Journal of Geosciences, Osaka City University

Vol. 49, Art. 4, p. 49-58, March, 2006

Turbidite channel and overbank-levee sedimentation ofthe Permo-Carboniferous Talchir Formation,

Talchir Gondwana basin, Orissa, India

Wataru MAEJIMA J, Rabindra Nath HOTA2 and Banabehari MISHRA3

I Department of Geosciences, Osaka City University, Sumiyoshi-ku, Osaka 558-8585, Japan2 P. G. Department of Geology, Utkal University, Vani Vihar, Bhubaneswar - 751004, Orissa, India

3 P. G. Department of Geology, Khallikote Autonomous College, Berhampur - 760 001, Orissa, India

Abstract

Channel and overbank-levee deposits occur in the lacustrine turbidite succession belonging to thePermo-Carboniferous Talchir Formation of the Talchir Gondwana basin, Orissa, India. The channel

sandbodies are enclosed within the overbank-levee deposits and are higWy lenticular with restrictedlateral extent in cross section normal to the paleo-slope direction, suggesting that channels did notsignificantly rrngrate laterally but were filled dominantly through aggradation of in-channel deposits.

Multiple occurrence of single storey channels in relatively thin interval is either suggestive ofcoexistence of closely spaced, feeder channels on the basin marginal slope or frequent avulsion of achannel in the upper slope area. Well-developed overbank-levee deposits of thinly interbedded

sandstones and shales are indicative of significant spill-over of sediments from the channel. The upperportion of the channel flow was probably directly overspilled from a channel. The overbank-leveedeposits, at some places, are arranged into small-scale bedding cycles of a decimeter-scale level,

thickening-upward motif. This bedding cyclicity was most likely resulted from increase in the volume

of sediments over-spilled from a channel with the infilling and consequent shallowing of a channel;

Key-words: Talchir Formation, turbidite sedimentation, channel deposits, overbank-levee deposits,

Indian Gondwanas.

Introduction

The Penno-Carboniferous Talchir Formation extendsinto all the regions of the Gondwana basins in India (Fig.1) and marks the beginning of Gondwana sedimentation(d. Veevers and Tewari, 1995). Since the first

environmental interpretation of the Talchir rocks as glaciallake deposits (Blanford et aI., 1856), various facies withinthe Talchir succession have been attributed to glacial,glaciofluvial, glaciolacustrine and locally glaciomarinesedimentation (Casshyap and Tewari, 1982; Bose et aI.,1992; Sen and Banerji, 1996; Ramasamy et aI., 2000;Bhattacharya et aI., 2002; among others). It is, hence,commonly accepted that the Talchir Formation was

deposited in glacially scoured depressions and that the

Talchir glaciogene sedimentation was a consequence of theglaciation that extensively covered the Gondwana

Supercontinent in Late Paleozoic time (cf. Veevers andTewari, 1995). On the contrary, some workers suggested

the possibility of the major part of the Talchir Formationbeing deposited in a post-glacial warm climatic condition

(Rishi, 1971; Sen and Hatim, 1977; Pandya, 1987, 1998).Recent study of lithofacies and environments of

deposition of the Talchir Formation in the Talchir basinhas revealed that the sedimentation and basin evolutionduring Talchir time were largely controlled bydeglaciation, which first gave rise to the deepening of thelake basin as a result of the base-level rise and then broughtabout the rapid lake-level fall as a consequence of the

50 Turbidite channel and overbank-levee sedimentation, Talchir Gondwana basin, India

regional uplift due to post-glacial isostatic rebound(Maejima et aI., 2004). During the lake-level rise,

lacustrine turbidite channel-fan system was developed inlake-margin slope and base-of-slope environments

(Maejima et aI., 1999). This paper deals with a part of the

deposits of this turbidite system, focusing on channel and

associated overbank-levee sedimentation.

Geologic Setting

The Talchir basin is a northwest-southeast trending

elongated basin covering an area of about 3,150 km2• It

lies near the southeastern end of the Son-Mahanadi graben

between the Eastern Ghats mobile belt to the south and the

Singhbhum craton to the north (Fig. 1). The basin fill is

represented by more than 1,000 m thick clastic strata

ranging in age from Permo-Carboniferous to Triassic. The

succession is subdivided into the Talchir, Karharbari,

Barakar, Barren Measures and Kamthi formations, in

ascending order (Fig. 1).The area under study lies near the southeastern

boundary of the Talchir basin (Fig. 1). It is located aroundBedasar villag (latitude 20° 52' 30" N, longitude 85° 4' 0"

E) of Angul district, Orissa (Fig. 2). The Talchir

Formation of the present area is underlain by the

Precambrian basement rocks of the Eastern Ghats Group to

the south with a faulted contact. Locally unconformable

nature of the contact is also observable. The formation

strikes in a direction between N70° E to East and dips

uniformly towards the north at low angles ranging from 2°

to 10°, forming a homoclinal structure. Overlying the

Talchir succession is the Karharbari Formation, which is

represented by vertically stacked, fining-upward sandstone

sequences and has been attributed to braided fluvial

sedimentation (Das and Pandya, 1997; Hota and Maejima,

2004).The Talchir Formation immediately overlying the

Precambrian basement is represented by about 260 m of

strata comprising a variety of clastic sediments such as

diamictite, conglomerate, sandstone and shale. The

succession is subdivided into unit A-I, unit A-II, unit Band

unit C from base to top (Maejima et al., 2004) (Fig. 2).

Unit A-I comprises mud-matrixed, very poorly sorted

diamictites and interbedded thin sandstone and shale

yielding dropstones. This basal part of the formation

represents deposition in a proglacial lake environment.

The succession of unit A-II is dominated by pebble to

boulder conglomerates and sandstones. They were

deposited from various kinds of high-energy sediment

gravity flows, both subaerial and subaqueous, and formed

steep-faced fan-delta on the margin of the basin. Unit B is

composed of shale, rhythmite and interbedded sandstone

and shale. Thick sandstone bodies occur in the uppermost

part of this unit. Unit B demonstrates turbidite

sedimentation in lake-margin slope and base-of-slope

environments. Unit C dominantly consists of shaJe with

intercalations of siltstone and sandstone and forms a large­

scale coarsening-upward sequence, which represents delta

progradation over the deep lake-basin deposits.

Turbidite Channel-Overbank Deposits

The succession of unit B within the Talchir Formation

has been studied and interpreted to represent a turbidite

+ + + + + + +85° 15' 85° 30

+ SINGH + + + + + + NCftqroZHIJ/,4

f+ + + + + + +

+ 0 10 20 Km·I I I+ + + + + +

+ + + + +

++

+

+ +

+

+

+

+ + +

+

20'

78" 82°. 86" II B I-III ~~.I~_· +ifi1'" Kolkata ", II, ......

\

BhUbaneswarA

IV .---"-~ITALCHIR

Hyder~bad ). BASIN16° ).'

12'

A

Chennai ~ Kamthi Formation500 Km E3 Barren Measures Formation

k..,.-.,...."._L~====:J.~~-JD Barakar FormationI:Koel-Damodar valley basins ETIill Karharbari FormationII:Son-Mahanadi valley basins ~ Talchir FonnationIII:Satpura basin [±] Precambrian basementIV:Prahnita-Godavari valley basins ~ Fault

Fig. I (A) Distribution of Gondwana basins in the eastern part of Peninsular India and location of the Talchir basin. (B) Geologic

sketch map of the Talchir basin and location of the study area (modified after Raja Rao, 1982).

Wataru MAEJIMA, Rabindra Nath HOTA and Banabehari MISI-IRA 51

N

8alaidhar St

reamKUIO

+ +

+ + +

+ + + + + + +

+ + + + + __ =-_- ~\'lel =- - + + + + +

~ ~;~ ~:::: ~ ~~-"~::; :2OC1--

-- i~OI.-

+ + + + +----- \lcN -- - - - -~~ -- + + + + + + + +

+ + + + -------------- ---------- + + + + + + + + +PARANGA

+ + + + a+ ------------ + + + + + + + + + + + +----------

+ + + + + + + + + + + + + + +

+ + + + + + + + + i?> Paleocurrents

+ + + + + + + D Karharbari Formation

JARASINGHA ~ uo,c 1+ +a T T + + + ~ Unit BTalchir Formation

+ + + + + + + + + + + + + + + + ~ UnitA·1I

1 2km 0 Unit A-I+ + + + + + + + + + + +

~ Precambrian Basement

Fig. 2 Geologic map of the study area. Locations of measured sections and paleocurrent azimuths are shown.

sedimentation in a sublacustrine channel-fan system

developed on a margin of a lake basin (Maejima et aI.,

1999, 2004). The channel-overbank deposits, in

association with slope mud, are present in the uppermost

part of the succession.

ChannelThe channel deposits are 2 to 5 m thick and

dominantly comprise 0.4 to 2 m thick, commonly

amalgamated beds of pebbly sandstone and coarse- to very

coarse-grained sandstone (Fig. 3). The beds are graded and

essentially unstratified, but some show crude subhorizontal

stratification and locally ripple cross-lamination in the

uppermost part. Rjpped-up mud clasts, up to 1 m in long

dimension, are contained in many of beds, either scattered

or concentrated in discrete layers. Some of thick

sandstones accompanied by subordinate interbedded

sandstones and shales are organized into thinning- and

fining-upward sequences. Others show no such

sedimentation motif and have an abrupt upper contact with

interbedded sandstones and shales.

Thick, pebbly sandstones and coarse-grained

sandstones are interpreted as the deposits of high-density

turbidity currents (Lowe, 1982). Massive beds with

restricted occurrence of stratification towards their tops

represent fast settling from high-concentration suspension.

Subhorizontal stratification and ripple cross lamination in

the upper parts of some beds suggest that flow fluctuations

locally led to high-rate traction sedimentation in the final

stage of deposition. The thinning- and fining-upward

sequences made up by the deposits of high-density

turbidity currents are interpreted to have been formed by

filling and abandonment of channels or by lateral shifting

of acti ve channels (Walker, 1985). Thinly interbedded

sandstone and shale at the top of thinning- and fining­

upward sequences represent final infilling of an abandoned

channel or deposition on the margin of a channel.

Mud-filled channelA few mud-filled channels occur in the uppermost

part of the Unit B succession. They are discernible with a

markedly channeled urface veneered by coarse to very

coarse, locally granular sand (Fig. 4). Up to 2 m deep

scours are observed. Infilling a channel are shales, which

locally intercalate millimeters-thick layers of siltstone and

very fine-grained sandstone. Shales tend to drape up

against the channeled surface.The deep erosion surface, together with a veneer of

coarse sediment on it, undoubtedly represents

channellization of the substrate. Channels were not filled

52 Turbidite channel and overbank-levee sedimentation, Talchir Gondwana basin, India

Fig. 3 Thick, amalgamated channel-fill sandstone resting on interbedded sandstone and shale of an overbank-levee origin.

Fig. 4 Mud-filled channel cutting down into the overbank-levee deposits.

with sand but channel flows left behind only coarsest

materials on the floor as a lag. Tbis indicates that channels

were not gradually abandoned nor laterally shifted away

but were suddenly abandoned. The abandoned channel

depressions were gradually filled with suspended mud.

Tbin intercalations of siltstone represent occasional

invasion of currents and deposition of fine materials from

slowly moving, dilute suspension clouds.

Wataru MAEJIMA, Rabindra Nath HOTA and Banabehari MISHRA

Fig. 5 Overbank-levee deposits comprising thinly interbedded sandstone and shale.

53

Overbank and leveeThe overbank and levee deposits are manifested in

close association with channel sandstones. They are

represented by successions of thinly interbedded sandstone

and shale (Fig. 5). Individual beds are generally less than 5

cm thick but at places may be 20 cm thick. The

sandstone:shale ratio is around I: l. The wavy and

lenticular bedding is common. Beds are, at places,

discontinuous with wedging and lensi ng out.

Amalgamation of sandstone beds is common. Sandstone

shows wide variability in grain size, from fine- to very

coarse-grained. Some beds contain ripped-up shale clasts.

Most of the sandstone beds are graded, but their tops are

generally in sharp contact with overlying shales. Internally

sandstones show the Ta-c, Tbc, or Tc sequences. Ta and Tb

beds are locally present.

The succession of thinly interbedded sandstone and

shale is well comparable with the deposits interpreted in

previous works on turbidite systems as natural levee or

overbank deposits. These generally have thin bed

thickness, a high sandstone:shale ratio, coarse grain size of

sandstones and irregular and discontinuous beds (Mutti,

1977; Winn and Dott, 1979; Walker, 1985; Stow, 1985;

Tanaka, 1989, 1993). All these features are characteristic

of thinly interbedded succession of sandstone and shale.

The occurrence of these successions accompanying

channel deposits is consistent with an overbank-levee

in terpretation.

Channel Sandbody Geometry

The architecture of turbidite channels was examined

along the Mutukuria stream, which cuts down the

uppermost part of Unit B and runs roughly parallel to the

strike of the strata (Fig. 2). The measured sections were

correlated by lateral tracing of distinctive beds and the

geometry of channel sandbodjes was worked out (Fig. 6).

The paleocurrents obtained from outcrops along the

Mukuturia stream show consistent northward sediment

dispersal (Fig. 2). Das and Pandya (1997) also reported the

regional paleoflow pattern broadly towards the north

during Talchir sedimentation. Accordingly, the profile

shown in Fig. 6 is considered to be roughly normal to the

paleo-slope direction and the channel sandbody geometry

represents cross-sectional channel forms.

Detailed stratigraphic correlation of closely spaced

and continuous outcrops shows that channel sandbodies are

lenticular in shape (Fig. 6). They are seldom traced

54 Turbidite channel and overbank-levee sedimentation, Ta.lchir Gondwana basin, India

250 mW ......f--------.=~.:..---------. E2

2

om

w ... 20 m. E1

4

2

om

Unit C

Unit B

3

Fig. 6 Stratigraphic correlation of measured sections.

2

om

Wataru MAEJIMA, Rabindra Nath HOTA and Banabehari MISHRA

Unite

Unit B

..../

: : : I.. ·1

.... :: :: 1. :> ..• ::<~ ::1

iii~E3

~L.:.:.:.J

250 m

5

Fig. 6 Continued.

Sand-filled channel

Mud-filled channel

Shale

Interbeddedsandstone and shale

Sandstone

55

laterally for more than 200 m and pinch out into the

interbedded sandstones and shales of an overbank-levee

origin. Some have thin wings of sand extending into the

overbank deposits. Lower bounding surfaces of some

sandbodies display considerable erosional relief. At the

lateral terminus of the sandbodies, the lower bounding

surfaces tend to be steeply curved. The channel

sandbodies are generally isolated in the overbank-levee

deposits, and many of them can be termed as single storey

bodies. Rare example of multistory sandbodies is observed

at the locality 3 (Fig. 6).

Mud-filled channelbodies are highly lenticular and

ribbon-like with steep and relatively smoothly curved

lower bounding surfaces. They are commonly less than

100 m wide and have higher width:thickness ratios than

channel sandbodies.

Bedding Cyclicity in Overbank-Levee Deposits

The overbank and levee deposits generally form, on

the whole, a monotonous succession of interbedding of

thin sandstones and shales (Fig. 5). However, detailed

examination of the succession reveals that the

overbank-levee deposits are, at some places, arranged into

small-scale bedding cycles, which are defined by a

decimeter-scale, thickening-upward sequence (Figs. 7, 8).

The th icken ing-u pward seq uence is ei ther vertically

stacked or isolated within the monotonous interbedding of

sandstone and shale. No reversal trend of bedding

cyclicity is observable in any of the outcrops examined.

Individual thickening-upward sequences are up to 1 m,

most commonly 40 to 70 cm, thick. The basal part of the

sequence is dominated by shale with intercalations of

commonly less than 2 cm thick sandstone. In some

equences, the sandstone intercalations in the basal part are

discontinuous and show wavy and lenticular bedding.

Above the basal part, sandstones are generally 3 to 10 cm,

locally 20cm, thick and tend to increase in thickness

upward. Shale interbeds are 2 cm or so in thickness. In the

uppermost part of the sequence, amalgamated beds of

sandstone are common.

Discussion and Conclusions

During deposition of unit B of the Talchir Formation

of the present area, coarse sediments were supplied

transversely into the lacustrine basin that had a steep basin­

margin slope, and turbidite sedimentation took place

forming a sublacustrine channel and fan system on the

lake-margin slope and base-of-slope environments

(Maejima et aI., 1999,2004). The uppermost part of unit B

documents channel and associated overbank-levee

56 Turbidite channel and overbank-levee sedimentation, Talchir Gondwana basin, India

Fig. 7 Logs of the overbank-levee deposits showing decimeter­scale, thickening-upward bedding cycles.

~Thickening­upwardsequenceRipple cross

lamination

Parallellamination

OJQ.o

V5

Sandstone

Shale•D

wccro

..cU

Wccro

..cU

2 2

OJOJ>OJ-r

...::<:c:ro OJ

of? OJ>OJ OJ> -r0

..:::Lc:ro-eOJ>

0

sedimentation of this turbidite depositional system. The

profile roughly normal to the paleo-slope direction well

displays the interrelationship of the channel sandbodies

and overbank-levee deposits (Fig. 6).Consistently thin channel-fill sequences reveal that

feeder channels were of small-scale. The development of

small channels was probably related to a small catchment

of the hinterland, in which only local streams drained. It

has been indicated that the Gondwana glacier had

disappeared in the area of the Talchir basin at the time of

deposition of unit B (Maejima et aI., 2004). Post-glacial

base-level rise would have prevented enlargement of a

catchment of the hinterland and stored detritus in the

drainage basin. The channel sandbodies enclosed within

the overbank-levee deposits are highly lenticular with

restricted lateral extent in cross section, suggesting that

channels did not significantly migrate laterally but were

filled dominantly through aggradation of in-channel

deposits. Multiple occurrence of single storey channels in

relatively thin interval (Fig. 6) is either suggestive of

coexistence of closely spaced, several feeder channels on

the basin margin slope or frequent avulsion of a channel in

the upper slope area. Mud-filled channels represent

avulsion and sudden abandonment of a channel without

infilling of it.

Well-developed overbank and levee deposits closely

associated with the channel fills are indicative of

Fig. 8 Thickening-upward sequence in the overbank-levee deposits covered by thick channel-fill sandstone

Wataru MAEJIMA, Rabindra Nath HOTA and Banabehari MISHRA 57

significance of spill-over of sediments from the channel.The shallow depth of the channels would have been

primarily responsible for such active spill-oversedimentation on the levee and overbank area. The sand

wings extending from the channel sandbodies into theoverbank-levee deposits undoubtedly represent leveesadjacent to the channel. The upper portion of the channelflows was probably directly overspilled (cf. Chough and

Hesse, 1980; Tanaka and Maejima, 1992). The resultantoverbank and levee deposits, thus, show features indicative

of deposition from high-energy turbidity currents, namelybasal scours, amalgamated beds, coarse grain size in spiteof thin bed-thickness, and presence of ripped-up mudclasts. The entrained layer of the channel flows spread

further outside the zone of active spill-over sedimentationonto the slope as a low-concentrated suspension cloud.Fall-out of fine materials from such a dilute cloud, in

conjunction with hemipelagic suspension fall, formed thin

shale interbeds in the distal overbank area.The bedding cycles in the overbank-levee deposits are

defined by upward increase in bed thickness of sandstonethat was originated by spill-over of sediments from an

adjacent channel. Bedding cyclicity could be attributed tovariations in hydrodynamic regime as a result of extra­basinal processes such as tectonic instability and base-level

fluctuations. However, the bedding cycles in unit Boverbank-levee deposits are of small scale, having a

thickness of the order of decimeters. These small-scalebedding cycles were most likely resulted from an intra­

basinal process.The bed thickness of a single-event spillover deposit

would be primarily controlled by the distance from achannel and by the volume of over-spilled sediments. Abed of spill-over sedimentation is generally expected to

decrease its thickness as it goes away from a channel.Such a lateral bed-thickness trend of overspilled deposits is

well demonstrated by sand wings extending from channelsandbodies (Fig. 6). The sand wings decrease in thickness

laterally away from their source channel and eventuallythin out into overbank-levee deposits. In this context, the

thickening-upward bedding cycles could be interpreted torepresent increase in proximity to a channel, whichapproached the depositional site as a result of lateral

migration. However, as evident from Fig. 6, the channelsandbodies are highly lenticular with restricted lateralextent in cross section and are suggestive of channels beingfilled dominantly through aggradation of in-channeldeposits. Lateral migration of channels Was likely notsignificant. Exclusion of lateral channel migration for thecause of the bedding cycles is further suggested by thecomplete absence of the reversal motif, that is thinning-

upward cycle, which could have been produced while a

migrating channel goes away from the depositional site.Alternatively, the thickening-upward bedding cycles in the

overbank-levee deposits were most likely resulted from

increase in the volume of sediments over-spilled from achannel. As the channels tended to be filled withaggradational in-channel deposts without significant lateralchannel migration, channel depths should have been

progressively shallowed. Channel flows were liable tospill over from a shallowed channel. With the infilling of achannel, the volume of spilled-over sediments would haveincreased and thicker beds were deposited on the

overbank-levee area. Frequent switching of the channelcourse resulted in the repetitive occurrence of small-scale,thickening-upward bedding cycles.

Acknowledgments

We are indebted to J. Tanaka and T. Nakajo for theirsuggestions and discussions. The manuscript benefitedfrom reviews by N. K. Mahalik and H. K. Sahoo. Partialfunding for this research was provided to W.M. from OCDOversea Science Mission Program and from a Grant-in-Aid

for Scientific Research (C) from the Japan Society for thePromotion of Science.

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