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Sand Composition in the Bengal Basin, Bangladesh

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Sand Composition in the Bengal Basin, Bangladesh Cenozoic history of the Himalayan-Bengal system: Sand composition in the Bengal basin, Bangladesh Ashraf Uddin* Department of Geology and National High Magnetic Field Laboratory, Florida State University, Tallahassee, Florida 32306 Neil Lundberg Department of Geology, Florida State University, Tallahassee, Florida 32306 ABSTRACT contain abundant argillitic and low- to The timing of initial collision of the Indian medium-grade metamorphic lithic fragments plate with Eurasia has been debated (Cochran, Stratigraphic sequences preserved in the and feldspar grains (Tipam: Qt61F19L19; Dupi 1990; Butler, 1995). Suggestions range from the Bengal basin provide detrital information Tila: Qt70F13L17), suggesting continued oro- Cretaceous-Tertiary boundary, on the basis of pa- that documents a significantly older history of genic unroofing. These younger sands are rich leomagnetic work (Klootwijk et al., 1992), to the eastern Himalaya than that available in potassium feldspar (P/F = 0.30, 0.20) relative various times in the Eocene (Rowley, 1996). An from Ocean Drilling Program and Deep Sea to plagioclase (P)-rich Bhuban and Boka Bil early Eocene collision between Asia and sedi- Drilling Project cores recovered from the sandstones (P/F = 0.66 and 0.48), suggesting a mentary rocks of the leading edge of India (a so- Bengal fan. The Bengal basin, formed as a re- granitic source, probably the Miocene called “soft” collision) at about the time of mag- sult of the Himalayan collision, is located at leucogranites of the High Himalayan Crys- netic anomaly 22 at 53 Ma is suggested on the the juncture of the Indian craton to the west, talline terrane. basis of a 50% decrease in spreading rates in the the Shillong massif and the Himalayan belt to These results document for the first time central Indian Ocean (Sclater and Fisher, 1974).A the north, and the Indo-Burman ranges to the contrasts in orogenic history recorded in the middle Eocene date is based on the similarity of east. Modal analyses of Eocene and Oligocene Bengal system vs. western Himalayan foreland mammalian fossils between India and Mongolia sandstones of the Cherra, Kopili, and Barail basins. Sands deposited in the Bengal basin are (Sahni and Kumar, 1974), and on paleomagnetic Formations document compositions that are generally more quartzose and less lithic than data and plate motions (Dewey et al., 1988).A late dominated by subangular monocrystalline those from the western Himalayan foreland Eocene collision has been proposed on the basis of quartz grains with scarce to no feldspar basins, and pre-Miocene strata in the Bengal radiometric dating of plutonic rocks of the Trans- grains, and few lithic fragments (Cherra and system show little to no evidence of orogenic (Tethys) Himalaya, inferred to represent the end Kopili: Qt99F1L0; Barail: Qt90F3L7; Qt—total activity. In part, this probably reflects west to of subduction of oceanic crust at the leading edge quartz, F—feldspar, L—lithic fragments). east progression of the Himalayan collision, of India (Honeggar et al., 1982; Petterson and These compositions are similar to sands de- but it probably also results from sedimentary Windley, 1985). Beck et al. (1995) suggested, on rived from the Indian craton, suggesting that systems propagating southward, ahead of the stratigraphic grounds, that initial collision they underwent intense chemical weathering, advancing mountain belt as it has been consum- occurred between 66 and 55.5 Ma; there is firm likely in a source with low relief and consider- ing the remnant ocean basin trapped between evidence of collision by 49 Ma (early–middle able transport. Himalayan tectonism during the Indian craton and the Burmese block. Eocene time).This is considerably earlier than the this time was probably significantly more dis- middle Miocene age, originally postulated by tant from the Bengal basin than at present. INTRODUCTION Gansser (1964), for initial uplift of the Himalaya. Sandstones of the Miocene Surma Group The collision between India and Eurasia did (Bhuban and Boka Bil Formations) are rich in The collisional history of the Himalayan not take place simultaneously along the entire feldspar grains, argillite, and very low-grade mountain chain, developed along a region once Himalayan belt (Dewey et al., 1989; Burchfiel, metamorphic lithic fragments (Bhuban: occupied by the west-northwest–south-southeast 1993). From 45 Ma to the present, India has ro- ° Qt66F15L19; Boka Bil: Qt57F23L20) relative to Tethys ocean, is recorded in sediments deposited tated 33 counterclockwise, the motion relative to older sandstones, suggesting onset of uplift and in subsiding foreland basins to the south (Burbank Asia having changed from predominantly north- erosional unroofing in the eastern Himalaya, et al., 1996), including the Bengal basin of east to more northerly, accompanied by a 50% re- and initiation of stream systems supplying oro- Bangladesh (Fig. 1). This basin is predominantly duction in velocity. Most geological information genic detritus to the Bengal basin. Sands of the a huge delta complex, covering about 144 000 constraining the timing of collision has been pro- upper Miocene to Pliocene Tipam Group and km2 onshore and 63 000 km2 offshore, and con- duced from the western portion of the system. the Pliocene–Pleistocene Dupi Tila Sandstone tains as much as 16 km of synorogenic Cenozoic The stratigraphic record of the collision has been sequences derived from the eastern Himalayas studied in some detail in the western Himalaya, *e-mail: [email protected] and the Indo-Burman ranges. beginning with the classic study of Krynine GSA Bulletin; April 1998; v. 110; no. 4; p. 497–511; 11 figures; 2 tables. 497 UDDIN AND LUNDBERG (1937); relatively few hard data on collisional from ODP and DSDP cores recovered from the Cenozoic time, and what do the changes ob- timing have been reported from the eastern Him- Bengal fan. Because of its location between the served suggest about orogenic processes? alayan foreland basin. Distal eastern equivalents eastern Himalaya and the Indo-Burman ranges, (2) What source-rock types are suggested by of the Siwalik sequences have been studied in the Bengal basin sequences contain detrital sedi- sandstone composition? (3) Can sandstone Bengal fan (Fig. 1), in seismic surveys (Curray, ments that yield information potentially relat- modal data help constrain the unroofing history 1991), and on two drilling legs (Deep Sea ing to the uplift and unroofing history of both of the eastern Himalaya, in particular the early Drilling Project [DSDP] Leg 22 and Ocean orogens. However, few detailed provenance stages of orogenesis, predating the record ob- Drilling Program [ODP] Leg 116; Ingersoll and studies have been carried out on the sediments tained from the Bengal fan? Suczek, 1979; Cochran, 1990; Amano and Taira, of the Bengal basin. Quantitative analyses of 1992). Drilling has recovered strata as old as sands derived from the developing mountain BORDERING OROGENS about 18 Ma, and detrital geochronology and iso- belt may help to evaluate the initiation and evo- topic studies of these strata indicate that orogen- lution of orogenic uplift and consequent ex- The 2500 by 300 km east-west Himalaya and esis had begun prior to this time (e.g., Copeland humation in this active continental collision. the 1500 by 230 km north-south Indo-Burman et al., 1990; France-Lanord et al., 1993, 1994). This paper reports the results of a petro- ranges formed as India collided with Eurasia and The Bengal basin, the land pathway that graphic investigation of Eocene through Pleis- the Burma platelet. The Himalayan belt is made links the Himalaya to the Bengal fan, is a mod- tocene sand and sandstone of the Bengal basin, up of four longitudinal lithotectonic units, juxta- ern collisional foreland basin that contains both in order to interpret the tectonic history of the posed along generally north-dipping thrust faults pretectonic and syntectonic stratigraphic se- eastern Himalayas and the Indo-Burman (Fig. 1). The lithologic and tectonic characteristics quences. These sequences provide detrital in- ranges. Specifically, this paper addresses the of these belts remain constant over long distances formation on the eastern Himalaya and record a following questions. (1) How has the composi- along strike (e.g., Gansser, 1964; Windley, 1983). significantly older history than that available tion of Bengal basin sandstones varied through From south to north, these units are (1) the Sub- Figure 1. Location map of Bengal basin and adjacent regions, showing lithotectonic belts of Himalayan and Indo-Burman orogens and loca- tions of units discussed in the text. Indian shield and Shillong Plateau expose Precambrian crystalline rocks. Deep Sea Drilling Project Sites 217 and 218 and area drilled by Ocean Drilling Program Leg 116 are shown on Bengal fan. Modified from Sengupta et al. (1990), Critelli and Garzanti (1994), and Uddin and Lundberg (1998). 498 Geological Society of America Bulletin, April 1998 SAND COMPOSITION IN THE BENGAL BASIN, BANGLADESH Himalaya, representing the Miocene to Pleisto- cene molasse deposits of the Siwaliks, separated from the Indo-Gangetic Plain by the Main Frontal thrust; (2) the Lower, or Lesser, Himalaya, which represent southward-directed thrusts and nappes composed of Precambrian and Paleozoic sedi- mentary rocks, crystalline rocks, and granites; (3) the Higher Himalaya, located north of the Main Central thrust, composed of schists, gneisses, and granites, and located across the Indus-Tsangpo suture; and (4) the Tethys Himalaya and Trans- Himalaya, representing fossiliferous Cambrian to Eocene sedimentary rocks (shallow-water depos- its, such as limestone, calcareous sandstone, and dolomite), batholiths, and volcanic rocks. The su- ture between India and Asia is marked by ophi- olitic rocks, and is located south of the Trans- Himalaya and locally adjacent to the Precambrian Central Gneiss of the Higher Himalayas (Jain and Kanwar, 1970). The Indo-Burman ranges are made up mainly of Cretaceous to Eocene pelagic strata overlain by thick Eocene to Oligocene tur- bidites and upper Miocene to Pleistocene mo- lasse (Fig.
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