Palynostratigraphic correlation of lower Gondwana sediments in the Chuparbhita and Hura Basins, Rajmahal Hills, Eastern India

Review of Palaeobotany and Palynology, 65 (1990): 239-255

239

Elsevier Science Publishers B.V., Amsterdam

Palynostratigraphic correlation of Lower Gondwana sediments in the Chuparbhita and Hura Basins, Rajmahal Hills, Eastern India Manju Banerjee and Ashalata D'Rozario

Department of Botany, University of Calcutta, Calcutta-700 019 (India) (Received November 4, 1988; revised and accepted January 25, 1990)

ABSTRACT Banerjee, M. and D'Rozario, A., 1990. Palynostratigraphic correlation of Lower Gondwana sediments in the Chuparbhita and Hura Basins, Rajmahal Hills, eastern India. Rev. Palaeobot. Palynol., 65: 239-255. Correlation of palynostratigraphic zones of the adjacent Chuparbhita and Hura Basins reveals similar depositional environments. Distinct changes in climatic and ecological phases are key features of the depositional environment in the two adjacent basins. Three climatic phases recognised in the Chuparbhita Basin are (I) monosaccate Plicatipollenites-Parasaccites, (II) nonstriate disaccate Scheuringipollenites and (III) striate disaccate Striatopodocarpites-Striatites, while a single climatic phase of nonstriate disaccate Scheuringipollenites is recognised in the Hura Basin. Climatic phases are suggested from the relative abundance of the different saccate types viz., monosaccates, nonstriate disaccates and striate disaccates as cool, temperate and warm humid conditions respectively.Ten ecologicalphases have been identified in the Chuparbhita Basin within the three climatic phases and seven in the single climatic phase of the Hura Basin. Scheuringipollenites is the most extensive climatic phase of deposition in both the basins in which identical ecological phases are recognised at some corresponding horizons. Two marker horizons are recognised within the Scheuringipollenites climatic phase in the Chuparbhita and one in the Hura Basin. The marker horizons contain a distinctive assemblage of trilete and monolete taxa in addition to diverse acritarchs and prasinophytes viz., Peltacystia, Circulisporites, Tetraporina, Kagulubeites, Haplocystia and Maculatasporites. The Marker horizon I of PN H-5 of Hura is distinguished by the occurrence of diverse acritarch suites along with the key trilete genus Lalmatiasporites. PN C-9, with the key trilete genus Ghoshiatriletes and diverse acritarch suites identified as Marker horizon II, has not been encountered in the Hura Basin. The marker horizons may be considered as representing phases of brackish water transgression in the essentially continental sequence of deposition. Palynological evidence indicates an Early Permian age for both basins.

Introduction

Materials and methods

The C h u p a r b h i t a a n d the H u r a Basins are two adjacent basins in the R a j m a h a l g r o u p o f coalfields of eastern India, e x t e n d i n g in a n o r t h - s o u t h direction ( 2 4 ° 1 5 ' - 2 5 ° 3 0 ' N lat. to 8 7 ° 1 5 ' - 8 7 ° 4 5 ' E long.) within a 125 k m 2 area (Fig.l). T h e Lower G o n d w a n a sequence o f the two basins is overlain u n c o n f o r m a b l y by the D u b r a j p u r F o r m a t i o n (Early Jurassic) a n d u n c o n f o r m a b l y overlies Arc h a e a n m e t a m o r p h i c s (Ball, 1877). T h e generalised stratigraphic sequences in the two basins are s h o w n in T a b l e I.

The p a l y n o s t r a t i g r a p h i c study e x a m i n e d 84 samples o f 3 a n d 8 bore cores from the C h u p a r b h i t a a n d the H u r a Basins respectively (Figs.2, 3). Samples of coal, shaly coal a n d c a r b o n a c e o u s shale were first t h o r o u g h l y washed with distilled water a n d dipped in absolute alcohol to avoid surface c o n t a m i n a t i o n . T e n grams o f crushed sample from each lithology were treated with 4 0 % H F to dissolve the silica, then washed several times to m a k e the samples acid free. Microfossils were isolated by m a c e r a t i o n with Schulze's solution,

0034-6667/90/$03.50

© 1990 - - Elsevier Science Publishers B.V.

240

TABLE

M. BANERJEE

AND

A. D’ROZARIO

I

Generalised Basins.

stratigraphic

sequence

Chuparbhita (Madabhushi,

Upper Gondwana Unconformity Lower Gondwana

in Chuparbhita

Basin 1979)

Rajmahal Trap Dubrajpur Formation and overlap Barakar Formation Karharbari Formation Talchir Formation

and Hura

Hura Basin (Roy and Mukherjee, 1978) Rajmahal

Trap

CHUPARBHITA

Barakar Formation

07”3

7”20’ CHB/MA/017

RCH-3

RCH-2

Depth I” M

Talchir Formation

S

c

Unconformity Archaean

IOC

200 ?OO’_

300

4 Y+

PACHWARA MAHUAGARHI

!

24”30’-

400

Fig. 1. Location India.

of Chuparbhita

and Hura

Basins, in northeast

followed by treatment with 5% KOH to dissolve humic matter. The washed residues were sieved through a 100 mesh sieve. The macerated samples were stained with 2% bismarck brown solution, if necessary, to facilitate study of minute structures

500

Fig.2. Chuparbhita Basin, with borehole localities, lithologies, sample numbers (5) and palynological zones (PN).

CORRELATION OF LOWER GONDWANA SEDIMENTS

of the miospores and for better photomicrographs. The samples are preserved in 50% glycerine. Slides were prepared in glycerine jelly and are lodged in the repository of the Paleobotany-Palynology Laboratory, Department of Botany, University of Calcutta. Frequency counts have been made from study of 10 slides. For identification of miospore taxa, available type slides at Birbal Sahni Institute of Paleobotany, Lucknow, India, were studied and extensive literature consulted. Palynostratigraphy in Chuparbhita and Hura Basins and comparison with other similar zonations Analysis of the bore cores allows recognition of 10 palynoassemblage zones in the stratigraphic sequence developed in the Chuparbhita Basin and 7 in the Hura Basin (Table I, Figs5, 7). These assemblage zones, recognised as palynostratigraphic zones (PN), are distinguished on the basis of variability in the dominance, appearance and disappearance of monolete and trilete spores and saccate pollen and the occurrence of diverse acritarch swarms.

Saccate dominance in the palynostratigraphic zones In the 10 palynostratigraphic zones identified in Chuparbhita Basin, three successive phases of significant influence of different saccate groups were distinguished, viz., (1) radial monosaccates Plicatipollenites-Parasaccites, (2) nonstriate Scheuringipollenites and (3) striate (taeniate) Striatopodocarpites-Striatites disaccates, while a single phase of nonstriate disaccate Scheuringipollenites influence was observed in the 7 palynostratigraphic zones of the Hura Basin. The late Palaeozoic palynostratigraphic zonations of the Southern Hemisphere (Kemp et al., 1977; Schopf and Askin, 1980) including the Indian Lower Gondwana (Bharadwaj, 1971; Tiwari, 1973) have been primarily established on the basis of the appearance, dominance and disappearance of different types of saccate pollen grains, viz., radial monosaccates, nonstriate disaccates and striate disaccates. The differential occur-

241

rence of saccate types in the Indian Lower Gondwana is considered to be related to changing climatic conditions viz., cool, temperate and warm humid, during the depositional period (Bharadwaj, 1966, 1975; Tiwari, 1973; Kar, 1976). Megafossil and faunal records, sedimentological and mineralogical evidence also suggest similar changes in the climatic phases in Indian Lower Gondwana (Lele, 1976; Shah, 1976; Laskar and Mitra, 1976; Singh, 1976). However, the reasons for occasional climatic fluctuations within prolonged climatic phases need to be further investigated.

Dominance of trilete, monolete and other taxa in the palynostratigraphic zones Differential dominance of trilete and monolete genera viz., Callumispora, Brevitriletes, Laevigatosporites, Lophotriletes, Cyclogranisporites, Microfoveolatispora and two newly described trilete genera, Lalmatiasporites and Ghoshiatriletes, distinguishes each of the palynostratigraphic zones. The zones of the two basins more or less correspond with each other and some are almost identical (Figs.4, 5, 7). Variable combinations and frequencies of taxa other than saccates in the palynoassemblages in the sequences indicate changing ecological facies of deposition within the same climatic phase. Climatic phases may be prolonged in a fixed geographic position, whereas ecological conditions may vary within shorter time periods due to a variety of factors as well as changing facies of deposition (Scott and Collinson, 1983). Variability of ecological facies is distinct in the palynostratigraphic sequence of the Indian Lower Gondwana; diverse forms of monolete and trilete genera occupy dominant or subdominant positions in the different climatic phases of deposition (Tiwari, 1974). Factor analysis of these genera has not been possible yet, since the corresponding eutaxa (Meyen, 1987) are not known. But the variable combination and dominance of certain taxa in the sedimentary sequences suggest ecofacies variation at short intervals of time. Acritarch genera are also known to occur in palynoassemblages of the Indian Lower Gondwana as well as in

Hi

H.

Fig.3. Hura

200

175

150

125

100

75

50

25 ;

DJ

S

7

PN.H 3

C

Basin, with borehole

Coal CG fCoarse graine@ carbsandstone Interbanded sandstone and shale Sandy shale FG fFine grained) sandstone CG (Coarse grained/ sandstone

a m a a a

localities,

lithologies,

PNH 1-H-I

Garb shale Shaly coal

MG (Medium grained) sandstone Shaly sandstone

IO

9

73

lt310KMl096

m H

a m

W”3

I

ECL-XIII)

C

H-II 0Or.

H-II TOP

H-III

l+IV

H-V

H-VI

(9,

H-VIII

H-IX

numbers

rH

i

tiRVCM/OW

coal seams (CT) and palynological

HRcxbvQ70

Fm/WB/131

zones (PA’).

.._ .:: -. :, .:’ ... II

sample

S

18\O/CM/ 104

HURA

16lO/WB1136

Scale 1 : 253,

181O/WWi44

H-I

Scheuringipollenites

H-VI, H-V, HIV, H-Ill, H-n Top and Bottom (Bore holeHRC/CM/070) H-II Top and Bottom (Bore hole-ECL-3(lll)

Scheuringipollenites dominant

Scheuringipollenites-dominant

dominant-subdominant

Scheuringipollenites-dominant

occasional

Scheuringipollenites-

Intermediate Horizon, H-VII

H-V 111

Scheuringipollenites-

subdominant

Brevitriletes Laevigatosporites Zone, acritarehs rare viz., Peltacystia and Prasinophytes Haplocystia

Marsupipollenites

acritachs absent with occurrence of

Laevigatosporites-LophotriletesCyclogranisporites Zone, acritarchs occasional viz., Circulisporites, Peltacystia and Prasinophytes Haplocystia, Maculatasporites Laevigatosporites-Apiculatisporis Zone,

Zone, acritarchs occasional viz., Peltacystia, Circulisporites and Prasinophyte Haplocystia

Maculatasporites Lalmatiasporites- Microfoveolatisporalndotriradites Zone, acritarchs diverse and frequent viz., Circulisport~es, Peltacystia, Tetraporina, Kagulubeites and Prasinopbytes Haplocystia, Maculatasporites Striatopodocarpites-Laevigatosporites

Laevigatosporites-Horriditriletes Zone, acritarehs occasional viz., Peltacystia, Circulisporites, Tetraporina and Prasinophytes Haplocystia,

PN.H-!

PN.H-2

PN .H-3

PN.H-4

PN.H-5

PN.H-6

PN. C- 1

PN.C-2

PN.C-3

PN . C - 4

PN.C-5

PN.C-6

PN.C-7

PN.C-8

PN.C-9

PN. C-10

H-IX

Circulisporites, Tetraporina, Peltacystia and Prasinophytes Haplocystia

PN.H-7

Cyclogranisporites Laevigatosporites Zone, aeritarehs occasional viz.,

Scheuringipollenites

dominant-subdominant

H-XII H-XI H-X

Scheuringipollenites dominant Callumispora Zone, Prasinophyte Maculatasporites Ginkgocycadophytus Zone, acritarch Quadrisporites

absent

subdominant

Plicatipollenites- Parasaccites

dominant-subdominant

Plicatipollenites-Parasaccites

Scheuringipollenites dominant

dominant-subdominant

Scheuringipollenites

dominant-subdominant

Scheuringipollenites

Scheuringipollenites dominant

Scheuringipollenites subdominant

Cyclogranisporites Striatopodocarpites Cyclogranisporites Marsupipolleniees Leiotriletes Laevigatosporites-Brevitriletes Zone, acritarchs acritarehs absent

Subphases

Scheuringipollenites su bdominan t-occasional

C/36 C/38 C/37

C/33 C/34

ci32

C/27

C/25

C/23

C/17 C/19 C/21

C/14 C/15

C/13

C/II

c/5 c/7 c/8 c/9

C/l c/3

Striatopodocarpites Striatites dominant-subdominant

Sample No.

Climatic phase taxa

LaevigatosporitesLophotriletes Zone,

Cyclogranisporites-Microfoveolatisporalndotriradites-Lalmatiasporites Zone, acritarchs diverse and frequent viz., Peltacystia Circulisporites, Tetraporina, Kagulubeites and Prasinophytes Haplocystia, Maculatasporites Cyclogranisporites Zone, acritarchs occasional viz., Peltacystia, Circulisporites and Prasinophytes Maculatasporites

absent

Acanthotriletes-Laevigatosporites Zone, acritarchs rare viz., Peltacystia, Kagulubeites Striatites Cyclogranisporites Zone, acritarchs

Maculatasporites, Haplocystia

Ghoshiatriletes Zone, acritarchs diverse and frequent viz., Peltacystia, Circulisporites, Kagulubeites, Tetraporina and Prasinopbytes

acritarchs absent

Laevigatosporites-Cyclogranisporites Zone,

Ecological phase taxa

Palynostratigraphic zone (PN)

Ecological phase taxa

Climatic phase taxa

Sample of coal seams Palynostratigraphic zone (PN)

Chuparbhita Basin

Hura Basin

Climatic and ecological phases encountered in Chuparbhita and Hura Basins.

TABLE II

© Z

>

C~ 0

244

M. BANERJEEAND A. D'ROZAR]O

%1 !--.a.~, .........

55 60

;7~- ...................

P{ ¢olipollenites Paras dECires

.~/ ~ ~.i .9i i o~/ ~ i \ ~ ~/! I\

55 50

~\

45

I \'\ / i "\', ii

~' =~ /a~,

40

---

Plicatipollenites ....

~ ~,\ ', "'.

....

Parasaccites

i

/

~,

i ,,.\

,

, //

~5

,

,:

x

..,.'~-., % . . * " / -.% ~.~;~

C/27

:

~ ' ,.., .

,

'\• .//

~

.~ ~,,:

o

°

// / ' \ ~ . - ' _ , ' M" * /"

"--~.

C/J9 d7

C123

f

,

•

'"~

C/33

~], ~/~

i

i

,

l

C/37

/

/

•

~i

•-*~."'-"~"

~ /x striatites #

, ,

J/

--

Striotopodocorpites IStriotites

Scheuringipoilenit es

Striatopodocarpites .... C[.Ph.-- Climatic Phase

\ 2o

c{.Ph~- ....

c,.P~ ..............................

Sc heuringi p~llenit es

c/t5I

CA~

o

;

~. L

#

",~\ ; ~';, ~ "- _~ ~ . ."=-'~L.~..~ [ .......... *,t,..,'-'~°t"~ c II13

~i~

Cl.~I

C/B

c/7I

CA

c13I

CA

Fig.4. Chuparbhita Basin data, showing frequency in percent of major pollen type and their grouping into climatic phases

(CLph.).

75

~N~;~---P~ ~ 2---FPNC~ [ ......

70

PN.C4........

]---

-PN.C 5-- -.~: I! . . . .

---P~.C~--1-P~-l~..~,

I ....

~.c~---

l .... ~.o0---I

65 60

Gink gocycodophy'~us

-.~

Laevigat osporites

CaHumlsporo

~

Brevit riietes

55

.....

Lophot riietes Marsupipol[enite~

50-

. . . . . . C ycIogron~sporites ~[:

--~--

~[ .o~~

45-

----- G~oshiatriletes

Microfove0(otisporo

@ Lolmatiasporites

~ - - ~ - Acanthotriletes p N .-paLynos t ra tigr~phic zone

u

'~/ Y

~¢

Y

'

~

~

"

*~ \

-

-

.

_~__/X

/

2

~

o/

~

:

If~i,,

;A.

~

~I~,

"

,o

.o , c/37 '°°°'°'

~

%

•

ch6

c/e

c/3~

;

c/~

cb2

I

c/ 7

c/2~

I

c/ ~

c/~2~

.~'k" : ' ~

4° ch7L

cn~

!

c/3

c/,

I

c/9

c/~

...'~ ." "~_~

/

c/

c/'s

[

c/~

c/i

Fig.5. Chuparbhita Basin, showing frequency of spore taxa used to define palynologica] zones (PN) and ecological phases.

marine beds (Sinha, 1969; Lele and Chandra, 1972; Chandra and Lele, 1979). In addition to the saccates and trilete or monolete genera, the palynostratigraphic zone

assemblages of both basins contain a few other taxa viz., Peltacystia, Circulisporites, Tetraporina, Quadrisporites, Haplocystia and Maculatasporites which are in general recognised as acritarchs and

245

CORRELATION OF LOWER G O N D W A N A SEDIMENTS

occur along with Leiosphaeridia in palynoassemblages recorded from Singrauli (Sinha, 1969), Chirimiri (Chandra and Lele, 1979) and Jharia Coalfields (Tiwari et al., 1981). Leiosphaeridia occurs frequently in marine sediments of Umaria (Lele and Chandra, 1972; Chandra and Lele, 1979). A nearshore palaeoenvironment for the leiospheres and brackish water as a common facies association for the tasmanids have been suggested by Tappan (1980). Maculatasporites and Haplocystia are assigned to the Tasmanitaceae of the Prasinophytes (Tappan, 1980). The spherical alete genus Kagulubeites which splits into two hemispherical, parts, was originally recorded from the Congo basin (Bose and Maheshwari, 1968). The genus is grouped here with the acritarchs. The weak zone of splitting in Kagulubeites is organisationally similar to Peltacystia and the Holocene Concentricystes. Kagulubeites has been recorded earlier along with other acritarchs viz., Pilaspor-

prasinophytes (Tappan, 1980). The palynostratigraphic zones PN C-6, PN C-9 and PN H-5 have diverse and frequent representations of acritarch and prasinophyte taxa. PN C-6 and PN H-5 can be correlated easily by means of similar palynoassemblages with frequent acritarchs (Figs.6, 8). Occasional records of acritarch genera may not be of much importance but occurrence of frequent and diverse acritarchs in a restricted sedimentary succession may have ecological significance. Affinity of these genera is uncertain, although ecology of acritarchs and prasinophytes in general has been interpreted as marine (Meyen, 1987).

Ecology and affinity of the acritarch and prasinophyte taxa A fresh or brackish water origin has been suggested for the acritarch taxa Peltacyst&, Circulisporites and Tetraporina (Balme and Segroves, 1966). Van Geel (1979) suggested a fresh water zygnemataceous affinity for Tetraporina and Peltacystia from study of Holocene sediments. Svenolov (1986) remarked on the resemblance between Tetraporina and modern algae. Sen and Banerjee (1988a,b) observed the differential frequency of occurrence of two types of Concentricystes in fresh and brackish water Holocene sediments of the Bengal Basin. The split half of Concentricystes rubinus (Type-I) with rough ribs (cf. striae) resembles Circulisporites except for the occurrence of fovea at the polar regions of both halves in the Holocene specimen. Peltacystia, Circulisporites, Maculatasporites and Quadrisporites are known to

ites, Balmella, Peltacystia, Brazilea, Maculatasporites, Quadrisporites, Spheripollenites etc. (Bose and Maheshwari, 1968; Tiwari, 1969). The palynostratigraphic zones of the Chuparbhita and Hura Basins thus reveal the influence of both climatic and ecological factors at the time of deposition.

Environmental phases of deposition in Chuparbhita and Hura Basins Distinct changes in the climatic and ecological phases are the key features of the palynostratigraphic zones recorded in the almost complete

MARKER. ]

L

HORZON-IJ Tetraporino

9 8

MARKER

HORIZON-If

J

Haploc ystla

7

K ogmubeit es

6 5

I

~ O . u ad risporit~s

4

Moculotosporites

3 2

Sample

No

•

I

C/37

i C136

I CI38

Cl3~i

I C/33

C/~i

I ~/~i CI27

I C/23

~2~i

I CI19

C#,7

I C 15

C/'4i

I Ct13

C.i

I C/9

Fig.6. Chuparbhita Basin, showing frequencyof acritarch taxa and position of marker horizons.

C¢~i

C/Si C/7

C/,I C/3

246

M. BANERJEE AND A, D'ROZARIO

85

. . . . . . . . . . . . . . . . . . . . . . . . . .

.o 75

T .................

4

70

60

~

~

Brevitri[etcs

Laevigat ospori tes

...... Lophotriletes

Marsupipollenltes

---

55

HorriditriteteS

5O .'A

40

25

2o

^. i'D

15

,b

10

,&~

.~

$

'~'

.

...,.>~

_

:

I

...... Cyclogranisporites

o

~-~-

Microfoveo[atispora

@ Lalrnatiasporites ....

lndotriradites

--x-

Striat opodocarpites

~

.1'

~\.

i

\

~.\

iS'

ir"".\i

~

"-"~,.,~

"

~ t

,,.....,

H-IV H-IV

..

:. ,~

H-V

/

'

~',

,"t,

/ ~:/. I' ;[

i

.~ :

'

~!

t

;~,

,

~,

t i

"

,."

i

', ~

,

- __,

H-VI

,"

~

://~(

~. ,+

" -:.+."~--

H-V'

A,: "

I

.\..

~÷--~-...-"~+-

H-Ill

~..

,,,s

t

o., .-. ~ . ' ".

..,

-.. "* ~

H-Ill

.".

: ~ ",

..

:

Z

!

'./

/

i

"

~' " \

• ~..~

V

:

.h-~..

Coal H-I H-II H-II H-II H-II Seams Bottom Top Bottom Top

1

. . . . .

.~'[

.'t ,:

\. .

-

i'~

..t i..-",-v"

•

/..

Ii

-

".

7 :,%/'

~ ,? -~, .:/'

"1

i

./' \. / '-,

i

~

<" ,:tY~,

.~ ~'

,\

]

/

/

[

T

~/ \

^

i

./ •

! !

-4

?. •X

/ •/ i i

i

f i

~" £! ~ /

Apiculatisporis

- -

45

'

+

PN-Pa|ynostragraphic zone

. . . . . Sc heuringipollenit es

F

T ///*

................

C[.Ph.-Chmattc Phase

65

f

Ct. Ph, Scheu ringipod ehites . . . . . . . . . . . . . . . . . . . . . .

~LL.~ ~

Intl,- H-VII H-VIII H-IX H-IX mediate

H-X

H-Xl

H-Xll

Fig.7. Hura Basin data, showing percentage of major spore and pollen taxa, climatic phases (Cl.ph.), palynological zones (PN) and ecological phases.

109 e

C}rculisporites

7

Ha c~|atasporites

6

Tetra porina

5

Pellacystia

4

Hap[ocystia

3

Kagulubeites

_._i "1 ~

2

Samp|e~/° -- ~

No

"

.

~

,,"

~3

Hi9

~

"

l~

I

H/7

Coal H-I H-II H-II H-It Seams Bottom Top Bottom

H-II Top

H-Ill

H-Ill

H/46

I

H-IV H-IV

H/44

I

~31

H-V

H-V

H-Vl Inter- H-VII H-VIII H-IX mediate

Fig.8. Hura Basin, showing frequency of acritarch taxa and marker horizon.

I.

H/29

t";I/42

'

f27 m6

/2 H-IX

- - I~ H / 2 } H-X

H-Xl H-Xll

CORRELATIONOF LOWERGONDWANASEDIMENTS

sedimentary succession in the two adjacent basins. Moreover, corresponding environmental phases of deposition are identified in both basins. Three distinct climatic phases were noted in the sediments from the Chuparbhita Basin while deposition occurred in a single climatic phase in the Hura Basin (Table III). Ecological phases changed within each climatic phase and identical ecological phases were recognised in the corresponding horizons of the two basins (Figs.4, 5, 7). The climatic and ecological phases are named on the basis of dominant, significant and ecologically significant representatives of the palynostratigraphic zones (Table II, Fig.9).

Ecological phases within the climatic phases of the Chuparbhita Basin Each of the 10 palynostratigraphic zones identified in the basin are ecologically distinct. Climatic Phase Plicatipollenites-Parasaccites (Figs.4, 5) Two ecological phases (Ecol.Ph.) of deposition are distinguished in this climatic phase: Ecol.Ph. Ginkgocycadophytus (PN C-l) This genus (Fig.10f) is encountered in higher frequency than the climate indicator genera. The morphological organisation of the type-material of Ginkgocycadophytus has been recently doubted by Meyen (1987) as probable saccate pollen folded and with boat shaped configuration, simulating a TABLE III Climatic phases in Chuparbhita and Hura basins. Chuparbhita Basin Climatic Phase I -

Climatic Phase II-

Climatic Phase III-

Hura Basin

Monosaccate

PlicatipollenitesParasaccites

Not encountered

Cool Climate Phase Nonstriate disaccate

Nonstriate disaccate

Scheuringipollenites

Scheuringpollenites

Temperate Climate Phase Striate disaccate

Temperate Climate Phase

StriatopodocarpitesStriatites

Not encountered

Warm, Humid Climate Phase

247

monocolpate pollen. The trilete genus Callumispora (Fig.10g) follows in order of dominance. Quadrisporites (Fig.10p) is recorded in this phase. Ecol.Ph. Callumispora (PN C-2) Callumispora (Fig. 10g) and the radial monosaccate climate indicator taxa are almost of equal prominence in this phase of deposition. Climatic Phase Scheuringipollenites (Fig. 10c) Seven ecological phases are distinguished within this climatic phase. Ecol.Ph. Laevigatosporites-Brevitriletes (PN C-3) Laevigatosporites (Fig.10h) and Brevitriletes (Fig. 10i) contribute significantly to the assemblage in this phase of deposition. Ecol.Ph. Laevigatosporites-Lophotriletes (PN C-4) Laevigatosporites continues to be prominent in a considerable phase of deposition followed by Lophotriletes (Fig. 10k). This prolonged ecological phase of deposition, however, has distinct changes in its subsequent dominant representation in the assemblages and 5 ecological subphases are recognised, viz., Ecol. Subphases Leiotriletes (Fig.ll,1), Marsupipollenites (Fig.10,w,x), Cyclogranisporites (Fig.10,1) and Striatopodocarpites (Fig.10,d), followed by another subphase of Cyclogranisporites. Some of these genera are also significant ecological phase indicators in the adjacent Hura Basin. Ecol.Ph. Cyclogranisporites (PN C-5) Cyclogranisporites becomes the prominent member of the palynoassemblages for a prolonged phase of sedimentary succession after a continued influence of Laevigatosporites. Few acritarchs are present in this zone. Ecol.Ph. Cyclogranisporites-Microfoveolatispora-Indotriradites-Lalmatiasporites with diverse acritarchs and Prasinophytes (PN C-6) The exclusive dominance of the ecological indicator genus of the previous phase is obscured due to the prevalence of Microfoveolatispora (Fig. 10,m), Indotriradites (Fig. 11,q) and Horriditriletes (Fig.ll,m-p), in this phase. In addition, appearance of the trilete genus Lalmatiasporites (D'Rozario and Banerjee, 1987a,b; Banerjee and D'Rozario, 1987) in this phase (Fig.10,n; Figs.ll,a-g,r) is also characteristic; this genus dominates palynoassemblages in a thick sedimentary sequence in the adjacent Hura Basin (PN H-5)

248

M. BANERJEE A N D A. D'ROZARIO

CHUPARBHITA StratigraphiCagestral~raPal'/n°" posl~llonSam [e

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Fig.9. Schematic representation of data from Chuparbhita and Hura Basins, showing the palynological zones, climatic and ecological phases and marker horizons, correlated against lower Gondwana stratigraphy and age.

and is regarded as the indicator of an ecological phase of the basin. The occurrence of diverse acritarchs in high frequencies, viz., Circulisporites (Fig.10,v), Peltacystia (Fig.10,q,r), Tetraporina (Fig. 10,u), Kugulubeites (Fig. 10,t) and the Prasinophytes Haplocystia (Fig.10,y) and Maculatasporires (Fig.10,j) is also noteworthy. The combination

of the dominant genera, the appearance of Lalmatiasporites and the diverse acritarch suites distinguish this phase of deposition from the previous one. Ecol.Ph. Striatites-Cyclogranisporites (PN C-7) Cyclogranisporites continues as the dominant ecological indicator genus of this phase. Prevalence

Fig.10. (Magnification indicated by bar = 201~m) (a) Plicatipollenites indicus Lele 1964, S1. No. C/36/3 (b) Parasaccites obscurus Tiwari 1965, S1. No. H/21/4 (c) Scheuringipollenites barakarensis (Tiwari) Tiwari 1973, S1. No. H/42/7 (d)Striatopodocarpites subcircularis Sinha 1972, S1. No. C/1/6 (e) Striatites communis Bharadwaj and Salujha 1964, S1. No. C/15/2 (f) Ginkgocycadophytus sp. Sinha 1972, S1. No. C/7/5 (g) Callumispora tenuis Bharadwaj and Srivastava 1969, S1. No. C/15/5 (h) Laevigatosporites collienisis (Balme and Hennelly) Venkatachala and Kar 1968, SI. No. C/8/5 (i) Brevitriletes levis (Balme and Hennelly) Bharadwaj and Srivastava 1969, S1. No. H/16/5 (j) Maculatasporites indicus Tiwari 1964, SI. No. C/3/2 (k) Lophotriletes rarus Bharadwaj and Salujha 1964, S1. No. H/16/6 (1) Cyclogranisporites gondwanensis Bharadwaj and Salujha 1964, SI. No. C/15/4 (m) Microfoveolatispora foveolata Tiwari 1965, S1. No. H/27/5 (n) Lalmatiasporites barakarensis D'Rozario and Banerjee 1987, S1. No. H/27/6 (o) Ghoshiatriletes gondwanensis D'Rozario and Banerjee 1987, S1. No. C/3/I (p) Quadrisporites horridus Potoni~ and Lele 1959, S1. No. C/37/3 (q) Peltacystia venosa Balme and Segroves 1966, S1. No. C/7/4 (r) Peltacystia venosa Balme and Segroves 1966, 2 halves S1. No. C/7/10 (s) Kagulubeites sp. S1. No. C/11/1 (t) Kagulubeites verrucosus Bose and Maheshwari 1968, S1. No. C/9/5 (u) Tetraporina sp. S1. No. C/3/3 (v)Circulisporites parvus De Jersey 1962, S1. No. H/16/10 (w) Marsupipollenites striatus Balme and Hennelly 1956, SI. No. H/7/6 (x) Marsupipollenites triradiatus Balme and Hennelly 1956, S1. No. C/14/9 (y) Haplocystia pellucida Segroves 1967, SI. No. C/14/7

CORRELATION OF LOWER GONDWANA SEDIMENTS

Fig.lO.

249

250

of striate disaccates viz., Striatites (Fig.10,e) and Striatopodocarpites (Fig. 10,d) in the Scheuringipollenites phase suggests a temporary climatic fluctuation. Ecol.Ph. Acanthotriletes-Laevigatosporites (PN C-8) The Cyclogranisporites phase suddenly becomes insignificant and Acanthotriletes (Fig.ll,k) gains dominance along with Scheuringipollenites and Laevigatosporites. Few acritarchs are present in this zone. Ecol.Ph. Ghoshiatriletes (PN C-9) This phase represents another distinct phase of deposition in this basin with the newly described trilete genus Ghoshiatriletes (D'Rozario and Banerjee, 1987) (Fig.10,o; Figs.ll,h-j,s) as dominant member of the association. Scheuringipollenites is sparsely represented in this zone. Acritarchs such as Peltacystia, Circulisporites, Tetraporina, Kagulubeites and the Prasinophytes Haplocystia and Maculatasporites are significantly represented in this zone. These characteristics distinguish this phase from the other phases of deposition. Climatic Phase Striatites-Striatopodocarpites The nonstriate disaccates which characterise zones up to the previous one become remarkably insignificant and give way to the striate disaccates Striatites-Striatopodocarpites. A change of climate is suggested from the dominance of these groups in the assemblage. The combination and dominance of ecological indicator taxa, however, has not changed in this climatic phase. Ecol.Ph. Laevigatosporites-Cyclogranisporites (PN C- 1O) These two genera are the subdominant representatives in this climatic phase.

M. BANERJEEAND A. D'ROZARIO

Ecological phases encountered in the Scheuringipollenites climate phase of the Hura Basin Climatic Phase Scheuringipollenites Seven distinct ecological phases of deposition are encountered in the Hura Basin: Ecol.Ph. Brevitriletes-Laevigatosporites (PN H- 1) Brevitriletes is the most prevalent genus next to Scheuringipollenites. Laevigatosporites and Apiculatisporis are also prominent members of the assemblage. The acritarch taxa Peltacystia and Prasinophyte Haplocystia occur sporadically. Ecol.Ph. Laevigatosporites-Apiculatisporis (PN H-2) with Marsupipollenites The subdominant ecological phase indicator genus of the previous phase is dominant in this phase. The representation of Marsupipollenites in appreciable frequency is distinctive. This genus is rare and of low frequency in other Lower Gondwana basins of Peninsular India. Ecol.Ph. Laevigatosporites- Lophotriletes-C yclogranisporites (PN H-3) The three genera, with Scheuringipollenites, occur in varying combination and account for slightly fluctuating phases while maintaining the main ecological characteristics. Ecol.Ph. Striatopodocarpites-Laevigatosporites (PN H-4) Striate disaccates suddenly become more frequent in this phase and are well represented by Striatopodocarpites. Ecological phase indicator taxon Laevigatosporites is next in dominance. The prevalence of striate disaccates in the Scheuringipollenites climatic phase suggests fluctuating climatic conditions.

Fig. 11. (Magnification indicated by bar = 201am) (a-c) Lalmatiasporites &dicus D'Rozario and Banerjee 1987, SI. Nos. H/27/1, H/27/3. (d-g) L. barakarensis D'Rozario and Banerjee 1987, S1. Nos. H/27/6, H/27/5, H/27/1 (h-j) Ghoshiatriletes gondwanensis D'Rozario and Banerjee 1987, S1. Nos. C/3/2, C/3/1 (k) Acanthotriletes jhariaensis Kar 1968, S1. No. H/16/1 (1) Leiotriletes brevis Sinha 1972, SI. No. C/8/6 (m) Horriditriletes ramosus Bharadwaj and Salujha 1964, S1. No. C/37/3 (n-p) H. rajmahalensis D'Rozario and Banerjee 1987, S1. Nos. C/19/7, H/21/3. H/19/5. (q) Indotriradites surangei Tiwari 1965, SI. No. H/27/3 (r) Scanning Electron Microphotograph of proximal surface Lalmatiasporites barakarensis. (s) Scanning Electron Microphotograph of Ghoshiatriletes gondwanensis proximal face showing nature of trilete mark and rugulate ornamentation.

CORRELATION OF LOWER GONDWANA SEDIMENTS

251

I

I

20,urn

' 20tum-~

Fig.l ].

252

Ecol.Ph. Lalmatiasporites- MicrofoveolatisporaIndotriradites (PN H-5) The climatic phase indicator genus Scheuringipollenites suddenly dwindles and becomes almost negligible in abundance. A newly described genus, Lalmatiasporites D'Rozario and Banerjee 1987 (Fig.10,n; Figs.ll,a-g, r) dominates this phase with a number of other trilete genera. Lalmatiasporites resembles the trilete spores described by Rigby and Hekel (1977, pl.1, figs.9,10) as cf. Punetatisporites gretensis Balme and Hennelly from Permian sediments of Central Queensland. The same authors described as ?Punetatisporites gretensis (Rigby and Hekel, 1977, pl.l, fig.12) another trilete spore with irregular small spherical structures described as Ubisch bodies, apparently similar to the verrucate structures of Lalmatiasporites. The other significant trilete genera are Microfoveolatispora and Indotriradites. In addition, diverse acritarch genera are also frequently represented in this ecological phase, viz., Peltaeystia, Tetraporina, Cireulisporites, Kagulubeites and the Prasinophytes Haploeystia and Maeulatasporites. This assemblage is distinct from all previously described assemblages in having the restricted occurrence of Lalmatiasporites in high frequency and a low representation of saccates along with diverse acritarchs and Prasinophytes. Ecol.Ph. Laevigatosporites-Horriditriletes (PN H-6) The monolete genus Laevigatosporites dominates this assemblage followed in abundance by Horriditriletes. Acritarchs are represented by Peltacystia, Circulisporites and Tetraporina. Ecol.Ph. Cyclogranisporites-Laevigatosporites (PN H-7) These two genera occur in varying frequency in the assemblage and are the dominant representatives of the phase. Discussion

Evaluation and correlation of the environmental phases of deposition in the Chuparbhita and Hura Basins (Fig.9) Three climatic phases of deposition are suggested in the Chuparbhita Basin by the compara-

M. BANERJEE AND A. D'ROZARIO

tive prevalence of the climate indicator taxa. The basal cool climatic phase is not encountered in the Hura Basin. The youngest phase of deposition has been distinguished in the Chuparbhita Basin by the frequency of the warm climate indicators Striatopodoearpites-Striatites, with remarkably poor representation of nonstriate disaccate taxa. The Seheuringipollenites climatic phase of deposition, however, is common to both basins and is prolonged. In the Seheuringipollenites phase identical ecological conditions prevailed in the adjacent basins during several intervals of sedimentary succession. Fluctuating climatic conditions are also apparent in both basins during this phase. The following corresponding ecological phases are identified in both the Chuparbhita and Hura Basins: (i) The basal sediments of the Seheuringipollenites phase were deposited in the same ecological conditions with dominance of Brevitriletes. (ii) Laevigatosporites is the major ecological representative in both basins for a considerable period of deposition. In the Hura Basin this phase shows the occasional influence of acritarch taxa. (iii) The influence of Marsupipollenites in appreciable frequencies in the Laevigatosporites ecological phase of these two easterly basins of the Indian Lower Gondwana is significant because this taxon is represented as one of the dominant genera in the Scheuringipollenites climatic phase in Lower Gondwana sediments of Bhutan, Eastern Himalaya (Banerjee and Dasgupta, 1983; Banerjee et al., 1986). The genus is infrequently reported in negligible frequency from other Lower Gondwana basins of peninsular India. Marsupipollenites triradiatus Balme and Hennelly and M. striatus Balme and Hennelly are recorded in these two basins. Laevigatosporites, the infrequent genus of peninsular Lower Gondwana, is common in the Bhutan palynoassemblages. (iv) The Laevigatosporites, Lophotriletes and Cyelogranisporites combination has identical sequences of dominance in the subsequent phase of deposition in the two basins. (v) The Laevigatosporites-Striatopodoearpites combination occurs in both basins. (vi) The Lalmatiasporites ecological phase of the Hura Basin has identical representation of taxa, viz., Mierofoveolatispora, Indotriradites in the Chu-

253

CORRELATION OF LOWER GONDWANA SEDIMENTS

parbhita Basin; Lalmatiasporites, which is dominant in the Hura Basin occurs in low frequencies in the Chuparbhita Basin and the reverse situation occurs for Cyclogranisporites (Figs.5,7). Correlation of this ecological phase is proposed on the basis of the occurrence of a similar combination of taxa in the two basins. In addition, Lalmatiasporites appears to have a restricted range in both basins. Moreover, this ecological phase can be distinguished from previous phases by the diverse and frequent occurrence of acritarch suites. The subsequent ecological phases of the Chuparbhita Basin are not encountered in the Hura Basin.

Identification, correlation and significance of marker horizons (Fig.9) The ecology of the acritarch suites recorded from the Chuparbhita and Hura Basins discussed earlier suggests possible brackish water ecological conditions. The increased influence of these acritarch taxa at particular stratigraphic levels in the sedimentary succession of the two basins is noteworthy (Figs.6,8). Diverse and frequent acritarch suites occur in the Lalmatiasporites ecological phase of deposition in both basins. Similar acritarch swarms are present in the slightly younger Ghoshiatriletes ecological phase in the Chuparbhita Basin. Lalmatiasporites and Ghoshiatriletes represent different ecological phases at different stratigraphic levels but with identical acritarch suites. The type of ecological conditions responsible for the prevalence of these two different trilete genera is unknown. But the restricted occurrence and significant influence of acritarch suites have been used to distinguish these ecological phases as marker horizons (Meyen, 1987). The Lalmatiasporites diverse acritarch suite ecological phase is thus proposed as marker horizon I, which is identified in both basins. The Ghoshiatriletes diverse acritarch ecological phase is labelled as marker horizon II, and occurs only in the Chuparbhita Basin. The acritarch swarms at different stratigraphic levels may be considered as traces of marine transgression in the dominantly continental facies of deposition (Meyen, 1987).

Conclusions

The environmental phases of deposition in both basins show a change in the dominance of saccate genera from radial monosaccate, nonstriate disaccare to striate (taeniate) disaccates. This occurs in a similar sequence to that in Late Paleozoic basins in the southern hemisphere as well as in Indian Lower Gondwana sediments. The depositional environment of the two basins is however distinguished from the other Indian peninsular basins in that Laevigatosporites is dominant for a considerable depositional phase; in the appreciable frequency of Marsupipollenites at the basal phase of deposition; in the dominance of two new trilete genera viz., Lalmatiasporites and Ghoshiatriletes at different levels and the use of these as marker horizons. The marker horizons, with the new genera occurring in stratigraphically restricted sequences, are characterised by the frequent occurrence of diverse acritarch suites. The fluctuating pattern of the acritarch suites in the Chuparbhita Basin suggests possible phases of marine transgression in dominantly continental deposits. Correlation of the environmental phases of the two basins, including marker horizon I, suggests an isochronous depositional history. Palynoassemblages constituting the palynostratigraphic zones and environmental phases in these Rajmahal coalfields are comparable with most palynoassemblages of the Indian Lower Gondwana in the dominance and subdominance of saccate genera. The ecological indicator assemblage pattern is however somewhat different. The palynostratigraphic zones recorded by Bharadwaj and Sinha (1969) from the Singrauli coalfield show an extensive Scheuringipollenites climatic phase with occasional striate disaccate prevalence. A critical examination of the palynostratigraphic zonation diagram from the Singrauli coalfield shows two phases of diverse and abundant acritarchs (described by the authors as "Aletes") at different stratigraphic levels in this climatic phase. The fluctuating influence of acritarch suites at two stratigraphic levels in the Scheuringipollenites phase in the Singrauli coalfield compares with the present observation of two marker horizons and might be related to the same

254

phenomenon of marine transgressions. Thorough palynostratigraphic succession analysis in other basins of the Indian Lower Gondwana should show conclusively whether the occurrence of acritarch suites at particular stratigraphic levels coincided with eustatic or tectonic movements. The effect of eustatic movements have been recorded in marine sediments of the Talchir Formation; continuation of the effect of fluctuating movements in younger horizons is not unlikely (Banerjee, 1987).

Age of the Lower Gondwana sediments of Chuparbhita and Hura Basins The same relative frequencies of occurrence of saccate genera are remarkably consistent throughout the stratigraphic sequences of the Indian Lower Gondwana (Bharadwaj, 1971; Tiwari, 1974). Dominance by radial monosaccates is suggested to have occurred during basal Early Permian, i.e. in the Talchir and Karharbari Formations. Nonstriate disaccates, including Scheuringipollenites, dominated in the Barakar Formation of middle Early Permian and striate disaccates dominated during Late Permian i.e., the Raninganj Formation. But striate disaccate dominance, in association with Scheuringipollenites, is recorded from Upper Barakar sediments (late Early Permian) from a number of Indian Lower Gondwana basins (Tiwari, 1974). The dominance of the monosaccate genus Densipollenites in the Middle Permian Barren Measure Formation may reflect drier climatic conditions. The palynoassemblages recorded from the Chuparbhita and Hura Basins have been compared with the palynoassemblages from the Indian Lower Gondwana (Bharadwaj, 1966, 1971; Tiwari, 1974). The climatic phase Plicatipollenites-Parasaccites of the Chuparbhita Basin, with the ecological phases PN C-1 and PN C-2, are comparable to biozones in the Talchir and Karharbari (Banerjee, 1987); the Scheuringipollenites phase of both the Chuparbhita and Hura Basins is similar to the palynoassemblages recorded from the Middle Barakar Formation; and Striatopodocarpites-Striatites, in association with Scheuringipollenites, is similar to Upper Barakar Formation assemblages. As such an Early Permian age for the

M. BANERJEEAND A. D'ROZAR10

Lower Gondwana sediments of both the Chuparbhita and Hura Basins is suggested from the palynological evidence.

Acknowledgements The authors are thankful to the authorities of Coal India Ltd. and to Mr. S.K. Saksena, Mr. S.K. Pande, Mr. K. Dasgupta, Mr. U. Kumar, and Mr. N. Ahmad in particular for their kind cooperation during collection of samples. Financial assistance provided by University Grants Commission is thankfully acknowledged. The Director General, Geological Survey of India, has been kind enough to allow consultation of unpublished reports.

References Ball, V., 1877. Geology of Rajmahal Hills. Geol. Surv. India, Mem., 13(2): 1-94. Balme, B.E. and Segroves, K.L., 1966. Peltacystia gen. nov. - a microfossil of uncertain affinities from the Permian of Western Australia. J. R. Soc. West. Aust., 49(1): 26-31. Banerjee, Manju, 1987. Karharbari: a formation or biozone. Palaeobotanist, 36: 37-50. Banerjee, Manju and Dasgupta, R., 1983. Lower Permian Mioflora from the Gondwana of Bhutan, Eastern Himalaya. Himalayan Geol., 11(1): 166-179. Banerjee, Manju, Dasgupta, R., Chandra, D., Ghosh, R. and Choudhur, S.G., 1986. Palyno-petrography and depositional environment of Lower Gondwana coal from Bhutan, Eastern Himalaya. Indian J. Earth Sci., 13(1): 76-80. Banerjee, Manju and D'Rozario, A., 1987. Palynostratigraphy and environment of deposition in the Lower Gondwana sediments of Chuparbhita coalfield, Rajmahal Hills. Workshop on Concepts, Limits and Extension of Indian Gondwana. Birbal Sahni Inst. Palaeobot., Lucknow, pp.10-11 (Abstract). Bharadwaj, D.C. 1966. Distribution of spores and pollen grains dispersed in the Lower Gondwana Formations of India. Proceedings of the Symposium on Floristics and Stratigraphy of Gondwanaland. Palaeobot. Soc., Spec. Sess., December 1964, pp.69-84. Bharadwaj, D.C., 1971. Palynostratigraphy of Lower Gondwana succession in India. Ann. Dep. Geol., Aligarh Muslim Univ., 5 and 6: 390-419. Bharadwaj, D.C. 1975. Palynology in biostratigraphy and palaeoecology of Indian Lower Gondwana formations. Palaeobotanist, 22(2): 150-I 57. Bharadwaj, D.C. and Sinha, V., 1969. Sporological succession and age of Jhingurdah seam, Singrauli coalfield, M.P. Palaeobotanist, 17(3): 275-287. Bose, M.N. and Maheshwari, H.K., 1968. Palaeozoic sporae dispersae from the Congo. VII: Coal measures near lake Tanganyika, South of Albertville. Mus. R. Afr. Cent. Ann. S~r. in - 8 °, Sci. Grol 60: 14-110.

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