H6lzer von Green Harbour auf Spitz- bergen. Kongl. Vet.-AM Forkandlingar 1890 (l). 5-10.

Sarrensen, L. 1981: Et regiunalt &dim av minemlogi og diagenese i HelvatiaJellet Fonaarjonen ( a m ) , M b d . Unpublished cand. real. thesis, University of m e n , 125 pp.

Spatz, EH. 1983: The Cretaceous sequence of Midterhuken peninsula, Spitsbergen. M.S. thesis, University of Wisconsin-Madison. 1-145.

Steel, R.J. 1977: Observations on some Cretaceous and Tertiary sandstone bodies in Nordenskiold Land, Svalbard. Norsk Polarinstitutt Arbok 1976.43-68.

Steel, RJ., Gjelberg, J. & Ham, G. 1978: Helvetiafjellet Formation (Bmmian) at Festningen, Spitsbergen - a field guide. Norsk Polar- institutt Arbok 1977,111-128.

Weitschat, W. & Lehmann, U. 1978: Biostratigraphy of the uppermost part of the Smithian Stage (Lower Triassic) at the Botneheia, West Spitsbergen. Mitteilungen, Geologisch-Paliiontologisches Institut der Universitit Hamburg 48, 85-100.

Wierzbowski, A., Kulicki, C. & Pugaczewska, H. 1981: Fauna and stratigraphy of the uppermost Triassic and the Toarcian and Aalenian deposits in the Sassenfjorden, Spitsbergen. Acta Palaeontologica Polonica 26 (3-4).

4.4 Central and western Spitsbergen: Tbrtiary succession of Central T d r y Basin

Birkemmjer, K. & NareW. W. 1963: Doletite drift blocks in marine Tertiary of Smkapp Land and some remarks on the geology of the eastern part of this area. Norsk Polarinstitutt drbok 1962,68-89.

Birkenmajer, ,K. Fedorowski, J. & Smuliowski, W. 1972: Igneous and fossiliftrow sedimentiuy drift pebbles in marine Tertiary of Torell Land, Spitsbmgen. Norsk Polarinstitutt Arbok 1970,146-1 64.

Brendel, R. 1985: Geologischer Aufbau und Stmtigmphie eines Ge- bietes zwischen dem Hollendardalen und dem Grendalen im Norden- skiiild Land Spitrberpn. Unpublished Diplom thesis, University of Kiel. 1-57.

Croxton, C.A. & Pickton, C.A.G. 1976: The Van Mijenfjorden Group (Tertiary) of SW Nordenskiiiid Land, Spitsbergen. In W.B. Harland et al.: Some coal-bearing strata in Svalbard. Norsk Polarinstitutt Sknper 164,2946.

Dalland, A. 1977: Erratic clasts in the lower Tertiary deposits of Sval- bard - evidence of transport by winter ice. Norsk ~olarinstitutt Arbok 1976, 151-166.

Dypvik, H. L. Nagy, J. 1979: Early Tertiary bentonites from Svalbard. Geological Magazine 11 6,457-468.

I-Egg, R. 1925: A new Tertiary Fauna from Spitsbergen. Geologiska Zn- stitutionen Uppsala Bulletin 20, 39-55.

Hansen, O.K. 1982: Den sedimentologiske utvikling og dens innvirk- ningpd Aulldannelse i nedre Firkantfonnasjonen (Pa1eocen)pd nordsiden av Adventdalen, Spitsbergen. Unpublished cand. real. thesis, University of Bergen. 1-155.

Haugsbe, H.A. 1988: Sedimentologiske unders0kelser av nedre del av Ba@eIrformasjonen i Bmgniarifella, Spitsbergen. Unpublished cand. scient. thesis, University of Tromw.

Head, M.J. 1989: Palynostratigraphy of the Central Basin (Paleocene- Lower Eocene?), Spitsbergen. Abstract. Palynology 13,283.

Heer, 0. 1866: Om de af A.E. Nordenskiold och C.W. Blomstrand p& Spetsbergen upptiickta fossila vkter. Kongeliga Svenrkn Veenskaps Akademiens Handlingar 23,149- 155.

Helland-Hansen, W. 1985: Sedimentology of the Battfjellet Formation (Paleogene) in Nordenskiold Land, Spitsbergen. Unpublished cand. scient. thesis, University of Bergen, 1-322.

Helland-Hansen, W. 1990: Sedimentation in a Paleogene foreland basin, Spitsbergen. American Association of Petroleum Geologists, Bulletin.

Kalgraff, K. 1978: Aspects of sedimentation in Firkanten Formation, Tertay, Svalbard. Unpublished cand. real, thesis, University of Bergen. 1-178.

Kotlukov, VA. 1936: GeologiEeskoe stroenie i uglenosnost' rajona Barencbprga i tundry Bogemana (Zap. Spicbergen). (Geological structure and coal content of the Barentsburg region and Boheman- flya, West Spitsbergen.) Leningmdrkij geologiCa~kij trest, %a'y 11. Leningrad.

LivSic, Ju.Ja. 1965: Paleogenovye otldenija Zemli Norddl 'da (Zap. Spicbergen). (Paleogene deposits of Nordenskiold Land, Vestspits- bergen.) Pp. 193-215 in Sokolov, VN. (ed.): Materialy po geologiiSpicbergena. [English translation in Harland, WB. et al.(ed.): Geology of Spifsbergen. National Lending Library of Sci- ence and Technology, Boston Spa., Yorkshire 1970.1

LjutkeviE, E.M. 1937: Geologija tretitnich uglenosnych otloZenij S~itsbergena rajona Ajs-fiorda. (Geology of the Tertiary coal-bearing deposits of Spitsbergen, Isfjmden area.) NIIGA, %dy 76.

Lundstrmq R 1987: A compamtive sedimentological study of two coal-bearing deltaic successions: The Nordmela Fm. (early Jumssic) of Hammeflest Basin and the Todalen Mb. (eurly Paleocene) of Cen- tml Spitsbergen Basin. Unpublished cand. scient. thesis, University of Bergen, Volume 1 (text) 149 pp. and volume 2 (illustrations) 124 PP.

Maier, J. Mischke, W., Skowronek, F. & Zimmermann, J. 1987: Geolo- gische Kartierung des Tertiiirs im siidlichen Nathorst Land und nordlichen Torrell Land, Spihbergen. Unpublished Diplom thesis, University of Kiel, 1-179.

Manum, S.B. & Throndsen, T. 1978: Dispersed organic matter in the Spitsbergen Tertiary. Norsk Polarinstitutt drbok 1977, 179-187.

Manum, S.B. & Throndsen, T. 1978: Rank of coal and d i v e d organic matter and its geological bearing in the Spitsbergen Tertiary. Norsk Polarinstitutt Arbok 1977,159-1 77.

Manum, S.B. 1960: Some dinoflagellates and hystrichosphaerids from the Lower Tertiary of Spitsbergen. Nytt Magasin for Botanikk 8, 17-26.

Manum, S.B. 1963: Notes on the Cretaceous-Tertiary boundary in Basilikaen, Vestspitsbergen, and a new report of Gihkgo from the Spitsbergen Tertiary. Norsk Polarinstitutt Arbok 1962, 149-152.

Matthiessen, J. 1985: Kartierung der tertiriren Sedimente im siidlichen Nathorst Land (Spitsbergen, Svalbard). Unpublished Diplom thesis, University of Kiel, 145.

Matthiessen, J. 1986: Biostratigraphie tertiarer Ablagerungen (Palaoziin) am Van Keulendonien (Spitsbergen) nach Dinofagel- laten-Zysten. Unpublished Diplom thesis, University of Kiel. 1-94.

Monsen, T.N. 1984: Studie av terti~re avsetninger i l b m s I omrddet basert pd branndata og seismik studie av tidlig terti~re avsetninger pi Svalbard med hovedvekt pd en sedimentologisk studie av Endalen sandstein kmpp. 2 vol. Cand. scient. these, University of Bergm

Miiller, D. 1985: Geologischer Aufbau und Stmtigmphie des Gebietes zwischen GrenJorden und Hollendardalen im nordwestlichen Nordenslii6ld Land, Spitsbergen. Unpublished Diplom thesis, Uni- versity of Gel, 1-56.

Miiller, R.D. & Spielhagen, R E 1990: Evolution of the Central Tertiary

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Basin of Spitsbergen: Towards a synthesis of sediment and plate tectonic history. Palaeogeogmphy, Palaeoclimatology, Palaeoecology 80,153-172.

Nsttvedt, A. 1982: Chamcteristics and evolution of the Askeladden Delta Sequence (Paleocene) on Spitsbergen - with comparison to the Ravenscar Group Deltaic sequence of Northeast England. Dr. scient. thesis, University of Bergen, 1-18 1.

NeMredt, A. 1985: Askeladden Delta Sequence (Paleocene) on Spits- bergen - sedimentation and controlls on delta formation. Polar Re- search 3,21-48.

Niimberg, D. 1985: Geologische Kartierung der terticiren Schichtfolge im siimvestlichen Nathorst Land (Spitsbergen, Svalbard). Unpub- lished Diplom thesis, University of Kiel, 1-54.

Nysaether, E. 1966: Petrografisk undersekelse av sedimentrere bergarter fm tidmmmet Mtt-tertizr i Nathorst Land, Vest Spits- bergen. Unpublished cand. real. thesis, University of Bergen. 1-168.

Ram, J.P. 1922: On the mollusca of the Tertiary of Spitsbergen. Resul- tater Norske Spitsbergenekspedisjoner. ShQ?er om Svalbard og Ishavet 1 (2), 1-28.

Schaupeter, W. & Struck, U. 1988: Fl&henhafte Kartierung der mesozoischen und Riinozoischen Sedimente auf Bohemanjlya und Erd- mannfya am nordlichen Isjordenufer, Spitsbergen, Svalbard. Un- published Diplom thesis, University of Kiel. 1-96.

Schulz, R. 1985: Geologischer Aujbau und Stmtigmphie des Gebietes zwischen Colesbukta und Grendalen im Nordenskiold Land, Spits- bergen. Unpublished Diplom thesis, University of Kiel. 1-46.

Schulz, R. 1985: Quantitative Komponentenanalyse pbklastischer, paliiogener Sedimentgesteine aus dem nordwestlichen Nordenskiold Land, Spitsbergen. Unpublished Diplom thesis, University of Kiel.

Schweitzer, H.J. 1974: Die "tertiaren" Koniferen Spitzbergens. Palaeontogmphica 8-149, 1-89.

Spielhagen, R. 1985: Geologischer Aujbau und Stmtigmphie des Gebi- etes zwischen HoNendarbukta, Colesbukta und Hollendardalen im nordwestlichen Nordenskiold Land, Spitsbergen. Unpublished Diplom thesis, University of Kiel, 1-55.

Spielhagen, R. 1985: finglomemte und Glendonite im Miir des nordwestlichen Nordenskiold Land, Spitzbergen. Unpublished Diplom thesis, University of Kiel.

Steel, RJ. 1977: Observations on some Cretaceous and Tertiary sandstone bodies in Nordeuskiiild Land, Svalbard Norsk Polarinstitutt h b o k 1976,43-68.

Steel, R.J. 1992: The Tertiary succession of the Central Basin: Se- quence stratigapby and its tectonic implications. In Dallmann, WK., Andresen, A. & Krill, A. (eh.): Post-Caledonian tectonic evolution of Svalbard Proceedings abstract. Norsk Geologisk lFdrsImQ? 72(1).

Steel, RJ., Dalland, A., Kalgraff, K & Larsen, X 1981: The central Tertiary basin of Spitsbergen - sedimentary development in a sheared margin basin. Pp. 647-664 in Kerr, J.W. & Fergusson, A.J. (eds.): Geology of the North Atlantic Borderlands. Canadian Society of Petroleum Geologists, Memoir 7.

Throndsen, T. 1977: Sammensehing og termisk omdannelse av organisk materiale i Svalbards terh'm~: Unpublished cand. real. thesis, University of Oslo. 1-266.

Throndsen, T. 1982: Vitrinite reflectrauce studies of coals and dispersed organic matter in Tertiary deposits in the Adventdalen area, Svalbard. Polar Research 2,77-91.

Tmseth, D. 1981: The sedimentary history offirkanten Formation (Pa- leocene) in the Adventdalen area (Spitsbergen). Unpublished cand real. thesis, University of Bergen, 1-181.

Vonderbank, K. 1970: Geologie und Fauna der terti&en Ablagerungen Zentral-Spitsbergens. Norsk Polarinstitutt Skiper 153, 1-1 19.

Weinelf, M. 1985: Geologische Kartierung tertiiirer Schichten urn den Yan Karlen#orden, Spitsbergen, Svalbard. Unpublished Diplom thesis, University of Kiel, 1-50.

Wolf, T. C. W. 1985: Verbreitung und Ausbildung der tertiiiren Sedi- mentfblge um den Yan Keulenaorden. Unpublished Diplom thesis, University of Eel, 1-32.

Wolf, T. C. W. 1986: Sedimentpetmgmphische Untersuchung an ter- tiBmn Gesteinen der Bat@elIet- und Aspelintoppen-Formationen des Yan Keulenjorden-Gebiettw, Spitsbergen, Svalbard. Unpublished Diplom thesis, Univmity of Kiel, 1-53.

Ytreland, G.K. 1980: Sedimentation along the western margin of the Centml Tertiary Basin (Fihnten Formation), Spitsbergen. Unpub- lished cand. real. thesis, University of Bergen. 1-1 83.

4.5 Central and western Spitsbergen: T e r y succession @f Renardodden

Dallmann, W.K. 1989: The nature of the Precambrian-Tertiary boundary at Renardodden, Bellsund, Svalbard. Research Note. Polar Re- search 7 (2), 139-145.

Head, M.J. 1984: A palynological investigation of Tertiary strata at Renardodden, West Spitsbergen. 6th International Palynological Conference, Abstmcts., 61.

Thiedig, E Pickton, C.A.G., Lehmann, U., Harland, W.B. & Anderson, H.J. 1979: Das Tertii von Renardodden. Mitteilungen des Geolo- gisch-Paliiontologischen lnstihrts der Universitiit Hamburg 49, 135-146.

5 Northwestern Spitsbergen

5.1 Northwestern Spbbergen, entire succession

Barbaroux, L. 1967: Etude giologique et sidimentologique de la Presqu'ile de Bregger, Baie du Roi, Vastspitrbergetz. Unpublished thesis, University of Marseille, Pts. 1 (1-185) & 2 (annexe).

Brommer, A. 1994: Geologie der E' B r ~ h a l b i n s e l in NBcSpitz- bergen: Lithologie und tektonische Untersachungen im NJS&ment des Westspitsbergen Fold-and-17rwt Belts, Svalbard. Unpublished Diplom Thesis, University of Miinster. 1-122.

Challinor, A. 1967: The structure of Bwggerhalvraya, Spitsbergen. Geol. Mug. 104 (4).

Holtedahl, 0. 1914: New features in the geology of northwestern Spitzbergen. American Journal of Sciences, =I, No. 221. 415- 422.

Orvin, A. 1934: Geology of the Kings Bay region, Spitsbergen. S h y e r om Svalbard og lihavet 57, 1-196.

5.2 Northwestern SpitsBergen: Upper PaCaeozoic succession

Barbaroux, L. 1967: Le9 formations 'Wtritiqu6s-corallig&nes' Car- bonif&es de la Presqu'lle & B- (Baie du Roi - %&spitsbergen). BUN& Sod6rCi WoIogique da h m e (7. serib) 9,714-722.

Buggisch, W., Hiineke, H., Joachhdd, M., Liiher, H. & Thiedg, E, in press: Conbdwt of the Carboniferous and Pdmian strata from Bmggehdwya and Billefjorden Trough (Svalbd). Ge- ologisches Jahrbsrch, Harmover.

Buggisch, W., Piepjolm, K, Thicdig, E & Gosen, W. von 1994: A Middle Carboniferous cmodont fa- from Blomstrandhalvraya (NW Spitsbergen): Implications an the age of post-Deronian h t i - fication and the Svalbardian deformation. Polarforschung 62 (2/3), 83-90.

Dineley, D.L. 1958: A review of the Carboniferous and Permian rocks of the west coast of Vestspitsbergen. Norsk geologisk Tidssk~Q? 38 (2), 197-217.

Fairchild, I.J. 1982: The Orustdalen Formation of Bmggerhalveya, Svalbard: A fan delta complex of DinantianlNamurian age. Polar Re- search 1, 17.

Ludwig, P. 1988: Termb-ische bisfachmarine Mittelkarbon-Sedimente der Br0ggerhalbimel (West-Spitsbergen, Svalbard, Norwegen). Dr. rer. nat. thesis, University of Hamburg, 1-1 17.

Ludwig, l? 1991: The marine transgression in the Middle Carbonifer- ous of Bmggerhalvraya (Svalbard). Polar Research 9 (l), 65-76.

Saalmann, K. 1995: Lithologie und Tektonik der nordostlichen BrwggerhaZbinsel, W-Spitzbergen. Unpublished Diplom Thesis, University of Miinster. 1-139.

Sidow, H. 1988: Strukturelle, mikmfananeeNe und diagenetische Unter- suchungen an Gesteinen der nordlichen Briiggerhalbihsel, M- Spitzbergen, Svalbard. Unpublished Diplom thesis, Uniwrsity of Hamburg. 1-130 + 16,4 PI.

Weber, A. 1990: Geologische Kartiennzg, Gesteins- und StncRhnunrer- suchungen auf der westlichen Bmggerhalwya (NIP-S'tzbergen). Unpublished Diplom thesis, University of Hamburg. 1-132.

Wuthenau, K von 1988: Geolog&che M e r u n g 1:10.000 und Vorstel- lung eines neuen Shuhrmodells der westlichen Bmggerhalvqya (iVWSpitzbergen). Unpublished Diplom thesis, University of Ham- burg. 1-95.

http://jurassic.ru

7. BIBLIOGRAPHY

5.3 Northwestern Spitsbergen: Tertiary succession of Forlandsundet Graben

Atkinson, D.J. 1962: Tectonic control of sedimentation and the interpretation of sediment alternation in the Tertiary of Prins Karls Forland, Spitsbergen. Geological Society of America, Bulletin 73, 343-364.

Bruce, W.S. 1907: Prince Charles Foreland. Scottish Geologi'cal Maga- zine 1907, 23, 141-156.

Bruce, W.S. 1908: The exploration of Prince Charles Foreland, 1906- 1907. Geological Journal 1908, 32, 139-150.

Craig, R.M. 19 16: Outline of the Geology of Prince Charles Foreland, Spitsbergen. Transactions Geological Society ofEdinburgh 1916, 10, 276-288.

Feyling-Hanssen, R.W. & UlIeberg, K. 1984: A Tertiary-Quaternary section at Sarsbukta, Spitsbergen, Svalbard, and its foraminifera. Polar Research 2, 77-1 06.

Gabrielsen, R.H., Kbqan, O.S., Haugsbs, H., Midbse, P., Nsttvedt, A., Rasmussen, E. & Skott, P.H. 1992: The structural outline of For- landssundet Graben, Prins Karls Forland, Svalbard. In Dallmann, W.K., Andresen, A. & Krill, A. (eds.): Post-Caledonian tectonic evolution of Svalbard. Norsk Geologisk Tidsskift 72(1).

Kleinspehn, K.L. & Teyssier, C. 1992: Tectonics of the Pelaeogene For- landsundet Basin, Spitsbergen: A preliminary report. In Dallmann, W.K., Andresen, A. & Krill, A. (eds.): Post-Caledonian tectonic evolution of Svalbard. Norsk Geologisk Tidsshf7 72(1).

Kubisch, M. 1986: Geologische Kartierung tertiarer Sedimente auf Prins-Karls-Forland (Svalbard). I: Selvdgen- und Marchaise- laguna-Formation. Unpublished Diplom thesis, University of Kiel, 1-76.

Magnus, S. 1986: Geologische Kartierung tertiarer Sedimente auf Prim-Karls-Forland (Svalbard). N: Aberdeenfya-Formation. Un- published Diplom thesis, University of Kiel, 1-56.

Pagels, U. 1986: Geologische Kartierung tertiarer Sedimente auf Prins-Karls-Forland (Svalbard). IZZ: Reinhardpynten- und Kroko- dillen-Formation. Unpublished Diplom thesis, University of Kiel, 1- 56.

Rye Larsen, M. 1982: Forlandssundet Gmben (Paleocen) - Svalbards vestmar@nsedimentasjon og tektoniske utvikling av et basseng ved en transform plategrense. Unpublished cand. real. thesis, University of Bergen, 1-380.

Tyrrell, G.W. 1924: The geology of Prince Charles Foreland, Spits- bergen. Royal Society of Edinburgh Transactions 53 (2), 443-478.

Wollenburg, I . 1986: Geologische Kartierung tertiarer Sedimente auf Prins-Karls-Forland (Svalbard). II: Sesshngda-Formation. Unpub- lished Diplom thesis, University of Kiel, 1-80.

Zastawniak, E. 1981: Tertiary plant remains from Kaffinyra and Sarssyra, Forlandsundet, Spitsbergen. Studia Geologica Polonica 73, 37-42.

5.4 Northwestern Spitsbergen: Tertiary succession of Kongs- fiorden area

Midbse, P.S. 1985: Kongsjordfeltet (Paleocen) - Spitsbergen. Unpub- lished cand. real. thesis, University of Bergen, 1-226.

Orvin, A. 1934: Geology of the Kings Bay region, Spitsbergen. Sknyer om Svalbard og Zshavet 57, 1-1 96.

Schloemer-Jager, A. 1958: Alttertare Pflanzen aus Flozen der Bragger-Halbinsel Spitsbergens. Palaeontopphica B-103, 39-103.

5. S Northwestern Spitsbergen: Tertiary laws

Hoel, A. & Holtedahl, 0. 191 1: Les nappes de lave, les volcans et les sources thermales dans les environs de la Baie Wood au Spitsberg. Edenskaps Selskapets S h y e r I, Matematisk-Naturvitdenskapelig Klasse No. 9. Kristiania.

Prestvik, T. 1978: Cenozoic plateau lavas of Spitsbergen - a geological study. Norsk Polarinstitutt Arbok 1977, 129-143.

6 Eastern Spitsbergen and eastern islands

6.1 Eastern Spitsbergen and eastern islandr, entire succession

Eiken, 0. 1984: Prosessering av seismiske data fra Storfjorden, Sval- bard. Seismo-series No. 2, Seismic Observatory, University of Bergen, 1-25.

Falcon, N.L. 1928: Geology. In: The Cambridge Expedition Edge Is- land. Geogmphical Journal 72, 134- 139.

Holland, M.E.W. 1961: The geology of certain parts of Eastern Spits- bergen. Norsk Polarinstitutt Shifter 122, 1-45,3 maps.

Lock, B.E., Pickton, C.A.G., Smith, D.G., Batten, D.J. & Harland, W.B. 1978: The geology of Edgesya and Barentssya, Svalbard. Norsk Polarinstitutt S h y e r 168, 1-64.

Lowell, J.D. 1968: Upper Paleozoic and Lower Mesozoic stratigraphy of southwestern Nordaustlandet, Spitsbergen. Geological Magazine I05 (4), 348-355.

Nathorst, A.G. 1901: Bidrag till Kung Karls lands geologi. Geologiska Foreningens Forhandlingar 23 (208). 34 1-378.

Nordenskiofd, A. 1863: Geografisk och geognostisk beskrihing ofver nordSstra delarna af Spetsbergen och Hinlopen ,Strait. Kongl. Svenska Vetensk. Akad. Handl. 4 (7).

Svarc, BL. 1985: Litologo-stratigrafiEeskoe raschlenenie razreza shaZiny Raddedalen-l (0. fi&, Spicbergen). Pp. 44-58 in M.L. Verba (ed.), GeologiEeskoe shoenie Barencevo-Karskogo ielya, PGOSevmorgeologija", Leningrad.

6.2 Eastern Spitsbergen and eastern islands, Upper Palaeo- zoic succession

Cutbill, J.L. 1968: Carboniferous and Permian stratigraphy of Ny Fries- land, Spitsbergen. Norsk Polarinstitutt Arbok 1966, 12-24.

Klubov, B.A. 1965: On the occurence of Permian rocks on Barentssya. Dokl. Akad. Nauk SSSR. 162,629-63 1 (in Russian).

Lauritzen, 0. & Worsley, D. 1973: Observations on the Upper Paleo- zoic stratigraphy of the Ny Friesland area. Norsk Polarinstitutt Arbok 1973,41-51.

Lauritzen, 0. 1981: Investigations of Carboniferous and Permian sediments in Svalbard: D. The Carboniferous and Permian stratigraphy of the Wahlenbergfjorden area, Nordaustlandet, Svalbard. Norsk Polar- institutt Sknifer 176,23-44.

Mangerud, G. & Konieczny, R.M. 199 1 : Palynological investigations of Permian rocks from Nordaustlandet, Svalbard. Polar Research 9 (2), 155-167.

Olaussen, S., Gloppen, T.G. & Knarud, R 1984: Statoilb Svalbard- ekspedisjon 1982. Description and interpretation of two sedimentaiy sequences of the Lower/Middle Carboniferousfrom Nordaustlandet and Lomjorden (Ismisestranda and Bivrastfonna). Unpublished report, Statoil.

Olaussen, S., Johansen, R., Johannessen, E.P. & Knag, G.O. 1986: Statoilb Svalbardekspedisjon 1985. Karbon (Moskva) overgangslag p i Malte Brunjellet, Ny Friesland blokka, Spitsbergen. Unpublished report, Statoil.

PEelina, T.M. & KorEinskaja, M.B 1973: Permskie i triasovye otlozenija central'noj i jugo-zapadnoj Easti ostrova fi& i ostrova NadeZda. (Permian and Triassic deposits of the central and southwestern parts of Edgesya and Hopen.) Unpublished report, P W "Sevmorgeologija ", Leningrad. Report on fieldwork in 197 1 - 1972.92 pp.

Skarpnes, 0. 1984: Statoil b Svalbardekspedisjon 1982, Spitsbergen: A sedimentological profile through Upper Hecla Hoek and Lower?/Middle Carboniferous clastics and carbonates, Ditlovtoppen - Ny Friesland. Unpublished report, Statoil.

6.3 Eastern Spitsbergen and eastern islands, Mesozoic succession

Birkenmajer, K. & Wierzbowski, A. 1991: New Kimmeridgian ammonite fauna from East Spitsbergen and its phyletic significance. Polar Research 9 (2), 169-179.

Birkenmajer, K. 1979: Lower Cretaceous twin dolorite sills at Agardh- bukta (East Spitsbergen) and the problem of the thermal metamor- phism of Mesozoic palynomorphs. Studia Geologica Polonica 60, 57-63.

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Birkenmajer, K. 1984: Regressive deposition in the De Geerdalen For- mation (Rhaeto-Liassic) at Agardhbukta, East Spitsbergen. Studia Geologica Polonica 80, 47-58.

Kikenmajer, K. 1984: Sedimentary features of the Helvetiafjellet For- mation (Barremian) at Agardhbukta, east Spitsbergen. Studia Geo- logic~ Polonica 80, 59-70.

Birkenmajer, K., Pugaczewska, H. & Wierzbowski, A. 1982: The Janusfjellet Formation (Jurassic-Lower Cretaceous) at Myklegard- fjellet, east Spitsbergen. Palaeontologica Polonica 43, 107-140.

Bjaerke, T. & Manurn, S.B. 1977: Mesozoic palynology of Svalbard - I. The Rhaetian of Hopen, with preliminary report on the Rhaetian and Jurassic of Kong Karls Land. Norsk Polarinstitutt Skriifter 165, 1-48.

Bjaerke, T. 1975: Atlas of Palynomorphs from the Upper Triassic of Hopen, Svalbaml report 1975. Royal Norwegian Council for Science and Industrial Research (NTNF), Continental shelf division.

Bjaerke, T. 1977: Mesozoic palynology of Svalbard 11. Palynomorphs from the Mesozoic sequence of Kong Karls Land. Norsk Polarinsti- tutt Idrbok 1976,83-120.

Bjaerke, T., Edwards, M.B. & Thusu, B. 1976: Microplankton from the Janusfjellet Subgroup (Jurassic-Lower Cretaceous) at Agardhfjellet, Spitsbergen. A p r e h m r y report. Norsk Polarinstitutt Arbok I974, 63-68.

Bliithgen, J. 1936: Die Fauna und Stratigmphie des Oberjum und der Unterkreide von Konig Karl Land. Grimmen in Pommern, 1936, 1-91.

Bodylevskij, V. 1929: Fauna niZnego doggerea (?) iz buchty Mona (Mohns Bay) na vostoEnom pobereZ'i Spicbergena. (Faune du Dogger infMeur (?) provenant de Mohn Bay, sur la c6te orientale du Spitsberg.) Doklady Akademii Nauk SSSR (Compte rendu de l'acadkmie de I'URSS), Leningrad, 256-258.

Bodylewski, W. (Bodylevskij, V.) 1926: Contributions to the natural history of Hope Island. Fossil Shells. In: Iversen, T., Year 1926, Hopen, d t s . Norske Spitsbergenekpedisjoner I (10), 1-34.

Doyle, l?, Kelly, S.R.A. 1988: The Jurassic and Cretaceous belemnites of Kong Karls Land, Svalbard. Norsk Polarinstitutt Sknjier 189, 77 PP.

Edwards, M.B. 1976: Growth faults in Upper Triassic deltaic sediments, Svalbard. Bulletin American Association of Petroleum Geolo- gisrs 60 (3), 341-355. -

Edwards, M.B., Bjaxke, T., Nagy, J., Winsnes, T.S. & Worsley, D. 1979: Mesozoic stratigraphy of Eastern Svalbard: A discussion. Geological Magazine 11 6 (I), 49-54.

Eiken, 0. 1981: En seismisk underx0kelse av den sedimentmre lag- rekken i Agardhdalen, Svalbard. Unpublished cand. real. thesis, Uni- versity of Bergen. 1-85.

Flood, B., Nagy, J. & Winsnes, T.S. 1971: The Triassic succession of Barentseya, Edgenrya and Hopen (Svalbard). Norsk Polarinstitutt Meddelelser 100, 1-24.

Haremo, E?, Swensson, E. & Andresen, A. 1992: Evidence of Mesozoic extension along the Lomfjorden Fault Zone, Agardhbukta. In Dall- mann, W.K., Andresen, A. & Krill, A. (eds.): Post-Caledonian tectonic evolution of Svalbard. Proceedings abstract. Norsk Geologisk l ldsshji 72 (I), 136-137.

Hoeg, O.A. 1926: Fossil plants. Hopen (Hope Island), Svalbard. Re- sults of a reconnaissance in the summer 1924. Skrif?er om Svalbaml og Ishavet 10,44 pp.

Iversen, T. 1926: Hopen (Hope Island), Svalbard. Results. Norske Spits- bergen Ehpedisjon. Nr. 10,144.

Klubov, B.A. & Vasil'ev, YN. 1964: GeologiEeskie issledovanija v rajone Mysa Freden i na ostrovachVil'gel'ma, Barenca, g&. (Geolog- ical studies in the Kapp Frceden area and on Wilhehaya, Barentsnrya and Edgewa.) Unpublished report, PGO"Sevmorgeologija", Leningrad. Report on lithostratigrafic studies of Permian, Triassic and Jurassic deposits in 1963. 179 pp.

Klubov, B.A. 1963: GeologiEeskie issledovanija na ostrove &. (Geo- logical study on Edgearya.) Unpublished report, PG0"Sevmorge- ologija ", Leningrad. Report on fieldwork in 1962. 16 1 pp.

Klubov, B.A. 1965: GeologiEeskoe stroenie ostrova Barenca i sev- emogo poberet'ja ostrova g&. (Outline of the geology of Barents- Bya and the north coast of Ed-a.) Unpublished report, PG0"Sev- morgeologzija", Leningrad. Report on the thematic project from 1962-1964. 144 pp.

Lsfaldli, M. & Nagy, J. 1980: Foraminiferal stratigraphy of Jurassic deposits on Kongsnrya, Svalbard. Norsk Polarinstitutt SRr@er 172,63- 96.

h h k , A., Elvebakk, G., Forsberg, A.W., Hounslow, M.W., Nakrern, H.A., Vigran, J.O. & Weitschat, W. 1999: The type section af the Vikingbgda Formation - a new Lower Triassic unit in Central and Eastern Svalbard. Polar Research I 8 (I), 51-82.

Nagy, J., L~faldli, M. & Backstrom, S.A. 1988: Aspects of foraminiferal distribution and depositional conditions in Middle Jurassic to Early Cretaceous shales in Eastern Spitsbergen. Abhand- lungen der Geologischen Bundesanstalt Wien 30,287-300.

Nemec, W., Steel, R.J., Gjelberg, J., Collinson, J.D., Prestholm, E. & Oxnevad, I.E. 1988: Anatomy of collapsed and re-established delta front in Lower Cretaceous of Eastern Spitsbergen: Gravitational sliding and sedimentation processes. American Association of Petroleum Geologists Bulletin 72 (4), 454-476.

Nemec, W., Steel, RJ., Gjelberg, J., Collinson, J.D., Prestholm, E., Oxnevad, LE. & Worsley, D. 1988:,Exhumed rotational slides and scar infill features in a Cretaceous delta front, eastern Spitsbergen. Polar Research 6 (I), 105- 1 12.

ObruEev, S. 1927: GeologiEeskij &erk vosmnogo poberet'ja Spic- bergena m& vllivami Ukjls-baj i Agard-bay. (Geologische Skizze der Ostkiiste von Spitzbergen zwischen den Busen Whales Bay und Agardh Bay.) PmvyEego Morskogo NauEnogo Znstituta (Berichte des Wusenschaftlichen Meeresinstihrtes), 2 (3), Moskva, 57-88.

PEelina, T.M. & KorCinskaja, M.V. 1973: Permskie i triasovye otloZenija central'noj i jugo-zapadnoj Easti ostrova i ostrova Nadeda. (Permian and Triassic deposits of the central and southwestern parts of Edgesya and Hopen.) Unpublished report, PW"Sevmorgeologijo", Leningrad. Report on fieldwork in 1971- 1972.92 pp.

PEelina, T.M. & Sokolov, V.N. 1967: Mezozojskie otloZenija vostoEnogo pobereZ6ja ostrova Zapadnyj Spicbergen v svjaZi S per- svektivami neftenazonosnosti. (Mesozoic de~osits of the east coast o? Spitsbergen G the context df petroleum potential.) Unpublished report, PG0 "Sevmorgeologija ", Leningrad. Report on fieldwork in 1966.286 pp.

PEelina, T.M. 1972: On the age of the sedimentary succession of the island of Hopen, Svalbard. Pp. 75-8 1 in: Sokolov, W. & Vasilevskaja, N.D. (eds.): Mezozojsk otlofenija Svalbarda. NIIGA, Leningrad. (In Russian.)

PEelina, T.M. 1977: Permskie i triasovye otloltenija ostrova g& (Sval'bard). (Permian and Triassic deposits on Edgewa, Svalbard.) Pp. 59-71 in: Stratigrafija i paleontologija dokembrija i paleozoja severa Sibiri. (Stratigraphy and palaeontology of the Precambrian and Palaeozoic of northern Siberia.) Sbornik nau8nych hcdov (Col- lection of scientific papers), NIIGA, Leningrad.

PEelina, T.M. et al. 1967: Mezozojskie otloZenija vostotnogo poberelt'ja Zap. gpicbergena v svjazi S perspektivami neftegazonosnosti (otEet otrjada No. 3 Spicbergenskoj ekspeditsii o rabotach 1966 g. (Mesozoic deposits of the eastern coast of Spitsbergen related to oil and gas prospecting: Report of party no. 3 of the Spitsbergen Exmt ion on studies carried out in 1966.) Unpublished report, P W "Sevmorgeologzja ", Leningrad.

Pickton, C.A.G., Harland, W.B., Hughes, N.F. & Smith, D.G. 1979: Mesozoic stratigraphy of Eastern Svalbard. A reply. Geological Mag- azine 116, 1,55-61.

Pompeckj, J.F. 1899: Marines Mesozoicum von Konig-Karls-Land: vorlaufiger Bericht. Kongl. Vet-Akad. Forhandlingar I899 (5). 449- 464.

Smelror, M. 1988: Bathonian to Early Oxfordian dinoflagellate cysts and acritarchs from Kong Karls Land, Svalbard. Review of Palaeob- otany and Palynology 56,275-304.

Smith, D.G. 1974: Late Triassic pollen and spores from the Kapp Toscana Formation, Hopen, Svalbard - A preliminary account. Re- view of Palaeobotany and Palynology 17, 175-178.

Smith, D.G. 1975: The stratigraphy of Wilhelmsya and Hellwaldfjellet, Svalbard. Geological Magazine 112 (5), 48 1-491.

Smith, D.G., Harland, W.B. & Hughes, N.F. 1975: The geology of Hopen, Svalbard. Geological Magazine 112 (l), 1-23.

Smith, D.G., Harland, W.B., Hughes, N.F. & Pickton, C.A.G. 1976: The geology of Kong Karls Land, Svalbard, Geological Magazine 113 (5), 193-304.

Tozer, E.T. 1973: Lower and Middle Triassic ammonoids and bivalves fromNordaustlandet (Spitsbergen) collected by Dr. Oskar Kulliig in 193 1. Geologiska Fiireningens i Stockholm Forhandlingar 95, 99- 104.

Tjnell, G.W. 1933: Stratigraphical observations in the Stor Fjord region of Spitsbergen. Tknsactions of the Royal Society of Edinburgh 57 p), 675-690.

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7. BIBLIOGRAPHY

Verdenius, J. G. 1978: A Valanginian calcareous nannofossil associa- Gjelsvik, T. 1989: A primitive alkali basalt stratovolcano and associ- tion from Kong Karls Land, Eastern Svalbard. Norsk Polarinstitutt ated erutive centres, northwestern Spitsbergen: Volcanology and tec- Arbok 1977,350-352. tonic significance. Journal of Volcanology and Geothermal Research

Worsley, D. & Heintz, N. 1977: The stratigraphical significance of a 37, 1-19. marine vertebrate fauna of Rhaetian age, Kong Karls Land Norsk Polarinstitutt h b o k 1976,69-81.

Worsley, D. 1973: The W~lhehwya Formation - a new lithostratigraphic unit from the Mesozoic of Eastern Svalbard. Norsk Polarinstitutt Maps (Fig

7 Quaternary eruptive centres

Abakumw, S.S., Kovaleva, G.A. & Teben'kov, A.M. 1984: Magmatizm gpicbergena. (Magmatism of Svalbard.) Unpublished report, PGO"Sevmorgeo1o~ja ", Leningrad. Project report, based on the data obtained in fieldwork in 1981-1984.305 pp.

Amundsen, H.E.F. 1987: Evidence for liquid immiscibility in the upper mantle. Natutz 327 (6124). 692495.

Amundsen, H.E.F., M m , W.L. & O'Reilly, S.Y. 1987: The lower crust and upper mantle beneath northwedtern Spitsbergen: evidence from xenoliths and geophysics. Tectonophjwics 139,169-1 85.

Amundsen, H.E.F., W m , W.L. & O'Reitly, S.Y. 1988: The nature of the lithosphere beneath northwestern Spitsbergen: xenolith evidence. NGU &ecial Publication 3,58-65.

Burov, Ju.F'. & MuraSov, L.G. 1964: Trachibasal'ty Bok-fiorda, nedif- ferencirovannye intruzii doleritov i permskie otlokenija jugo- zapadnogo pobere'ja Severo-Vostot%oj Zemli i s l a b differen- cirwannye intmzii o s t m B m c a . (Trachybasalts in Bockfjorden, undifferentiated dolerite intrusions and Permian deposits on the southwest coast of Nardawtlandet and poorly differentiated intrusions on Barentwya) Unpublished report, P W "Sevmorgeologija ", Leningrad. Report on fieldwork in 1963. 191 pp.

Burov, J U . & MuraSav, L.G. 1964: Tmhybasal'ty Bok-fiorda, nedif- ferencirovannye infruzii doleritw i pennskie otloknija jugo-zapadnogo poberek'ja Sevem-BosWnoj Zemli i slabo differencirovannye intruzii ostrova Barenca. (Trachybasalts in Bockfjorden, undifferentiated dolerite intrusions and Permian deposits on the southwestern coast of Nmdaustlandet and poorly poorly merentiated intrusions on Barentsnrya.) Unpublished report, P G 0 "Sevmorgeologija ", Leningrad 191 pp.

Burov, Ju.P. & Zagruzina, I.A. 1976: (Results of a determination of the absolute age of Cenozoic basic rocks of the northern part of the island of Spitsbergen.) In: Geologija Sval'barda, 139-140. NIIGA, Leningrad

E v d o k h , A.N., Germanov, E.V, Da%vskaja, D.M. & GenSaft, Ju.S. 1991 : Kajnozojskij magmatizm, g id ro tedna ja dejatel'nost' i per- spektivy rudonosnosti zony razlomov &anan-fiord -Vud-fiord, os- trov Zapadnyj Spicbergen. (Cenozoic magmatism, hydrothermal activity and ore potential of Ekmanfjorden and Woodfjorden fault zone, Spitsbergen.) Unpublished report, PG0 "Sevmorgeologija", Leningrad. Project report, 1989-1991. 186 pp.

Feden, R.H., Vogt, PR., Fleming, H.S. 1979: Magnetic and bathymet- ric evidence for the "yermak" hot spot northwest of Svalbard. Earth and Planetary Science Lettres 44, 18-38.

Gjelsvik, T. 1963: Remarks on the structure and composition of the Sverrefjellet volcano, Bockfjorden, Vestspitsbergen. Norsk Polar- institutt Arbok 1962,50-54.

Goldschmidt, W.M. 191 1: Petrographische Untersuchung einiger Erup- tivgesteine von Nordwestspitzbergen. Videnskaps Selskapets S h y e r I, MatematiskNaturvidenskapelig Klasse No 9, Ktistiania.

Halvorsen, E. 1972: A palwmagaetic study of two volcanic formations from northern Spitsbergen. Norsk Polarinstitutt I(rbok 1970,70-75.

Hoel, A. & Holtedahl, 0. 1911: Les nappes de lave, les volcans et les sources thermales dam les environs de la Baie Wood au Spitsberg. Videnskaps Selskupets Sh@r l , Matematisk-Naturvitdenskapelig Klasse No. 9. Kristiania.

Hoel, A. 1914: Nouvelles observations sur le district volcanique du Spitsberg du nord. Videnskaps Selskapets Skr@er 1, Matematisk- Naturvitdenskapelig Klasse No. 9. Ktistiania.

Kovaleva, G.A. & Burw, Ju.P 1981: Bazitovye kompleksy maozo- jsko-kajnozojskogo vozrasta severnoj Easti Barencevomorskoj pmvincii. (Mesozoic and Cenozoic complexes of basic rocks in the northern Barents Shelf.) Unpublished report, PW"Sevmorge- ologija ", Leningrad. Project report, 1979-1981. 147 pp.

Skjelkv&le, B.L., Amundsen, H.E.F., O'Reilly, S., Griffin, W.L. &

8.1 NP Overview msgl:l million

Winsnes, T.S. 1988: Bedrock map of Svalbard and Jan Mayen 1:1,000,000. Norsk Polarinstitutt Temakart No. 3. (with short description)

8.2 NP Regional maps 1:500,000

1G: Flood, B., Nagy, J. & Winsnes, T.S. 1971: Geological map of Sval- bard 1:500,000, sheet 1G Spitsbergen southem part. Norsk Polar- institutt S m e r I54 A. (with short description)

lG(new): Dallmann, W.K. (4.) 1993: Geological map of Svalbard 1:500,000, sheet 1G Spitsbergen southern part. Revised, preliminary edition (offset colour print). Norsk Polarinstitutt.

2G: Winsnes, T.S. & Worsley, D. 1981: Geological map of Svalbard 1:500,000, sheet 2G, Edgeraya. Norsk Polarinstitutt Shj?er 154 B. (with short description)

3G: Hjelle, A. & Lauritzen, 0. 1982: Geological map of Svalbard 1:500,000, sheet 3G, Spitsbergen northern part. Norsk Polarinstitutt S h y e r 154 C. (with short description)

4G: Lauritzen, 0. & Ohta, Y. 1984: Geological map of Svalbard 1:500,000, sheet 4G, Nordaustlandet. Norsk Polarinstitutt S h i e r I54 D. (with short description)

8.3 NP Detailed maps 1:100,000 to 1:50,000

(Publication status: May 1998, see Fig. 7-01 for maps in preparation i digital map data)

A4G: Ohta, Y., Hjelle, A. & Dallmann, W.K. (eds.): Geological map of Svalbard 1:100,000, sheet A4G Vasahalv~ya, prehinary edition, colour plot. Norsk Polarinstitutt.

A7G: Hjelle, A., Piepjohu, K., Saalmann, K., Ohta, Y., Thiedig, E, Salvigsen, 0. & Dallmann, W.K. 1999: Geological map of Svalbard 1 : 100,000, sheet A7G Kongsfjorden. Description in prep. Norsk Po- larinstitutt Temakart No. 30.

B8G. Bergh, S.G., Ohta, Y., Andresen, A., Maher, H.D., Braathen, A. & Dalhaun, W.K. 1993: Geological map of Svalbard 1 : 100,000, sheet B8G St.Jonsfjorden, preliminary edition, black-and-white. Norsk Polarinstitutt.

B9G: Ohta, Y., Hjelle, A., Andresen, A., Dallmann, W.K. & Salvigsen, 0. 199111992: Geological map of Svalbard 1:100,000, sheet B9G Is- fjorden. With description. Norsk Polarinstitutt Temakart No. 16.

BIOG: Hjelle, A. Lauritzen, PI., Salvigsen, 0. & Wmnes, T.S. 1986: Geological map of Svalbard 1:100,000, sheet BlOG Van Mijen- fjorden. With description. NorskPolarinstitutt Temakart No. 2.

B 11G: Dallmann, W. K., Hjelle, A., Ohta, Y., Salvigsen, O., Maher, H.D., Bjornerud, M., Hauser, E.C. & Craddock, C. 1990: Geological map of Svalbard 1 : 100,000, B l lG Van Keulenfjorden. W~th description. Norsk Polarinstitutt Temakart No. 15.

B12G: Ohta, Y. & Dallmann, W.K. (eds.) 1994: Geological map of Svalbard 1 : 100,000, sheet B12G Torellbreen, preliminary edition. Final edition in press, description in prep. Norsk Polarinstitutt.

C7G: Dallmann, WK., Ohta, I., Birjukov, A.S., Karnou%nko, E.P. & Sirotkin, A.N. 1994: Geological map of Svalbard 1:100,000, sheet C7G Dicksonfjorden, preliminary edition, colour plot. Norsk Polar- institutt.

C8G: Lauritzen, PI., Salvigsen, 0. & Winsnes, T.S. 1989: Geological map of Svalbard 1:100,000, sheet C8G Billefjorden. With description. Norsk Polarinstitutt Ternakurt No. 5.

C9G: Major, H. &. Nagy, J. 196411972: Geology of the Adventdalen map area. Norsk Polarinstitutt Skrifter 138, 1-58. (with map, published in 1964)

C9G(new): Major, H., Nagy, J., Haremo, F'., Dallmann, W.K.,Andresen, A. & Salvigsen, 0. 1992: Geological map of Svalbard 1:100,000, sheet C9G Adventdalen, preliminary edition, colour plot. (Revised after Major, H. & Nagy, J. 1964). NorskPolarinstitutt.

http://jurassic.ru

7. BIBLIOGRAPHY

ClOG: Salvigsen, 0. & Wmsnes, T.S. 1987: Geological map of Sval- bard 1:100,000, sheet ClOG Braganzavhgen. Description by Steel, RJ., Wmsnes, T.S. & Salvigsen. NorskPolarinstitutt Temakart No. 4.

Cl lG / C12G: Dallmann, W.K., Birkenmajer, K., Nagy, J. & Winsnes, T. 1994: Geological map of Svalbard 1:100,000, sheets Cl lG and C12G. Description by Dallmann, W.K., Nagy, J. & Salvigsen, 0. Norsk Polarinstitutt Temakart No. 22/23.

C12G: see C1 1G. C13G: DaUmann, W.K., Birkenmajer, K., Hjelle, A., M@rk,A., Ohta,Y.,

Salvigsen, 0. & Andresen, A. 1993: Geological map of Svalbard 1:100,000, sheet C13G Smkapp. Description by Winsnes, T.S., Birkenmajer, K., Dallmam, W.K., Hjelle, A. & Salvigsen, 0. Norsk Polarinstitutt Temakart No. 17.

D8G: Miloslavskij, M.Ju., Bijukw, A.S., Sl8nskij, S.N. & Dallmann, W.K. 1998: Geological map of Svalbard 1:100,000, sheet D8G Negribreen. Description by Miloslavskij, M.Ju., DaUmam, W.K. & Salvigsen, 0. Norsk Polarinstitutt Mukart No. 25.

D9G: Miloslavskij, M.Ju., Bijukov, AA., Slhki j , S.N., Hansen, S., Larsen, B.T., Dallmann, W.K. &Andresen, A. 1993: Geological map of Svalbard 1:100,000, sheet DQG A g a e l l e t . Description by Miloslavskij, M.Ju., Dallmann, W.K., Dypvik, H., Krasil'gl!ikov, A.A., Birkeland, 0. & Salvigsen, 0. Norsk PoImMnstitutt Temakart No. 21.

D20G. D a l h , W.D. & Krasil'SEikov, AA.. (eds.) 1996: Geological map of Svalbard 1:50,000, sheet D20G Bjmmya. Norsk Polarinsti- tutt Temakart No. 27. (Description in prep.)

8.4 Mapspublished by others than the Norwegian Polar Institute:

Biienmajer, K. 1990: Geology of the Hornsund area, Spitsbeeen, Ex- planations to the map 1:75,000 scale. Silesian University, Polish Academy of Sciences, 42 pp., 1 map.

Horn, G. & M u , A.K. 1928: Geology of Bear Island. Srbifter om Svalbani og Ishavet 15, 1 - 1 52.

Sigmond, E.M.O. (ed.) 1992: Berggrunnskart, Norge med havomrdder (Bedrockmap, Norioay and adjacent ocean areas). Scale 1:3 million. Norges geologiske undersnrkelse.

9 Barents Sea

Gabrielsen, RH., Fierseth, RB., Jensen, L.N., Kalheim, J.E. & Riis, E 1990: Structural elements of the Norwegian continental shelf. Part I: The Bmuts Sea region. Norwegian Petroleum Directomte Bulletin 6,33pp, 16 pls.

Gading, M. 1993: Triassic evolution in the Barents Sea, Norwegian and Russian Sectors, a seismic and sequence stratigmphic approach. Dr. ing. thesis. NTH, University in Zbndheim, 235 pp.

Gramberg, LS., Aleein, S.V, Armisw, A.M., Baturin, D.G., Borisov, A.% Bro, E.G., Verba, W, Vinogradov, A.V, Volk, YE., GureviC, W., Daraga-Susova, LA., Z d e v , VA., Zaidze, VS., Ivanw, N.M., Kaww, N.I., ~ i ~ i k o v , A.A., LiHic, Ju.Ja., Malovickij, Ja.P., MMotiua, G.P., OstisQj, B.K., PreobraZenskaja, E.N., PEelina, T.M., Rouba, Z.Z., Seain, B.V, Cilev, Wt., SopelkeviC, Ju.Y, Sipolw, E.V, Junov, A.Ju & Jasin, D.S. 1988: Barentsevskaja Selfo- vavaja plita (Bmwrts SheEfPlate). V N I I O ~ e o l o g i j a Trudy 196, 263 pp.

Grogan, l?, 0stvedt-W, A.-M., Larseen, G.B., Fotland, B., Nyberg, K., Dahlgm, S. & Eibrin, T. 1988: Structural Elements and Petro- leum Geology of the Norwegian Sector of the Northern B m t s Sea. In Fleet & Boldy (eds.): Pmceedings of We 5th C o n a ~ n c e on the Petroleum Geology of Northwest h p e . Geological Society of London Kelly, S.R.A., 1988: Jurassic through Crehxous stratigraphy of the Barents Shelf. Pp. 109-130 in Harland, W.B. and Dowdeswell, BK. (eds.), Geological evolution of the Barents Shelf Region, Graham & Trotman Ltd., London,.

Nilsson, I., Mangerud, G. &Mark, A. 1996: Permian stratigraphy of the Svalis Dome, southwestern Barents Sea. Norsk Geologisk l ldshj l 76, 127-146.

Smelror, M. 1994: Jurassic stratigraphy of the Western Barents Sea Region: a review. Geobios, M.S. 17,441-45 1.

Smelror, M., Mi&,A., Monteil, E., Rutledge, D. & Leereveld, H. 1998: The Klippfisk Formation - a new lithostratigraphic unit of Lower Cretaceous platform carbonates on the Western Barents Shelf. Polar Research 17 (2), 181 -202.

Vigran, J.O., Mangerud, G., Wk, A., Bngge, T. &-Weitschat, W. 1998: Biostratigraphy and sequence d g r a p h y of the Lower and Middle Triassic deposits from the S d i s Dome, Central Barents Sea, Nor- way. Palynology 22,89-141. ,

Worsley, D., Johmsen, R & Kristensen, S.E. 1988: The Mesozoic and Cenozoic sumssion of Tro-t. Pp. 42-65 in Dalland, A., Worsley, D. &G Ofstad, K (eds.), A lithosn~ltigmphic schemefor the Mesozoic and Cenoroic succession offshom mid- and northern Norway. Norwegian Petroleum Di~ectomte Bulletin, 4. -

http://jurassic.ru

7. BIBLIOGRAPHY

rLBARD GEOLOGICAL MAPS, statu- d1 .O1 .l 999 Norsk Polarinstitutt

'I printed in colour preliminary edition

l,,,,, , , , $ l l preliminary edition scale 1 :500,000 (revised from older printed map) scale 1 :l ,OOO,oOO fax+477775050

l map in preparation X digital map data available

1- Fig. 7-01: Bedrock map series of Svalbard, Norwegian Polar Institute: Map index and publication status.

http://jurassic.ru

Aakvik, R. 1981: Facies analyse av undre karbonske kullj0rende sedi- mentec BilleJorden, Spitsbergen. Unpublished thesis, University of Bergen. 1-219.

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hhus, N., Kelly, S.RA., Collins, J.S.H. & Sandy, M. R 1990: Sys- tematic palaeontoloy and biostratigraphy of two Lower Cretaceous condensed sections from the Barents Sea. Polar Research 8 (2), 165- 194.

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Atkinson, D. 1956: The occurence of chloritoid in the Hecla Hoek formation of Prince Charles Foreland, Spitsbergen. Geological Maga- zine 93 (I).

Atkinson, D.J. 1962: Tectonic control of sedimentation and the interpretation of sediment alternation in the Tertiary of Prins Karls For- land, Spitsbergen. Geological Society ofAmerica, Bulletin 73, 343- 364.

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Bickstrcim, S.A. & Nagy, J. 1985: Depositional history and fauna of a Jurassic phosphorite conglomerate (the Brentskardhaugen Bed) in Spitsbergen. Norsk Polarinstitutt S h y e r 183, 1-61.

Barbaroux, L. 1967: Les formations 'D6tritiques-~orallig&nes' Car- bonieres de la Presqu'fle de Bmgger (Baie du Roi - Vestspits- bergen). Bulletin SociJti Gkologique de Fmnce (7. serie) 9,714-722.

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Birkenmajer, K 1964: Devonian, Carboniferous and Pennian formations of Homund, Vestspitsbergen. Studia Geologica Polonica 11, 47-123.

Birkenmajer, K. 1972a: Megaripples and phosphorite pebbles in the Rhaeto-Liassic beds south of Van Keuledjorden, Spitsbergen. Norsk Polarinstitutt ldrbok 1970, 117-127.

Birkenmajer, K. 1972b: Tertiary history of Spitsbergen and continental drift. Acta Geologica Polonica 22 (2), 193-218.

Birkenmajer, K. 1975: Jurassic and Lower Cretaceous sedimentary formations of SW Torell Land, Spitsbergen. Studia Geologica Polonica 44,743.

Birkenmajer, K. 1977: Triassic sedimentary formations of the Hom- sund area, Spitsbergen. Studia Geologica Polonica 51, 1-74.

Birkenmajer, K. 1978: Ordovician succession in south Spitsbergen. Studia Geolonica Polonica 59,47-82.

Birkenmajer, K. 1979a: Paleotransport and source of Early Carbonifer- ous fresh-water clastics of South Spitsbergen. Studia Geologica Polonica 60, 3943.

Birkenmajer, K. 1979b: Channelling and orientation of Rugose corals in shallow-marine Lower Pennian of south Spitsbergen. Studia Geo- logica PoIonica 60,4546.

Birkenmajer, K 1980: Jurassic-Lower Cretaceous succession of Agard- hbukta, East Spitsbergen. Studia Geol. Polon. 66.

Birkenmajer, K. 1981: The geology of Svalbard, the western part of the Barents Sea, and the continental margin of Scandinavia. In Nairn, A.E.M., Churkin, M. & Stehli, F.G. (eh.): The ocean basins and mam'ns, vol. 5: The Arctic Ocean. Plenum Press, New Yorknondon. 265-329.

Birkenmajer, K 1984a: Mid-carboniferous red beds at Homsund, south Spitsbergen: Their sedimentary environment and source area. Stzrdia Geologica Polonica 847-23.

Birkemjer, K. 1984b: Cyclic sedimentation in mixed alluvial to marginal-marine conditions: The Wkelodden Formation (?Upper Car- boniferous and Lower Permian) at Hornsun4 south Spitsbergen. Stu- dia Geologica Polonica 80,25-46.

Birkenmajer, K. 199 1: The Jarlsbergian unconformity (Proterozoic/ Carnbrian boundary) and the problem of Varangian tillites in South Spitsbergen. Polish Polar Research I2 (3), 269-278

Birkenmajer, K. & Czamiecki, S. 1960: Stratigraphy of marine Car- boniferous and Permian deposits in Homund (Vestspitsbergen), based on brachiopods. Bulletin of the Polish Academy of Sciences, Earth Sciences 8 (3), 203-209.

Birkenmajer, K. & Logan, A. 1969: On the fauna and age of the Can- crinella Limestone (Permian) at Kopernikusfjellet, Vestspitsbergen. Norsk Polarinstitutt Arbok 1967,2845.

Birkenmajer, K. & Pugaczewska, H. 1975: Jurassic and Lower Creta- ceous marine fauna of SW Torell Land, West Spitsbergen. Studia Geologica Polonica 44,45-92.

Birkenmajer, K & Turnau E. 1962: Lower Carboniferous age of the so-called Wijde Bay Series in Homsund, Vestspitsbergen. Norsk Polarinstitutt ldrbok 1961,41-6 1.

Birkenmajer, K & Wienbowski, A. 1991: New Kimmeridgian ammonite fauna from East Spitsbergen and its phyletic significance. Polar Research 9 (2), 169-179.

Birkenmajer, K, Pugaczewska, H. & Wierzbowski, A. 1982: The Janusfjellet Formation (Jurassic-Lower Cretaceous) at Myklegard- fjellet, east Spitsbergen. Palaeontologica Polonica 43, 107-140.

Bj~rke, T. 1977: Mesozoic palynology of Svalbard 11. Palynomorphs from the Mesozoic sequence of Kong Karls Land. Norsk Polarinsti- tutt Arbok 1976,83-120.

Bjsxke, T. 1978: Mesozoic palynology of Svalbard 111. Dinoflagellates frmn the Ruriktjellet Member, Janusfjellet Formation (Lower Creta- ceous) of Spitsbergen. Palynol. Nun. Extmord. I, 69-93.

Bjierke, T. & Dypvik, H. 1977: Sedimentological and palynological studies of Upper %assic - Lower Jurassic sediments in Sassen- fjorden, Spitsbergen. Norsk Polarinstitutt Arbok 1976, 131-150.

Bjornerud, M.G. 1990: Upper Proterozoic unconformity in northern Wedel Jarlsberg Land, southwest Spitsbergen: Lithostratigraphy and tectonic implications. Polar Research 8,127-140.

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Steel, R.J., Gjelberg, J., Helland-Hansen, W, Kleinspehn, K, NsMredt, A. & Rye Larsen, M. 1985: The Tertiary strike-slip basins and orogenic belt of Spitsbergen. Society of Economic Paleontologists and Minemlogists, Special Publication 37,339-360.

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REFERENCES

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Worsley, D. & Mmk, A. 1978: The Triassic stratigraphy of southern Spitsbergen. Norsk Polarinstitutt ldrbok 1977,43-60.

Worsley, D., Johansen, R. & Kristensen, S.E. 1988: The Mesozoic and Cenozoic succession of Tromserflaket. F'p. 42-65 in Dalland, A., Wonley, D. & Ofstad, K. (eds.), A lithostratigmphic scheme for the Mesozoic and Cenozoic succession offshore mid- and northern Nor- way. Norwegian Petroleum Directomte Bulletin, 4.

Worsley, D., Agdestein, T., Gjelberg, J., Kirkemo, K., Mmk, A. Olaussen, O., Steel, RJ. & Stemme& L. in press: Late Paleozoic basinal evolution of Bjsmsya, Svalbard, Norway: Implications for the Barents Shelf. Submitted to Norsk Geologisk Ztdsslarji.,

Ytreland, G.K. 1980: Sedimentation along the western margin of the Cenhal Tertiay Basin (Firkanten Formation), Spitsbergen. Unpub- lished cand. real. thesis, University of Bergen. 1-183.

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INDEX FOR STRATIGRAPHIC UNITS CONTAINED IN THIS VOLUME

rage numbers refer to: Bold: Def i t ion Regular: Scheme Italics: Illustration

The Russian stratigr~phic rank 'svita ' is here tmnslated with Yormation '

Aberdeenflya Formation, 252,2 17 Adriabukta Formation, 48,32-33,49, 50 Adventdalen Group, 184, 134-135,178, 185-206 Adventfjorden Beds (A. Schichten), 261 Agardhtjellet Formation, 185, 134-135,178, 185, I86 Akkar Member, 182,134135 Alfredfjellet Formation, 124 Alge Member, 195,134-135 Ambigua limestone, 126 Anasiberites horizon, 213 Anhydrite member, 126 Anservika Beds (Member), 124 Arctoceras-Schichten (A. Horizont), 213 Argillite unit, 213 Arnesenodden Shale Be4 210 Askeladden Delta Sequence, 261 Aspelintoppen Formation, 238,217,224,238 Aucellenschichten (A. Shale), 213 Austjnrkelen Forzbtion, 210 Balanuspynten conglomerates, 2 56,2 17 Barentsburg Formation, 261 Barentssya Formation, 210 Basal Bed, 213 Basal member, 213 Basilika Formation, 230,217,224 Battfjellet Formation, 237,217,224,234 Bayelva Member, 246,217 Berzeliusdalen Member, 261 Billefjorden Group, 41,32-33,41, 53 Birger Johnsonfjellet Member, 45,32-33 Bjarmeland Group, 112,32-33 Bjmbogen Formation, 210 Bjmbogen Horizon, 210 Bjmbogen Member, 210 Bjmonfjellet Member, 235,217 Black Crag Beds, 88,32-33, 68 Black shales and yellow flags, 213 Bladegga member (Formation), 81,32-33 Blanknuten Member, 161, 134-135,160, 161, 164 Blue and purple shales, 213 Bockfjorden VoIcanic Complex, 264,217,265, 266 Bogen Be4 210 Bogevika Member, 105,32-33,105 Botneheia Formation (Member), 160, 134-135,144, 152,

161, 164 Botneheia Horizon, 210 Bottom shale, 213 Brachiopod cherts, 126 Brachiopod Cherty Limestone, 126

Brachiopod formation, 126 Brattberget member, 81,32-33, 79, 81 Bravaisberget Formation, 156, 134135,144, 145,156,158 Brentskardhaugen Be4 180, 134-135,180, 181 Brentskardhaugen Member, 210 Brevassfjellet Be4 148,134-135,148 Brevassfjellet Myalina Be4 210 Brnrggerbreen Formation, 245,2 17 Braggertinden Formation, 72, 32-33, 72 Brucebyen Beds, 91,32-33 Buchananisen Group, 247,2 17 Biinsowbukta Member, 190, 134- 135 Cadellfjellet Member, 87, 32-33, 84, 88 Calciferous Sandstone Series, 126 Calypsostranda Group, 258,217,258 Camp Morton Member, 261 Campbellryggen Subgroup (Limestones), 60,32-33,42, 60-71 Cancrinella limestone, 126 Carbonate Member, 126 Carolinefjellet Formation, 203, 134-135,203, 206 Carronelva member (Beds), 69,32-33,68 Charlesbreen Subgroup (Group), 71, 32-33, 72, 73,77 Claraia Zone, 213 Colesbukta Formation, 261 Collinderodden Formation, 261 Continental series, 213 Cora limestone, 126 Cretaceous shale, 213 Culm sandstones, l26 Cyathophyllum limestones, 126 Dalkjegla Member (Formation), 205, 134-135,203 Daonellenkalk (D. schichten, D.-Niveau), 213 De Geerdalen Formation, 165, 134-135,164, 166 Deltadalen Member, 153, 134-135, I53 Dentalienschichten, 213 Diabasodden Suite, 209,201 Dickson Land Subgroup, 84,32-33,59, 84, 88, 94, 96 Ditrupa-Schichten (D. shale series), 213 Drevbreen beds, 124 Drevbreen Formation, 210 Drmbreen Be4 210 DunCrfjellet Shale Member, 211 Ebbabreen sandstone beds, 124 Ebbabreen shale beds, 124 EbbadalenFormation, 62,32-33,42, 60, 63, 65, 66, 67, 68 Ebbaelva Member, 65,32-33,60, 61, 65 Edgesya Formation, 211 Efuglvika Member, 105, 32-33 Elatides-Schichten (E. Niveau), 213 Elsabreen (conglomerate) beds, 124

160, Endalen Member, 228,217, 224,226,229 Escarpment shales, 213 Eutomoceras-Teilzone, 213 Evaporite series, 126 Fardalen Beds (F. Schichten), 261 Ferrieaellet Breccia, l24

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Festningen sandstone member, 199, 134-135,194, 198, 200 Festungssandstein - see Festningen sandstone member Finlayfjellet Beds, 92, 32-33 Firkanten Formation, 225,217,224,226,229 Fisch-Niveau, 213 Fissile sandstone series, 262 Flaggy Sandstone Series, 262 Flatsalen Formation, 174,134-135 Forlandsundet Group, 262 Fortet Breccia, 124 Fortet member, 71,32-33, 68, 71 Fosse Sandstein, 213 Fruholmen Formation, 182, 134-135 Frysjaodden Formation, 232,217,224,234,235 Fugle Subformation, 124 Fuglen Formation, 195, 134-135 Fusulina limestone, 126 Gerritbreen beds, 89, 32-33 Gerritelva sandstone Member, 124 Gilsonryggen Member (Formation), 234,217,224,234,235 Ginkgo-Schichten (G. Niveau), 214 Gipsdalen Group, 59,32-33,59-111 Gipshuken Formation, 94,32-33,59, 94, 96 Glitrefjellet Member, 211 Green Sandstone, 262 Green sandstone formation, 262 Green Sandstone Member, 262 Green sandstone series, 262 Grey Sandstone, 262 Grey Sandstone Member, 262 Grippia-Niveau, 214 Grmfjorden Be4 226,217,226 Grumant Formation, 262 Grumantbyen Formation, 231,217,224 Grumantdalen Beds (F. Schichten), 262 Gry tvh Be4 124 Gymnotoceras-Teilzone, 214 Gypsum beds, 126 Gypsum member, 126 Hahnfjella Formation, 211 Hahuljella Horizon, 211 Haitanna Member, 49,32-33,49 Halobia limestone, 214 Halobia shales, 214 Halobia zitteli be4 214 Halvdanpiggen Eruptive Centre, 265,266 Hambergfjellet Formation, 114,32-33 Hhbardbreen Formation, 102,32-33 Hiirfagrehaugen Member, 200,134-135,201 Hiirfagrehaugen Sandstone Member, 211 Havert Formation, 162, 134-135 Heimfjella beds, 211 Hekkingen Formation, 195, 134-1 35 Hellwaldfjellet Be4 177, 134-135 Helvetiafjellet Formation, 198, 134-135, 178, 194, 198, 200,

201 Hieroglyphic series, 214 Hjelmen member, 80,32-33, 79, 80 HoeIbreen Member, 44, 32-33,41 Hsgsletta Member, 192, 134-135 Hollendardalen Formation, 236,217 Hsrbyebreen Formation, 41,32-33,41, 42, 43 Holarmndneset Formation (Beds), 50,32-33, 79 Hovtinden member, 117,32-33

Hultberget Fonnation, 61, 32-33, 41, 54 60, 61 Hustediakalk, 214 Hyrnefjellet Formation (Beds; B-R), 79,32-33, 79,

80, 81 Hyrnefjellet Formation (P~ELJNA,), 211 Idunfjellet Member, 93,32-33 Ingebrigtsenbukta member, 187, 134- 135 Ingnydjupet Subgroup (Group), 162, 134-135 Innkjegla Member, 205, 134-135,203, 206 Isfjorden Member (Formation), 167, 134-135 Iskletten Member, 150, 134-135 Iversenfjellet Formation, 211 Janusfjellet Subgroup (Formation), 185,134-135,178, 185,

186,193,194 Johnsenberget Sandstone Member, 211 Jotunfonna beds, 125 Julbmrgda Member, 49,32-33,50 Jutulslottet member, 77, 32-33, 77 Kaosfjellet Member, 151, 134-135 Kapitol Member, 85,32-33 Kapp D M h Formation, 111,32-33,111 Kapp Fanshawe Formation, 125 Kapp Hanna Formation, 109,32-33,109 Kapp Harry Member, 58,32-33 Kapp W e Formation, 104, 32-33,105 Kapp Koburg Formation, 211 Kapp Levin Member, 55,32-33 Kapp Starostin Formation, 115,32-33,59, 94, I16 Kapp Toscana Group, 163, 134-135,164-181 Kapp Ziehen unit, 125 kentoppen Member, 158,134-135,158 Keilhauijellet member (Formation), 171, 134-1 35 Keisarkampen Member, 179,134-135 Kkerfjellet Beds, 92,32-33 Kikutodden Member, 211 Kistefjellet Member (Formation), 148,134-135,148 Klappmyss Formation, 163, 134-135 Klippfisk Formation, 196,134-135 Kloten member, 97,32-33 Knorringijellet Formation (Member), 172,134-135,172. 180 Knortodden Be4 125 Knurr Formation, l%, 134-135 Kobbe Formation, 163,134-135 Kobbebukta Formation, 125 Kobbebukta Member, 188,32-33 Kolfjellet Member, 262 Kolhaugen Member, 241,2 17 Kolje Formation, 197,134-135 Kolmule Formation, 208, 134- 135 Kolthotlberget Member, 228,2 17 Kong k l s h d Flows, 201, 134-135,203 Kong k b Land Formation, 211 Kongressfjellet Subgroup (Formation), 211 Kongsfjorden Formation, 240,217,240,242,244 Kongsqa Formation (revised), 178,134-135,178 Kongssya Formation (S- et al.), 211 Konussen Formation, 211 Krabbe Member, 183, 134-135 Krill Member, 196, 134-1 35 Krokodillen Formation, 250,2 17 Kiikenthalfjellet Sandstone Member, 211 Kutling Member, 197, 134-1 35 Kvalv4gen Formation, 211 Kveite Formation, 208, 134-135

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Kviting Formation, 209,134-135 Laksvatnet Formation, 125 Lankdingsvika Formation, 103,32-33, 103 Langstakken Member, 206, 134-135,203, 206 Lardyfjellet Member, 189, 134-135 Leirhaugen Member, 245,2 17 Lias conglomerate, 214 Light Sandstone, 262 Limestone A, 126 Limestone B, 126 Lindstroemi-Horizont, 214 Lingula Sandstein, 214 Lioplaxschichten, 214 Lower argillite formation, 262 Lower black shale formation, 262 Lower black shale series, 262 Lower Coal Horizon, 263 Lower coal-bearing sandstone formation, 263 Lower Continental Series, 214 Lower Dark Shale Series, 263 Lower Dolomite member, 126 Lower Gypsiferous series, 126 Lower Gypsum zone, 126 Lower lamina sandstones, 214 Lower light sandstone series, 263 Lower Posidonia (Posidonomya) shales, 214 Lower Redbed Facies, 126 Lower sandstone series, 263 Lower transitional formation, 263 Lowest nodule beds, 214 Lusitaniadalen Member, 153, 134- 135 Lyngefjellet Formation, 211 Malte Bnmfjellet.Formation, 100, 32-33,100 Marchaise Formation, 262 Marchaislaguna Formation, 252,217 Margaretha Conglomerate Facies, 125 Marbgda Bed, 181,134-135,181 Mwstranderbreen Member, 234,217 Mathewbreen beds, 89,32-33 Mathiasbreen member, 171, 134-135 McVitie Formation, 262 McVitiepynten Formation, 262 Mendelejevbreen Member, 262 Meranfjellet Member, 50,32-33 Middle shale series, 263 Mmkinfjellet Formation (Member), 67,32-33,42, 60, 68, 71 Misery Subformation, 125 Miseryfjellet Formation, 123, 32-33, 123, 154 M o W g d a Member, 177, 134-135,178 Mohnhragda Sandstone Member, 211 Mmbekken Be4 244,2 17,244 Mmebreen Member, 85,32-33 Mumien Formation, 44,32-33,41, 42 Myalinaskifer (M. Niveau, M. beds), 214 Myklegardfjellet Be4 193, 134-135,193 Myophoria-Sandstein, 214 Nathomtites-Niveau, 214 Negerfjellet Formation, 211 Nordaustpynten Shale Member, 211 Nordenskioldbreen Formation, 125 Nordenskioldfjellet Beds (N. Schichten), 262 Nordhamna Member, 22,32-33 Nordkapp Formation, 56,32-33 Nordmela Formation, 184,134-135

Nordvestbanken Group, 212 Ny-mesund Subgroup (Formation), 238,217,240, 242, 244 Nygrunnen Group, 208, 134-135 Oberes Saurierniveau, 214 Odellfjellet Member, 66, 32-33,42, 60, 66 Oil shale member (0. sh. series), 214 Oozy mound beds, 214 Oppdalen Member, 188, 134- 135 Oppdalssita Member, 189, 134-135 Orustdalen Formation, 46,32-33,46 Palanderbukta, 119, 32-33 Passage beds, 126 Passage unit, 214 Passet Clay Member, 212 Passhatten Member, 157, 134-135,144, 156 Petrellskaret Formation, 74, 32-33, 72 Petrelskardet Shale Formation, 125 Pitnerodden Formation, 212 Pityophyllurn-Schichten (E!-Niveau), 214 Plateau flags, 214 Polakkfjellet Be4 188, 134-135 Posidonomyenkalk (P.schichten), 214 Productus-bearing limestones and cherts, 126 Pseudomonotiskalk, 214 Pseudomonotisskifer, 2 14 Ptychites beds, 214 Pyefjellet beds, 88, 32-33 Pyrarnidenbeds, 125 -den conglomerates, 125 Ragnarbreen Breccia, 125 Realgrunnen Subgroup (Group), 182, 134-135 Red conglomerate, 126 Reinhardpynten Formation, 249,2 17 Reinodden Formation, 125 Reke Member, 183, 134-135 Renaidodden Formation, 260,217 Retziakalk, 214 Retziusfiellet Shale Member, 212 Revtanna member, ll8,32-33 Rifleodden Conglomerate Be4 125 Rsedvh Formatio~~, 52,32-33,53, 123 Rurikfjellet Formation, 192,134-135,185, 193, 194 Rurikfjellet Horizon, 212 San- beds, 122,32-33 Sandsteinreihe, 214 Sandstone and shale series, 214 Sandstone unit, 214 Sarkofagen Formation, 262 Sars Formation, 262 Sarsbukta conglomerate, 256,217 Sarstangen conglomerate, 257,217 Sassendalen Group, 144, 134-135, 79, 144-164 Saurian be4 214 Scheteligfjellet Formation (Member), 73,32-33, 73 Schonrockfjellet member, 207, 134-135,206 Seidfjellet Formation, 260,2 17,260 Selander Formation, 125 Selanderneset member, 119, 32-33 Selmaneset member, 146, 134-135 Selvilgen Formation, 247,2 17 Sergeijevfjellet Formation (Beds), 51,32-33 Sessbgda Formation, 248,217 Shaley green sandstone formation, 263 Shore sandstone, 214

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Sigurdfjellet Eruptive Centre, 266 Shaken member, 147, 134-135 Singerfjella Formation, 212 Singerfjella Horizon, 212 Sjagrenfjellet Member, 177, 134-135,177 Sjogrenfjellet Sandstone Member, 212 Skansdalen member, 98,32-33,94 Skilisen Be4 151, 134-135 Skilvika Formation, 258,217,258 Skrekk Subformation, 125 Skuld Formation, 168, 134-135,123, 154 Slottet Bed, 169, 134-135,170 Slottsnwya Member, 190, 134-135 Smalegga Formation (Member), 170, 134-135,170 Snadd Formation, 168, 134-135 Somovbreen Member, 158, 134-135,144, 156 Sanfonna member, 98, 32-33 Smkapp Formation, 212 Spirifer limestone (ANDERSSON), 126 Spirifer limestone (NORDENSKIOLD), 126 Sporehsgda Member, 45,32-33 Starostin Formation, 125 Steinkobbe Formation, 161, 134-135 Stensiofjellet member, 118,32-33 Sticky Keep Formation (Member), 212 Star Formation, 184, 134-135 Storbreen Subgroup, 212 Storfjorden Subgroup, 164, 134135,164, 166 Storvola Formation, 262 Siisswasserschichten mit Lioplax - see Lioplaxschichten* Sutor conglomerate, 262 Sutorfjella conglomerate (member), 261 Svenbreen Formation, 125 Svenskeegga member, 117,32-33 Svensluaya Formation (revised), 175, 134-1 35, 175, 177, 178 Svensksya Formation ( S m et al.), 212 Sverrefjellet Volcano, 265,265 Sylodden Formation, 212 Thkanten (Sandstone) Formation, 75,32-33, 72, 77 Taxodium shale, 263 Teistberget member (Formation), 173, 134-135 Teistengrunnen Group, 212 Teltfjellet Member, 125 Teltvika Be4 126 Tempelfjorden Group, 115,32-33,59, 94, 116, 123, 154 Templet member, 98,32-33, 94 Terrierfjellet member, 70,32-33, 60, 68 ~irolarpasset member, 187, 134-1 35 Todalen Member, 226,217,226 Tokrossaya Beds, Lower and Upper, 126 Tokrossaya Formation, 121,32-33 Tordenskjoldberget Limestone Member, 212 Tordenskjoldberget Member, 197, 134-1 35 Torell Land Group, 212 Transitional beds, 214 Transitional member, 214 Treskelen Subgroup, 78, 32-33, 79-83 Trehlodden Formation (Beds), 82,32-33, 79, 83 Trikolortjellet Member, 67, 32-33, 60, 63, 67 Triungen Member, 43,32-33,41, 43 Trygghamna Formation, 126 Tscherrnakfjellet Formation, 165, 134-135,164 Mden Formation, 183, 134-135 lidingodden Formation, 213 Tumlingodden Horizon, 213

Tumlingodden Member, 213 Tunheim Member, 56,32-33 Tunheim Subformation, 126 Tverrbekken member, 172,134- 135 Tvillingodden Formation (MPIRK), 149,134 135,144,145,

148 Tvillingodden Formation (PEELINA,), 213 Tvillingvann Member, 262 Tvilbgvatnet Member, 241,217,242,244 Tyrrellfjellet Member, 90,32-33,84 Uleneset Member, 213 Ullaberget Member, 194, 134-135,194 Unteres Saurierniveau, 214 Upper argillite formation, 263 Upper black shale formation, 263 Upper black shale series, 263 Upper coal-bearing sandstone formation, 263 Upper coal-bearing series, 263 Upper Continental Series, 214 Upper Gypsiferous series, 126 Upper Gypsum Zone, 126 Upper lamina sandstones, 214 Upper nodule beds, 214 Upper Plant-Bearing Sandstone Series, 263 Upper Posidonia (Posidononya) shales, 214 Upper Redbed Facies, 126 Upper sandstone formation, 263 Upper sandstone series, 263 Upper shaley sandstone formation, 263 Upper transitional formation, 263 Urd Formation, 154,134-135,123, 154 Urmstonfjellet Limestone Bed, 126 Urnetoppen member, 147,134-1 35 Ursa sandstone, 126 Van Keulenfjorden Member (Formation), 159,134-135 Van Mijenfjorden Group, 224,217,224-244 V ~ d ~ b a Formation, 145, 134-135,144,145,146,148 VardebuktaHorizon, 213 ' .- - Vegard Formation, 126,32-33 3?::.;: 3- . Vegardfjella Formation, 46 -2. - .I(.

Vendomdalen Member, 154, 134-135 ( ,

Vengeberget member, 95,32-33,94,96 Verdande Be4 155, 134-135 Vesalstranda Member, 55,32-33 Vikin&gda Formation, 152, 1341 35,144, 152, 153, I64 Vmingen Member, 117,32-33 Vrakbukta Bed, 179, 134-135 Wibebreen member, 147,134- 135 Wichebukta Formation, 213 Wichebukta Horizon, 213 Wilhelmsya Subgroup (Formation, Member), 169,134-1 35,

170-181 Wimanfjellet Member, 193, 134-135 Wordiekammen Formation (limestones), 84,32-33,41, 42, 59,

60, 68, 84, 88 Yellow sandstone, 126 Ymerbukta Formation, 213 Zeipelodden member, 96, 32-33 Zillerberget member, 206, 134-135,203, 206

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APPENDIX 1 : Biostratigraphic tables

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APPENDIX 1

j SNADD /

-

2: From Hochuli et al. 1989: Svalbard - Barents Sea Solid lithostratigraphic boundaries are biostratigraphlcalh/ dated 3: From MBrk et al. In press: Vildnghprgda Formation Broken lithostratigraphic boundaries are Inferred 4: From Merrk et al. 1990: BjWnsya 5: From Vigran et al. In press: Svalls Dome

Previous page: Above: Fig. A-1: Biostratigraphic correlation scheme of the late Palaeozoic of Fig. A-2: Biozones of the Mesozoic of Svalbard; Sassendalen Group.

Svalbard. References to biozones: Cutbill & Challinor 1965; Compiled by Atle Msrk. Mange~d & Konieczny 1993; Nakamuca et al. 1987; Nakrem et al. 1992; Nilsson 1988, 1993; Nilsson & Davydov 1992; Sosipatrova 1967; Swift & Al&ridge 1985; Vigran 1991 @em. comm.), 1994 (unpubl.). Compiled by David Worsley and Inger Nilsson.

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APPENDIX 1

VENSKOYA Formation

I I - -

\ \ Compiled by Atle Mark 8 Morten Smelror 1998 \\ b r t y da td Triasslc ammonold zonatlon from Dagys & Weitschat 1993

Bold Triassic arnrnonoid zones are confirmed in Svalbard

Remanle fauna Jurasslc ammonoid zonation compiled from Koplk & Wierzbowski 1988, Smelror 1994 and Kelly in Harland et al. 1997

Solld llthostratigraphic boundaries Jurasslc patynozones from Smelror & Below 1993 are biostratlgraphlcalty dated Palynozones A-K from Hochull et al. 1989

Palynozones S,-S, from Vlgran et al. In press

Fig.A-3: Biozones of the Mesozoic of Svalbard; Kapp Toscana Group. Compiled by Atle Merk.

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APPENDIX 1

Lithostratigraphy Barents Sea Oinoflagellatw Sve'bard Bjarmeland -. .. Hsrnrnerfest - .

Biostratigraphic compilation modified from Kelly in Harland et al. 1997 Complled by Atle Mark & Morten Smelror 1998 (Foraminifera zonation originally from Nagy et al. 1990, Solid l~dlgraphicaI boundaries are Jurassic dinocyst zones from Smelror & Below 1993 and biistratigraphlcally dated Cretaceous dinocyst zonation from Grtasfjeld .fQg2. The Kimmeridgian ammonite zonation is from Wietzbowski & Smelror 1993).

Fig. A-4: Biozones of the Mesozoic of Svalbard; Adventdalen Group. Compiled by Atle Mnrrk.

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Extract from: 'Rules and recommendations for naming geological units in Norway' by the Norwegian Committee on Stratigraphy (Nystuen, ed., 1989)

2 General rules for naming and defining geological unit (e.g. nappe, fault, basin, plug, syncline, etc.). In three part names, units the middle part can be a descriptive name placed between the proper or

characterizing name and the part signifying rank or lithology. Such 2.1 Formal and informal units and names: definition three part names should be used as little as possible. . . ...

The Code distinguishes between formal and informal geological units. These have formal and informal names, respectively. Formally defined units are given protected status, affording priority to the specific proper or characterizing names used for them. Names of informal units do not have such protection, but can be protected following evaluation by NSK. Protection can be lifted if names are not in practical use. Formal and informal names can be distinguished in various ways in writing and orally.

The following demands have to be fulfilled before geological units occurring on Norwegian territory, . . ..., can be given or have formal status and thereby a formal, protected name: (a) the unit has to be defined, erected and named in accordance with the requirements of this Code; (b) the erection of the unit has to be reported to, and the proposed names approved by, NSK prior to publication; (c) old established names of geological units can be approved by NSK as formal names when the units are unambiguously understood; if necessary, they can be defined in accordance with the Code at a future date; (d) any changes in the definition, rank, category and name of an established geological unit are to be reported to NSK along with applications for approval of a new name.

Informal names are names given to geological units that have not been erected in accordance with the rules given in this Code for definition of formal unitk, and which have not been approved as formal names by NSK. Informal names also include trivial names (popular names), i.e. traditionally used descriptive names of the sort that do not conform with the rules for formal nomenclature.. . ..

2.2 Names of formal units

2.2.1 The reason for having formal units

Formal geological units are to be dermed with the aim in view that the names given to them will be able to function for a long time retaining a stable, unambiguous geological signrjkance. The name is to be used (a) on official geological maps, @) in published scientific works and technical reports, and (c) in other reports and documents connected with business, public administration and administrative bodies of a political nature. The practical need for a unit, and a certain level of knowledge about it, will need to be demonstrated before the unit can be formally defined and erected.

2.2.2 Construction of formal names

Names of formal geological units are compound terms, usually made up of two or three parts. In the case of geological units that are looked upon as single, physical entities the first component of the name is the proper name. For geological units of a collective nature (see Section 1.3), such as a period of time, this is a distinguishing collective name. It may be a geographical term or some other sort of name representing the type section, type locality or type arealarea of distribution. The second component of two part names may denote (a) the rank of the unit in the classification system (e.g. group, formation, lithodeme, biozone, etc.), (b) the principle lithology of the unit (e.g. sandstone, basalt, conglomerate, etc.), or (c) the rank andtor distinguishing character of the

2.2.3 Naminggeological units on land

Geological units exposed on land are given a proper or characterizing name. This is a geographical name from the type section, type Locality or type area for the unit. The geographical name should preferably be on an official topographical map and is to be written as it is spelt on the map except when this conflicts with rules for spelling compound names. However, the guiding principle when spelling geographical na mes should be that the long-standing, local pronunciation should form the basis for the spelling, as is the case in the rules for spelling official geographical names.. . . .

2.2.6 How to write formal names in Norwegian

Formal names are to be written in Norwegian in accordance with the rules for pronouncing and spelling compound Norwegian words. Com- pound names which can be pronounced as one word are also to be written as one word, using an initial capital letter and without hyphenating the individual components of the name. . . ...

It is important to note that the definite articles -en, -a, -et, -ene at the end of geographical names are usually omitted in compound names. A genitive s can be inserted between the components of the compound name.

Even though the general rule is that the definite article of a geographical name is omitted when names are compounded, this should not be followed if the compound name thereby becomes unrecogniz- able as being related to the original geographical name. Such abbrevi- ations may also lead to direct misunderstanding as regards the origin of the part formed by the geographical name. The -en ending of some geographical names is not the d e f i t e article, but a derivative of the old - - ending -vin, as in Lmten, Lwken, Fannen, Sinsen, Bleiken, Horgen, Hverven, Bergen, etc. In such words the -en ending is to be retained in compound names. . . . ..

2.2.7 HOW to mite formal names in English and other foreign languages

In English, formal names must conform to English orthography and the rules given in ISSC (1976). The proper or characterizing name is to be written in 111 as it is spelt according to official Norwegian orthographical rules and approved forms of names. In contrast to the Nor- wegian way of writing the name, the Norwegian definite articles -en, - a, -et, -ene are to be retained if they are part of the official name (when the definite article "the" is used in front of the unit name it signifies that the entire unit name is to be understood in a definite form). In two part or three part unit names each part is written as a separate word with an initial capital letter. Rendalsformasjonen is therefore written in Eng- lish as "the Rendalen Formation" and Sjodekket as "the Sjoa Nappe". . . ... If the formal name is to be written in other languages the way of writing it should be adapted in a corresponding manner to the national orthographical rules in question. The Norwegian letters ae, 0 and B are, however, to be retained when the name is written in English or other

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APPENDIX 2

languages. Exceptions can be made for typographical reasons. ..... Units which have been named after international waters or other large regional areas, can be spelt according to the rules of Norwegian, Eng- lish or other desired languages, according to what is most appropriate. An example here is the Barents Sea Group (Barentshavsgruppen).

22.9 Changes in the oflcial way of writingproper names

If a change takes place in the official way of spelling a geographical or other name that is being used as a proper or characterizing name for a formal geological unit, the new version is to be used provided the change is insignificant and will not lead to misunderstanding. If the type section, type locality or type area is given an entirely new name on new editions of topographical maps, the name originally assigned to the unit is to be retained.

2.3 Names of informal units

2.3.1 The reason for having informal units, their use and status

Informal units can be introduced for temporary use (a) when canying out geological mapping, @) during ongoing scientific, engineering or economic investigations, (c) when preliminary research results are being published, (d) when writing internal reports, theses, etc., that are not going to be published, and (e) for more lasting use when for various reasons it is not practical to erect formal units.

Informal units need not be erected in the manner required for formal units in this Code ..... or in ISSC (1976).

Irrespective of how they are defined or documented, all names given to geological units that are described and named in internal reports, unpublished undergraduate or dootorate theses, compendiums, textbooks, circulars, guide books (except those published in large editions), etc., are to be looked upon as being informal (see Section 2.4.14).

2.3.3 Ways of writing informal names

Informal names are written in Norwegian according to usual orthographical rules. If the name is understood and used as an ordinary type designation it is a collective name and is to be written with a lower-case initial. If the informal designation is understood and used as the name for a specific entity (unit), it is a proper name and is to be written with an upper-case initial. For example, the informal name Grefsensyenitt (the Grefsen syenite) which, when written in this way, is the proper name for a specific body (lithodeme) of syenite at Grefsen. The petrographic variety of this syenite is also found in other places and may then be called grefsensyenitt as a collective name (in English the collective name should include the word 'type' - Grefsen syenite-type), i.e. with a lower case initial letter in Norwegian, but not in English.

Informal names are written in English according to English orthographical rules. Names which are understood as proper names are written with upper-case initials for the first part of the name and lower-case for succeeding parts. Informal designations which are understood as collective names are written with lower-case initials.

2.4 Rules for erecting formal geological units

The erection of any formal geological unit must always be based on certain fundamental information about the unit. This is crucial if unam biguous defiitions are to be achieved. NSK advises authors to follow the recommendations listed in Sections 2.4.1 to 2.4.14, when erecting a formal unit.

The reasons and practical need for erecting a new formal geological unit, changing the rank and defiition of an existing unit, or completely rejecting an already defied and named formal unit should be clearly stated.

2.4.2 Historical background andprevious investigations

When a new formal unit is being erected, previous investigations and any informal designations of the unit are to be referred to. If the introduction of a new name is desired, reasons are to be given for why the old name of the unit should be changed.

2.4.3 Categofy and rank

The category and rank of geological units are to conform with the main definitions given in this Code. It is very important that the unit is investigated sufficiently thoroughly to enable it to be erected in the correct category, class and type, and with an appropriate rank. The area1 extent of the unit is particularly important in this respect. This also applies to units on the continental shelf.

2.4.4 Name

The choice of name must conform with the rules given above (Sections 2.1 and 2.2) and, if necessary, with the special rules relating to the category and unit in question, and those applicable for units on the continental shelf. Responsibility for ensuring that a proposed proper or characterizing name has not been used previously, rests with the proposer. Previous usage will be checked prior to any approval of the m e by NSK.

2.45 lJpe section, fype locali@, @pe area, rcfrence section

The definition of a formal geological unit should be based on its occurrence in one or more type sections, a type locality or a type area (its stratotype). The occurrence of the unit here has to be as far as possible representative for that found throughout its area of distribution.

The type section or stmtotype (typesnitt) comprises the unit stmtotype (typesnitt for enheten) and boundary stmtotype (typesnitt for grensen). The stratotype contains the entire unit, including its lower and upper boundaries. Stratigraphical units of limited vertical extent can be readily defined on the basis of such stratotypes. In the case of thicker stratigraphical units, e.g. a group or supergroup, it will often be d s i - cult to locate a representative section covering the whole unit. The unit can then be defined using a composite stmtoiype (sammensatt typesnitt) which consists of a boundary stratotype and one or more reference sections (which may also include a unit stratotype). A type section may be a mountain slope, stream section, roadcut or some similar section which it may be assumed will remain generally accessible far into the future. Drill cores, driU logs and excavated sections can form stratotypes for subsurface units.

The type locality (typelokalitet) is the geographical area containing the boundary stratotype and one or more sections through all or part of the unit. Many well-established units have been given names from type localities or type areas without a stratotype having been defined and described. A reference section (see below) can be erected for such units.

The type area (typeomrilde) is the more wide-ranging geographical area within which a geological unit has been defmd and which may contain the type section andlor type locality. A type area will often be more suitable for defining lithodemic, geomorphological, structural and morphostratigraphical units than one or more type sections. The type area for subsurface units can be defined by a set of drill cores, drill logs and seismic profilp~

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APPENDIX 2

A reference section or hypostratotype (referansesnitt) may constitute the unit stratotype for lower-ranking stratigraphical units which, together with a boundary stratotype, defines a higher-ranking stratigraphical unit in a composite stratotype. Reference sections may also be sections that are suitable for (a) demonstrating variation and hetero- geneity in a unit, beyond that shown by the type section, (b) replacing a type section that has been destroyed, and (c) describing old established and named, formal units which lack a type section. A reference section need not be located within the type area of the unit.

ISSC (1976, p. 26) gives specific designations for various kinds of type section.

2.4.9 Age

Knowledge about their age plays no direct role in definition and erection of formal geological units, other than time units. The age of a geological unit will nonetheless be of considerable interest and should be mentioned.

In the case of a metamorphic lithodeme, the metamorphic age should be kept distinct from the age of formation of the primary rock (pro- tolith). The basis for age assignments is to be given. The relative age of movement and deformation forms the basis for distinguishing between complexes and systems in the structural and tectonostratigraphical cat- egories.

Minor changes in defition of boundaries may be desirable following new investigations. If such revision only alters a small portion of the original unit, its name can be retained See Chapter 4 for time units.

A unit can be changed in rank without needing to have its boundaries redefined or the geographical part of its name changed. A unit can be revised in this way both within and outside its type area, or only outside it.

A unit can be changed in category, in which case its proper (geographical) name usually has to be changed. If a unit is redefined to a closely related category, for example from a metamorphic lithodemic unit to a metamorphic lithostratigraphical unit, the original proper name can be retained.

If a unit is divided into two or more units having the same rank as the original one, the original proper name must not be used for any of the new ones. The proper name of the original unit may be retained if the rank of that unit is raised following the new division.

2.5.2 Rejection of formal units

A formal unit may be rejected, or its use abandoned, if it proves to (a) be equivalent to a previously formally defined unit, (b) be defined in the wrong category, (c) not have any application, and (d) be used in many different ways. The proper name of a formal or an informal unit that has been rejected may be used for a subsequently newly erected unit if a long period has passed after the name was used in its original meaning.

2.4.11 Correlation

For the sake of clarity newly-erected geological units should be corre- 2.5.3 Approval lated with corresponding units outside the type area. The basis for the correlation is to be given. Amendments and rejections of formal unit names are to be approved by

NSK prior to publication.

2.4.13 Approval by the Norwegian Committee on Siratgraphy (NSg)

When formal geological units are beimg erected, the basis for their establishment is to be reported to NSK to provide the grounds for possible approval of the proposed name. The purpose of this requirement is to ensure that the unit is (a) adequately &Fled according to the rules laid down by ISSC (1976) and this Code, (b) given an unambiguous name which is constructed and written according to the rulings of this Code, (c) recorded in the register of names at the Norwegian Commit- tee on Stratigraphy, and thereby secured priority, protection and status as a formal name. . . ...

2.4.14 Publishing

For a unit to become valid as a formal unit it must be defined in a pub- licly available scientific journal, map description, published well description, or a guidebook printed in a large edition. .. ...

2.5 Amendment and rejection of formal units

2.5.1 Amendment of formal units

Formally erected geological units can be redefined or revised. Redefinition involves giving a new description of the content of a unit

without changing its boundaries, rank or category. A formation, for example, may originally have been characterized as shale, whereas more recent investigation has shown that the unit chiefly consists of limestone. In the formal compound formation name, "shale" can be replaced by "limestone" without the proper name (geographical term) needing to be changed.

Revision involves (a) minor changes in the definition of one or more boundaries of the unit, (b) change in rank, (c) change in category, or (d) changes in two or more of a-c.

3 Geological units defined on the basis of material content or other physical properties

3.2 Lithostratigraphical units

3.2.1 General properties and rules

..... A lithostratigraphical unit is a body of sedimentary, volcanic, metamorphosed sedimentary or metamorphosed volcanic beds delineated on the basis of characteristic lithological properties and stratigraphical position. Lithostratigraphical units conform to the "Law of Superposi- tion", i.e. younger beds are deposited on older ones.

Lithostratigraphical units are defined independently of inferred geological history, mode of genesis or biological development. Their boundaries are in principle independent of time horizons, and most are time-transgressive. .....

Lithostratigraphical units serve as units when geological mapping is being carried out. They are used in the field and when writing descrip tions, elucidating the geological history and assessing economically exploitable deposits (oil, ores, minerals, gravel, groundwater, etc.).

Lithostratigraphical units are, in decreasing order of rank, supergroup, group, formation, member and bemow. The fonnation is the fundamental unit.

3.2.2 Formation (Formasjon)

3.2.2.1 A formution is a body of rock or superficial deposits occurring as part of a succession. It is characterized by its stratigraphical positian in the succession and by a set of characteristic lithological properties that distinguishes it from adjacent units of rock or superficial deposits. Formations often have a three-dimensional shape such as a sheet, slice, lens, wedge or tongue.

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f' APPENDIX 2

3.2.2.2 Formation is the fundamental formal unit for lithostratigraphical classification and nomenclature. Formations have a practical use when geological maps are being made and when the geological, geophysical and geotechnical properties of an area and its geological history are being described. A formation can be subdivided into members, and two or more formations can be defined as a group.

3.2.2.4 A formation must be mappable at the surface or traceable in the subsurface. A formation exposed at the surface has to be mappable on ordinarily available base maps (official topographical maps, land-use maps, or privately produced, but openly available maps). A formation must also be capable of being portrayed on specially constructed maps, or sections on the same scale, intended to show its extent and three-dimensional form in the subsurface. A particularly thin formation can be portrayed as a single, thin line on maps and sections. A formation is mapped on the surface and recorded in the subsurface by ordinary field geological methods, excavation of sections, drilling and geophysical measurements.

3.2.2.5 ..... A formation is recognized by at least one lithological property, such as mineral composition, chemical composition, fossil content, structures, grain size and other textural features. The boundaries of a formation may be lithologically sharp, or they may need deflning by a change in at least one lithological property if there is a gradual transition between two adjacent lithostratigraphical units. A formation may be characterized by electrical, thermic, magnetic, radiometric, hydraulic, seismic and other physical characteristics which derive from lithological properties. It may contain two or more unconformity surfaces, which may, for example, be reflected by a lack of continuity in fossil content. The fossil content of a formation may define one or more biozones.

3.23 Group (Gruppe)

3.2.3.1 A group is a stratified body of rock or superficial deposits comprising two or more formations, or a corresponding number of informal lithostratigraphical units.

3.2.3.3 The thickness and extent of; group is determined by the total thickness and regional extent of the formations or informal lithostratigraphical units constituting it. A group need not consist of the same formations throughout its area of distribution (Fig. 4).

3.2.3.4 A group is mappable at the surface and traceable in the subsurface with the help of geological and geophysical methods. It is usually a practical lithostratigraphical unit for portrayal on small-scale regional maps.

3.2.3.5 ..... The formal or informal lithostratigraphical units in a group are closely re lhd as regards geological evolution and mode of genesis. There may also be a certain similarity in Lithology, but tbis is not essential. ..... 3.2.3.7 A group may change character regionally, making it more practical to designate it as a formation in an area away from its type area. The proper name of the originally defined group can be retained even though the stratigraphical rank in such areas is changed to formation. In certain cases it may be desirable to divide the group into subgroups (undergrupper). These can be formal having their own names, or informal having designations such as "lower", "middle" and "upper" (Sec- tion 2.3.2).

3.2.5 Member (Zedd)

3.2.5.3 The extent of a member is usually less than the extent of the formation of which it forms a part. A member can pass laterally from one formation into another.

3.2.5.4 A member need not be mappable on the same base map as is required for the portrayal of the formation of which it forms a part. It may be traceable in the subsurface using geological and geophysical methods.

3.2.5.5 A member is defined when it is desirable to distinguish a particular lithostratigraphical part of a heterogeneous formation. A formation need not be subdivided into members. The entire formation or parts of it may be erected as members. A member may consist of beds or flows, but cannot contain other members.

3.2.6 Bed (Lug), Flow (Strem)

3.2.6.1 A bed is the smallest formal lithostratigraphical unit in sedimentary sequences. Aflow is the correspondingly smallest unit in volcanic rocks and deposits formed by flowing lava or ash.

3.2.6.2 Beds and flows have lithostratigraphical rank next beneath members, but may also be formally erected in formations lacking formally erected members.

3.2.6.4 Beds and flows are usually not mappable other than on special, particularly large-scale maps. They can be portrayed on sections of suitable scale. They may be traceable in the subsurface using geological and geophysical methods.

3.2.6.5 A bed usually represents a single depositional event in a sedimentary sequence and is characterized by composition, structure and texture. A flow is a volcanic extrusive rock fomed during a single eruption. It is characterized by composition, structure, texture, palaeo- magnetism and other properties, .....

3.3 Lithodemic units

3.3.1 General properties and rules

A lithodemic unit consists of one or more bodies of igneous rocks which may be plutonic, intrusive or extrusive rocks andlor strongly metamorphosed and deformed rocks (Figs. 1, 5). The unit is defined entirely on the basis of lithological character. In contrast to lithostratigraphical units, the classification of lithodemic rocks does not follow the principle of younger rocks being formed above older ones. Litho- demic units are therefore erected in areas where rocks do not succeed one another in compliance with the "Law of Superposition", or where it is very. difficult to prove such a relationship.

Lithodemic units serve as units when geological mapping is being canied out in areas where the bedrock lacks stratification. They are used during field work, when writing descriptions, elucidating the geological history and assessing economically exploitable deposits. Con- tacts with other geological units may be sedimentary, intrusive, metamorphic or tectonic in origin.

Lithodemic units are, in decreasing order of rank, supersuite, suite and lithodeme. The lithodeme is the fundamental unit. Complex is not ranked, but will usually correspond in sue to suite or supersuite. .....

Formal lithodemic units should only be defined and erected if they serve a practical purpose. Names of informal lithodemic units are not to be constructed using a geographical name (or an alternative name in the case of the continental shelf) and a formal hierarchical unit designation.

3.2.5.1 A member is a body of rock or superficial deposits that occurs in a stratified formation.

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APPENDIX 2

3.3.2 Lithodeme (Litodem)

3.3.2.1 A lithodeme is a body of intrusive, volcanic or highly metamorphosed and/or thoroughly deformed rock that lacks primary structures. It is characterized by having a set of lithological properties that distinguishes it from adjacent geological units.

3.3.2.2 Lithodeme is the fundamental formal unit in lithodemic classification and nomenclature. Two or more lithodemes of the same class can be defined as a suite.

3.3.2.3 No limitations are placed on the dimensions of a lithodeme except that it must be mappable at the surface or traceable in the sub-surface.

3.3.2.4 A lithodeme should be mappable at the surface or traceable in the subsurface using geological and geophysical methods. It should be mappable on ordinarily available base maps (official topographical maps, land-use maps, and privately-produced, but openly available maps).

3.3.2.5 A lithodeme consists of a rock that can be identified by its lithological properties using field geological methods. ..... A lithodeme may be an intrusive rock occurring, for example, as a pluton, diapu, stock, laccotith, sheet or plug, a body of volcanic rocks which have mutually complex boundary relationships, or a body of strongly metamorphosed rock ..... A lithodeme may be characterized by electrical, thermic, magnetic, radiometric, hydraulic, seismic and other physical characteristics derived from its lithological properties.

3.3.2.7.a Lithodeme corresponds in rank to formation in the lithostratigraphical classification system, also when used informally on maps or in descriptions.

3.3.2.7.b A lithodeme may change its character regionally. It may therefore be more practical to designate the unit as a suite beyond its type area; the original proper name may then be retained (see Section 2.5.1).

3.3.3 Suite (Suite)

3.3.3.1 A suite is a lithodemic unit consisting of two or more lithodemes. or informal lithodemic units. Individual lithodemes in a suite must belong in the same class, i.e. be either igneous or metamorphic rocks.

3.3.3.2 Suite is a formal lithodemic unit ranking next above lithodeme. Two or more suites of the same or a different class can be defined as a supersuite.

3.3.3.3 A suite usually has a regional extent, or consists of a few distinct units which together have a regional extent.

3.3.3.4 A suite is mappable at the surface and traceable in the subsu- face using geological and geophysical methods.

3.3.3.5 A suite consists of formal lithodemes andlor informal, unnamed lithodemic units that belong to the same class of rock. These may be either igneous or metamorphic (including metasomatic and highly deformed rocks). A suite may therefore be, for example, a platonic, intrusive, dyke or metamorphic suite. The individual formal or informal units in a suite have one or more characteristic features in common that often unite them in a common geological history or mode of origin.

3.3.3.6 Suites are only given formal names, this beiig done in accordance with the "general rules for naming and defining geological units". The name may consist of a geographical name (or an alternative name in the case of the continental shelf) between the words "the ... Suite", but a descriptive term, such as "Intrusive" or '%ietamorphic", may in addition be placed in front of "Suite".

3.3.3.7.a Suite corresponds in rank to group in the lithostratigraphical classification system.

3.3.3.7.b A suite may change in character regionally, making it more practical to designate the unit as a lithodeme in areas beyond its type area. .....

3.3.5 Complex (KompIek.$

3.3.5.1 A complex is a lithodemic unit consisting of a mixture or assemblage of rocks belonging to two, or all, of the classes of rocks, i.e. igneous, sedimentary and metamorphic rocks.

3.3.5.2 Complex has no rank in the lithodernic classification system.

3.3.5.3 No limitation is placed on the dimensions of a complex, but it generally has a regional extent.

3.3.5.4 A complex is mappable at the surface and traceable in the subsurface using geological and geophysical methods.

3.3.5.5 The individual, associated bodies of different rock units making up a complex may be formally named lithodemes, lithostratigraphical units, and/or informal and unnamed lithological units. They have often been deformed together to form a complicated structural pattern, but this is not a prerequisite. A complex of large regional extent may contain other complexes of smaller area1 distribution.

3.3.5.6 A complex is given a formal or an informal name in accordance with the ''general rules for naming and defining geological units" (Chap. 2). Names made up of a geographical name between the words "the ... Complex" should preferably only be used for formally defied complexes (see Section 2.3.2).

3.3.5.7.a A complex is a practical mapping entity in areas where it is difficult or impractical to distinguish individual lithodemic or stratigraphical units on the map scale in question.

3.3.5.7.b A complex is often comparable in size to a suite or supersuite.

3.3.5.7.cA volcanic complex is an assemblage of different kinds of volcanic rocks and associated intrusive and weathering products. Volcanic complexes or intrusive volcanic complexes that are included in a thick sequence of sedimentary rocks can be defined together with these as a supergroup.

3.3.5.7.d A srmctuml complex is an assemblage of different kinds of rocks intermixed by tectonic processes (Fig. 1).

Reference:

ISSC (International Subcommission on Stratigraphic Classification of IUGS Commission on Stratigraphy) 1976: International Stratigraphic Guide: A Guide to Stratigraphic Classification, Terminology and Pro- cedure (ed. Hedberg, H.D.), 200 pp. John Wiley & Sons, New York.

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LEGEND FOR STRATIGRAPHIC TYPE SECTIONS

grain size scales

1) for clastic rocks: lithology cl: clay structure si: sik

VC. very coarse

p: pebbles cb: cobbles

X b: boulders

2) for carbonate rocks: M: mudstone

X W wackestone X P: packstone

G: grainstone B: boundstone

scale grain size

LITHOLOGY:

1. Siliciclastic rocks Breccia

Conglomerate

Gravelstone/gritstone

Pebbly sandstone m Sandstone

Silty sandstone

m Siltstone

Sandy shale -.-. B - - - Shale, mudstone, claystone -

Sandy chert

Chert

Paper shale

2. M.ixed carbonate-siliciclastic rocks .....,....., Calcite-cemented sandstone

....,,? .:: Dolomite-cemented sandstone

m Calcareous shale - Dolomitic shale

m sakiy limestone

H Silty limestone

Clayey limestone

Cherty limestone

m. Sandy, dolomitic limestone

Sandy, calcitic dolomite

Sandy dolomite m ..t,.:t Siderite-cemented sandstone

3. Carbonate rocks m Limestone, calcareous ... m Dolomite. dolomitic ... .I

Dolomitic limestone - H Calcitic dolomite

m Siderite

4. Other layered lithologies Gypsum 8 anhydrite

L ", " 1 Dolerite sill / dvke U

Basalt lava

5. Secondary lithological content Cherty nodules Calcareous nodules Dolomitic nodules Sideritic nodules Gypsiferouslanhydritic nodules Pyritic nodules Septarian nodules Phosphate nodules Sandstone lens Clay-ironstone or siltstone nodules Conglomerate beds Polymict conglomerate beds . Mud flakes Mud clasts Sandy Silty Shaley Cherty Calcareous Dolomitic Sideritic Gypsiferouslan hydritic Halitic Coaly, coal lenses or fragments Bentonite Glauwnite Quartzite Caliche

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STRUCTURE: 3. Plant fossils

Trough cross-bedding, undifferentiated

B Troughlplanar cross-bedding, adjusted to appearance in outcrop Tabularlplanar cross-bedding

m Herringbone cross-bedding

BioheWreef

MPS I

#

Maximum particle size (cm) Beds distinct Unbedded Cross bedding, ripple lamination Ripple structures Climbing ripple lamination Dunes Flaser beddingllenticular bedding Wave ripples Wavy lamination Planar lamination Cone in cone Convolute lamination and soft-sediment deformation Flow structures Karst Stylolites Mud cracks Hiatuslerosion surface Loading Hummocky beddingllamination

FOSSILS AND PARTICLES:

1. Vertebrate fossils 4 Vertebrates -- Fish remains

2. Invertebrate fossils Calcispheres Corals Bivalves Rudists Gastropods Brachiopods Lingula Bryozoans Trilobites Sponges Foraminifera, undifferentiated Foraminifera, benthic Foraminifera, encrusting Foraminifera, planktonic Fusulinids Orbitolina Ostracods Molluscs Cephalopods, mostly belemnites Ammonoids Echinoderms Crinoids Palaeoaplysina

Laminar stromatolites Columnar stromatolites Encrusting algae Green algae Red algae Phylloid algae Algae lamination Girvanella Stromatoporids Stigmaria Plant fragments Tree trunks Roots

4. Trace fossils Burrows, horizontal Burrows, vertical Burrows, undifferentiated Increasing bioturbation Arenicolites Trails Ophiomorpha Rhizocorallium Skolithos . Terebellina Thalassinoides Zoophycos Chondrites Palaeophycus, planolites Diplocraterion

5. Others Fossils, undifferentiated Microcodium Tubiphytes Coquina beds Ooids Oncoids Pellets Peloids Bioclasts lntraclasts Lithoclasts

VARIOUS:

Break ,-- Fault C Covered section

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mapping in the Norwegian polar regions. The lnstitute also advises the Norwegian authorities

on matters concerning polar environmental management

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