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Alam, M, Alam MM, Curray JR, Chowdhury ALR, Gani MR.  2003.  An overview of the sedimentary geology of the Bengal Basin in relation to the regional tectonic framework and basin-fill history. Sedimentary Geology. 155:179-208.   10.1016/s0037-0738(02)00180-x   AbstractWebsite

The Bengal Basin in the northeastern part of Indian subcontinent, between the Indian Shield and Indo-Burman Ranges, comprises three geo-tectonic provinces: (1) The Stable Shelf; (2) The Central Deep Basin (extending from the Sylhet Trough in the northeast towards the Hatia Trough in the south); and (3) The Chittagong-Tripura Fold Belt. Due to location of the basin at the juncture of three interacting plates, viz., the Indian, Burma and Tibetan (Eurasian) Plates, the basin-fill history of these geotectonic provinces varied considerably. Precambrian metasediments and Permian-Carboniferous rocks have been encountered only in drill holes in the stable shelf province. After Precambrian peneplanation of the Indian Shield, sedimentation in the Bengal Basin started in isolated graben-controlled basins on the basement. With the breakup of Gondwanaland in the Jurassic and Cretaceous, and northward movement of the Indian Plate, the basin started downwarping in the Early Cretaceous and sedimentation started on the stable shelf and deep basin; and since then sedimentation has been continuous for most of the basin. Subsidence of the basin can be attributed to differential adjustments of the crust, collision with the various elements of south Asia, and uplift of the eastern Himalayas and the Indo-Burman Ranges. Movements along several well-established faults were initiated following the breakup of Gondwanaland and during downwarping in the Cretaceous. By Eocene, because of a major marine transgression, the stable shelf came under a carbonate regime, whereas the deep basinal area was dominated by deep-water sedimentation. A major switch in sedimentation pattern over the Bengal Basin occurred during the Middle Eocene to Early Miocene as a result of collision of India with the Burma and Tibetan Blocks. The influx of elastic sediment into the basin from the Himalayas to the north and the Indo-Burman Ranges to the east rapidly increased at this time; and this was followed by an increase in the rate of subsidence of the basin. At this stage, deep marine sedimentation dominated in the deep basinal part, while deep to shallow marine conditions prevailed in the eastern part of the basin. By Middle Miocene, with continuing collision events between the plates and uplift in the Himalayas and Indo-Burman Ranges, a huge influx of elastic sediments came into the basin from the northeast and east. Throughout the Miocene, the depositional settings continued to vary from deep marine in the basin to shallow and coastal marine in the marginal parts of the basin. From Pliocene onwards, large amounts of sediment were filling the Bengal Basin from the west and northwest; and major delta building processes continued to develop the present-day delta morphology. Since the Cretaceous, architecture of them Bengal Basin has been changing due to the collision pattern and movements of the major plates in the region. However, three notable changes in basin configuration can be recognized that occurred during Early Eocene, Middle Miocene and Plio-Pleistocene times, when both the paleogeographic settings and source areas changed. The present basin configuration with the Ganges - Brahmaputra delta system on the north and the Bengal Deep Sea Fan on the south was established during the later part of Pliocene and Pleistocene; and delta progradation since then has been strongly affected by orogeny in the eastern Himalayas. Pleistocene glacial activities in the north accompanied sea level changes in the Bay of Bengal. (C) 2002 Elsevier Science B.V All rights reserved.

Audleycharles, MG, Curray JR, Evans G.  1977.  Location of Major Deltas. Geology. 5:341-344.   10.1130/0091-7613(1977)5<341:lomd>;2   Website
Audleycharles, MG, Curray JR, Evans G.  1979.  Significance and Origin of Big Rivers - Discussion. Journal of Geology. 87:122-123.Website
Curray, JR, Emmel FJ, Moore DG, Raitt RW.  1982.  Structure, Tectonics, and Geological History of the Northeastern Indian-Ocean. Ocean Basins and Margins. 6:399-&.Website
Curray, JR, Moore DG, Belderso.Rh, Stride AH.  1966.  Continental Margin of Western Europe - Slope Progradation and Erosion. Science. 154:265-&.   10.1126/science.154.3746.265   Website
Curray, JR.  1994.  Sediment Volume and Mass beneath the Bay of Bengal. Earth and Planetary Science Letters. 125:371-383.   10.1016/0012-821x(94)90227-5   AbstractWebsite

Rates of sediment accumulation and the amount of sedimentary fill in depocenters lying downstream of erosion in the Himalayas and Tibet can provide some insight into tectonics and geological history. The objective of this paper is to put on record the best estimates which are possible with existing data of the volume and mass of sediments, sedimentary rock and metasedimentary rock beneath the sea floor of the Bay of Bengal. The sedimentary section in the Bay of Bengal is divided into two parts: (1) Eocene through Holocene, sediments and sedimentary rocks which post-date the initial India-Asia collision: volume - 12.5 X 10(6) km3; mass = 2.88 X 10(16) t; this is most of the Bengal Fan, including its eastern lobe, the Nicobar Fan, plus some of the outer Bengal Delta; (2) Early Cretaceous through Paleocene, pre-collision sedimentary and metasedimentary rocks: volume = 4.36 X 10(6) km 3; mass = 1.13 to 1.18 X 10(16) t; these are interpreted as continental rise and pelagic deposits.

Curray, JR, Emmel FJ.  1981.  Demise of the Diamantina Dent. Marine Geology. 40:M69-M72.   10.1016/0025-3227(81)90140-7   Website
Curray, JR, Moore DG, Kelts K, Einsele G.  1982.  Tectonics and Geological History of the Passive Continental-Margin at the Tip of Baja California. Initial Reports of the Deep Sea Drilling Project. 64:1089-&.Website
Curray, JR.  1956.  The Analysis of 2-Dimensional Orientation Data. Journal of Geology. 64:117-&.Website
Curray, JR.  1991.  Possible Greenschist Metamorphism at the Base of a 22-Km Sedimentary Section, Bay of Bengal. Geology. 19:1097-1100.   10.1130/0091-7613(1991)019<1097:pgmatb>;2   AbstractWebsite

Reinterpretation of seismic refraction and reflection data in the Bay of Bengal suggests a maximum thickness of sedimentary deposits of more than 22 km beneath the Bangladesh continental shelf. Revised correlation of an early Eocene unconformity-which is interpreted as representing the time of the India-Asia collision-subdivides these deposits into (1) a Cretaceous and Paleocene continental-rise section up to 6 km thick off the Indian margin and (2) 16 km of overlying Bengal Fan sediments and sedimentary rocks derived mainly from erosion of the region uplifted following the collision. Pressure and temperature conditions within the deeply buried continental rise are in the field of greenschist facies metamorphism. The resulting metasedimentary rocks would have velocities and densities compatible with the refraction data and isostatic calculations.

Curray, JR.  1977.  Modes of Emplacement of Prospective Hydrocarbon Reservoir Rocks of Outer Continental-Margin Environments. Aapg Bulletin-American Association of Petroleum Geologists. 61:778-778.Website
Curray, JR, Moore DG.  1982.  Introduction to the Guaymas Basin and Hydrothermal Symposium. Initial Reports of the Deep Sea Drilling Project. 64:1119-1121.Website
Curray, JR, Nason RD.  1967.  San Andreas Fault North of Point Arena California. Geological Society of America Bulletin. 78:413-&.   10.1130/0016-7606(1967)78[413:safnop];2   Website
Curray, JR.  1996.  Origin of beach ridges: Comment. Marine Geology. 136:121-125.   10.1016/s0025-3227(96)00040-0   AbstractWebsite

Tanner (1995) has proposed that most common strand plain sandy beach ridges (his swash-built type) have been formed by a sea level rise-and-fall couplet of 5-30 cm, with a periodicity which is most commonly 30-60 years, but which ranges from as little as 3 to as much as 60 years. While such a mechanism could perhaps apply to beach ridges in lakes, if sea level has fluctuated with such regularity for the past several thousand years, all open ocean beach ridge periodicities should be the same, and furthermore this sea level signal would surely have been detected by physical oceanographers. Curray et al. (1969) described a strand plain of several hundred beach ridges on the western Mexican coast with cyclic formation of ridges varying from 12.2 to 16.5 years. The mechanism of formation invoked was periodic building of offshore bars to above sea level after sufficient sand had been transported into the area and during an optimal combination of oceanographic conditions.

Curray, JR.  1980.  Ipod Program on Passive Continental Margins. Philosophical Transactions of the Royal Society of London Series a-Mathematical Physical and Engineering Sciences. 294:17-33.   10.1098/rsta.1980.0008   Website
Curray, JR.  1989.  The Sunda Arc - a Model for Oblique Plate Convergence. Netherlands Journal of Sea Research. 24:131-140.   10.1016/0077-7579(89)90144-0   Website
Curray, JR, Shepard FP, Veeh HH.  1970.  Late Quaternary Sea-Level Studies in Micronesia - Carmarsel Expedition. Geological Society of America Bulletin. 81:1865-&.   10.1130/0016-7606(1970)81[1865:lqssim];2   Website
Curray, JR, Moore DG, Smith SM, Chase TE.  1982.  Underway Geophysical-Data from Deep-Sea Drilling Project Leg-64 - Navigation, Bathymetry, Magnetics, and Seismic Profiles. Initial Reports of the Deep Sea Drilling Project. 64:505-507.Website
Curray, JR.  2005.  Tectonics and history of the Andaman Sea region. Journal of Asian Earth Sciences. 25:187-228.   10.1016/j.jseaes.2004.09.001   AbstractWebsite

The Andaman Sea is an active backarc basin lying above and behind the Sunda subduction zone where convergence between the overriding Southeast Asian plate and the subducting Australian plate is highly oblique. The effect of the oblique convergence has been formation of a sliver plate between the subduction zone and a complex right-lateral fault system. The late Paleocene collision of Greater India and Asia with approximately normal convergence started clockwise rotation and bending of the northern and western Sunda Arc. The initial sliver fault, which probably started in the Eocene, extended through the outer arc ridge offshore from Sumatra, through the present region of the Andaman Sea into the Sagaing Fault. With more oblique convergence due to the rotation, the rate of strike-slip motion increased and a series of extensional basins opened obliquely by the combination of backarc extension and the strike-slip motion. These basins in sequence are the Mergui Basin starting at similar to 32 Ma, the conjoined Alcock and Sewell Rises starting at similar to 23 Ma, East Basin separating the rises from the foot of the continental slope starting at similar to 15 Ma; and finally at similar to 4 Ma, the present plate edge was formed, Alcock and Sewell Rises were separated by formation of the Central Andaman Basin, and the faulting moved onshore from the Mentawai Fault to the Sumatra Fault System bisecting Sumatra. (c) 2005 Elsevier Ltd. All rights reserved.

Curray, JR.  1961.  Late Quaternary Sea Level - a Discussion. Geological Society of America Bulletin. 72:1707-1712.   10.1130/0016-7606(1961)72[1707:lqslad];2   Website
Curray, JR, Munasinghe T.  1991.  Origin of the Rajmahal Traps and the 85-Degrees-E Ridge - Preliminary Reconstructions of the Trace of the Crozet Hotspot. Geology. 19:1237-1240.   10.1130/0091-7613(1991)019<1237:ootrta>;2   AbstractWebsite

The 85-degrees-E Ridge is a buried aseismic ridge approximately parallel to and west of the Ninetyeast Ridge in the northeastern Indian Ocean. It was previously shown to be of probable volcanic origin emplaced on very young oceanic crust, but no satisfactory model of emplacement of the rocks was offered. We propose a model of origin of the Rajmahal Traps of northeastern India, the 85-degrees-E Ridge, and Afanasy Nikitin Seamount as the trace of the hotspot that now lies beneath the Crozet Islands in the southern Indian Ocean. This reconstruction places the Kerguelen hotspot, which formed the Ninetyeast Ridge, at the triple junction between Greater India, Australia, and Antartica before the breakup of eastern Gondwana.

Curray, JR, Shor GG, Raitt RW, Henry M.  1977.  Seismic Refraction and Reflection Studies of Crustual Structure of Eastern Sunda and Western Banda Arcs. Journal of Geophysical Research. 82:2479-2489.   10.1029/JB082i017p02479   Website