Mineral resource of Orissa.pdf

8/17/2019 Mineral resource of Orissa.pdf

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GEOLOGY

AND

MINERAL RESOURCES

OF

THE STATES OF INDIA

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Ç F ⁄F[ PÊF£FFŒF JÊFk

äFPŒF°F ıFkıFFÕFŒF GEOLOGICAL SURVEY OF INDIA

Miscellaneous Publication

No. 30, Part III – ODISHA

⁄FFfi∂FU‹F ⁄F[ÊFY£FFPŒFÇ ıFÊFWaáFµF PÊFPÊFÕF “Ç FËFŒF ıFk -30⁄FFçF III

Published by order of the Government of India

2011

© Govt. of India

Controller of Publication

ISSN 0579-4706

PGSI. 337

700-2011 (DSK-II)


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© INDIA, GEOLOGICAL SURVEY (2011)● 1st Published 1974● 2nd edition 2012

Compiled by

the officers of Operation: Odisha

Manuscript processed for printing by

Ibha Chowdhury, Basudev Ray and Amjad Ali Senior Geologists

under the supervision of S Ramamurthy, D. K.Choudhury, K. Sanyal, B.C. Roy and Pradip De

DirectorsPublication Division,

Price:

Rs. 463.00 9 $ 6£

Published by the Director General, GSI, 27 J. L. Nehru Rd. Kolkata 700016 and printed at M/s Arunima Printing Works, 81 Simla Street, Kolkata 700006, Phone: 91-33-22411006, E-mail: [email protected]


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Foreword

A country’s economy depends on its natural resources, like the minerals and fuels for industry, soil for

agriculture and water for irrigation and power. The Geological Survey of India, the national agency, has

been carrying out Systematic Geological Mapping since 1851, to assess the potentiality of minerals

and fuels. It brings out the Geological Maps and Publications as the outcome of the geological work done. The

first edition of the, “Geology and Mineral Resources of the states of India, part-III, Orissa” was printed in 1974.

This series of publication gives an up to date account of the geology and mineral resources of the state.

A lot of data has been accrued to the Specialized Thematic Mapping, Quaternary / Geological Mapping,

Exploration of the minerals and research oriented projects. This immense data is synthesized in the present

volume. Odisha is bestowed with rich resources of Iron, Bauxite and Chromite. The minerals of the state, viz.,

nickel, manganese, cassiterite and vanadiferous magnetite are promising. Most of the mineral deposits of the

state are of the proven category. Owing to the discovery of Late Quaternary Volcanic Ash in river basins, the

Quaternary Geology of Odisha is defined for the first time, as will be seen in this volume.

The state of Odisha is swayed by the Precambrian rocks, over an area of 89,000 sq. km. The Dimension

Stones, having a wide variety, about twenty in number, and lineated all over the compass of the state, owe their

origin to the Eastern Ghat Mobile Belt, Singhbhum-Bastar Cratonic intrusives like anorthosite, granophyre,

alkali syenites and gabbro-dolerite dykes, etc. The chapter on ‘Dimension Stone’ is included in this volume to

provide information on its occurrence, mining feasibility and district wise locations.

The information furnished in this publication will be of immense help to district level administrators dealing

with the planning; geoscientists, academicians, entrepreneurs, students, and to them aspiring for the welfare

and development of the state which, in turn, will step up the commitments of Geological Survey of India to

contribute/ disseminate geoscientific information.

Kolkata (A. Sundaramoorthy)

Dated Director General

Geological Survey of India


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iv

Rocks are records of events that took place at the time they formed.

They are books. They have a different vocabulary,

a dif ferent alphabet, but you learn how to read them.

JOHN MCPHEE


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Contents

Page

FORWORD iii

INTRODUCTION 1

PHYSIOGRAPHY AND DRAINAGE 2

GENERAL GEOLOGY AND STRATIGRAPHY 3

GEOLOGY OF THE PRECAMBRIAN TECTONIC DOMAINS 3

Eastern Indian Craton (ELC) and Singbhum-Gangpur Mobile Belt 3Archaean 5

Archaean-Proterozoic 8

Proterozoic (Undifferentiated) 9

Palaeo Proterozoic 10

Bastar Craton 14

Archaean 14

Archaean- Proterozoic 14

Proterozoic 14

Meso-Neoproterozoic 15

Eastern Ghat Mobile Belt 16

Archaean-proterozoic 17

Gondwana Supergroup 23

Palaeozoic-Mesozoic 23Late Cretaceous Volcanics and Sediments 25

Cainozoic Formations 26

Tertiary Formations 26

Quaternary Formations 27

MINERAL RESOURCES 31Asbestos 31

Kalahandi District: 31

Sundargarh District 31

Mayurbhanj District 31

Basemetals 31

Lead & Zinc 31

Sundargarh district 31Mayurbhanj District 32

Bolangir District 32

Kalahandi District 32

Deogarh District 32

Copper 32


Sambalpur district 33

H∞UËFF Ç F ⁄F[PÊF£FFŒF JÊFk äFPŒF°F ıFkıFFÕFŒF GEOLOGY AND MINERAL RESOURCES OF ODISHA


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viii

Bauxite 33

Kendujhar District 33

Phulbani District 34



Nuapada District 34Rayagada District 34

Beach Sand Minerals 34

Cassiterite (TIN ORE) 34

Malkangiri District 34

Sonepur District 35

Boudh district 35

Malkangiri District 35

CLAY 35

China Clay 35

Koraput District 35

Cuttack District 35

Dhenkanal District 35

Sundergarh District 35

Ganjam District 36



Balasore District 36


Bolangir District: 36

Fire Clay 37

Sundergarh district 37

Cuttack District 37

Puri District 37


Sambalpur District 37COAL 37

Talchir Coal Field 38

Ib River Coal field 38

Chromite 39

Jajpur District 39



Balasore District 42

Koraput District 42


Gemstones 42

Kalahandi District 42

Bolangir District 42Sonepur District 43

Sambalpur District 43

Nuapada District 43

Rayagada District 43

Boudh District 43

Angul District 44

Deogarh District 44

Page


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ix

Jharsuguda District 44


Glass Sand 44

Cuttack District 44



Koraput district 44

Mayurbhanj district 44

Gold 44

Angul District 44


Koraput district 45


Sundargarh district 46


Graphite 46

1. Sargipalli Belt 46

2. Titlagarh Belt 47

3. Tumudibandh belt 47

4. Nishikal – Kinchikhal Belt 47

5. Muniguda belt 47

6. Dhandatapa Belt 48

Iron Ore 48

Sundargarh district 49

Kendujhar district 49

Kyanite 50

Angul district 50



Limestone and Dolomite 50

Sundergarhgarh district 50Biramitrapur 50

Lanjiberna 50

Purnapani 50

Hatibari 51

Pahartoli 51

Dublabera 51

Gotitanger 51

Khatukurbahal 51

Purkapali 51

Koraput district 51

Malkangiri district 51

Nawarangpur district 51

Baragarh district 52Kedunjhar district 52

Nuapada district 52

Manganese 52

Bolangir district: 53



Mica 54

Kalahandi district 54

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Koraput district 54

Phulbani district 54

Bolangir district 54

Sundergarh distric 54

Nickel 54

Jajpur district 54Kendujhar distric 55


Platinum 55

Jajpur district 55



Pyrophyllite 56

Quartz / Quartzite 56


Bolangir district 56

Sillimanite 56

Sundergarh district: 56


Soapstone 57

Cuttack district 57


Koraput district 57



Vanadiferous Magnetite 57


Kendujhar and Balasore Districts 58

Dimension Stone-Granite 58

Ganjam-Nayagarh-Khurda-Cuttack-Phulbani-Baudh Segment 59

Koraput-Rayagada Segment 59Kalahandi-Bolangir-Nuapada Segment 59

Sambalpur-Deogarh-Sundergarh segment 59

Sambalpur-Angul-Dhenkanal Segment: 59

Kendujhar-Mayurbhanja-Balasore Segment 59

Resources 60

Districtwise Occurrence of different Commercial varieties of Dimension Stone-Granite 60

REFERENCES 62

LOCALITY INDEX 70

APPENDIX 74

PLATE : Geological and Mineral map of Odisha (1:2,000,000 scale)

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MISC. PUB. NO. 30(III) 1

Introduction

The State of Odisha lying along the east coast of Indiawithin latitudes 17o48’ – 22o34’ North and longitude81o24’ – 87o29’ East, has an area of about 1,55,842 Sq.kmand a sprawling 480 km of coastline against Bay of Bengalto the east. It is bounded by the states of Jharkhand, AndhraPradesh, Chhattisgarh, and West Bengal to the north,south, west, and northeast respectively. The statecomprises dominantly of Pre-cambrian rocks (73%)ranging in age from Mesoarchaean to Neoproterozoic.Phanerozoic rocks, represented by the GondwanaSupergroup (Late Palaeozoic – Middle/Late Mesozoic)and minor Tertiary patches, constituting about 8% of thestate. The remaining 19% of the state is covered byQuaternary formations.

In view of its vast mineral resources and excellentlypreserved rock record ranging in age from EarlyPrecambrian to Recent, the state represents a veritable

paradise for earth scientists and justifiably remained thehunting ground for geologists ever since the beginningof geological studies in India in 1850s. Since then forover a century, several scientific studies were made.These include : (i) recognition of the Talchir boulderbed, postulation of early Gondwana glaciationhypothesis and discovery of the coal measures of Talchirand Ib river basins (Oldham, 1856; Blanford, 1872 andBall, 1877) (ii) studies on aluminous laterites andbauxites (Ball, 1877; Fox, 1934, 1942 and Krishnan,1935) (iii) coining of the term khondalite for the highgrade metasupracrustals of the Eastern Ghats belt after

the Khond inhabitants of Kalahandi (Walker, 1902), (iv)

discovery of major iron ore deposits at Gorumahisani –Badampahar area of Mayurbhanj (Bose, 1907) (v)discovery of Tertiary beds near Baripada (Bose, 1904)(v) classification of manganese ores (Fermor, 1909), (vii)studies on charnockite rocks (Fermor, 1911; Crookshank,1938; Ghosh, 1941), (viii) delineation of major iron-oredeposits of Bonai-Keonjhar region (Jones, 1934), (ix)studies on Gangpur Group of Metasediments(Krishnan,1937) and(x) identification of LateQuaternary volcanic ash in major river basins of Odisha(Devdas & Meshram, 1991)

Geological mapping and mineral explorationprogrammes in the state gathered appreciable momentumin post-independent India. Presently, the entire state hasbeen geologically mapped on 1:50,000/1:63,360 scaleby GSI. In addition, several crucial segments have alsobeen mapped on 1:25,000 scale. Besides GSI, other

Government agencies (State Directorate of Mines andGeology, Atomic Minerals Division, NGRI, OdishaMining Corporation and CMPDI etc.), many universitiesand research institutions have also contributedsignificantly to enrich our knowledge on the geologyand mineral resources of the state. An up-to-date synopsisof available information on the geological framework and mineral resources of Odisha is presented in thiscompilation. The text is accompanied by a 1:2,000,000compiled Geological and Mineral map of the state.During compilation, unpublished/ published informationof the department and published literature have been

consulted.

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Physiography and Drainage

Odisha is divisible into four major physiographicregions: the Northern Plateau, the Central River Basin,the Eastern Ghats hill ranges and the Coastal Plains.

The Northern plateau, covering the districts of

Mayurbhanj, Keonjhar, Deogarh, Sundargarh and partsof Dhenkanal, Balasore and Sambalpur, is an undulatingcountry having a general slope from north to south. Theaverage elevation of the plateau in the central area,forming the watershed of the Brahmani and Baitaranirivers, is about 1000 m above M.S.L. Hill ranges mark the northeastern part of the plateau with elevations above1000 m. Notable peaks are represented by Malaygiri(1188 m) in Dhenkanal district, Mankadanacha (1117m) in Kendujhar district and Meghasani (1166 m) inMayurbhanj district.

The Central River Basin occurs between the

Northern Plateau and the Eastern Ghat hill ranges andcovers parts of Bolangir, Sambalpur, Dhenkanal andCuttack districts. It comprises the catchment areas of the major rivers of the state, viz., Mahanadi, Brahmani,Tel and Baitarani rivers and their tributaries. Thoughlargely a peneplain, the Central River Basin isoccasionally marked by isolated hills, which rise abruptlyfrom the plains.

In the south and southwestern parts of the state, theEastern Ghats hill ranges stretch for about 400 km in aNNE-SSW direction covering the districts of Koraput,

Navrangpur, Malkanagiri, Ganjam, Kalahandi, Boudh,Phulbani and parts of Puri, Khurda, Cuttack, Dhenkanal

and Bolangir districts. Most of this segment has a generalelevation of ~ 900 m above M.S.L. and form thewatershed of some rivers. Major hill ranges in the EasternGhats rise above 1500 m; the notable peaks beingDeomali (1673 m) and Turiakonda (1599 m) in Koraput

district and Mahendragiri (1531 m) in Ganjam district.

The Coastal Plains form an extensive alluvial tractlying between the Eastern Ghat hill ranges and the coast.It stretches for about 480 km and include parts of Balasore, Cuttack, Puri and Ganjam districts. The ChilkaLake, the widest lagoon in India, is a prominent coastalfeature of Odisha.

The major rivers in Odisha are represented byMahanadi, Brahmani and Baitarani, others areSubarnarekha, Burhabalang, Indravati, Vansadhara,Nagavalli, Kolab, Rushikulya and Machkund. The

Northern Plateau is drained by the Baitarani,Subarnarekha and Burhabalang river systems, all flowingeastward through the coastal plains to the Bay of Bengal.The Central River Basin, consisting of the Gondwanagraben, is drained by the Ib-Mahanadi and Brahmani riversystems. These rivers also flow eastward into the Bay of Bengal. The Eastern Ghats hill ranges are drained bynorth and north-easterly flowing Tel River, southerlyflowing Vanshadhara and Nagavalli rivers and westerlyand south-westerly flowing Machhkund, Indravati andKolab rivers. The tributaries of the Rushikulya River inthe Eastern Ghats hill ranges flow in the N-S direction

and the Rushikulya River flows eastwards in the coastalplains into the Bay of Bengal.

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The State of Odisha exposes rocks ranging in agefrom Meso archaean to Recent. The generalizedgeological succession of rocks, is given in Table-I.

The Precambrian terrain in the state represents the

northeastern extension of the Indian Precambrian Shieldand exposes parts of two major cratonic domains (theEastern Indian Craton and Bastar Craton) as well asbordering mobile belts (parts of the Eastern Ghat MobileBelt and the Singhbhum - Gangpur segment of theSatpura Mobile Belt). The cratonic domains preserveappreciable volumes of medium to low-gradesupracrustal rocks as disconnected belts withingranitoids. The mosaic of granitoids and supracrustalrocks is overlain, at places, by platformal sedimentary/ volcano sedimentary successions and intruded by severalgenerations of mafic/ultramafic rocks, dyke swarms,younger granitoids and acid volcanics. The Eastern Ghat

Mobile Belt (EGMB) borders the Eastern Indian Craton(EIC) to the south and part of the Bastar Craton (BC) tothe east. EGMB exposes mainly high-grade granulitesderived from both sedimentary and igneous protoliths,granitoids and a varied assemblage of intrusive plutonicrocks. The Singhbhum – Gangpur segment of the SatpuraMobile Belt borders the EIC to the north and exposesmedium-grade supracrustal assemblages, mafic-ultramafic rocks and granite intrusives. The geographicdistributions of the major Precambrian lithotectonicdomains are :

● Eastern Indian Craton : Northern and(North Odisha Craton) Northwesternand Singhbhum-Gangpur OdishaMobile Belt

● Part of Bastar Craton : Western Odisha● Part of Eastern Ghats : Central and

Mobile Belt(EGMB) southernOdisha

The Phanerozoic rocks in the state are representedby the non-marine continental facies rocks of GondwanaSupergroup (Upper Palaeozoic–Upper Mesozoic) andthe marine Baripada Beds (Lower Tertiary). TheQuaternary formations are represented by laterite,

bauxite, sandstone and Quaternary sediments (includingvolcanic ash beds).

GEOLOGY OF THE PRECAMBRIAN

TECTONIC DOMAINS

Eastern Indian Craton (EIC) and Singbhum-Gangpur Mobile Belt

EIC represents an Archaean – Palaeoproterozoicgranite-greenstone terrain. It is bounded by two crustal-scale shear/thrust zones, viz., the Singhbhum (copperbelt) shear zone in the north (exposed in the state of

Jharkhand) and the Gohira – Sukinda shear/thrust zonein the south. These two shear/thrust zones isolate theEIC from the Singhbhum – Gangpur segment of theSatpura Mobile Belt occurring in the north & northeastand the EGMB occurring in the south respectively.

Despite several years of studies by a large numberof workers, the lithostratigraphic classification andcorrelation of the low-grade supracrustal rocks of theEIC and their time relation with the spatially associatedgranitoid components continue to remain debated. Majorlithostratigraphic components of the EIC, as envisaged

and designated by a large number of workers throughseveral years of work are enlisted below:

Supracrustal sequences : Older MetamorphicGroup (OMG), Iron Ore Supergroup, Garumahisani –Badampahar Group, Bonai Group (Lower and Upper),Dhanjori Group, Simlipal Group, Kolhan Group etc.

General Geology and Stratigraphy

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4 GEOL. SURV. IND

T a b l e - I

G e n e r a l i s e d s t r a t i g r a p h

i c s u c c e s s i o n o f t h e r o c k s o f d i f f e r e n t d

o m a i n s i n O d i s h a

A G E

S U P E R

G R O U P / G R O U P / F O R M A T I O N

L t . P l e i s t o c e n e t o E a r l y H o l o

c e n e

P r e s e n t d a y f o r m a t i o n ; B a

n k i g a r h F o r m a t i o n ; K a i m u n d i F o r m a t i o n ; B o l g a r h / N a i r a F o r m a t i o n

M i o c e n e

B a r i p a d a F o r m a t i o n

L o w e r C r e t a c e o u s t o P a l a e o c e n e

M i n o r I n t e r T r a p p e a n s

P e r m o - c a r b o n i f e r o u s t o l o w e r

J u r a s s i c C r e t a c e o u s

A t g

a r h F o r m a t i o n

C r e t a c e o u s

U p . P e r m i a n t o T r i a s s i c

K a m t h i F o r m a t i o n

M a h a d e v a F o r m a t i o n

R a

n i g a n j F o r m a t i o n

G o n d w a n a S u p e r g r o u p

U p . P e r m i a n t o L r . T r i a s s i c

B a r r e n M e a s u r e

E a r l y P e r m i a n

B a

r a k a r F o r m a t i o n

K a

r h a r b a r i F o r m a t i o n

L r . C a r b . T o P e r m a i n

T a l c h i r F o r m a t i o n

E A S T I N D I A

C R A T O N

& S I N G H B H U M - G A N G P U R M O B I L E B

E L T

B A S T A R C R A T O N

E G M B

N e o P r o t e r o z o i c

G a

n g p u r G r a n i t i c

P t 3

I n d r a v a t i ( P t 2 3

i j )

G r a n i t o i d s ,

( P

t 3 g

)

( N e o )

M e s o N e o C

h h a t t i s g a r h C h a n d a r p u r ( P t 2 3 c c )

a n o r t h o s i t e s

P r o t e r o z o i c S

u p e r g r o u p

S a b a r i G r o u p ( P t 2 3 s b ) A l k a l i n e

C o m p l e x e s

P a l a e o N e o

K o l h a n G r o u p ( P t 1 2

K h )

P t 2

P a i r i G r

o u p ( P t 2 P r )

P r o t e r o z o i c

( M e s o )

G r a n i t o i d

B h u a s a n i ( P t 1 b ) / T a m p a r k o l a ( P t 1 t ) /

R o m a p a h a r i ( P t 1 r )

P a l a e o

U p p e r B o n a i G r o u p ( p t 1 b ) /


S i m

l i p a l G r o u p ( P t 1 s i ) /

S i n

g h b h u m

G r o u p ( P t 1 s ) /

A l k a l i n

e & U l t r a m a f i c r o c k s ( P t s )

M i g m a

t i t e

G a

n g p u r G r o u p ( P t 1 g ) /

( P r o t e r o z o i c

u n d i f f e r e n t i a t e d )

G r o u p

D h a n j o r i G r o u p

( P t 1 d h ) /

B o n a i l a v a

( P t 1 b ) /

D a n g o a p o s i L a v a ( P t 1 d p ) /

D h a n j o r i L a v a ( P t 1 d h )

P t 1


G r a n o p h y r e ( M a y u r b h a n j G r a n i t e ( P t g )

( P a l a e o )

U n d i f f e r e n t i a t e d

N e w e r D o l e r i t e ( P t n )

G a

b b r o , n o r i t e , a n o r t h o s i t e ( P t )

G r a n

i t e g n e i s s e s a n d G r a n i t e s

E a s t e r n

( P t 1 / A ? P t 1 )

C h a r n o c k i t e

G h a t s

A R C H A E A N /

C h h o t a n a g p u r G n e i s s i c C o m p l e x ( A ? P t c )

G

r o u p

S u p e r

P R O T E R O Z O I C

U l t r a m a f i c s o f S u k i n d a - N u a s a h i ( A p t ) G r a n i t i c

A / P t

G r o u p

( A p t 1 b )

C o m p l e x o f N W O

d i s h a ( A p t 1 p )

B o n a i G r a n i t i c C o m p l e x ( G r a n i t o i d s o f

P a l l a h a r a , D e o g a r h , B h u b a n ) ( A p t 1 b )

K h o n d

a l i t e

L o w e r B o n a i G r o u p ( A p t 1 b )

I R O N

O R E

G r o u p

( A k )

S U P E

R

B e n g p a l G r o u p ( A b )

A R C H A E A N

G o

r u m a h i s a n i - B a d a m p a h a r G r .

G R O U P

( A g )

( A

s ) S B G r a n i t e / N i l g i r i G r a n i t e

( A o

t ) O M T G

( A o

) O M G

P R E C A M B R I A N


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Granitoids : Older Metamorphic Tonalitic Gneiss(OMTG), Singhbhum granitic complex, Bonai graniticcomplex, Nilgiri granitic complex, Mayurbhanj granite,Gneisses and granitoids of the Deogarh – Pallahara –Bhuban belt, Tamparkola granite – acid volcanics etc.

Mafic – ultramafic complexes : Baula – Nuasahiand Sukinda ultramafic complex.

Gabbro–anorthosite complexes : MayurbhanjGabbro- Anorthosite complex.

Mafic Dyke swarms: Newer Dolerite suite.

Singbhum-Gangpur Mobile Belt is represented byan arcuate segment stretching from north of Mayurbhanjdistrict in Odisha through Singhbhum district inJharkhand and further west to the Gangpur region of Odisha.It comprises an agglomeration of metasediments

of multiple depositional troughs with volcanics andvarious types of granitoids and igneous intrusives. Themetasediments and metavolcano sedimentaries along thismedium-grade (amphibolite-facies) mobile zone belongto two groups, viz. the Gangpur Group and theSinghbhum Group. Structural and geochronologicalstudies over the last three decades established that theGangpur-Singhbhum Groups of rocks form a curvilinearmedium-grade Proterozoic mobile zone skirting theArchean Eastern Indian Craton (EIC). The generalizedstratigraphic succession of EIC and Singbhum-Gangpur Mobile Belt is as follows:

Age wise (starting from Archaean) synopticgeological accounts of the major litho-stratigraphiccomponents of the EIC and Singbhum-GangpurMobile Belt are presented below.

Archaean

Older Metamorphic Group (OMG) : OMG,comprising a suite of amphibolite faciesmetasupracrustal rocks is considered to be the oldestrecognisable lithologic component of the EIC. Originallynamed as “Older Metamorphics” by Jones, (1934) and

designated as “Older Metamorphic Series” by Dunn,(1940), the suite was subsequently renamed as “OlderMetamorphic Group” (Sarkar and Saha, 1977). Thesetypically occur as enclaves ranging in size from a fewsquare meters to about 200 sq.km within youngergranitoids and gneisses. In terms of lithology, the OMGcomprises pelitic schists with several thick bands of paraamphibolite, relatively thin bands of quartzite, quartz-

sericite schist, local bands of quartz-magnetite –cummingtonite schists and talc-tremolite schists. Thetype area of the OMG is located west of Champua(22o04’E: 85o40’N) (Saha et al., 1988). Themetasediments of the OMG are intruded by sill-like

masses of ortho amphibolite and biotite -hornblende –bearing tonalitic – granodioritic rocks, the latterbelonging to the OMTG suite. The mineral assemblagein the OMG supracrustals indicates metamorphism inthe temperature range 620° C – 650°C at pressuresranging from 5-5.5 kb (Saha et al., 1984).

The OMG metasediments gave Ar-Ar (hornblende)ages of ca. 3.3 Ga and K-Ar (hornblende and biotite)ages of ca. 3.2 Ga (Sarkar et al., 1969; Baksi et al., 1987).On the basis of the above data, it is concluded that theclosing stage of metamorphism of the OMG

supracrustals as well as the associated OMTG suite of granitoids occurred at ca. 3.2 Ga (Saha et al., 1988).207Pb/ 206Pb dating of detrital zircons from OMGsupracrustals gave ages in the range 3.5 – 3.6 Ga andimplied an older limit of ca. 3.5 Ga for OMGsedimentation (Goswami et al., 1995; Mishra et al.,1999). U-Pb (zircon) dating studies by Basu et al., (1996)indicated a Pb-loss event at ca. 3.35 Ga.

Older Metamorphic Tonalitic Gneisses (OMTG) :OMTG comprises a suite of biotite – hornblende –bearing tonalitic – granodioritic gneisses. Believed by

most workers to be the oldest granitoid component inEIC, these intrude and partially granitise the OMGsupracrustals. These also occur as numerous rafts andenclaves of varying sizes in the younger granitoids. Thelargest patch of the OMTG rocks covers about 900 sq.kmextending from Champua in the west to Khiching in theeast and from Juldiha in the north to Palasponga in thesouth. Relatively smaller mappable enclaves of theOMTG rocks are also recorded near Rairangpur,Onlajhari and Asana – Manda areas (Saha et al., 1984).

The OMTG suite is considered to have beengenerated by moderate degrees of partial melting of

OMG ortho-amphibolitic rocks (Saha, 1994; Sharma etal., 1994). Moorbath et al., (1986) reported a whole-rock Pb-Pb isochron age of 3.38 Ga for the OMTG suite.The suite yielded Rb-Sr whole-rock isochron, K-Ar andAr-Ar ages in the range 3.0 – 3.2 Ga (Saha, 1994).

Dey (1991) reported dark-coloured tonalitic rafts asenclaves within Singhbhum Granite around Rairangpur.


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6 GEOL. SURV. IND

Designated as ‘Older Raft Tonalite or ‘ORT’, these rocksare considered by Dey (op. cit) to be the oldest granitoidcomponent in the EIC on which the supracrustals of Gorumahisani – Badampahar Group were deposited. Heconsidered the OMTG to be an earlier phase of

Singhbhum Granite and not related to ‘ORT’.

Singhbhum Granitic Complex: A major part of thegranite batholith, commonly referred to as theSinghbhum Granitic Complex, occupies large tracts inKeonjhar, Mayurbhanj and Dhenkanal districts of Odisha. The granitic complex, with numerous enclavesof granitised metasupracrustal rocks, cover an area of approximately 8,000 km2 of the EIC. This compositebatholithic complex comprises at least 12 magmaticbodies of biotite-granodiorite-adamellite-graniteemplaced in three distinct phases (Phase I - III) (Saha,

1972). Of the 12 magmatic bodies, 7 occur in the Stateof Odisha. Sarkar and Saha (1983), distinguished threephases of granitic activity in the batholith on the basisof increasing K

2O/Na

2O ratios. Phase-I rocks are

relatively K-poor granodiorite – trondhjemite whereasPhases – II & III comprise gradational suites of granodiorite – adamellite – granite. Subsequently, basedon REE patterns and Eu anomaly, Saha et al., (1988)grouped Phases – I & II into type-A (Singhbhum Granite/ SBG-A) and Phase – III into type-B (Singhbhum Granite/ SBG-B). From geochemical and geochronologicalstudies (Moorbath and Taylor, 1988; Ghosh et al., 1996;

Saha, 1994; Mishra et al., 1999), it was inferred that theSBG-A (Phases – I & II) was emplaced ca. 3.3 Ga go bypartial melting of freshly accreted amphibolite at thebase of the crust and SBG-B (Phase – III) was generatedat ca. 3.1 Ga ago by partial melting of a crustal protolith,probably a siliceous garnet-granulite (Saha et al., 1988;Saha, 1994). Saha et al. (1988) observed that only SBG-B (Phase-III) rocks show abundant enclaves of OMGsupracrustals, OMTG granitoids and Iron OreSupergroup supracrustals, whereas SBG-A (Phases – I& II) do not show such enclaves. The bulk chemicalcomposition of the composite batholith is estimated tobe granodioritic (Saha et al., 1984).

The Nilgiri Granite batholithic Complex coveringan area of approximately 1200 sq km occurs as an armof the eastern part of the Singhbhum Granitic Complexsouth of Simlipal and is separated from the mainSinghbhum granitic complex by a 5-8 km wide screenof metasupracrustal rocks. The massif is composed of tonalite – granodiorite – granite and migmatitic rocks.

According to Saha et al., (1984), the granite batholith iscomposite in nature and comprises four units. The Kaptipada tonalite – granodiorite and a granite suitefrom this complex have been dated at ca. 3.27 Ga andca. 2.37 Ga respectively by Rb-Sr whole-rock isochron

method (Vohra et al., 1991).

Iron Ore Supergroup (IOG): The BIF-bearing low-grade supracrustal sequences of IOG of the EIC are :Gorumahisani – Badampahar, Bonai – Kendujhar (alsoknown as Noamundi – Koira), Tomka – Daitari –(Mahagiri), Malayagiri and Deogarh. The mutualcorrelation of the above BIF-bearing sequences and theirstratigraphic relation with the granitoids arecontroversial. Three contrasting views exist in thisregard.

(i) All the isolated BIF-bearing supracrustalsequences of the EIC belong to a singlestratigraphic unit (Jones, 1934; Dunn, 1940; Dunnand Dey, 1942; Sarkar and Saha, 1962, 1977;Acharya, 1993; Sengupta et al., 1997. Sarkar andSaha (1962) redesignated all the BIF-bearingsupracrustals of the EIC as belonging to the ‘IronOre Group’ which were described earlier as IronOre Stage by previous workers. Dunn and Dey(1942) and Sarkar and Saha (1962) opined thatthe Singhbhum Granite is intrusive into the IOG.However, subsequently Saha et al., (1988)

considered that only part of the SinghbhumGranite (SBG-B) is intrusive into the IOG and theolder component (SBG-A) along with the OMGand OMTG suites formed the basement. However,several authors considered the SinghbhumGranitic complex as the basement for the IOGsupracrustals (Iyengar and Anand Alwar, 1965;Banerji, 1974; Mukhopadhyay, 1976; Banerjee,1982b).

(ii) According to Iyengar and Anand Alwar (1965),Iyengar and Banerjee (1964), Banerjee (1974),Iyengar and Murthy (1982) and Chakraborty andMajumdar (1986), the BIF-bearing supracrustalsequences belong to two stratigraphic units, theolder one typified by the Gorumahisani-Badampahar Group and the younger one typifiedby the Bonai – Kendujhar sequence (NoamundiGroup of Banerji, 1974). Iyengar and Banerjee(1964) correlated the Gorumahisani – Badampaharsequence with the Tomka – Daitari sequence.


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(iii) According to Prasad Rao et al., (1964) and Acharya,(1976, 1984), the BIF-bearing supracrustalsequences belong to at least three stratigraphicunits. In order of younging, these are:Gorumahisani, Tomka - Daitari and Bonai –

Kendujhar sequences. It may be noted that PrasadRao et al., (1964) envisaged at least six discretesequences of supracrustal rocks in parts of EIC inOdisha [including equivalents of Dhanjori andKolhan sequences for the fifth and sixth sequencesof Prasad Rao et al., (op.cit), Mazumder, 1978].

In general, rock types recorded in the various BIF-bearing metasupracrustal sequences are siliciclasticsediment, conglomerate, quartzite, quartz-schist, meta-argillite, ferruginous mica-schist, talc-tremolite,actinolite-chlorite and hornblende schist, amphibolite,

ferruginous shale and phyllites, banded haematite/ magnetite quartzite (BHQ/BMQ), banded haematite jasper (BHJ), banded chert, mafic/ultramafic rocks andvolcanics (both mafic and felsic) etc. Mineable iron and/ or manganese ore deposits characterize many of thesequences, viz., Gorumahisani – Badampahar, Bonai –Kendujhar, Gandhamardan, Tomka – Daitari (iron ore)and Bonai – Kendujhar (manganese ore). In detail, thereexists a subtle difference in the order, nature and packageof supracrustal assemblages in the various isolatedbasins.

The possibility of the existence of more than onegeneration of BIF-bearing sequences gained ground inGSI with the extension of mapping in different parts of the EIC. Iyengar and Murthy (1982) proposed the name‘Iron Ore Supergroup’ to include two sequences of BIF-bearing horizons, viz. older Badampahar Group(Gorumahisani Group of Banerji, 1974) and youngerKoira Group (includes BIF-bearing supracrustals of Bonai – Kendujhar area which is correlatable with theNoamundi Group of Banerji, 1974). The classificationand nomenclature of BIF-bearing formations, aspresently adopted in GSI are :

Iron Ore SupergroupLower Bonai Group (Archaean-Proterozoic)Gorumahisani–Badampahar Group (Archaean)

Archaean

Gorumahisani – Badampahar Group : In the type-area, Gorumahisani – Badampahar Group of rocks forman approx. 100 km long N-S trending easterly convex

arcuate belt extending from Rajnagar in SinghbhumDistrict to Jashipur in Mayurbhanj District. Themetasupracrustals in this belt comprises pillowedmetabasalts with interbedded chert, quartzite, BIF (BMQdominant), hornblende schists, epidiorite, and phyllite

with interlayers of acid volcanics and tuff. The maficvolcanics in the sequence are represented by frequentlypillowed and spinifex-textured peridotitic to basaltickomatiites, Sukinda high magnesia basalt (SHMB) andhigh-Mg tholeiites (Acharya, 1993). OMTG is reportedto intrude the Gorumahisani – Badampahar Group of rocks (Behera et al.1994; Jena and Behera, 1998).

The Tomka – Daitari, Malaygiri and Deogarh BIF-bearing sequences are considered to be equivalents of Gorumahisani – Badampahar Group (Prasad Rao et al.,1964; Iyengar and Murty, 1982; Banerjee et al., 1987).

The Tomka – Daitari sequence comprises metavolcanics,banded black chert, banded cherty quartzite andarenaceous to argillaceous phyllites in the basal part andBIF and quartzite in the upper part. The metalavas arerepresented by Sukinda high Mg-basalts (SHMB) andacid volcanics (Saha, 1994). The Malayagiri sequence,as depicted by Ray and Acharyya, 1997, comprisesschistose to pebbly quartzite/conglomerate and quartz-schists with interlayers of meta ultramafites in the basalpart followed successively by BIF, metapelites and meta-ultramafites.

The BIF-bearing supracrustal sequence of Deogarharea is exposed in the southwestern part of the EIC andhas been studied by GSI extensively for several years(Mazumder, 1996). The sequence overlies a migmatiticgranite-gneiss basement (with enclaves of tonaliticgneisses) with a basal polymictic conglomerate andcomprises quartzite, cherty quartzite with mica schist,phyllite, metapelite, psammopelite, metavolcanics andBIF. The supracrustal sequence is traversed by linearmasses of metapyroxenite and metagabbro. Micrograniticrocks, showing frequent gradations to sub-volcanicvariants intrude the sequence. The volcanic package inthe sequence is represented by high magnesia basalt(HMB), tholeiite, andesite, rhyodacite and rhyolite.

Stratigraphic relation between OMG and Gorumahisani – Badampahar Group: OMG rocks,considered to be the oldest supracrustals in the EIC, areexposed mainly in the Champua – Onlajhari areas of Kendujhar and Mayurbhanj districts. The continuousexposures of the Gorumahisani – Badampahar Group


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8 GEOL. SURV. IND

starts to appear near Jashipur and Raipada. TheSinghbhum Granitic Complex occupies the interveningzone between these two supracrustal belts, Recentdetailed mapping studies by GSI established thecontinuation of OMG-rocks across Singhbhum Granite

to Gorumahisani – Badampahar area through a chain of mappable xenoliths (Behera et al., 1994; Jena andBehera, 1998). Based on the above finding, Jena andBehera (op.cit) concluded that the supracrustal rocks of Champua (OMG) and Badampahar area (Gorumahisani– Badampahar Group) are temporally correlatable, thusreiterating the earlier opinion of Iyengar and Murty(1982). The OMTG suite shows distinct intrusiverelation with OMG supracrustals in the Champua –Onlajhari area.

Archaean-Proterozoic Lower Bonai Group: The Lower Bonai Group, in

its type area in the Bonai – Kendujhar region, exposesBIF-bearing horizons underlain by shale and volcanics(dominantly mafic with relatively minor acid andintermediate types), local dolomitic limestone,siliciclastic sediments and conglomerate. Shale andvolcanics overlie the BIF-bearing horizons in thissequence. Recent studies revealed that the BIF-bearingsupracrustals of the Bonai – Kendujhar area overlie bothSinghbhum and Bonai Granitic Complex with a basalquartz pebble conglomerate (QPC) horizon (Sinha et.al.,

1997) disposed in an asymmetric synclinal structure,described as ‘Horse Shoe Syncline’. A thick andextensive mafic volcanic – quartzite sequence flanks theBIF horizon of IOG rocks of Kendujhar – Bonai area(Lower Bonai Group) along its western, southern andeastern parts, is variously designated as Danguaposi Lava(Dunn, 1940; Banerjee, 1982b), Nuakot Volcanics(Iyengar and Murthy, 1982), Malangtoli Lava (Saha,1994), Nuakot Volcanic Province (Sahu et al., 1998).The basaltic flows of this sequence are in general quartz-normative and encompass the compositional range of tholeiitic basalt – basaltic andesite – andesite (Sahu etal.,op. cit.). The stratigraphic relation of thisvolcanosedimentary sequence with the IOG sedimentsof Bonai – Kendujhar area is highly debatable.

Bonai Granitic Complex : The Bonai GraniticComplex occurs to the west of the Singhbhum GraniteComplex. These two batholithic complexes are separatedby a wide belt (50-70 km) of supracrustal and volcanicrocks of the Iron Ore Supergroup. In areal extent, the

Bonai Granitic Complex is approximately one fifth of the size of the Singhbhum Granitic Complex (Sen, 2001).Essentially a composite granite batholith like theSinghbhum Granitic Complex, the Bonai GraniticComplex comprises mainly trondhjemite – granodiorite

– granite with zenolithic enclaves of older trondhjemiticrocks, banded gneisses, metasupracrustals, mafic/ ultramafic rocks, amphibolites and metalavas (Senguptaet al., 1991; Saha, 1994). The Pb-Pb and U-Pb (zircon)age of the xenolithic enclaves of older high Al

2O

3

trondhjemitic rocks range between 3.38 – 3.34 Gawhereas the younger host trondhjemites gave Pb-Pb ageof ca. 3.16 Ga (Sengupta et al., 1991, 1996).

The Granitoids of Deogarh – Pallahara – Bhuban Belt occurring in the south-central and south-westernparts of EIC, are variously designated as Pallahara

gneisses (Sarkar et al., 1990), Palkam Gneisses(Mahalik, 1994) etc. The granitic gneisses and granitoidsof this belt have several features, which distinguish themfrom the Singhbhum Granitic Complex and its temporalequivalents (Bonai, Nilgiri etc.). These include (i)syenomonzonitic affinity, (ii) presence of amphibole(hornblende, riebeckite) as mafic mineral with/withoutbiotite, (ii) presence of magnetite, allanite, zircon andprimary sphene as important accessories (Saha, 1994).The granitoids are often granophyric to microgranitic.

Recent mapping by GSI has revealed the presence

of mappable enclaves of biotite-tonalitic gneisses withinyounger granitoids in the Asanali area of the Deogarhsupracrustal belt. The younger granitoids (oftenmicrogranitic) in the Deogarh belt are emplaced alongmajor fractures/ductile shear zones and migmatise earliertonalitic – granodioritic gneisses. Several suites of theseyounger granitoids, showing distinct intrusive relationto the supracrustal sequences as well as older graniticgneisses, have yielded Rb-Sr whole-rock isochron agesin the range 2.3–2.4 Ga (GSI, unpublished data).?

From a 207Pb/ 206Pb (zircon) Ion Microprobe study,Mishra et al., (2000) infer a minimum age of 2.8 Ga for

some of the granitic gneisses of Bhuban area. The datedgranitic gneisses are reported to contain xenocrystalzircons of ca. 3.5 Ga age and show evidence of zirconovergrowth at ca. 2.48 Ga due to later metasomatic/ metamorphic effects (Mishra et al., op. cit).

Granitic Complex of Northwestern Odisha: In theKeshaibahal – Kuchinda belt of northwestern Odisha,


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Panda and Dash (1997) reported the presence of fourgenerations of granitoids. The oldest among these arecompositionally tonalitic to granodioritic. TheSambalpur Granite in this belt has been dated by Rb-Srwholerock isochron method at ca. 2.4 Ga (Choudhury

et al., 1996).

Mafic–Ultramafic Complex of Sukinda, Nuasahi:Major mafic-ultramafic complexes of the EIC are locatedin the Baula – Nuasahi and Sukinda areas. In addition,several small masses of mafic-ultramafic rocks areintermittently exposed along an arcuate belt in thesoutheastern marginal zones of the craton. In Baula –Nuasahi area of Kendujhar District, an ultramafic –mafic suite, comprising dunite – peridotite – pyroxeniteand gabbro/anorthosite, intrude meta-supracrustals(quartzite – quartz schist) equivalent to the Gorumahisani

– Badampahar Group. Granite and dolerite dyke swarm,in turn, intrude the ultramafic – mafic suite. The linearsteeply dipping intrusive mass extends for about 3 kmin N-S direction with a maximum width of 1 km. Thecomplex comprises an early suite represented byenstatitite/bronzitite, serpentinised dunite, hurzburgiteand chromitite and a younger suite of pyroxenite,metagabbro – leucogabbro (with Ti-V magnetite) (Nandaand Patra, 1994). The eastern marginal zones of thecomplex are brecciated. The complex hosts chromite,vanadium-bearing titaniferous magnetite and noble metalmineralization (Mukherjee, 1958, 1969; Auge et al.,

1999). The noble metal (PGE) mineralization in thecomplex is confined to the brecciated zones; thebrecciation of the ultramafic rocks has been induced bygabbro intrusion (Auge et al., op. cit). The gabbroic rocksof the complex (Bangur Gabbro) have yielded zircon(SHRIMP) age of 3122 ± 5 Ma making the Baula PGEmineralization as one of the oldest in the world (Augeet al., 2003). Auge et al., (op.cit) correlated the gabbro-anorthosites of this area with the Mayurbhanj Gabbro-Anorthosites.

Located in the Jajpur – Dhenkanal districts, theSukinda Complex occurs as a ~ 20 km long and 2-5 kmwide body trending ENE-WSW from Kansa to Maruabil.The complex is emplaced as a concordant mass withinmetasupracrustals of Tomka – Daitari – Mahagiri beltand is stated to form synformal structure in the host rocks(Banerjee, 1972; Chakrabarti et al., 1980). Basu et al.,(1997) considered the complex to be an integral part of the metasupracrustal, volcano-sedimentary sequence of Iron Ore Group. The intrusion comprises magnesite-

bearing serpentinised ultramafics (dunite-peridotite)with chromitite and pyroxenite and a major source of chromitite ore and the complex hosts six fairly thick (10-40m) chromite seams. High degree of lateritisationof the ultramafic rocks of the complex has given rise to

a nickeliferous laterite cover. The complex is intrudedby granitoids of ca. 2.3 Ga age (GSI, unpub. data) anddolerite dykes.

Page et al., (1985) opined that the Baula – Nuasahiand Sukinda complexes have ophiolitic affinity. Bose(2002) envisaged arc-type magmatism to explain thelithotectonic milieu of the mafic-ultramafic complexes.

Chhotanagpur Gneissic Complex : ChhotanagpurGneissic Complex is a composite mass of Archaean (?)to undifferentiated Proterozoic age and comprises mainly

granite gneiss, migmatites and composite gneiss withenclaves of para and ortho metamorphites, dolerite dykesand veins of pegmatite, aplite and quartz. A vast stretchof adjacent Jharkhand state is occupied by this gneissiccomplex and a small part of it extends southward andoccupies the northwestern part of Odisha in contact withGangpur Group of rocks.The para metamorphitesinclude crystalline limestone, calc-granulite,calc-silicaterocks and mica schist whereas the orthometamorphitesare represented by hornblende schist, metagabbro,anorthosite, metapyroxenite, metanorite, pyroxenegranulite, etc. The rocks of this complex generally trend

in NE-SW to ENE-WSW with moderate (40°

-50°

) dipstowards north.

Proterozoic (Undifferentiated)

Gabbro - anorthosite Complex : In Gorumahisaniarea of Mayurbhanj district, flanking the SimlipalComplex, gabbro-anorthositic rocks are reported. Theseare reported to intrude the meta supracrustal rocks of the Gorumahisani – Badampahar Group as well as theSinghbhum Granitic Complex (Saha et al., 1977;Chakrabarty et al., 1981). Auge et al., (2003) correlatedthe gabbro-anorthosites of this belt to the 3.122 Ma old

Bangur Gabbro of Baula area.

Newer Dolerite Suite of Dyke Swarms: Mafic dykeswarms constitute an important lithologic componentin the EIC and occur extensively in Singhbhum,Kendujhar and Mayurbhanj districts of Jharkhand andOdisha. Dunn and Dey (1942) coined the term ‘NewerDolerite’ to collectively denote these dyke swarms,


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10 GEOL. SURV. IND

which according to them represented the youngeststratigraphic unit in the terrain. The dykes are representedmainly by dolerites and gabbros, though minorultramafic, noritic and granophyric dykes are alsoreported. The dykes show broadly four orientations, viz.,

NE-SW, NW-SE, N-S and E-W of which the first twoare more common (Guha, 1963). Saha et al., (1973)distinguished three petrogenetic types in the ‘NewerDolerite’ suite viz., (i) accumulates (ultramafic andnoritic dykes), (ii) products of direct crystallization(dolerite – gabbro) and (iii) products of partial melting(leucogranophyric dykes). Reported K-Ar ages of thedykes range from 923-2144 Ma (Sarkar et al., 1969;Sarkar and Saha, 1977; Mallick and Sarkar, 1994).Mallick and Sarkar (1994) inferred three periods of maficdyke activity at 2100 ± 100 Ma, 1500 ± 10 Ma and 1100± 200 Ma. Verma and Prasad (1974) inferred the presence

of at least three generations of mafic dykes frompalaeomagnetic studies. Available data thus suggestmultiple generations of mafic dyke activity in the EIC.It may be noted that different generations of dykes havedistinct geochemical signatures (Mallick and Sarkar,1994).

Palaeo Proterozoic

Upper Bonai Group : The supracrustal sequences,lying west of the Bonai Granitic Complex, was mappedand described by Prasad Rao et al., (1964) and

Ramachandran and Raju (1982). Though subsequently

studied by many workers, the basic stratigraphicframework provided by the earlier workers has remainedunchanged. The lithostratigraphy of the various units inthis belt is given in Table – 2.

Three groups of supracrustals occur in the areaintervened by unconformities and intrusive and/orextrusive granitic activity. The rocks belonging to theoldest sequence (Group – I) are intruded by componentsof Bonai Granitic Complex and are correlated with theGorumahisani – Badampahar Group. Enclaves of theserocks abound in the Bonai Granitic Complex. TheGroup-II supracrustals rest over the Bonai granitoids aswell as the Gorumahisani – Badampahar Group with apronounced polymictic basal conglomerate with pebblesof fuchsite quartzite, banded chert, heamatite jasper andbasic rocks (Ramachandran and Raju, 1982). This

sequence lacks BIF and is designated as the Upper BonaiGroup. The Group – II or the Upper Bonai Groupdefines a northerly plunging synformal structure(Ramachandran and Raju, op. cit). They observed thatthe synformal fold is a syncline as it contains youngestbed at the core. The Upper Bonai Group of supracrustalsare intruded by granite (Tamparkola) – acid volcanicassociation (ca.2.8 Ga old).

The Group – III sequence overlies the Group – II rockswith a faulted contact for the most part and is reported toshow progressive Barrovian metamorphic zones from

south to north and finally merges with the Gangpur Group

Table – 2: Lithostratigraphy of rocks occurring west of Bonai Granitic Complex

(Modified after Ramachandran and Raju, 1982)

Group – III Garnet – staurolite bearing argillaceous schists with calc-silicate/calc-gneiss rocks; carbonphyllites – quartzites ——————————————————— Unconformity ————————————————Granite – acid volcanics (Tamparkola)

Group – II Ultrabasic/basic sills and dykesLava flows and tuffsFerruginous shaleIntraformational conglomerateMeta lavaIntercalated argillaceous and arenaceous

sedimentsBasal conglomerate ——————————————————— Unconformity ————————————————Granitoids of the Bonai Complex

Group – I Sheared quartz reefsMetabasic/ultrabasic intrusivesMetavolcanics (metalava, chlorite-schist, amphibolite etc.)Fuchsite quartzite, quartz-schist, mica-schistsBase not seen


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of rocks and post-dates intrusion of Tamparkola granitoids(Ramachandran and Raju, op.cit). The Group – III rocks,representing transition between the cratonic Upper BonaiGroup (correlated with Dhanjori sequence) and theGangpur Group of mobile zone are correlated with the

lower horizons (Chaibasa Formation) of the SinghbhumGroup. Mahalik (1987) combined all the lithologies lyingabove Bonai Granite (including Group – III supracrustals)under Darjing Group.

Dhanjori Group : The Dhanjori volcanosedimentarysequence (Dunn and Dey, 1942) is located in the NNEedge of the EIC. The sequence comprises a lowerformation (Lower Dhanjori Formation) dominated bymetapelites with volcanogenic components followedupwards by quartzite and conglomerate. The LowerDhanjori Formation is intruded by mafic-ultramafic

intrusives and interlayered with acid volcanics andintermittent Au-W-U bearing quartz pebbleconglomerate (QPC) bands (Gupta et al., 1985). Thepredominantly volcanic Upper Dhanjori formationcomprises high-Mg volcaniclastic, basaltic komatiite,alkali olivine basalt overlain by low-K tholeiiticmetabasalt (Gupta et al., op.cit). The type sequence of Dhanjori Group is confined within the geographicallimits of the State of Jharkhand. Iyengar and AnandAlwar, (1965) opined that the Dhanjori Group of rocksoverlie the Iron Ore Supergroup of rocks and arecorrelatable with the Simlipal Group.

Simlipal Group: Volcano-sedimentary rocks of theSimlipal basin has spectacular circular map pattern. Thislarge basin overlies the Gorumahisani – BadampaharGroup in its type area and is isolated from the Dhanjoribasin by the Mayurbhanj Granite batholith. The sequencestarts with a basal conglomerate and a dark phyllitesucceeded by a zone of volcanic breccia, spilitic lavaand tuff intercalated with quartzite. In this basin,volcanism was interspersed with sedimentation. Thevolcanic rocks in the basin are represented mainly byspilitic lava of ocean-floor affinity and extensive acidvolcanics. The volcanics alternating with siliciclasticsediments are intruded by mafic-ultramafic intrusives.A highly differentiated ~ 800 m thick sill (Amjhori Sill)(dunite – peridotite – picrite – gabbro – quartz diorite)occurs at the centre of the basin (Iyengar and Banerjee,1964; Iyengar et al., 1964; Iyengar and Anand Alwar,1965; Iyengar et al., 1981a).

Singhbhum Group : The Singhbhum Group,

represented by a lower arenaceous and an upperarenaceous to argillaceous and carbonaceousmetasedimentary sequence unconformably overlying theDhanjori and Gorumahisani Groups, occupy a very smallportion at the northeastern border of Odisha. This group

of metasediments of Singhbhum Mobile Belt is actuallybest developed in the north, covering a large area of adjoining Singhbhum district of Jharkhand State. Thebasal conglomerate contains pebbles of fuchsitequartzite, banded grey white chert, haematite-jasper andbasic rocks. In addition, there are four intraformationalconglomerate beds at different stratigraphic levels of thissequence. A crustal-scale ductile shear zone(Singhbhumshear zone) with polymetallic mineralization (speciallycopper) has affected the Singhbhum, Dhanjori andGorumahisani Group of rocks and running in an arcuateE-W to NW-SE direction entered into the Mayurbhanj

district of Odisha with a southeasterly swing and dieddown into the alluvium to the south of Kesharpur(22°07’:85°41’) . In Odisha, this group of rocks is represented byconglomerate, quartzite, mica schist, phyllite,garnetiferous phyllite, hornblende schist and epidioritewith repeated cycle of sedimentation forming severalbands of same rock formation in different stratigraphichorizons. These rocks are disposed in a NNW - SSE toN-S trends with moderate to high angle (45° - 65°) diptowards east and form a major northerly plungingsynform around the syntectonic Romapahari Granite asits core at Kesharpur- Dudhiasol –Madansahi copper

prospect. Both the rocks of core and limbs bear theimprints of shearing and faulting. Intrusive and extrusiveigneous activities, represented by meta ultramafic andmafic sills and dykes (now amphibolite) are alsorecorded in this sequence. Proterozoic Singhbhum Groupstratigraphically correlatable with the Gangpur Group,have signatures of polyphase deformation,metamorphism and crustal reworking.

Gangpur Group : In the northwestern part of Odisha,a Group of psammopelite and calcareous metasedimentswith a basal sheared conglomerate is found tounconformably overlie the Lower Bonai Group forminga conspicuous hill range all along its southern bounderyand was described as Gangpur Series byKrishnan(1937). This group of metaspracrustalsbelonging to Singhbhum-Gangpur Mobile Belt of Lower Proterozoic age include a sequence of arenaceous,carbonaceous, calcareous,and argillaceous rocks. Thebasal conglomerate which marks an erosionalunconformity is designated as Raghunathpally


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12 GEOL. SURV. IND

conglomerate and contains pebbles of vein quartz,greyquartzite, and carbonaceous quartzite. Earlier, theGangpur Group of rocks were believed to be folded intoa sigmoidal anticlinorium plunging eastward (Krishnan,1937) and were overlain by the Iron Ore Series of rocks

of Jones(1934). Subsequent studies (Banerjee, 1968;Kanungo and Mahalik, 1967, 1975) revealed that theGangpur Group of rocks are disposed in a synclinoriumand is younger than the Iron Ore Group.However recentlypublished geological quadrangle map (GQM) of 73 Bconfirms the fold to be synclinal synclinorium. The basalconglomerate band is succeeded upward by mica schistsand phyllites containing thin bands and lenses of Gondite.The carbonaceous and calcareous beds occurring moreor less continuously in definite horizon form thelithostratigraphic marker horizons. The carbonaceousrocks with small lenses of banded magnetite quartzite

are invaded by basic sills at several places, representedby epidiorite, amphibolite, and talc chlorite schist. Therevised lithostratigraphic succession of the GangpurGroup as established by GSI in the Sundargarh Districtof Odisha (Banerjee, 1968) is given below:

• Dublabera Dolomite• Jharbera carbonaceous phyllite and quartzite• Mica schist and Gondites• Kumarmunda banded carbonaceous quartzite• Grey and purple phyllite and quartzite• Birmitrapur – Lanjiberna Limestone and dolomite

• Laingar carbon-quartz phyllite• Katang Limestone and dolomite• Mica-schist and quartzite• Raghunathpalli Conglomerate

Based on the palaeocurrent data of the Gangpurrocks,Kanungo and Mahalik (1975) suggested that thesediments are transported from the southern cratonicdomain. The palaeoslope directions reported for boththe Gangpur and Singhbhum Groups indicate northerlysediment transport from south (see Mazumder, 1978 andthe references therein). The Gangpur Group is correlatedwith the Singhbhum Group (Annon, 1974). Structuralstudies by Chaudhuri et al., (1980) indicated that thetectonic history of the Gangpur Group is similar to thatof the Chaibasa Formation (lower stratigraphic horizonof the Singhbhum Group). This justifies the correlationof the Gangpur Group with the Singhbhum Group ratherthan considering it to be homotaxial with the Kolhansas postulated by Iyenger and Murthy (1982).

Mafic sills and dykes and several small stocks of S-type Neoproterozoic granitoids (Etma, Ekma, Timnaetc.) intrude the Gangpur Group of rocks. The rocks bearevidence of multiple deformation and metamorphismresulting in disruption of earlier fold geometry and

thermal metamorphism of surrounding sediments .Banerjee (1968) envisaged at least two episodes of prograde metamorphism: the first one leading to thedevelopment of garnet-bearing assemblages.Development of staurolite is attributed to contactmetamorphism induced by later intrusion of granitoids.The S-type granitoids intruding the Gangpur Group haveyielded (Rb-Sr isochron )ages within the range 1000-800 Ma (Pandey et al., 1998).

Dhanjori Lava : In Odisha small exposures of Dhanjori lava are occurring in the north eastern part of

EIC, south of Rakha (Jharkhand), adjacent to easternpart of Singhbhum Granite and northern part of Mayurbhanj Granite. They are underlain by quartzitesand metapelites of Dhanjori Group. At places the lavasare interbedded with grey sericite phyllite .The Dhanjorilavas are fine grained epidiorite,which is a fine grainedhornblende rock with little quartz, occasionalfeldspar,and abundant epidote, and chlorite. Leucoxeneare also noticed in some cases.Sometimes the hornblendeis tremolitic. The rocks are vesicular-amygdaloidal, theamygdules are formed by epidote, chlorite,calcite andchalcedony. The Dhanjori lavas and interbedded tuffs

are sheared and metamorphosed to hornblende schistand biotite schist along the shear zone. From petrologicalpoint of view the Dhanjori lava shows a close similaritywith Dalma volcanics and they are thought to be nearlycontemporaneous (Saha,1994). The Dhanjorimetavolcanics are essentially tholeiitic in composition(Dunn and Dey,1942),while Gupta et al(1985) groupedthe Dhanjori metavolcanics into two units i.e a) Mafic-ultramafic high –Mg vitric tuff and b)Low K tholeiitewith locally alkali rich olivine basalt.

Bonai Lava (Malangtoli Lava): The thick andextensive mafic volcanic rocks flanking the Iron oreGroup of rocks of the ‘Horse Shoe Synclinorium’ of Bonai-Keonjhar region, along its western and southernparts are designated as Bonai lava (Malongtoli lava).The volcanics/lavas are exposed over 800 sq. Km. area(Saha, 1994) to the west of Kendujhargarh and the northof Palalahara (21 28’ : 85 15’). The lavas are in generalquartz-normative tholeiitic basalts – basaltic andesite –anderite in composition. The lavas are vesicular and the


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vesicles are filled up by quartz, chlorite – zeolite andchert. The lavas are, at places, intercalated with shaleand is associated with ash beds and agglomeratic rocks.

Close interbedded / intercalated relationship of lava

and shale probably indicates a sub aqueous origin forthe lava.

Dangoaposi / Jagannathpur Lava : An area of about200 sq. Km. lying south of Jagannathpur at the Jharkhand– Odisha border and at the NE corner of Horse Shoe isoccupied by Synclinorium composed of extensive flatlying lava flows – designated as Jagannathpur / Dangoaposi Lava, which are very weaklymetamorphosed, locally basaltic rocks of havingtholeiitic, andesitic in composition. The bulk composition of the basaltic rock is andesite tholeiite with

differentiates of oligoclase andesites.

Saha (1994) on the basis of major element chemistryand disposition opined that they represent continentalsetting of eruption. The K-Ar whole rock date (1629 +39 Ma) of Jagannathpur lava is probably suggestive of contemporaneity of the metamorphism of Dalma andJagannathpur lava suites (Saha, 1994).

Mayurbhanj Granite : Mayurbhanj Graniterepresents a composite granite batholith occurring alongthe eastern fringe of the EIC, flanking the Simlipal

complex . The batholith comprises three phases. In orderof emplacement, these are:

a) a fine-grained, homophanous, biotite-hornblendebearing granite with granophyric texture,representing the main Mayurbhanj Granite bodyoccurring along the northwestern and southeasternmargin of the Simlipal basin, A suite of MayurbhanjGranite has yielded a Rb-Sr whole rock isochronage of ca. 2.08 ± 0.7 Ga (Iyengar et al., 1981 b).The 207Pb/ 206Pb zircon ages (Ion Microprobe) of the granite are reported to be much higher, viz., :Phase – I : 3092 ± 5 Ma and Phase – II : 3080 ± 8

Ma (Mishra et al., 1999). According to them thisage may be considered as the time of broadstabilization of Singhbhum Craton.

b) a coarse grained, occasionally foliated andgneissose ferrohastingsite-biotite granitedesignated as Bhuasani Granite occurring as anelliptical body of an area around 15 sq. km at thenortheastern corner of the Simlipal complex in the

Chakdar pahar area( 22°00’;86° 30’).It is a solitarycomposite mass of sodagranite, considered to bean offshoot of Mayurbhanj Granite,composed of very fine grained matrix of quartz andfeldspar,(Iyengar,1956). Subsequent study revealed

that the body is a composite one with a core of moderately coarse ferrohastingsite-biotite granitewith granophyric textures enveloped by apliticleucogranite (Saha,1994).

c) a N-S elongated granite body designated asRomapahari Granite occurring at the northeasternextremity of Odisha state and at the Odisha-WestBengal border and west of Baharagora. It is finegrained, composed mostly of microclineperthite,quartz and oligoclase. Biotite is mostlyaltered and marginally granulated . Saha, (1994)defined it as biotite aplogranite.The Rb-Sr whole

rock isochron age of the Romapahari Granite isfound to be 1895±46 Ma (Saha,Op cit). Thesegranitic rocks, having ‘A’ type geochemical affinity,are reported to show intrusive relations withSinghbhum Granite, Iron Ore Supergroup, DhanjoriGroup, Singhbhum Group and the gabbro-norite-anorthosite suite of rocks (Saha et al., 1984).

Tamparkola Granite – Acid Volcanics : The granite– acid volcanics suite of Tamparkola crop out as aroughly ovoid body just west of the Upper Bonaisequence in western Odisha. The suite comprises

amphibole-bearing microgranite-granophyre – medium– grained granite along with rhyolitic volcanics. Thissilicic volcano-plutonic assemblage intrudes the olderGorumahisani – Badampahar Group of supracrustals aswell as the younger Upper Bonai sequence. Themicrogranitic suite from this association has yielded aRb-Sr whole rock isochron age of ca. 2.78 Ga (GSI,unpub. data). In situ Pb-Pb (zircon) dating by IonMicroprobe revealed the following ages : granite : 2809± 8 Ma, rhyolite : 2836 ± 67 (Bandopadhyay et al., 2001).

Kolhan Group : The Kolhan Group is representedby an undeformed platformal sequence comprising basalpolymictic conglomerate, fine to medium grained purplequartzite-sandstone, gritty quartzite with some shale-slate and minor limestone. The type area of this grouplies in Jharkhand state, north of Koira area. Only a fewpatchy exposures of this group, occurring as outliers,have been mapped in the Koira area of Odisha. Thepolymictic conglomerate at the base contains pebblesof banded iron formation, quartzite, vein quartz and at


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places iron ore. The pebbles in the Kolhan basalconglomerates indicate that the sequence was depositedas a platformal cover sediment over a basementcomprising the Singhbhum Granite and the Iron OreSupergroup of rocks. The outlier, occurring to the east

of Roida on Durgaparbat (toposheet 73 F/8), is the largestexposure of Kolhan sequence (~1sq. km) so far mappedin the Odisha state.

Bastar Craton

Part of the eastern marginal zone of the BastarCraton is exposed in western Odisha. This cratoniccrustal strip is bounded by the Mahanadi graben in thenortheast and the Eastern Ghats Mobile Belt in the eastand southeast. The major lithostratigraphic componentsof the Bastar Craton, exposed in parts of western Odisha

are : Archean supracrustals of the Bengpal and BailadilaGroups, granite gneisses and granitoids ranging inage from Neo archaean to Palaeoproterozoic, a widevariety of post-tectonic silicic intrusives with alkalineaffinity, mafic/ultramafic rocks and several Meso-Neoproterozoic sequences of platformal sediments.Agewise (starting from Archaean) synoptic geologicalaccounts of the major litho-stratigraphic components of the Bastar Craton are presented below.

Archaean

Archaean Supracrustals : The Archean supracrustalassemblages of the Bastar Craton are divisible into threemajor lithostratigraphic units. In order of younging, theseare represented by Sukma, Bengpal and BailadilaGroups (Crookshank, 1963; Ramakrishnan, 1990).Mappable exposures of supracrustal rocks belonging tothe Sukma and Bailadila Groups are not reported fromwestern Odisha. However, a small outcrop of interbanded quartzite and banded heamatite quartzite(BHQ), possibly belonging to the Bailadila Group, isrecorded in the Hirapur hills.

A group of low grade volcano-sedimentary rocks

exposed as small lenses and bands and also as long linear

bands within the granite gneiss-migmatite country at thesouthwestern part of Odisha near the border withChhattisgarh are called Bengpal Group after the nameof a small village Bengpal (18 ° 08 ; 81 ° 11 ’) inChhattisgarh from where they were first described. A

major outcrop of Bengpal Group of rocks is noted inthe Tulsi Dongar Hill Range area. The Bengpal Groupof rocks are represented by phyllite, quartz-sericiteschist, feldspathic quartzite,mica schist, andalusiteschists and gneiss,grunerite gneiss,BMQ,BHQ,amphibolites, ultrabasic rocks, talc-tremolite-chloriteschist . These are considered to be equivalents of therocks of Iron Ore Super Group (Gorumahisani Group)because of their similarity in lithological assemblage byiron bearing sediments with metavolcanic sequence andtheir age has been considered to be Archaean. TheBengpal group of rocks are exposed mostly in

Chhattisgarh and a small part has been extended toOdisha.

Archaean- Proterozoic

Granite-gneisses and Granites : The cratoniccrustal strip in western Odisha represent the immediatecratonic foreland to the Eastern Ghats Mobile Belt.Granite gneisses and granitoids constitute a significantlithologic component in this zone. The granitic gneissesare represented by epidote-hornblende-bearing fissilegneisses, hornblende-biotite gneisses, biotite-gneisses,

feldspathised pink porphyroblastic granite gneisses andbanded migmatitic gneisses. The granitic rocks aregenerally massive and contain amphibole and/or biotiteas mafic minerals. In contrast to the largely per-aluminous EGMB granitoids, these granitoids are largelymetaluminous and lack garnet. Granitoids of Neoarchean(?) and Palaeoproterozoic ages are reportedfrom this zone (Table-3).

Proterozoic

Alkaline and Ultramafic Rocks : In the Khariar –Paikmal – Padampur segment of western Odisha, several

post-tectonic dykes of granophyre, microgranite,

Table – 3. Isotopic ages of granitoids in the cratonic zone of western Odisha

Granitoids Age/method References

1. Granitic gneisses, west of Kolab 2.67 Ga (Rb-Sr WRI) Sarkar et al., (1994 a,b.c,d)2. Pujariguda granite 2.11 Ga (Rb-Sr WRI) Pandey et al., (1989)3. Cholanguda granite 2.30 Ga Pandey et al., (1989)


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analcime-bearing syenite, syenite, monzo syenite gradingto garnet – hornblende – biotite albite syenite arerecorded within granitic gneisses of Bastar Craton closeto the EGMB. The rocks are unmetamorphosed andlocally display chilled margins and flow structures. In

the same belt, ultramafic rocks (harzburgite, Iherzolite)intruding granitic gneisses are also reported (Nanda etal., 2000). In the Bhela – Rajna area of Nuapara District,Pattanaik (1996) reported an epizonal to sub-volcanicigneous complex comprising silica-oversaturatedalkaline rocks of ‘A’ type magmatic lineage, theemplacement of which was controlled by N-S trendingcrustal fractures. Pattanaik and Mishra (2000) envisagedlinkage between developments of crustal fracture,emplacement of the alkaline complex and grabenformation related to deposition of the sediments inKhariar basin.

Meso-Neoproterozoic

Chhattisgarh Supergroup : Five disconnectedexposures of Meso-Neoproterozoic platformal/coversediments belonging to Chhattisgarh Supergroup areexposed in western Odisha . Some of these representthe eastern and southeastern edges of larger basins,which lie to the west in the Chhattisgarh State. Ball(1877) considered these to be parts of a single continuousbasin.

The lithounits of Chhattisgarh Supergroup occurringwithin Chhattisgarh Basin represents multiple cyclesof sedimentation (Das et al., 1992; Das et al., 2001)andcovers extensive areas in southern Chhattisgarh and alsoextend into the adjoining Odisha State. The southeasternand easternmost margins of the main basin, comprisingrespectively, the lithocomponents of the oldest Singhoraand Barapahar protobasins, are exposed in Odisha. Inthe Barapahar area of Odisha, nearly 1000 m thick sedimentary pile is exposed (Pascoe, 1973) and thesediments are intensely folded and faulted. The easternmargin of the basin shows faulted contact with theGondwana sediments along Mahanadi lineament and the

EGMB. The sequence in the Singhora protobasin hasbeen subdivided into four formations, which essentiallyrepresent alternations of arenaceous and argillaceoushorizons. The arenaceous formations mainly consist of feldspathic sandstone, quartzite, siltstone, shale andlimestone whereas the argillaceous formations arerepresented by calcareous shale of purple to reddish-brown colour. The evidence of syndepositional volcanic

activity is noted in the Singhora protobasin (Chakraborti,1997; Das et al., 2001).

The elongated oval-shaped Khariar Basin coversa total area of more than 1500 sq.km in parts of

Chhattisgarh and Odisha states. The eastern margin of the basin, bordered by the EGMB in Odisha, isstructurally disturbed. In Odisha, the sedimentaries lieover the granitoids of Bengpal Group with a pronouncedunconformity. The sedimentary sequence of the Khariar– Nawagarh Plateau, comprising dominantly areniteswith argillites and calcareous intercalations (withstromatolites), is formally designated as Pairi Groupand is divided into six formations (Das et al., 2001). InOdisha, the sedimentary sequence attain a maximumthickness of 700 m and comprises a lower sequence of gravel-sandstone-subarkose with thin shale intercalations

and disseminations of glauconite pellets, a middlesequence of rhythmic pebble-gravel beds and sandstoneand an upper sequence of alternate bands of cross-beddedsubarkose and wave-ripple marked sandstone(Srivastava, 1997). Srivastava (op. cit) designated thesequence in Odisha as Khariar Group and correlatedit with the Chandarpur Group of ChhattisgarhSupergroup of Murti, (1996) and Singhora Group –Chandrapur Group of Das et al., (1992). The kimberlitediatremes, occurring beyond the western margin of thebasin in Chhattisgarh state, are reported to containxenoliths of Khariar sediments implying their post-

Khariar emplacement.

A sedimentary basin located just south of the Khariarbasin and west of Ampani (Ampani Basin) is occurringas an outlier of approximately 220 sq.km area. Theeastern margin of the basin is marked by a NNE-SSWtrending boundary fault along which the basementgneisses as well as the overlying sedimentaries displayeffects of shearing. The sequence comprises grittyconglomerate at the base followed upwards bysandstone, siltstone and purple-coloured shale withcalcareous bands (Balakrishnan and Babu, 1987). Dutt(1963,1964) considered the Ampani sequence to be apart of Chhattisgarh – Indravati master basin andcorrelated with Upper Kurnool. Balkrishnan and Babu(op. cit) opined that the Ampani sediments are equivalentto Chandrapur Group of Chhattisgarh Supergroup. Dutt(1963) proposed the name ‘Indravati Series’ for asequence of sedimentaries of Bastar and adjoining partsof Odisha after the name of the river draining the largestexposure where the entire sequence is exposed. The


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sequence was later redesignated as Indravati Group(Sharma, 1975). Bulk of the roughly quadrangle-shapedIndravati basin (~ 900 sq.km) fall in the Bastar districtof Chhattisgarh State; only the eastern part of the basinis exposed in Odisha. The southeastern margin of this

craton-marginal basin displays a pronounced tectoniccontact with the EGMB.

The Indravati sequence comprises conglomerate,sandstone, shale, limestone and stromatolitic dolomite.Ramakrishnan (1987) divided the sequence into fourformations, viz., the lowermost Tirathgarh Formationfollowed upwards by Chitrakut Formation, KangerLimestone and Jagdalpur Formation. The basinalrocks are nearly flat-lying with low dips towards thecentre of the basin. The sequence is intruded bykimberlite pipes in Bastar area of Chhattisgarh State.

The eastern margin of the triangular-shaped SabariBasin (~ 700 sq.km) (Ghosh, 1934) is exposed inextreme southwestern part of Odisha. The sedimentarysequence, correlatable with the Indravati Group,comprises a basal conglomerate and quartzite followedupwards by purple shale, limestone and interbands of shale and phyllite.

Eastern Ghat Mobile Belt

The Eastern Ghats constitute a major Precambrian

Mobile Belt of the Peninsular India designated asEastern Ghat Mobile Belt (EGMB). It extends for over1000 km from Odisha to southeastern parts of AndhraPradesh along the east coast of the Indian Peninsula,representing one of the most highly deformed andmetamorphosed crustal segment of the Indian Shield.The belt is widest in Odisha (~ 300 km) and covers themajor part of southern Odisha. The Gohira – Sukindashear/thrust belt, separates it from the Eastern IndianCraton lying to the north. The e

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