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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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