Neogene evolution of the Himalayan-Tibetan region: constraints from ODP site 758, northern ninetyeast ridge; bearing on climatic change

Klootwijk, Chris; Gee, Jeffrey S.; Peirce, John W.; Smith, Guy M.

doi:10.1016/0031-0182(92)90167-4

Cited by 42 publications

(16 citation statements)

References 68 publications

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“…The principal sources of Neogene clastic input to the Indian Ocean are the Indus and GangesBrahamaputra Rivers. The mean sediment flux shows a relatively constant rate for most of the Cenozoic following the collision of India with southern Asia (Klootwijk, 1992). An increase in sedimentation commences around 11 Myr (Rea, 1992) and the first strong peak of terrigenous sediment flux to the Indian Ocean occurs between 9 and 8 Myr (Fig.…”

Section: Discussion: Uplift and Climate Changementioning

confidence: 96%

Late Miocene and mid-Pliocene enhancement of the East Asian monsoon as viewed from the land and sea

Zheng

Powell

Rea

et al. 2004

Global and Planetary Change

138

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Section: Discussion: Uplift and Climate Changementioning

confidence: 96%

Late Miocene and mid-Pliocene enhancement of the East Asian monsoon as viewed from the land and sea

Zheng

Powell

Rea

et al. 2004

Global and Planetary Change

138

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“…Thus, the pre-Eocene continental-rise deposits of the intraplate margins of west and east India are overlain by the Eocene to Holocene Indus and Bengal fans, respectively, and predecessors in Pakistan and the Indoburman Range (Curray andMoore, 1971, 1974;Kolla and Coumes, 1987;Curray, 1991;Uddin and Lundberg, 1998;Clift et al, 2001). Initial deposition was relatively slow, but by the early Miocene, vigorous uplift of the Himalayas and Tibet resulted in rapid building of the submarine fans (Alam, 1989;Cochran, 1990;Copeland and Harrison, 1990;Klootwijk et al, 1992;Harrison et al, 1993;Qayyum et al, 1996Qayyum et al, , 1997Clift et al, 2001). Since the Miocene, most sediment has been transported by the Indus and Ganges/ Brahmaputra river systems to their respective deltas (e.g., Uddin and Lundberg, 1998); much of the fluvial sediment bypasses the deltas and is transported, in places, over 3000 km as turbidity currents to form the Indus and Bengal/Nicobar fans (Curray andMoore, 1971, 1974;Bowles et al, 1978;Kuehl et al, 1989;Cochran, 1990;Lindsay et al, 1991;Clift et al, 2001).…”

Section: Bengal/nicobar and Indus Submarine-fan Systemsmentioning

confidence: 98%

Remnant-ocean submarine fans: Largest sedimentary systems on Earth

Ingersoll¹,

Dickinson²,

Graham³

2003

Extreme Depositional Environments: Mega End Members in Geologic Time

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The final stages of continental collision result in the development of remnant ocean basins, within which accumulate the most voluminous sedimentary deposits on Earth. The rapid uplift of continental crust during attempted subduction of buoyant crust results in huge sediment flux from the collision zone into nearby remnant ocean basins, where collision has yet to occur. Sediment is transported across and through foreland basins to deltas, which feed submarine fans. As diachronous suture zones migrate along strike, older remnant-ocean sediments are uplifted and recycled into younger remnant ocean basins.The largest two active sedimentary systems on Earth are the Bengal and Indus fan systems, each of which easily surpasses the size of all other modern submarine fans, deltas, or alluvial/fluvial systems. These fans are fed by the Ganges/Brahmaputra and Indus River systems, respectively, which derive their immense sediment loads from the greatest uplifted continental crust on Earth, the Himalaya and Tibetan Plateau. Ancient analogous remnant-ocean fan systems include the Triassic Songpan-Ganzi complex of northern Tibet and the Carboniferous-Permian Ouachita-Marathon flysch deposits of Arkansas, Oklahoma, and Texas. The diachronous collision of the south and north China blocks provided voluminous detritus to the Songpan-Ganzi remnant ocean basin, which was finally closed when the North Tibet block collided. The uplifted southern Appalachians provided most of the sediment fed westward into the Ouachita remnant ocean basin; sequential suturing from northeast to southwest recycled sediment westward into remnant ocean basins, culminating in Permian terminal suturing of Laurasia and Gondwana and development of the Permian basin of west Texas.There is no known or suggested mechanism that can equal the volume of sediment deposited in remnant ocean basins during suturing of continents. Ancient remnant-ocean deposits are preserved as highly deformed accretionary masses that contribute significantly to the building of continental crust. Their recognition as such is a significant step in our understanding of the creation and recycling of continental crust.

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“…Around 59 Ma ago, the northern corner of Greater India collided with Eurasia, causing the Indian Plate to rotate anticlockwise until 55 Ma (Klootwijk et al 1992). Between 55 and 45 Ma, India was indenting the Eurasian margin and rotating the subduction zone in a clockwise direction, bending the NW Sunda subduction and increasing the obliquity of the subduction (Curray 2005).…”

mentioning

confidence: 99%

Chapter 13 Anatomy of the Andaman–Nicobar subduction system from seismic reflection data

Singh¹,

Moeremans²

2017

Memoirs

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The Andaman–Nicobar subduction system is the northwestern segment of the Sunda subduction system, where the Indian Plate subducts beneath the Sunda Plate in a nearly arc-parallel direction. The entire segment ruptured during the 2004 great Andaman–Sumatra earthquake (Mw=9.3). Using recently acquired high-resolution seismic reflection data, we characterize the shallow structure of the whole Andaman–Nicobar subduction system from west to east, starting from the nature of the subducting plate in the Bay of Bengal to back-arc spreading in the Andaman Sea. We find that the Ninety-East Ridge is overlain by thick continental margin sediments beneath the recent Bengal Fan sediments. The boundary between these two sedimentary units defines the plate interface. We observe evidence of re-activation of fracture zones on the subducting plate beneath the forearc, influencing the morphology of the upper plate. The forearc region, which includes the accretionary wedge, the forearc high and the forearc basin, is exceptionally wide (250 km). We observe an unusually large bathymetric depression within the forearc high. The forearc high is bounded in the east by a normal fault, whereas the forearc basin contains an active backthrust. The forearc basin is floored by the continental crust of Malayan Peninsula origin. The active sliver strike-slip fault lies in a deep basin, created during the rifting of the forearc continental crust and the Malayan Peninsula. The sliver fault connects with the Great Sumatra Fault in the south and with the Sagaing Fault in the north, via the Andaman Sea spreading centre and a large transform fault in the Andaman Sea.

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Neogene evolution of the Himalayan-Tibetan region: constraints from ODP site 758, northern ninetyeast ridge; bearing on climatic change

Cited by 42 publications

References 68 publications

Late Miocene and mid-Pliocene enhancement of the East Asian monsoon as viewed from the land and sea

Late Miocene and mid-Pliocene enhancement of the East Asian monsoon as viewed from the land and sea

Remnant-ocean submarine fans: Largest sedimentary systems on Earth

Chapter 13 Anatomy of the Andaman–Nicobar subduction system from seismic reflection data

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