Field Report-Mianwali

7/23/2019 Field Report-Mianwali

1/42

ROVING TH MUS UM OF

G OLOGY

AFIELDTRIPTOWESTERNSALTRANGE,NAMMALGORGE&CHICHALIGORGE

ABDUL WAHAB KHAN

2ND

SEMESTER MSc. GEOPHYSICS10THDECEMBER, 2015.


2/42

TABLE OF CONTENTS

CONTENT PAGE

NO

i.

LIST OF FIGURES 1

ii. PREFACE 3

iii.

AKNOWLEDGEMENT 4

1.

INTRODUCTION

1.1

INRTODUCTION TO THE AREA1.2 INTRODUCTION TO THE STUDY

5

55

2.

LOCATION OF THE AREA

2.1

GEOGRAPHICAL LOCATION

2.2

TECTONIC LOCATION

6

6

7

3. OBJECTIVE OF THE STUDY 8

4. GEOLOGY OF THE AREA

4.1.1 IDENTIFIED LITHOLOGY IN NAMMAL GORGE

4.1.2

IDENTIFIED LITHOLOGY IN CHICHALI GORGE

4.1.3

STRATIGRAPHIC COLUMN & SECTION

4.2

IDENTIFIED STRUCTURES

4.3TASKS

4.3.1 IDENTIFIYING ROCKS

4.3.2 USE OF BRUNTON COMPASS

4.3.3 CALCULATING STRIKE AND DIP

9

9

18

25

27

38

38

38

39

5.

REFERENCES 40


3/42

1

LIST OF FIGURES

Figure 1.Location Map of Salt Range

Figure 2. Location of the study area with reference to regional tectonic

framework

Figure 3. Chert nodules in dolomite of Wargal Formation

Figure 4. Wargal Limestone

Figure 5. The demarcation of PT BOUNDARY

Figure 3. Brachiopod fossil embedded in limestone.

Figure 4. Productus fossil in Chiddru Formation

Figure 5. Phosphoric nodules in Chiddru Formation

Figure 6. Kathwai Member

Figure 7. Narmia Member.

Figure 8. Tridan Formation.

Figure 9. Kingriali Formation.

Figure 10. Datta Formation.

Figure 11. Nodular Limestone of Sakesar Formation

Figure 12. Chert Nodules in Sakesar Formation

Figure 13. Greyish to green fossilferrous shale of Nammal Formation

Figure 14. Blackish shales and intertwining bed of limestone in Patala

Figure 15. Belemnite fossils, characteristic of this formation

Figure 16. Coal and Sulphur are present in Hangu Formation

Figure 17. Stratigraphy of Central Indus Basin (after Kadri, 1995).

Figure 18. Regional Stratigraphy Section of Salt Range

Figure 19.Fold of local scale visible in the Molass deposits in Chapri Village

Figure 20. Intra sedimentary folds


4/42

2

Figure 21. Faulting in Chiddru Formation

Figure 22. Joints in Hangu Formation

Figure 23. The cave in Nammal Gorge

Figure 24. Fresh water coming from the Aquifer

Figure 25. Ripple Marks

Figure 26.Cross Bedding

Figure 27. Mud Cracks

Figure 28. Honey Comb Weathering

Figure 29. Convolute Bedding

Figure 30. Pseudo morph Salt Crystals

Figure 31. Load Casts

Figure 32.These are Hollow structures which are found in Salt Range

Formation.

Figure 33. Chopboard Weathering

Figure 34. Burrows

Figure 35. A Brunton Compass

Figure 36. Using the Brunton Compass to find strike and dip.


5/42

3

PREFACE

Today's students are tomorrow's decision-makers, whether their future careers

are in politics, finance, technology, medicine, geology, or other sciences. It is their

decisions that collectively will decide the fate of our planet-earth. My teachers in Dept.of Earth sciences ensure that their students have the opportunity to obtain a sound

understanding of the Earth so that they are equipped to make informed,

environmentally responsible decisions in their future careers.

I had the opportunity to visit Pakistan's unique field museum of geology and

paleontology and found it a wonderful experience. I convey the message that

understanding the Earth is exciting, and that it enriches and heightens our sense of

awareness of the world around us.

Our field trip to Western Salt Range was to recognize and understand various

lithologies and structures in the sedimentary strata ranging from the Pre-Cambrian to

recent age of the geologic time scale. If, at the end of my report, you feel the urge to

have a glance over again, then I will have definitely paid due regard to all that I have

learned during my field trip.


6/42

4

ACKNOWLEDGEMENT

We live in amazing times. In the past few decades we have learned an enormous

amount about our Earth, and new information confronts us almost daily. We can

scarcely watch the news or read a newspaper without learning of some new andexciting discovery related to Earth. This information had come at such a bewildering

pace, that it was difficult to assimilate it all without the help of my teachers.

I feel highly obliged to the Dept. of Earth Sciences for arranging this field trip which

augmented a hands-on chapter to my all my learning so far. It has greatly improved

my understanding of all the theoretical knowledge that I have gained.

My teachers at the field encouraged and taught me on every step of the way. Their

expertise and cheerfulness kept me motivated and ensured my keen interest inlearning out there. Dr. Aamir Ali, Dr. Anwar Qadir and Dr. Tauqeer Shah satisfied my

curiosity and made it a pleasurable experience as they navigated us through all of the

members, formations and groups of the Western Salt Range that we observed. I am

greatly indebted to Dr. Mona Lisa for opening the door to various tactics of report-

writing which made substantial improvements to this text.


7/42

5

1 INTRODUCTION

1.1 INTRODUCTION TO THE AREA

The Salt Range contains the most important geologic and paleontologic localities in

Pakistan, and is one of the outstanding field areas in the entire world. Despite its easy

accessibility, it has a wealth of geological and paleontological features. In fact, itrepresents an open book of geology where various richly fossiliferous stratified rocks

are very well exposed due to lack of vegetation. These rocks also provide an excellent

opportunity for appreciation of tectonics in the field. (Sameeni, 2009)

1.2 INTRODUCTION TO THE STUDY

A three-day field trip was carried out i.e. 27thNovember, 2015 to 29thNovember, 2015.

Our target location was Namal Gorge and Chichali. The focus of the study was to

acquaint ourselves with the knowledge of sedimentary rocks and structural features in

the Eastern Salt Range.


8/42

6

2 LOCATION OF THE AREA

2.1 GEOGRAPHICAL LOCATION

The Salt Range is confined between 3218N to 3306N and7150E to

7345E.

Figure 1.Location Map of Salt Range


9/42

7

2.2 TECTONIC LOCATION

Figure 2. Location of the study area with reference to regional tectonic framework


10/42

8

3 OBJECTIVE OF THE STUDY

Identifying and Differentiating Rocks

Lithological Correlation

Stratigraphic Relationship

Observing Sedimentary Structures

Marking Unconformity

Understanding Environment of Deposition of Formations

Measurement of Strike and Dip


11/42

9

4 GEOLOGY OF THE AREA

4.1.1 IDENTIFIED LITHOLOGY IN NAMMAL GORGE

A.Wargal Formation:

Etymology: The name Wargal limestone was approved by the Stratigraphic

Committee of Pakistan proposed by Teichert (1966) to the unit formerly known as

Middle Products limestone of Waagen (1879) and Wargal group of Noetling (1901).

Type Locality:Its type section is Wargal village in the central salt range.

Age:The age of Wargal Formation is Permian.

Lithology: Lithologicaly the formation is composed of limestone and dolomite of light

grey to medium grey, brownish grey and olive green colors. In Zaluch nala the

formations lithology is divided into 10 parts which shows alternate beds of sandstone,

limestone and dolomite.

The formation is 183m thick in Zaluch nala while in Marwat and Khisor ranges it is

about 174m.

Contacts: The contact of Wargal limestone with underlying Amb formation is

confirmable while upper contact with Chiddru formation is transitional.

Figure 3. Chert nodules in dolomite of Wargal Formation


12/42

10

Figure 4. Wargal Limestone


13/42

11

B.Chiddru Formation:

Etymology: The name Chiddru formation was introduced by Dunbar (1932) to the

Chiddru beds of Waagen (1891) and Chiddru group of Noetling (1901).

Type Locality: The type locality is at Chiddru Nala.

Age:The age of Chiddru Formation is Late Permian.

Lithology: The formation at the base is composed of shale unit of yellowish grey to

medium dark grey color with small phosphatic nodules. Above shale beds of calcareous

sandstone with few sandy limestones are present. The top most part is a white

sandstone bed which is medium to fine grained with subordinate shale partings and

contains abundant fossils.

Contacts: The formation has a transitional contact with underlying Wargal formation

while its upper contact is marked by a major unconformity the P-T boundaryabove

which is the Mianwali formation of Triassic age.

Figure 5. The demarcation of PT BOUNDARY

Figure 3. Brachiopod fossil embedded in limestone.


14/42

12

Figure 4. Productus fossil in Chiddru Formation

Figure 5. Phosphoric nodules in Chiddru Formation


15/42

13

C.Mianwali Formation:

Etymology: The name Mianwali Series was used by Gee and later modified by

Kummel (1966) into a formation.

Type Locality: The formation is best exposed in Zaluch Nala and Khisor Range.

Age: Triassic

Lithology: The following three members have been recognized by Kummel (1966).

1. Kathwai Member.

2. Mittiwali Member.

3. Narmia Member.

1. Kathwai Member:The unit consists of dolomite in the lower part and limestone

in the upper part. The dolomite is finally crystalline and includes fossil fragments

(mainly echinoderms) and quartz grains. The upper unit is grey to brown

glauconitic limestone. The total thickness of Kathwai Member is 3.7 in Zaluch

Nala and 2.4m in Tappan Wahan.

2. Mittiwali Member:The lithology consists of grey, fine-grained, non-glauconitic

limestone with abundant ammonites. The basal beds consist of limestone. The

rest of the unit consists of greenish to greyish shale, silty shale with some

sandstone and limestone interbeds. The unit is richly fossiliferous.

3. Narmia Member:The basal bed of Narmia member is a 3 m thick limestone

which in Zaluch Nala consists of dark grey to brown fragmental limestone, sandy

in part and containing brachiopods, bivalves and ammonoids. The rest of the

unit consists of grey to black shale with interbeds of sandstone and lenticular

limestone or dolomite. The topmost bed is a grey to brown massive dolomite.

Contacts: The lower contact with the Chiddru Formation of Late Permian age is marked

by a para conformity while the upper contact with the Tradian Formation is sharp andwell-defined.


16/42

14

Figure 6. Kathwai Member

Figure 7. Narmia Member.


17/42

15

D.Tradian Formation:

Etymology:The name Tradian Formation was introduced by Gee to replace, in part,

his earlier name Kingrali Sandstone.

Type Locality:Its thickness is 76 m in the Zaluch section of the Salt Range.

Age: It is regarded as Middle Triassic.

Lithology: The formation comprises of two members; the lower is Landa Member

(Kummel, 1966) and the upper is the Khatkiara Member (Shah 1967).

1. Landa Member: It consists of sandstone and shale. The sandstone is

micaceous and varies in colour from pinkish, reddish grey to greenish

grey. It is thin to thick-bedded, with ripple marks and slump structure.

2. Khatkiara Member: It is massive, thick-bedded white sandstone that

grades into the overlying Kingrali Formation with the inclusion of some

dolomite beds in its upper part.

Contact:Its lower contact is with Mianwali Formation and upper contact with Kingrali

Formation.

Figure 8. Tridan Formation.


18/42

16

E.Kingriali Formation:

Synonym: The name Kingrali Dolomite was used by Gee(1945) and later amended as

Kingrali Formation, because several lithological facies are represented. The name

originates from Kingrali Peak in the Khisor Range.

Type Locality: Good sections of the formation occur in Zaluch Nala in the Western Salt

Range, Landa Nala In the Surghar Range and in the Tapan Wahan Gori Tang Nala in the

Khisor Range.

Age: Late Triassic.

Lithology: The formation consists of thin to thick-bedded, massive, fine to coarse-

grained, light grey-brown dolomite and dolomitic limestone with interbeds of greenish

dolomitic and shale in the upper part.

Contact: Its lower contact is with the Tradian Formation which is transitional and upperdisconformable contact with Datta Formation.

Figure 9. Kingriali Formation.


19/42

17

F. Datta Formation:

Etymology: The name Datta Formation was introduced by Danilchik (1961) and

Danilchik and Shah (1967) to replace the name Variegated Stage of Gee (1945) and

earlier workers.

Type Locality: The type section is located in Datta Nala in the Surghar Range.

Age: Early Jurassic.

Lithology: The formation is mainly of continental origin and consists of variegated (red,

maroon, grey, green and white) sandstone, shale, siltstone and mudstone with

irregularly distributed calcareous, dolomitic, carbonaceous, ferruginous, glass sand

and fireclay horizons. The fireclay is normally present in the lower part while the upper

part includes a thick bed (4 to 7 m) of maroon shale easily recognizable in Salt Range

and Trans-Indus Ranges.

Contacts: It rests unconformably on the Kingrali Formation and the lower contact with

the Shinawari Formation is gradational.

Figure 10. Datta Formation.


20/42

18

4.1.2 IDENTIFIED LITHOLOGY IN CHICHALI GORGEA.Sakesar Formation:

Etymology: Name Sakesar Limestone by Gee in 1935 was accepted by the

Stratigraphic committee.

Age:Due to the presence of these fossils, the age assigned to this formation is Early

Eocene.

Lithology:Bulk of lithology of this formation is limestone which is cream to light gray

in color, nodular, and massive in the upper part and also highly fossiliferrous. Light gray

colored Marl is also found in the top most part and having Chert nodules.

Contacts: Upper contact is with Chorgali formation and this contact is transitional and

conformable.Lower contact is with Nammal formation and it is also conformable.

Figure 11. Nodular Limestone of Sakesar Formation


21/42

19

Figure 12. Chert Nodules in Sakesar Formation


22/42

20

B.Nammal Formation

Etymology: Nammal limestone and shale by Gee (1935), Nammal Marl by

Danilchik andShah (1967), is named as Nammal formation by Stratigraphic Committee

of Pakistan.

Age: Due to the presence of these fossils, age assigned to this formation is Early

Eocene.

Lithology: Main lithology of this formation is shale, marl and limestone alterations.

Shale is gray to green and fossiliferrous. Lime stone is gray to bluish, argillaceous and

highly fossiliferrous. Marl is light gray to bluish gray and is also fossiliferrous.

Contact: Upper contact of this formation is with overlying Sakessar formation and is

transitional and conformable. Lower contact of this formation is with underlying Patalaformation and this contact is also conformable.

Figure 13. Greyish to green fossilferrous shale of Nammal Formation


23/42

21

C.Patala Formation

Etymology: Davies and Pinfold (1937) named it as Patala shale which later was

renamed as the Patala Formation by the Stratigraphic Committee of Pakistan.

Age: Age assigned to this formation is Late Paleocene.

Lithology:It is comprised of shale and marl with subordinate limestone and sandstone

interbeds. The shale is dark greenish grey, carbonaceous as well as calcareous, and

friable with selenite crystals distributed throughout. The limestone is light to dark grey

in color, medium bedded and nodular, whereas the sandstone is yellowish brown and

is located in the upper part of the formation. In Salt Range, it contains coal seams.

Contact: Upper contact with overlying Nammal formation is transitional and

conformable. Lower contact is with Lockhart formation and it is also transitional andconformable.

Figure 14. Blackish shales and intertwining bed of limestone in Patala Formation


24/42

22

D.Lockhart Formation

Etymology: Davis (1930) introduced the term Lockhart Limestone for a paleocene

limestoneunit in the kohat area.

Age: Paleocene

Lithology:Grey to dark gray, medium to thick massive bedded, brecciated limestone.

The limestone displays very well developed nodularity.

Contact: Upper contact with Patala formation is transitional and conformable.lower

contact is with Hangu formation and the contact is also conformable.

E.

Hangu Formation

Etymology: The Hangu Shale and Hangu Sandstone by Davies (1930) have been

formalized by the stratigraphic committee of Pakistan as Hangu formation.

Age :Early Paleocene

Lithology: This formation consists of dark grey, rarely variegated sandstone, shale,

carbonaceous shale, and some nodular argillaceous limestone. The sandstone is white,

lightgray, and reddish brown, weathers dark rusty brown, fine to coarse grained and

medium tothick bedded.

Contacts: Upper contact of this formation is with Lockhart formation and this contact

istransitional and conformable.Lower contact of the formation is unconformable with

Lumshiwal Formation.

Figure 15. Belemnite fossils, characteristic of this formation


25/42

23

Figure 16. Coal and Sulphur are present in Hangu Formation


26/42

24

F.Lamshiwal Formation

Etymology: Davies (1930) named this formation as Main sandstone series. Gee

(1945) suggest the name Lumshiwal sandstone. The name has been since formalised

as Lumshiwal Formation by the Stratigraphic Committee of Pakistan.

Age: Middle Cretaceous

Lithology: It is mostly grey, thick bedded to massive, current-bedded, feldspathic and

ferroginous sandstone, but contains silty, sandy glauconitic shale towards the base.

Northward and eastward, the formation grades into a mostly marine sequence of

sandstone, siltstone and shelly limestone.

Contacts: Upper contact of this formation is with overlying Kawagarh formation and

isdisconformable. Lower contact with underlying Chichali formation is gradationalandconformable.

G. Datta Formation:

Etymology:The name Datta Formation was introduced by Danilchik (1961) and

Danilchik and Shah (1967) to replace the name Variegated Stage of Gee (1945) and

earlier workers.

Type Locality: The type section is located in Datta Nala in the Surghar Range.

Age:Early Jurassic.

Lithology:The formation is mainly of continental origin and consists of variegated

(red, maroon, grey, green and white) sandstone, shale, siltstone and mudstone with

irregularly distributed calcareous, dolomitic, carbonaceous, ferruginous, glass sand

and fireclay horizons. The fireclay is normally present in the lower part while the

upper part includes a thick bed (4 to 7 m) of maroon shale easily recognizable in Salt

Range and Trans-Indus Ranges.

Contacts:It rests unconformably on the Kingrali Formation and the lower contact

with the Shinawari Formation is gradational.


27/42

25

4.1.3 STRATIGRAPHIC COLUMN & SECTION

Figure 17. Stratigraphy of Central Indus Basin (after Kadri, 1995).


28/42

26

Figure 18. Regional Stratigraphy Section of Salt Range


29/42

27

4.2 INDENTIFIED STRUCTURES

A.Folds:

Folds are formed due to compressive forces. Various folds were observed with a

variety in their types during the field.

Figure 19.Fold of local scale visible in the Molass deposits in Chapri Village

Figure 20. Intra sedimentary folds


30/42

28

B.Faults:

Figure 21. Faulting in Chiddru Formation

C.Joints:

Figure 22. Joints in Hangu Formation


31/42

29

D.Cave and Mouth of Aquifer

In Nammal Gorge a cave was visited which had a little pond that was made by

accumulation of fresh water from an aquifer.

Figure 23. The cave in Nammal Gorge

Figure 24. Fresh water coming from the Aquifer


32/42

30

E.Ripple Marks:

Ripple cross-laminae forms when deposition takes place during migration of

current or wave ripples. A series of cross-laminae are produced by superimposingmigrating ripples. The ripples form lateral to one another, such that the crests of

vertically succeeding laminae are out of phase and appear to be advancing upslope.

This process results in cross-bedded units that have the general appearance of

waves in outcrop sections cut normal to the wave crests. In sections with other

orientations, the laminae may appear horizontal or trough-shaped, depending

upon the orientation and the shape of the ripples. Ripple cross-laminae will always

have a steeper dip downstream, and will always be perpendicular to paleo flow

meaning the orientation of the ripples will be in a direction that is ninety degreesto the direction that current if flowing. Scientists suggest current drag, or the

slowing of current velocity, during deposition is believed to be responsible for ripple

cross-laminae. In the field we identified ripple marks in Sandstone.

Figure 25. Ripple Marks


33/42

31

F. Cross Bedding:

In geology, the sedimentary structures known as cross-bedding refer to (near-)

horizontal units that are internally composed of inclined layers. This is a case in geology

in which the original depositional layering is tilted, and the tilting is not a result of post-depositional deformation. Cross-beds or "sets" are the groups of inclined layers, and

the inclined layers are known as cross strata.

Cross bedding forms during deposition on the inclined surfaces of bedforms such as

ripples and dunes, and indicates that the depositional environment contained a

flowing medium (typically water or wind). Examples of these bedforms are ripples,

dunes, anti-dunes, sand waves, hummocks, bars, and delta slopes. In the field we

observed cross bedding in Khewra Sandstone.

Figure 26.Cross Bedding


34/42

32

G.

Mud Cracks:

Mud cracks (also known as desiccation cracks or mud cracks) are sedimentary

structures formed as muddy sediment dries and contracts. Naturally forming mud

cracks start as wet, muddy sediments desiccates, causing contraction. A strain is

developed because the top layer tries to shrink while the material below stays the

same size. When this strain becomes large enough, channel cracks form in the

desiccated surface material, relieving the strain. Individual cracks spread and join up

forming a polygonal, interconnected network. These cracks may later be filled withsediment and form casts on the base of the overlying bed.

Figure 27. Mud Cracks


35/42

33

H.Honey Comb Weathering:

Honeycomb weathering, also known as fretting, cavernous weathering,

alveoli/alveolar weathering, stone lattice, stone lace is a type of salt weathering

common on coastal and semi-arid granites, sandstones and limestone. Honeycombweathering is not limited to natural settings and can be seen to develop on buildings

where a rate of development can be established. This rate can be as fast as several

centimeters in 100 years.

Cause

For honeycomb weathering to occur, a source of salt is needed because the basic

mechanism for this kind of weathering is salt heaving. Salt is deposited on the surface

of the rock by saltwater spray or by wind. Moisture must be present to allow for the

salt to settle on the rocks so that as the salt solution evaporates the salt begins to

crystallize within the pore-spaces of the rock. Porous rock is also needed so that there

are pore-spaces for the salt to crystallize within. These salt crystals pry apart the

mineral grains, leaving them vulnerable to other forms of weathering. It takes

prolonged periods for this weathering to become visible, as the rock goes through

cycles of wetting and drying. We observed the honey comb weathering in Sandstone.

Figure 28. Honey Comb Weathering


36/42

34

I. Convolute Bedding:

Convolute bedding forms when complex folding and crumpling of beds or laminations

occur. This type of deformation is found in fine or silty sands, and is usually confined

to one rock layer. Convolutelaminations are found in flood plain, delta, point-bar, and

intertidal-flat deposits. They generally range in size from 3 to 25 cm, but there have

been larger formations recorded as several meters thick. We also observed it in

sandstone.

Figure 29. Convolute Bedding


37/42

35

J. Pseudo morph Salt Crystals:

In mineralogy, a pseudo morph is a mineral or mineral compound that appears in an

atypical form (crystal system), resulting from a substitution process in which the

appearance and dimensions remain constant, but the original mineral is replaced by

another. The name literally means "false form".

Figure 30. Pseudo morph Salt Crystals


38/42

36

K.Load Casts:

Load casts or Sole marks are sedimentary structures found on the bases of certain

strata that indicate small-scale (usually on the order of centimeters) grooves or

irregularities. This usually occurs at the interface of two differing lithologies and/orgrain sizes. They are commonly preserved as casts of these indents on the bottom of

the overlying bed (like flute casts). This is similar to casts and molds in fossil

preservation. Occurring as they do only at the bottom of beds.

Figure 31. Load Casts

L. Hollow Structures:

Figure 32.These are Hollow structures which are found in Salt Range

Formation.


39/42

37

M. Chopboard Weathering:

We observed chopboard weathering in Mianwali Formation.

Figure 33. Chopboard Weathering

N.Burrows:

Figure 34. Burrows


40/42

38

4.3 TASKS

4.3.1IDENTIFYING SEDIMENTARY ROCKS

We identified sedimentary rocks on the basis of their

Color

Clast Size

Hardness

Texture

Effervescence

4.3.2USEOFBRUNTONCOMPASSThe Brunton compass is used by more geologists for field mapping of geological

objects than other brands. This preference, especially in North America, is because

Brunton provides a precise sighting-clinometer and hand level capability, and can be

used at both waist and eye levels; advantages that are absent in other brands such as

Silva which lacks a leveling system for sighting bearings (Compton, 1985).

Figure 35. A Brunton Compass


41/42

39

4.3.3 CALCULATING STRIKE AND DIP WITH BRUNTON

COMPASS

Figure 36. Using the Brunton Compass to find strike and dip.

A bed was assigned to each group to find out its strike and dip by employing Brunton

Compass, I obtained the readings stated below

Strike ENE-WSW

Dip 33NNW


42/42

5 REFERENCES

1.Compton, R. R., 1985. Geology in the Field. John Wiley & Sons, New

York, 398p.

2.SAMEENI S.J. (2009). - The Salt Range: Pakistan's unique field museum

of geology and paleontology. - In: LIPPS J.H. & GRANIER B.R.C. (eds.),

PaleoParks - The protection and conservation of fossil sites

worldwide.- Carnets de Gologie / Notebooks on Geology, Brest, Book

2009/03, Chapter 6

3.Cotter.G.de P., 1933, The geology of the part of Attock District, west

of Longitude 7245 E: India Geol. Surv., Mem.,v.55,pp.63.

4.Danilchik, W., 1961, The Iron formation of the Surgar and western Salt

Range, Mianwali Distt, West Pakistan: U.S Geol. Surv., Prof. Paper 424-

D, pp.228-231.

5.Davies, 1930a, The fossil fauna of the Samana Range and some

neighbouring areas: Part 6, The Paleocene Foraminifera, An

Introductory note: India Geol. Surv., Mem., Paleont. Indica, New

Series, v.15, 15p.

6.Davies, and Pinfold, E.S., 1937, The Eocene beds of the Punjab Salt

range: India Geol. Surv., Mem., Paleont. Indica, New Series, v.24, no.1,

79p.

7.Gee, E.R., 1935, Recent observations on the Cambrian sequence of the

Punjab Salt Range: India Geol. Surv., Ress., v. 68, pt.1, pp.115-120.

8.Kazmi and Abbasi, 2008. Stratigraphy and Historical Geology of

Pakistan

9.Ibrahim Shah, 1977. Stratigraphy of Pakistan

Field Report-Mianwali

Documents

Transcript of Field Report-Mianwali