Paiaeoboranisl 52(2003) . 97-112 0031-0174/2003/97 -I 12 $200
Palynology of the Baratang Formation, . Andaman-Nicobar Islands and the significance of reworked palynomorphs
J. MANDAL, A. CHANDRA AND ANANTA P.BHATTACHARYYA
Birbal Salmi Institute of Palaeobotany, 53 University Road, Lucknow 226 007, India.
(Recei ved 08 November 200 I; revised version accepted 18 December 2002)
ABSTRACT
Mandal J. Chandra A & Bhattacharyya AP 2003. Palynology of the Baratang Formation, Andaman Nicobar Islands and the significance of reworked palynomorphs. Palaeobotanist 52(1-3): 97-112.
Spores-pollen and dinoflagellate cysts data from five sections of the Baratang Formation (Baratang Island) are analysed. The record of stratigraphic potential forms indicates an Early to Late Eocene age for the recovered assemblages. The palynoassemblages from this Formation are also associated with the reworked palynofossils belonging to Permian, Triassic and Jurassic-Cretaceous ages. The reworked taxa dominate over the poorly represented Eocene palynomorphs and have Gondwanic affinity. A comparison of Tertiary palynoflora of Baratang with Assam and Myanmar demonstrate the presence of some palynotaxa in all the areas but common occurrence of significant taxa such as Relilrisyncolpiles. Baculimonocolpiles and Lanagiopollis (regularis) shows more close relationship between Andaman and Myanmar flora than Assam. The recycled palynomorphs of Gondwanic affinity have provided valuable clue to locate the source and direction of sediments. Various views relating to provenance of reworked palynomorphs have been analysed on the basis of present data which suggest that Chindwin Basin of Myanmar mainly supplied reworked palynomorphs containing sediments. The palynological, palaeocurrent and lithological evidences do not support the origin of reworked elements from Wharton Basin, Assam Basin or autochthonous (Triassic) sediments.
Key-words-Palynology, Eocene, Baratang Formation, Reworked fossils.
~ ~~ ~-f1c61GfI mu~ ~~~~~~~~~B~~~-~ ~ ~ ~ ~ ~ ~ ~ ~~lT'l1~ ~ ~ B ~ ~\3ffifRm I 'l?T 'RfllT"OJ ~ ~~m ~ ~.o;r ~ ~ ~:~ ~, ~ (f~ B tRIf..q(f C1"HoqRl"1I(4 <:R"ffi I m ~ ~\3ffifR~ ~ ~ ~ ~ ~ ~ ~ if B f.rcl;cm qr:l'\ rrmt, ;;ft 'RfllT"OJ if 11'Tmif I ~ ~ ~m ~~ ~ ~cM ~ ~ ~ ~ ~ ~ ~.-t.T"1~ ~ © Birbal Salmi Institute of Palaeobotany, India 98 THE PALAEOBOTANIST ~ ~ ~ ~ qrc:qr~'1l ~ ~ ~ ~ ~-1ffi1~ ~ ~ m ~fcl; ett 'liT 'liT ~~~I ~,TT~~~~~~ettwcm~1 ~ ~ ~~, ~ ~' ~ qrc:qr~"tj. Q(I' II'jfcl$111, g1": INTRODUCTION HE Andaman-Nicobar groups of islands are a part of T Sunda Arc system that extends from Myanmar (Burma) to Sumatra. The sediments in these islands occur in two sets at------i 25 of exposures. The chain of north, middle and south Andamans km including Baratang forms the primary island part and the other NORTH set is the small islands lying on east and west of the main ANDAMAN • c;> chain. The primary chain of islands ranges in age from Late BARATANG ~Japani Cretaceous to Oligocene while the peripheral chain of islands ISLA~ND:/GOl~~e;~Y is Neogene in age. The sediments of main Andaman islands Hart • art are deep-sea flysch sediments, which were deposited through Creek turbidity currents (Karunakaran et ai., 1964; Pandey, 1972; Pandey et ai., 1992). These flysch sediments are classified •• k into two formations, namely the Baratang and the Port Blair formations (Chatterjee, 1967) with an unconformable junction. The Baratang sediments are mainly argillaceous and can be easily differentiated from the overlying arenaceous Port Blair Formation. 12· The marine fossils are meagre to absent in the flysch sequences of the main islands. Occasionally, the flysch Fig. I-Map of Baratang Island showing the locations of sections marked as * (Map adopted from Rajsekhar el al.. (990) sediments yield palynofossils as these sediments predominantly consist of land-derived clastics containing a ofBaratang Formation, Middle Andaman (Mathur & Mathur, variety of palynodebris. The palynological study is therefore, 1980) closely resembles with palynoassemblages of Laisong important for dating and correlation of these islands. The and Burdwan formations of Assam and Bengal basins present work reports the result of palynological investigation respectively. Late Triassic terrestrial palynomorphs and of Baratang Island for deciphering the age of sediments, dinoflagellate cysts were also documented from Middle relationship of flora with neighbouring areas and to deduce Andarnan (Sharma & Mehrotra, 1984; Sharma & Sarjeant. 1987). the provenance of reworked palynomorphs. Mandai et ai. (1994) recovered Early Eocene palynofossils from Middle Andaman and concluded that the assemblage PREVIOUS PALYNOLOGICALWORK compares grossly with those from Indian mainland and is closely similar to the Early Eocene flora of Myanmar. The mud The palynological data from the flysch-turbidites of of Mud volcano ooze from Baratang Island has yielded spores. Andaman-Nicobar Basin are few and are confined to the pollen and dinoflagellate cysts and the rich assemblage Middle Andaman and Baratang islands. Banerjee (1966) first consisted of palynomorphs belonging to Late Cretaceous to recorded palynoflora of Port Blair Formation from Baratang Oligocene (Mandai et ai., 1996). Recently Jafar and Tripathi Island. However, Jafar and Tripathi (2001) pointed out that (2001) reported Late Triassic mixed Late Cretaceous this section actually belongs to Baratang Formation. A variety palynoassemblage from the Middle Andaman. of angiosperm palynofossils were documented by Banerjee It is therefore clear that palynofossils have been recorded (1966) and he deduced a Palaeogene age by comparing this only from the Baratang Formation of the main Andaman islands palynoassemblage with that of Assam. In subsequent and the recorded assemblages do not resemble closely to each publicatidn, Banerjee, 1967 described an Upper Cretaceous other. This dissimilarity may be due to difference of facie or palynoflora from the Middle Andaman and he compared this interval time of deposition. However, the assemblages have assemblage with the assemblages from Assam, Bengal and one common feature in containing recycled palynomorphs of Krishna-Godavari basins. The palynoflora from the upper part different ages. MANDAL el ai-PALYNOLOGY OF THE BARATANG FORMATION, ANDAMAN-NICOBAR ISLANDS 99 ~ INDEX: ...... §Shale 5 4 ~:qSandy shale ...... S 4 ...... 1:-:-:[Sandstone ...... 3 ~ .:....::-:~ -:-:- -:-. 3 r?:~1Conglomeratic 2 .. 0. sanastone -:-~ -:- ~ 7"b 2 NS1 ~ Clay I bN01 - --- Section -1 Section-3 • Productive ~ o Unpoductive ~ ..:...----:...:.--:-...:.1:>1S • _0 _0_ . -'~PN012 14 -:- - c:>- '- :---:-.:-:4l ...... ·i ~tJ ~..:..-..:..~~"")11 ...... - -- 8 '7 ;- .-. -.~ 7 ...... 10 ...... 13 . 9 ...... 12 ...... 0':0"0· 6 . -' _ ...... 11 '0'· 0 '.0 _.-._. "_0_.- 5 10 9 SCALE -:-..:..-:--.:.-:-..:p 8 8 ...... _0_'- ...... 7 ~~ .:..---: ...:--:- ..:...-:~ 7 NO 6 I'm -.- :..--=1. NS 6 ~NG1 Section -2 Section-I. Section-5 Fig. 2-Lithocolumns showing the position of samples. MATERIAL AND METHODS Samples During the field session of 1984 two of us CAe& JM) Section 1 ( NiLambur-OraLkachcha Traverse) collected samples from different locations of the Baratang Island. Thirty-five samples belonging to Baratang Formation The section is exposed in a nala behind the Oralkachcha collected from five sections have been studied. The locations School. The rocks are black and green splintery shale, sandy of sections and Iithocolumns indicating the position of samples shale alternating with white, medium grained sandstone. have been shown in Figs. 1 & 2 respectively. 100 THE PALAEOBOTANIST Section 2 (Nilambur Church premises) one section (Section 4). The yield of palynomorph is poor to moderate and majority of the specimens are badly preserved. The section contains black shale, grey sandy shale, black Consequently, a number of specimens could not be identified. clay, nodular clay and conglomeratic sandstone. The samples The location of productive samples is indicated in Fig. 2. were collected from a well pit within the church premises. Sections 3 and 4 are rich in palynomorph contents than other sections. Minimum number of palynofossils has been Section 3 (Nilambur-Shastri Nala Traverse) recovered from Section 5. However, all the sections produced reworked palynomorphs of older ages. These recycled This pit section lies 4 km before Gandhi Jetty on right palynotaxa belong to Permian, Triassic and Jurassic side of Nilambur-Gandhi Jetty Road. The whole section Cretaceous ages and they out number the Tertiary consists of black clay. palynomorphs. Simultaneously, Lower Cretaceous taxa are more common than Permian and Triassic forms. In contrast, Section 4 (Forest Camp Office Section) Tertiary palynomorphs are meagre and require careful search to find them. Thus, no qualitative analysis is possible of these The section consists of black splintery shale, grey sandy assemblages. In this context it is important to mention that shale and white medium grained sandstone. The outcrop sections I and 5 did not yield any palynofossil of Tertiary age. section lies in a nala on west side of the Forest Camp Office. The following is the list of palynomorphs recovered from each section. The taxa (reworked) with asterisk mark indicate Section 5 (Nilambur-Gandhi Jetty Traverse) restricted vertical range. Other taxa occasionally cross the time boundaries. Some of the important palynomorphs have been The outcrop section is exposed on left side of Nilambur documented in plates 1-3. Gandhi Jetty Road near 13 km post which consists of grey splintery shale, black clay and white sandstone. Section 1 Methods Permian-*Faullipolleniles varius Bharadwaj emend. Tiwari el al., 1989; *Scheuringipollenifes maximus (Hart) The samples were chemically processed following the Tiwari, 1973; *Aurangapolleniles brevizonalus (Tiwari) Bharadwaj & Dwivedi, 1981. usual maceration procedure using HCI, HF, HN0 3 and 5% KOH solution. The polleniferous residue was mixed with polyvinyl Triassic-*Klausipollenifes schaubergeri (Potonie & alcohol and spread over the cover slip. After drying the cover Klaus) Jansonius, 1962. slip, it was mounted in Canada Balsam. The slides and Jurassic-Crelaceous-A raucariaciles ausfrali s photonegatives have been deposited in the Museum ofBirbal Cookson, 1947; Alisporiles grandis (Cookson) Dettmann, 1963. Sahni Institute of Palaeobotany, Lucknow. Commenl-Tertiary palynomorphs have not been found. RESULTS Section 2 Out of thirty-five studied samples, only sixteen samples Permian-*Faunipollenires varius Bharadwaj emend. have yielded spore-pollen including dinoflagellate cysts in Tiwari et al., 1989; *Corisacciles alufas Venkatachala & Kar, PLATEl /'" (Bars on the photographs represent 10 IJm. England Finder numbers are given within bracket afLer slide number) I. Alangiopollis sp., Slide No. BSIP 12651 (S30). 9. Spilliwllocolpile.l' bar·u!alu.\· Muller, 1968. Slide No. BSIP 12650 2. Lakiapollis ovalus Venkatachala & Kar, 1969, Slide No. BSIP (12114) 12649 (W48). 10. Polypodiaceaesporile.l' sp.. BSIP Slide No. 12666 (N 10/4) 3. Baculimonoeolpiles andamanensis MandaI el ai.. 1994, Slide No. II Millulilricolporiles millltlltol Kar, 1985. Slide No BSIP 12645 BSIP 12658 (K3311). (Y39/2). 4. Relilrisyncolpiles Ihaungii Mandai el al., 1994, Slide No. BSIP 12. Polypodiisporiles imparileT (Potonie & Sah) Dutta & Sah, 1970, 12653 (Q23). Slide No. BSIP 12659 (U 17/3) 5. Slriairileles susannae v.d. Hammen emend. Kar, 1979, Slide No. 13. Dandoliaspora lelollala Sah el ai, 1971, Slide No. BSIP 12642 BSIP 12661 (Y36). (R40). 6. Lanagiopollis regularis Morley, 1982, Slide No. BSIP 12644 14. Baculriporiles sp.. Slide No. BSIP 12659 (T 35/1). (SI8). 15. Dactylopollis magnificus Muller. 1968. Slide No. BSIP 12659 (X 7. PalaeocyslOdinium auslralinum (Cookson emend. Malley, 1972) 46). Lentin & Williams, 1976, Slide No. BSIP 12653 (11511). 16. Proxaperliles operCUlalltS v.d. Hammen, 1956, Slide No BSIP 8. SlrialOpollis sp., Slide No. BSIP 12648 (N34). 12662 (130/4). 17. Palynomorph type I, Slide No. BSIP 12654 (G 44). MANDAL et at.-PALYNOLOGY OF THE BARATANG FORMATION, ANDAMAN-NICOBAR ISLANDS 101 ~ 2 ~ ~ ~ ~ ~ ~ PLATE 1 102 THE PALAEOBOTANIST 1966; *Caheniasaccites indicus Srivastava, 1970; Triassic-*Klausipollenites schaubergeri (Potonie & *Chordasporites sp.; *Scheuringipollenites maximus (Hart) Klaus) Jansonius, 1962; *Falcisporites stabilis Balme. 1970; Tiwari, 1973; *Striatites varius Kar, 1968; *Crescentipollenites Chordasporites sp., Brachysaccus sp.; *Staurosaccites juscus (Bharadwaj) Bharadwaj et al., 1974; *Densipollenites quadrifidus Dolby in Dolby & Balme, 1976; *Playfordiaspora invisus Bharadwaj & Salujha, 1964; *Microbaculispora sp. cancellosa (Playford & Dettmann) Maheshwari & Banerjee Triassic- Verrucosisporites sp.; *Klausipollenites emend. Vijaya, 1995; *Goubinispora indica Tiwari & Rana, schaubergeri (Potonie & Klaus) Jansonius, 1962; 1981. *Falcisporites stabilis Balme, 1970; *Staurosaccites Jurassic- Cretaceous- *A equitriradites spinulosus quadrifidus Dolby in Dolby & Balme, 1976; *Ovalipollis sp.; (Cookson & Dettmann) Cookson & Dettmann, 1961; Alisporites Tikisporites complicatus Kumaran, 1980. grandis (Cookson) Dettmann, 1963; Podosporites d. P. Jurassic-Cretaceous-A raucariapollenites sp.; tripakshi Rao emend. Kumar. 1981; Cerebropollenites sp.; Cicatricosisporites sp.; *Aequitriradites dubius Delcourt & Podocarpidites khasiensis Dutta & Sah, 1970; Sprumont emend. Delcourt et al., 1963; *Callialasporites Ginkgocycadophytus sp.; Araucariapollenites sp.; dampieri (Balme) Sukh-Dev, 1961; *c. lucidus (Pocock) Cicatricosisporites sp.; * Callialasporites dampieri (Balme) Maheshwari, 1974; Alisporites grandis (Cookson) Dettmann, SUkh-Dev, 1961; *c. lucidus (Pocock) Maheshwari. 1974; 1963; Cerebropollenites sp.; Osmundacidites sp.; Polycingulatisporites reduncus (Bolkhovitina) Playford & *Triporoletes reticulatus (Pocock) Playford, 1971; Dettmann, 1964; *Contignisporites sp. Dacrylopollis magnificus Muller, 1968; BacUlriporites sp. Tertiary-Dandotiaspora telonata Sah et ai, 197 I; Tertiary-Cyathidites australis Couper, 1953; Lygodiul11sporites eocenicus Dutta & Sah, 1970; Dicryophyllidites sp.; Polypodiisporites impariter (Potonie Polypodiaceaesporites sp.; Minutitricolporites minulUS Kar, & Sah) Dutta & Sah, 1970; Polypodiaceaesporites sp.; 1985; Lwwgiopollis regularis Morley, 1982; Tricolporopilites Striatriletes susannae v.d. Hammen emend. Kar, 1979; S. pseudoreticulatus Kar, 1985. paucicostatus Kar, 1985; Retitrisyncolpites thaungii Mandai Comment-Only 3% specimens belong to Eocene age. et af.. 1994; Striacolporites cephalus Sah & Kar, 1970; Minutitricolporites minutus Kar, 1985; Polyadopollenites Section 4 miocenicus Ramanujam, 1966; Proxapertites operculatus v.d. Hammen, 1956; Baclllimonocolpites andamanensis Mandai Permian-*Crescentipollenites fuscus (B haradwaj) et al., 1994; Striatopollis sp.; Neocouperipollis brevispinosus Bharadwaj et al., 1974; Lunbladispora sp.; Densoisporites (Biswas) Singh & Sarkar, 1988; Phragmothyrites eocenicus sp.; *Scheuringipollenites maximus (Hart) Tiwari, 1973. Edwards emend. Kar & Saxena, 1976. Triassic-*Falcisporites stabilis Balme, 1970; Comment-Only 10% palynofossils belong to Eocene. *Staurosaccites quadrijidus Dolby in Dolby & Balme, 1976; *Klausipollenites schaubergeri (Potonie & Klaus) Jansonius, Section 3 1962. Jurassic-Cretaceous- *Aequitriradites spinuloslls Permian-*Crescentipollenites fuseus (Bharadwaj) (Cookson & Dettmann) Cookson & Dettmann, 1961; Alisporites Bharadwaj et al., 1974; */ndotriradites korbaensis Tiwari, sp.; * Callialasporites dampieri (Balme) Sukh-Dev, 1961; 1964; * Striatites varius Kar, 1968; Lundbladispora sp.; Cerebropollenites sp.; Podocarpidites klwsiensis Dutta & Del15oisporites sp.; *Scheuringipollenites maximus (Hart) Sah, 1970; Araucariapollenites sp., Bacutriporites sp. Ti wari, 1973; Vesicaspora sp.; * Trochosporites tripus Tertiary-Cyathidites australis Couper, 1953; Venkatachala & Kar, 1968; Aurangapollenites brevizonatus Polypodiisporites impariter (Potonie & Sah) Dutta & Sah, (Tiwari) Bharadwaj & Dwivedi, 1981. 1970; Retitrisyncolpites thaungii Mandai et al., 1994; R. PLATE2 /'...... (Bars on the photographs represenl 10 lIm. England Finder numbers are given within bracket after slide number) Caheniasaccite.l' indicus Srivastava. 1970, Slide No. BSIP 12654 6. CUllealisporile.l' exiguu.l' Salujha. 1965. Slide No. BSIP 12666 (P22/ (G44). 4). 2. Faunipollenites variu; Bharadwaj emend. Tiwari et al., 1989, 7 Calliala.lporile.\' dampieri (Balme) SUkh-Dev. 1961, Slide No. BSIP Slid~No. BSIP 12655 (G30). 12659 (T3613). 3. Tikisporite.l· complicatu; Kumaran, 1980, Slide No. BSIP 12660 8. Polycingulali.l'porile.l' reduncu.\' (Bolkhovitina) Playford & (Q25). Dettmann. 1964, Slide No. BSIP 12642 (LI4) 4. Callialasporiles lucidus (Pocock) Maheshwari, 1974. Slide No. 9. Sirialiles varius Kar, 1968, Slide No. BSIP 12661 (L46/1). BSIP 12664 (K46). 10 Conligni.lporiles sp., Slide No. BSIP 12647 (037/2). 5. Troc!Jmporiles Iripus Venkatachala & Kar. 1968. Slide No BSIP II SlaUTOSa(TileS quadrijidus Dolby in Dolby & Balme. 1976. Slide 12646 (V23/4) No. BSIP 12659 (W31). 12. Araucariapollenite.l' sp.. Slide No. BSIP 12642 (L40). MANDAL el al.-PALYNOLOGY OF THE BARATANG FORMATION, ANDAMAN-NICOBAR ISLANDS 103 J-----I • I----l J-----I • 9 I-i I----l 11 I-i PLATE 2 104 THE PALAEOBOTANIST reimannii Mandai et al., 1994; Monocolpites spinosus Baksi, Horizon-Baratang Formation, Late Cretaceous-Eocene. 1962; Spinizonocolpites baculatus Muller, 1968; Lakiapollis Description-Pollen grain prolate, longitudinally folded, ovatus Venkatachala & Kar, 1969; Proxapertites operculatus 93·5 11min equatorial view. Tricolpate, colpi long and slit-like. v.d. Hammen, 1956; Baculimonocolpites andamanensis Exine 2·5 11m, nexine thinner than sexine, 1 11m at equator, Mandai et al., 1994; Alangiopollis sp.; Acanthotricolpites indistinct at poles. Surface striate at poles and colpus margins; kutchensis (Kar & Kumar) Singh & Misra, 1991; striae fine, 111m wide, parallel to colpi, anastomose forming Neocouperipollis brevispinosus (Biswas) Singh & SarkaI', long narrow lumina, curve at margin and pass on to opposite 1988; Pellicieroipollis sp.; Phragmothyrites eocenicus surface. Surface foveo-reticulate in equatorial area, muri 111m, Edwards emend. Kar & Saxena, 1976; Notothyrites sp.; lumina circular to oval. irregular in arrangement which gradually Operculodinium centrocarpum (Deflandre & Cookson) Wall. change to striate pattern. 1967; Achomosphaera sp.; Cleistosphaeridium brevispinosum Comments-Single specimen has been found from Jain & Millepeed, 1975; Polysphaeridium subtile (Davey & Section 2. This specimen is very distinct and closely similar to Williams) Bujak et aI., 1980; Palaeocystodinium australinum Dactylopollis magnificus Muller, 1968. However. second (Cookson emend. Malley, 1972) Lentin & Williams, 1976. ornamentation type below the reticulate-foveolate zone could Comment-The reworked palynomorphs are about 500/0 not be recognised. Muller (1968) described this taxon from at the base of the section which gradually decrease and become Senonian to Palaeocene sediments of Malaysia but is unknown scare at the upper level. from India and Myanmar. Section 5 Genus-LANAGIOPOLLIS Morley, 1982 LANAGIOPOLLIS REGULARISMorley, 1982 Permian-*Cuneatisporites exiguus Salujha, 1965; *Striatites varius Kar, 1968. (pI. 1·6) Triassic-*Falcisporites stabilis Balme, 1970; Horizon-Baratang Formation, Late Cretaceous-Eocene. *Playfordiaspora cancellosa (Playford & Dettmann) Description-Pollen grain subtriangular, oblate. amb Maheshwari & Banerjee emend. Vijaya, 1995. convex, 60·5 11min polar view. Tricolporate, colpus and pore Jurassic-Cretaceolls- *Aequitri radites dubi us characters indistinct due to oblique preservation, pores appear Delcourt & Sprumont emend. Delcourt et al., 1963; costate. Exine 3·5 11mat mesocolpia; sexine 1·5 11m, thinner Callialasporites sp.; Araucariacites sp.; Alisporites grandis than nexine (211m); both sexine and nexine gradually thin out (Cookson) Dettmann, 1961 towards aperture. Exine tectate. tectum ca. 111m, columellae Comment-Tertiary palynofossils are absent in this distinct, closely placed, ca. 0·5 x 111m. Surface microreticulate section. on low focus; muri very low, simplicolumellate, lumina generally circular. SYSTEMATICS Comments-Single specimen has been recovered from Section 3. The thicker nexine and reticulate surface feature Descriptions of a few uncommon taxa and new to this compare with Lanagiopollis regularis Morley, 1982. However, area are given below. the present specimen has thinner exine and muri than the G£nus-DACTYLOPOLLIS Muller, 1968 holotype. The character of aperture is masked due to oblique DACTYLOPOLLIS MAGNlFICUSMuller, 1968 preservation. (pI. 1'15) ...... PLATE 3 7" (Bars on the photographs represent 10 I-lm. England Finder numbers are given within bracket after slide number) t Vesir:aspora sp., Slide No BSIP 12644 (En). 8 Cerebropollenites sp, Slide No. BSIP 12652 (U25/2). 2. Aequilriradite.\ dubius Delcoun & Sprumonl emend. Delcoun 1'1 9 Cresl'enlipollenile.l.lil.H·lIs (Bharadwaj) Bharadwaj el al. 1974. al. 1963. Slide No. BSlP 12663 (L49). Slide No. BSIP 12656 (Fll/1) 3 Klausipollellites se/wubergeri (Potonie & Klaus) Jansonius, 1962, 10. SI'!lellringipo/lenile.1 maximu.I (Han) Tiwari, 1973, Slide No. BSIP Slide No. BStP 12657 (GIO/I). 12655 (02512). 4. GoulJinispora indica Tiwari & Rana, 1981, Slide No. BSlP 12645 1I. Corisa('('iln alula.1 Venkatachala & Kar, 1966, Slide No. BSIP (P42) 12655 (SI5/4). 5 Falr:isporires slabili.\ Balme, 1970, Slide No. BSIP 12658 (H22/ 12. Brae/lysaTl'us sp., Slide No. BSIP 12642 (Q23) 3). 13. Ovalipo/lis sp., Slide No. BSIP 12643 (P27/2) 6. KlllkisporileI sp.. Slide No. BStP 12651(KI7). 14. Playjordiaspora I'anr:e/losa (Playford & Dettmann) Maheshwari 7 Aurangapollenite.\ brev;zonarus (Tiwari) Bharadwaj & Dwivedi, & Banerjee emend. Vijaya. 1995. Slide No. BSIP 12665 (H26/2) 1981, Slide No. BSIP 12647 (P37) MANDAL el aL,-PALYNOLOGY OF THE BARATANG FORMATION, ANDAMAN-NICOBAR ISLANDS 105 H ~'~~.i.:~~~ ,.; ...... ')010 , .••~ ,'.;" ,!": ., • L' I---l ~. ~~ l'!!i..~,~ ~~'_:'t! .. ~. (~ ~ 'of "':.:~~II"· ..... ~' r· ...· ~ ,!t; ~' .\:,* '.." H • I----l ...... -l 4 H 12 I----l 5 .... ,.~~,;' ,..' ",~~,~ """ ~'t.:;.I' ...... , -- I:'l 1 -'"" ;'>6. -,.p.-. ~: , , "~'...- t-----I 7 t-----I 8 PLATE3 106 THE PALAEOBOTANIST Genus-ALANGIOPOLLIS Krutzsch, 1962 lntubidinium Shanfu, 1999 in surface characters but the Chinese specimens have comparatively larger size, thinner wall ALANGIOPOLLIS sp. and more surface structures (canals) than the present form. (pI. 1'1) Horizon-Baratang Fonnation, Late Cretaceous-Eocene. COMPARISON OF ANDAMAN Description-Pollen grains rounded triangular in polar PALYNOFLORA view, 70 x 79 1ill1. Tricolporate, colpi long, 22 11m, tapering towards pole, margin granular; pore lalongate, 91ill1 in diameter, It is necessary to compare the Palaeogene palynotlora thickening absent on colpus and pore margins. Exine 3,5-4 recorded till date from Andaman with Assam and Myanmar to 11m;sexine-nexine not separable and thickness near aperture examine their relationship. Few palynological data generated not clear. Surface striate, striae parallel to colpi, varies in from Myanmar (potonie, 1960; Reimann & Thaung, 1981) allow thickness of width, 1-2 1ill1, thicker at equator, anastomoses limited but significant comparison. Several taxa namely occasionally forming long narrow lumen,·more common on Palmidites, Palmaepollenites. Dandotiaspora, Strialrileles, polar area, lumen width always lesser than the striae. Only a Dis ulci tes, N eocoupe ripoll is, Triporopoll en iles. single structural pattern (striate) present. Striacolporiles, Triorites. Proxapertites, Meliapollis, Comments-Two specimens have been recovered from Lakiapollis and Margocolporites are present in all the three Section 4. The character of exine is similar with the generic areas and a number of them are common at species level. In description of Alangiopollis by Morley (1982). The specimens addition to the similarity, a few genera like Retitrisyncolpites. are distinct having only one structural pattern and no Baculimonocolpites and LanagiopoLLis (regularis) are comparable forms could be found. common between Andaman and Myanmar. On the other hand. few taxa, such as Tricolpites phillipsii and Dislaverrusporiles Genus-STRlATOPOLLIS Krutzsch, 1959 margarilatus of Malaysian affinity are present in Myanmar STRIATOPOLLIS sp. but are unknown from Andaman. Similarly, DaClylopollis, Striatopollis and Meyeripollis are present in Andaman while (pI. H) they are absent in Myanmar. A few genera known from Andaman Horizon-Baratang Fonnation, Late Cretaceous-Eocene. like Matanomadhiasulciles, Dermatobrevitricolporiles, Description-Pollen grain folded, oblate, 82 11m in Sastripo[{enites, Minutitricolporites. Tricolporopil iles, equatorial view. Tricolpate, colpi long, slit-like, characters not Meyeripollis and Striatopollis are common in Assam and distinct due to fold. Exine 4 11m at mesocolpium, 2 11m at Andaman flora but many of them do not compare at species apocolpium, nexine indistinct, llill1 at mesocolpium. Surface level. intectate, columellae free, long, form pseudo-striate pattern The comparison thus indicates that though the on polar areas in low focus; 2 11m long, 1 Iill1 wide, closely Palaeogene palynoflora is grossly similar in Andaman, Assam placed, closer and shorter at apocolpia and absent near colpi. and Myanmar but the common presence offew dominant and Comments-Section 2 has yielded single specimen. The significant taxa like Relilrisyncolpites, Lanagiopollis and specimen is grossly comparable to Perfotricolpites neyvelii Baculimonocolpites point closeness of Andaman microtlora (Navale & Misra) Mandai & Kumar, 2000 but differs in being with Myanmar rather than with Assam. smaller in size. Moreover in the present specimen, columellae are not digitate and surface is pseudo-striate but not perforate AGE OF THE SEDIMENTS reticulate. In the absence of marine nannoplankton and scarcity of Palynomorph Type-I marine fauna, palynology plays an important role in determination of age of the Andaman flysch sequences. The (pI. 1'17) present assemblages contain palynomorphs of various ages Horizon-Baratang Fonnation, Late Cretaceous-Eocene. and thus the palynofossils indicating youngest age is Description-Single specimen, nearly circular, 37 x 39 11m, considered as the age of the sediments. Geologically the age aperture not discernible. Surface beset with some raised of Baratang Formation ranges from Late Cretaceous to Eocene structure~,about 18 structure on one surface, intrastructural (Chatterjee, 1967). Though the palynomorphs (Tertiary) are areas smooth; structures 2 11m high with little swollen base poor in number, some of them are important marker and the and flat tips. Each structure has 111m deep cavity at tips. Wall range of vertical distribution is well defined. Thus age has 21ill1 thick, ca. 4 11mincluding the structure. been postulated from their known distribution range. The Comments-Single specimen has been recovered from distribution of selected stratigraphically significant Section 2. The specimen grossly compares to algal taxon palynomorphs in the Baratang Formation has been presented in Fig. 3. MANDAL el at.-PALYNOLOGY OF THE BARATANG FORMATION, ANDAMAN-NICOBAR ISLANDS 107 Taxa Early Eocene Middle Eocene Late Eocene Dandoliaspora lelonala Baculimonocolpiles andamanensis Lakiapollis ovalus Pellicieroipollis sp. Spinizonocolpiles baClilalus Relilrisyncolpiles spp. Slrialrileles susannae Polyadopolleniles miocenicus MinUlilricolporiles minHlus Lanagiopollis regularis AcanlhOlricolpiles kUlchensis Fig. 3-Distribution of some stratigraphically important palynomorphs from Baratang Formation. Section 2 Section 4 The section yielded a variety of taxa that provide evidence The dinoflagellate cysts, Operculodinium centrocarpum, on the age of assemblage. The first appearance of Cleistosphaeridium brevispinosum and Polysphaeridium Retitrisyncolpites has been recorded in the Early Eocene of subtile recorded in this section are long ranging taxa (Eocene Myanmar (Reimann & Thaung, 1981) and Middle Andaman Miocene) but dominantly occur within the Eocene (Williams (Mandai et al., 1994). The taxon abundantly occurs till Middle et al., 1993). However, Palaeocystodinium australinum is Eocene and is rare in Late Eocene in Myanmar (Reimann & restricted within Early to Late Palaeocene. Considering the Thaung, 1981). Similarly Minulitricolporites and absence of other Palaeocene marker dinocysts and terrestrial Striacolporiles also appear at the same time (Kar, 1985) and palynofossils, the taxon Palaeocystodinium seems to be continued through Palaeogene. However, Striatriletes first reworked. appeared in the Middle Eocene in Indian main land (Kar, 1983) and is abundant in the overlying sequences. In Myanmar, the taxon appeared in Early-Middle Eocene as Cicatricosisporites 30 macrocostatus (Reimann & Thaung, 1981). However, in other \N tropical areas the taxon was recorded later in the earliest Neogene (Germeraad et al., 1968). The genus Polyadopo llenites is commonly known from Oligocene in Assam but has 1 o also been recorded from the Late Eocene of Nagaland (Mandai, ~ 1996). The above analysis indicates that the assemblage ranges from Middle to Late Eocene in age. In the absence of Oligocene marker taxa like Crassoretitrileles, Trisyncolpites and Meyeripollis the assemblage cannot be taken as younger than Late Eocene. Section 3 The meagre Tertiary palynofossils recovered from this section do not help much in age assignment. The taxa Minulitricolporites and Lanagiopollis regularis appear in Early Eocene (Morley, 1982; Kar, 1985) and are restricted within the Eocene. Dandotiaspora, except D. dilata also rarely extends beyond the Early Eocene. Other taxa or their association in the assemblage do not reflect Middle Eocene or younger ages. Thus, at least an Early Eocene age may be postulated from the palynoassemblage. Fig. 4-Palaeogeography and ocean circulation during the middle Cre taceous (after Hag, 1985 in Kunihiro & Kunio, 1991). 108 THE PALAEOBOTANIST The terrestrial taxa Retitrisyncolpites, (Banerjee, 1967; p. 213). Similarly the Oligocene assemblage Baculimonocolpites, Lakiapollis ovatus. Pellicieroipollis, includes the reworked taxa (e.g., Alisporites: Mathur & Mathur, Proxapertites, Acanthotricolpites and Neocouperipollis have 1980; pI. I, figs 8, 9). Recently Jafar and Tripathi (2001) claimed limited vertical distribution. They present abundantly in the the recovery of Late Cretaceous palynoassemblage from Late Palaeocene-Early Eocene sediments. Lakiapollis ovatus Middle Andaman but did not mention the names of taxa or and Pellicieroipollis range within Late Palaeocene to Eocene photo documented the specimens. (Thanikaimoni etal., 1984; Venkatachala et al., 1989) though The above synthesis demonstrates that the Late Lakiapollis is known to extend rarely to the Early Miocene Cretaceous palynoassemblage is still unknown from Andaman. (Rao, 1996; Singh et al., 1992). Retitrisyncolpites dominantly Thus, from the palynoassemblages of sections I and 5, occurs in Early to Middle Eocene sediment of Myanmar. The Cretaceous age connotation would be doubtful and age last appearance of Spinizonocolpites baculatus is recorded assignment remains unresolved. in the Early Eocene (Muller, 1968). Moreover, Proxapertites, Acanthotricolpites and Neocouperipollis are rare to absent SIGNIFICANCE OF REWORKED in overlying sequences of the Early Eocene. Thus, Early PALYNOFOSSILS Eocene age can be assumed from the abundance of Retitrisyncolpites and Baculimonocolpites and in absence In the studied five sections from Baratang Island, recycled of any other marker taxa of Palaeocene or younger ages. Permian, Triassic and Jurassic-Cretaceous pollen taxa of Dinoflagellate cysts are long ranging and do not help in precise Gondwanic affinity are present. The previously recorded age determination. assemblages from Andaman Islands, except one, reveal similar admixture of pollen-spores of di fferent ages. However, Permian Sections 1 & 5 palynotaxa have been recorded for the first time in the present assemblage. It is surprising that the Early Eocene assemblage Both the assemblages from sections I and 5 consist of recovered from lignitic sediments of Kadamtala, Middle Permian, Triassic and Jurassic-Cretaceous palynofossils Andaman (Mandai et al., 1994) is completely free of reworked without any Tertiary taxa. Obviously, Early Cretaceous age taxa. The sediments ofBaratang Formation are flysch in nature may be fixed for these two assemblages. However, it can be and were deposited through turbidity currents. How this mentioned that reworked palynomorphs are similar to other assemblage remained free from recycled palynomorphs within se~tionscontaining Tertiary taxa. This indicates same source such terrain remains an unsolved issue. of the sediments containing these recycled palynofossils. Only The presence of Triassic palynomorphs and dinoflagellate one sample in Section I and two samples from Section 5 (Fig. cysts (Sharma & Mehrotra, 1984; Sharma & Sarjeant. 1987) 2) have poorly yielded palynomorphs. Had more samples been has lead to conclusion that Triassic sediment present in productive, it seems that palynomorphs of younger age would Andaman Islands (Sharma & Mehrotra, 1984). This has have yield. The assemblages do not contain Aquilapollenites, aroused much debate. Several researchers (Pandey, 1986; Ariadnaesporites and Scordilla to support Late Cretaceous Kumar, 1990; Jafar & Tripathi, 200 I) ruled out the presence of age. However, Late Cretaceous taxa like Dactylopollis and Late Triassic sediment as inliner or exotic blocks in Middle Bacutriporites have been recorded here in the Eocene Andaman. According to them Late Triassic palynomorphs are assemblage. reworked. On the other hand Mehrotra and Sarjeant ( 1990) In Baratang Island, two horizons of fauna are known. conformed the presence of Triassic sediments in the Andamans The lower horizon has the indigenous Globotruncana and strongly argued for the authocthonous nature of the assemblage of Late Cretaceous age and the upper horizon Triassic elements. However, Jafar and Tripathi (200 I) reported contains recycled Cretaceous fauna ranging in age from Late Triassic palynomorphs at several levels in the Late Palaeocene to Late Eocene (Pandey et al., 1992). The Cretaceous succession of Chainpur Section- the locality from Cretaceous-Palaeocene microfauna are known from Baratang where Sharma and Mehrotra (1984) reported Late Triassic Formation (Guha & Mohan, 1965; Pandey, 1972; Pandey & sediments. Furthermore, microforaminifera of Cretaceous Rao, 1976; Kumar & Soodan, 1976). Cretaceous planktonic Palaeogene age have been recovered from the same samples foraminifera and marine algae are also recorded from this which Sharma & Mehrotra, 1984 had studied (Pandey, 1986). Formation (Rajshekhar et al., 1990; Badve & Kundal, 1986). Mehrotra, however, in a written communication disagreed with Thol,lgh Cretaceous faunal assemblages have been the observation of Pandey (1986) and states "the samples recorded, palynoflora of Cretaceous or Palaeocene age is not containing Triassic spores-pollen and dinocysts do not contain known from Andaman Islands. The only Cretaceous any younger palynomorphs. Pandey (1986) while preparing palynoassemblage (Banerjee, 1967) reported from Middle the Cretaceous- Palaeogene microforaminifera from these has Andaman, in fact contains Tertiary palynomorphs but not given details of sample nos. and recorded species." abundance of Cretaceous forms led him to fix age as Cretaceous MANDAL III al.-PALYNOLOGY OF THE BARATANG FORMATION. ANDAMAN-NICOBAR ISLANDS 109 '1 r 120° 60° 90° =-II-=... 300 600 , 90° \ " f- "." \ ' \ , A A A ~tNMAI --~.~,~:.\TIBEr.. _~1Y!'~1R-- 30° P~IBETI ~o-M...... ", .l...... _ ....- shelf =i' --4... FLYS H4' S~D -~C'_ -'L 1"-1~_Q", EDIM'~~ ':.' .,. Iv"s <' (.'1'0~ r . ( ~ A? ~",? ~)-/A -....~~.. I I 0 • <>\.;...,.; / /.,. / Iy ! /, A? 1- ~ S"a"o~, 0°- .I . I-- ~/~/~/ Y -,... ~/ ;.: :. // S --~ /~ 0° ' / ~ 1>-~ pshelf . ~ .,.... '. IND\AN~ . ..····;~helf\'),., : PLATE ,. / OECCA~··'.)... ===- I-- :/A TR~P..· ..... 30°- ; INO,'t)N PL.' : ') .... : I ...... , 30° i; :~~h':~..... 80my 60° 90° TIBET MAYANMAR .~\ 30° INDEX FLYSCH <"',.t. If S.P. ~ - - A? Andaman Ophiolite / /" Shelf '-:S--~ '. r'lNDIAN ? Shan .~1 SP Plateau ,- , eA~ ====- <) <.... PLATE =--- ~~A y Subduction zone «'1-" ~ is ~ Subduction zone -;- 0° Qssumed Spreading ~ ridge -". '.' # >::\~Spreading ridge At \~ assumed Direction of sediment ~ transport 30° A Volcanism l,Omy Fig 5-Plate tectonic maps during 80 my. 60 my. 40 my of Myallmar-Andamall area (after Bender. 1983). In the present work Triassic taxa recovered together with palynomorphs in age determination, they are very useful in palynofossils of different ages from all the sections. Such palaeogeographical reconstructions. recycling is expected in flysch turbidites of Middle Andaman. Jafar and Tripathi (2001) remarked that Late Cretaceous These Triassic specimens are reworked which were carried by sections of Andaman contain reworked Late Triassic the sediments with other Gondwanic elements and redeposited palynomorphs white Late Cretaceous fossils occur in the in Andaman. Though there is no signi ficance of these recycled Eocene assemblage. Although the present study shows that 110 THE PALAEOBOTANIST Maastrichtian taxa like Dactylopollis and Bacutriporites Exmouth Plateau which lies in the "Northeastern" sector of present in Eocene assemblage and therefore, such conclusion Andaman-Nicobar Basin. Late Triassic to Cretaceous marine needs verification. The taxa of Permian e.g., Caheniasaccites, strata is present in Wharton Basin (Rad et al., 1992) but Faunipollenites, Corisaccites and Scheuringipollenites: transportation of these sediments to Andaman Basin through Triassic e.g., Staurosaccites, Klausipollenites, the turbidity current during the Late Cretaceous remains Pla)1ordiaspora, Brachysaccus and Coubinispora in addition unanswered. The palaeogeographical maps of this region to Jurassic-Lower Cretaceous e.g., Callialasporites, during Cretaceous (Bender, 1983, fig. 66b; Acharyya, 1994, Cerebropollenites, Aequitriradites and Triporoletes occur fig. 4; Rich & Vickers-Rich, 1999, fig. 5) show position of together in the Eocene assemblage ofBaratang. Additionally, Andaman Islands at about 15°N latitude while Wharton Basin nearly same association of reworked taxa is also part of the lies near to 300 S (Jafar & Tripathi, 2001). The palaeocurrent assemblages of sections I & 5 which did not yield any Tertiary map of Cretaceous (Fig. 4) shows the flow of current from palynofossils. Moreover, as mentioned earlier. no Late Andaman side towards northern margin of Australia. The Cretaceous and Palaeocene palynofloral assemblages have authors also opined that the sedimentation provenance been documented from Andaman Islands. Hence the source changed after Late Cretaceous from Australian direction to of palynofossils must be the area around Andaman where the north. In fact, change in directional pattern of sediments both the terrestrial and marine sediments of these ages existed. started in Andaman area with the uplift of Andaman geanticlines at the Early Miocene (Karunakaran et al .. 1964; SOURCEOFTHE REWORKED Pandey, 1972), which stopped the pre-existing northerly PALYNOMORPHS turbidity channel. Palynological evidences also demonstrate identical recycled pollen-spore association in all the recorded Since the Cretaceous-Palaeogene sequences of Andaman assemblages. This indicates that source of sediment was same Islands are turbiditic deposits, recycled fossils have during deposition ofBaratang Formation. Still, the validity of Gondwanic affinity and Gondwana provinces were present the hypothesis can be tested only after the recovery of Late around Andaman Basin, three schools of thoughts have Cretaceous palynoassemblage from Andaman. emerged as to the provenance of the reworked taxa. Although The third view advocates that sediments in Andaman three groups agree on the Gondwana land origin of the came from Myanmar (Kumar, 1990; Pandey et al., 1992; Mandai reworked fossils, they differ markedly on the provenance of et al., 1994). The present palynological study substantiates sediments carrying these spores-pollen. Al'-:ording to Pandey the above contention. Most of the Eocene taxa like (1986) long distance transportation of sediments including Dandot iaspora, St riatriletes. Lakiapoll is, Striatopollis, Permo-Triassic palynomorphs in Andaman was from Neocouperipollis, Acanthot ricolpites, Retitrisyncolpites, "somewhere coalfield belt of Bihar". He postulated that long Spinizonocolpites, Proxapertites and Lanagiopollis recorded rivers draining through Bihar carried huge quantities of from Andaman also occur in Myanmar. However, the genera sediments and the mouth of the rivers opened in the Assam Retitrisyncolpites, DaCfylopollis and Lanagiopollis regularis areas. As a result, Laisong (Barail Group) spore-pollen mixed recorded in Andaman are not known from mainland of India. with Gondwana palynomorphs were deposited in Upper The genus Retitrisyncolpites is a dominant element of Baratang through turbidity actions (Pandey, 1986; fig. 11). Chindwin flora of Myanmar like Andaman. Similar composition of palynoassemblages with Gondwana In fact, Myanmar (western and southern part) was a part palynofossils in Assam and Andaman during the Upper part of Gondwanaland and was connected on the northern margin of Palaeogene supports this hypothesis. Moreover, the genus of Australia before fragmentation (Metcalfe, 1988; Acharyya, Meyeripollis, an Oligocene marker taxon in Assam is also 1994; Hutchison, 1989). A nearly continuous Palaeozoic and present in Andaman (Mathur & Mathur, 1980; Mandai et al., Mesozoic sequences including marine strata are present in 1996), which further strengthens the view. But the taxon Myanmar (Krishnan, 1982; Bender, 1983; Kumar, 1990). Meyeripollis occurs in several parts of southeast Asia (Morley, Lithologically the turbiditic sediments of Andaman Islands 1991). Additionally, the above view cannot answer the (Baratang Formation) show gradual coarsening towards north occurrence of Late Triassic dinoflagellate cysts and Eocene (Pandey et al., 1992). According to Ray (1982), Andaman flysch terrestrial palynomorphs like Retitrisyncolpites, sequence comprises material from distant extrabasinal Baculilllonocolpites, Lanagiopollis regularis, Alangiopollis distributive source situated far beyond the limits of this mobile sp., and Dactylopollis in Andaman. Marine Triassic sediment crustal belt and were brough·t within through turbiditic is not known from peninsular India, particularly from Bihar currents. Moreover, the evidences of palaeocurrents (Fig. 4) area. Moreover, the above-mentioned pollen taxa have not suggest that the current flow to Andaman Basin was from been recovered from any Indian section including Assam. NNE or NE direction before the Oligocene. These currents Jafar and Tripathi (200 I) ad vocated that Triassic taxa carried the flysch sediments to fill the fast subsiding including marine forms originated from Wharton Basin/ geosyncline and the provenance is the northern and MANDAL el at.-PALYNOLOGY OF THE BARATANG FORMATION. ANDAMAN-NICOBAR ISLANDS III northeastern frontiers of Myanmar or beyond it. The REFERENCES OCCUITenceof palynomorph type 1 that has gross resemblance with Chinese algal taxon IntubidiniulIl favours flow of Acharyya SK 1994. Accretion of Indo-Australian Gondwanic Blocks sediments from northern province also. However, there is no along Peri-Indian collision margins. II! . Proceedings of the IX'" evidence to establish flow from the continents situated on International Gondwana Symposium. Hyderabad. India. 1029 eastern and western sides of Andaman (Karunakaran et a/., 1049. Oxfrod IBH Publisher. Badve RM & Kunda! P 1986. Marine Cretaceous algae from the 1964, 1968). 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