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Sedimentation and Tectonics of the Sylhet Trough, Bangladesh

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Sedimentation and Tectonics of the Sylhet Trough, Bangladesh Sedimentation and tectonics of the Sylhet trough, Bangladesh SAMUEL Y. JOHNSON U.S. Geological Survey, M.S. 939, Box 25046, Denver Federal Center, Denver, Colorado 80225 ABU MD. NUR ALAM Geological Survey of Bangladesh, Segun Bagicha, Dhaka-1000, Bangladesh ABSTRACT mentary lithic fragments compared to older cene), to (2) a foreland basin linked to the Indo- rocks, reflecting uplift and erosion of the sed- Burman ranges (Oligocene and Miocene), to The Sylhet trough, a sub-basin of the Ben- imentary cover of the Shillong Plateau. If the (3) a foreland basin linked to south-directed gal Basin in northeastern Bangladesh, con- Dauki fault has a dip similar to that of other overthrusting of the Shillong Plateau (Pliocene tains a thick fill (12 to 16 km) of late Mesozoic Himalayan overthrusts, then a few tens of to Holocene). and Cenozoic strata that record its tectonic kilometers of horizontal tectonic transport evolution. Stratigraphic, sedimentologic, and would be required to carry the Shillong GEOLOGIC SETTING petrographic data collected from outcrops, Plateau to its present elevation. Uplift of the cores, well logs, and seismic lines are here Shillong Plateau probably generated a major The Cretaceous to Holocene Bengal Basin, used to reconstruct the history of this trough. (-300 km) westward shift in the course of the underlying the deltaic parts of Bangladesh and The Sylhet trough occupied a slope/basinal Brahmaputra River. adjacent India as well as the Bay of Bengal setting on a passive continental margin from (Fig. 1), forms a "remnant ocean basin" late Mesozoic through Eocene time. Sub- INTRODUCTION (Mitchell and Reading, 1986) at the juncture of sidence may have increased slightly in Oligo- the Indian plate and the Burma platelet (Curray cene time when the trough was located in the The Sylhet trough of northeastern Bangladesh and others, 1983). Basin development began in distal part of a foreland basin paired to the is a tectonically complex province of the Bengal the Early Cretaceous epoch (ca. 127 Ma) when Indo-Burman ranges. Oligocene fluvial-deltaic Basin (Figs. 1-3). This trough is bounded on the the Indian plate rifted away from Antarctica. strata (Barail Formation) were derived from north by the Shillong Plateau, on the east and After a plate reorganization ca. 90 Ma, the incipient uplifts in the eastern Himalayas. southeast by the Chittagong-Tripura fold belt of Indian plate migrated rapidly northward and Subsidence increased markedly in the Mio- the Indo-Burman ranges, and on the west by the collided with Asia between ca. 55 and 40 Ma cene epoch in response to western encroach- Indian Shield platform; the trough is open to the (Curray and others, 1983; Molnar, 1984). ment of the Indo-Burman ranges. Miocene to south and southwest to the main part of the The onshore part of the Bengal Basin has been earliest Pliocene sediments of the Surma Bengal Basin. Published estimates of the thick- divided into platform or shelf, slope or "hinge," Group were deposited in a large, mud-rich ness of late Mesozoic and Cenozoic strata in the and basinal facies (Evans, 1964; Salt and others, delta system that may have drained a signifi- Sylhet trough range from about 13 to 17 km 1986). Crystalline basement of the Indian plate cant proportion of the eastern Himalayas. (Evans, 1964; Hiller and Elahi, 1984), and underlies the shelf and bounds the Bengal Basin Subsidence rates in the Sylhet trough in- much of this strata is Neogene in age. The Sylhet to the west and north; the deeper basin to the creased dramatically (3-8 times) from Mio- trough has minimal topographic relief and is ac- east and southeast may be floored by oceanic or cene to Pliocene-Pleistocene time when the tively subsiding. Although many workers have transitional crust (Desikachar, 1974; Curray and fluvial Tipam Sandstone and Dupi Tila For- reported on the geology and hydrocarbon poten- others, 1983). Paleocene and Eocene strata in- mation were deposited. This dramatic subsid- tial of the Sylhet trough (for example, Lietz and clude carbonate platform and clastic shelf depos- ence change is attributed to south-directed Kabir, 1982; Hiller and Elahi, 1984, Khan and its of the Jaintia Group and their thick basinal overthrusting of the ShOlong Plateau on others, 1988), detailed sedimentologic and pet- correlatives, the Disang Group (Fig. 4). The the Dauki fault for the following reasons. rologic studies of basinal sediments are lacking basin has been characterized by deltaic sedimen- (1) Pliocene and Pleistocene strata thin for two reasons. (1) Outcrops are of poor quality tation since the Oligocene epoch. Today, the markedly away from the Shillong Plateau, and occur only on the uplifted basin margins. onshore part of the Bengal Basin is the site of the consistent with a crustal load emplaced on (2) The Sylhet trough is a frontier petroleum world's largest delta (about 60,000 km2) formed the northern basin margin. (2) The Shillong province that has not been extensively drilled, by rivers (Ganges, Brahmaputra/Jamuna, Pad- Plateau is draped by Mesozoic to Miocene and therefore only limited core is available for ma, Meghna) that drain a large proportion of the rocks, but Pliocene and younger strata are study. Our outcrop and core studies of Neogene Himalayas. This subaerial delta feeds the world's not represented, suggesting that the massif and Oligocene strata, together with observations largest submarine fan (Bengal Fan), which ex- was an uplifted block at this time. (3) South- based on examination of well logs and seismic tends more than 3,000 km south into the Bay of directed overthrusting of the Shillong Plateau data, allow reconstruction of the sedimentary Bengal (Curray and Moore, 1974). and tectonic evolution of the Sylhet trough. We is consistent with gravity data and with re- The Bengal Basin gradually is being en- propose that the Sylhet trough evolved from cent seismotectonic observations. Sandstone croached on by the Indo-Burman ranges, an (1) a passive continental margin (pre-Oligo- in the Tipam has a marked increase in sedi- ~230-km-wide, active orogenic belt associated Geological Society of America Bulletin, v. 103, p. 1513-1527, 12 figs., 1 table, November 1991. 1513 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/103/11/1513/3381148/i0016-7606-103-11-1513.pdf by guest on 01 October 2021 Figure 1. Schematic map showing the location of the Sylhet trough and surrounding tectonic elements. Abbreviations: C, Chittagong; Ca, Calcutta; CTFB, Chittagong-Tripura fold belt; D, Dhaka; HDT, Haflong-Disang thrust system; M, Mandalaya; MBT, Main Boundary thrust fault. Shillong Plateau is shaded. A-A', B-B', and C-C' are lines of section shown in Figure 6. Circled numbers show the approximate locations of the composite stratigraphie columns shown in Figure 4. Based on Ray (1982), Acharya and others (1986), and Salt and others (1986). Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/103/11/1513/3381148/i0016-7606-103-11-1513.pdf by guest on 01 October 2021 Age Upper Assam, Southwest Shillong Surma Basin, Naga Hills east of India Plateau, India Bangladesh Surma Basin, India 0 Ma Dihing Formation Dalu and Dupi Tila Dupi Tila Fm 1 (300-1500 m) p Rangapani Fms, Formation and Dihing Group Namsang Fm. , (95-130 m) _ (up to ?—-—r (1500-2500 m) 6375 m) Tipam Tipam Sandstone Sandstone (55-900 m) 5- Bilkona Formation Surma Group (450-880 m) Surma Group (3100 m) (2800-3250 m) Tipam Sandstone Surma Group - Figure 3. Remote sens- Angario li 10- (100-1450 m) ing image of the Sylhet Formation Boka Bil and Boka Bil and Bhuban Bhuban trough area, Bangladesh, (400 - 1170 m) and Formations Formations showing the Chittagong- Boldamgiri Tripura fold belt (TCFB), Surma Group? Formation the Sylhet trough (ST), 20- (260 m) (260-860 m) Barail Formation and the Shillong Plateau Barail Formation Barail Group Barail Group (SP). International border (1150 m) (800-1000 m) (2665 m) (1000 m) _ between Bangladesh and 40- Kopili Formation Kopili Formation Kopili and ' India is highlighted in (400-600 m) r (520 m) h Sylhet upper Disang white, aiding comparison Sylhet Limestone Sylhet Limestone (600- Group with Figure 2 which (400 m) (200 m) 800 m)' (1250-3000 m) shows approximately the Tura Formation .TuraFm. (400 m) 60- undifferentiated same area. Note the (250? m- ) Langpar and Cherra Formations Cretaceous and plunge of north-trending (70 m) early Tertiary folds into the subsurface Dergaon Mahadeo rocks (5000 m?) of the Sylhet trough, and Formation Formation deposited in shelt lower Disang the abundance of lakes 80- (546 m) (165 m) (northeast) to Group (darkest hues) in the basinal (2310+ m) trough. Scale bar (lower (southwest) left) is 20 km long. From granitic and Gumaghat setting 100- SPARRSO (1984). metamorphic Formation complex (150 m) Sylhet Traps Sylhet Traps 144- H (500 m?) and rift volcanics ? granitic and meta- morphic complex Figure 4. Chart showing the stratigraphy of the Sylhet trough and surrounding areas. The approximate locations of the numbered stratigraphic columns are shown in Figure 1. The latest Cretaceous Langpar Formation, Cherra Formation, Tura Formation, Sylhet Limestone, and Kopili Formation comprise the Jaintia Group. Ages of nonmarine units are based on palynol- ogy. Data from Baksi (1965), Chakraborty (1972), Holtrop and Keizer (1970), Gupta (1976), Murthy and others (1976), Baneiji (1981,1984), and Murty (1983). Note that the time scale is not linear. Wavy lines show unconformities. Time scale from Palmer (1983). Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/103/11/1513/3381148/i0016-7606-103-11-1513.pdf by guest on 01 October 2021 SEDIMENTATION AND TECTONICS OF SYLHET TROUGH, BANGLADESH 1515 with eastward subduction of the Indian plate 92° below Myanmar (Burma) (Brunnschweiler, 1966; LeDain and others, 1984; Sengupta and MmtMMmmMmmM: others, 1990).
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