Oolitic beach barriers of the last Glacial sea-level lowstand at the outer Bengal shelf

Wiedicke, Michael; Kudrass, H. R.; Hüebscher, C.

doi:10.1016/s0025-3227(98)00162-5

Cited by 53 publications

(32 citation statements)

References 29 publications

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“…Has compaction of the sediment column subsequent to deposition been important? Significant data sources included are from the Sunda Shelf (33,34), the Indian Ocean (35,36), the Bonaparte Gulf (37,38), New Zealand (39), Singapore (40,41), Malaysia (42), and from the South China Sea to the Bohai Sea. Many of the Asian observations are from large delta systems, and comparisons of such data with observations from adjacent sites often indicate lower levels of the former, corresponding to differential subsidence rates of the order of 1 mm·y −1 for the past ∼8 ka.…”

Section: Observational Evidencementioning

confidence: 99%

Sea level and global ice volumes from the Last Glacial Maximum to the Holocene

Lambeck

Rouby

Purcell

et al. 2014

Proc. Natl. Acad. Sci. U.S.A.

1,931

1,613

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The major cause of sea-level change during ice ages is the exchange of water between ice and ocean and the planet's dynamic response to the changing surface load. Inversion of ∼1,000 observations for the past 35,000 y from localities far from former ice margins has provided new constraints on the fluctuation of ice volume in this interval. Key results are: (i) a rapid final fall in global sea level of ∼40 m in <2,000 y at the onset of the glacial maximum ∼30,000 y before present (30 ka BP); (ii) a slow fall to −134 m from 29 to 21 ka BP with a maximum grounded ice volume of ∼52 × 10 6 km 3 greater than today; (iii) after an initial short duration rapid rise and a short interval of near-constant sea level, the main phase of deglaciation occurred from ∼16.5 ka BP to ∼8.2 ka BP at an average rate of rise of 12 m·ka −1 punctuated by periods of greater, particularly at 14.5-14.0 ka BP at ≥40 mm·y −1 (MWP-1A), and lesser, from 12.5 to 11.5 ka BP (Younger Dryas), rates; (iv) no evidence for a global MWP-1B event at ∼11.3 ka BP; and (v) a progressive decrease in the rate of rise from 8.2 ka to ∼2.5 ka BP, after which ocean volumes remained nearly constant until the renewed sea-level rise at 100-150 y ago, with no evidence of oscillations exceeding ∼15-20 cm in time intervals ≥200 y from 6 to 0.15 ka BP.he understanding of the change in ocean volume during glacial cycles is pertinent to several areas of earth science: for estimating the volume of ice and its geographic distribution through time (1); for calibrating isotopic proxy indicators of ocean volume change (2, 3); for estimating vertical rates of land movement from geological data (4); for examining the response of reef development to changing sea level (5); and for reconstructing paleo topographies to test models of human and other migrations (6). Estimates of variations in global sea level come from direct observational evidence of past sea levels relative to present and less directly from temporal variations in the oxygen isotopic signal of ocean sediments (7). Both yield modeldependent estimates. The first requires assumptions about processes that govern how past sea levels are recorded in the coastal geology or geomorphology as well as about the tectonic, isostatic, and oceanographic contributions to sea level change. The second requires assumptions about the source of the isotopic or chemical signatures of marine sediments and about the relative importance of growth or decay of the ice sheets, of changes in ocean and atmospheric temperatures, or from local or regional factors that control the extent and time scales of mixing within ocean basins.Both approaches are important and complementary. The direct observational evidence is restricted to time intervals or climatic and tectonic settings that favor preservation of the records through otherwise successive overprinting events. As a result, the records become increasingly fragmentary backward in time. The isotopic evidence, in contrast, being recorded in deep-water carbonate marine sediments, extends further...

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Section: Observational Evidencementioning

confidence: 99%

Sea level and global ice volumes from the Last Glacial Maximum to the Holocene

Lambeck

Rouby

Purcell

et al. 2014

Proc. Natl. Acad. Sci. U.S.A.

1,931

1,613

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“…from 26.5 ka to 19 to 20 ka (according to Clark et al, 2009). We do not have any information on the lithology of these small cliffs, which may correspond to a beach rock or a paleo-reef, as described in other similar sites (Wiedicke at al., 1999;Berné et al, 2007). This type of geological formation is currently observable along the west and south coasts of La Réunion Island.…”

Section: Shelf Break and Other Slope Changesmentioning

confidence: 99%

Direct sediment transfer from land to deep-sea: Insights into shallow multibeam bathymetry at La Réunion Island

et al. 2013

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Submarine canyon heads are key areas for understanding the triggering factors of gravity currents responsible for the transfer of detrital sediment to the deep basins. This contribution offers a detailed picture of canyon heads off La Réunion Island, with high-resolution multibeam bathymetry in the water depth range of 4-220 m. The present feeding of the Cilaos turbidite system, one of the largest modern volcaniclastic systems in the world, is deduced from morphological and sedimentological interpretations of newly acquired data. The study highlights small-scale sedimentary features indicating hydrodynamic and sedimentary processes.A direct connexion between the Saint-Etienne river mouth and submarine canyons is evidenced by the complete incision of the shelf and the presence of canyon heads connected to the modern deltaic bar. This direct connection, supplied by river torrential floods (cyclonic floods every two or three years), suggests the continuity of high-density fluvial flows to submarine gravity flows, forming hyperpycnal flows in the canyon.The initiation of secondary submarine gravity flows by storm waves (large austral waves and cyclonic waves) is also proposed for submarine canyons with large canyon heads developed in the surf zone from a sandy coastal bar. Bedforms in active canyon axis are considered as an indicator of the frequent activity of high-density turbidity currents.Moreover, a morphological record of last glacial and deglacial sea level variations is preserved, and particularly the Last Glacial Maximum sea level with the presence of small vertical cliffs, observed in this bathymetric data, which likely corresponds to a paleo-shoreline or paleo-reefs.2

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“…The Gangetic Plains witnessed a very cool and dry climate with reduced river discharges and decreased monsoonal activity during the Last Glacial Maximum (LGM) (18-22 Ka) and after the LGM the climate turned cool and slightly wetter (Cullen, 1981;Wiedicke et al, 1999;Goodbread, 2003). Climate ameliorated significantly by 10 Ka and turned warm and wet (Overpeck et al, 1996;Kutzbach, 1987, 1992).…”

Section: Role Of Climate In Soil Developmentmentioning

confidence: 99%