Origin of anomalous subsidence along the Northern South China Sea margin and its relationship to dynamic topography

Xie, Xinong; Müller, R. Dietmar; Li, Sitian; Gong, Zhigang; Steinberger, Bernhard

doi:10.1016/j.marpetgeo.2006.03.004

Cited by 254 publications

(170 citation statements)

References 40 publications

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“…Both Huon Peninsula and Barbados have been subject to uplift, and Tahiti to subsidence (SI Appendix, Text S1). The eastern Asian margin in many locations is characterized by rifting of Cenozoic age and postrift thermal subsidence (45), but the expected rates are small on time scales of the past 20 ka compared with the GIA signals and observational uncertainties, and no corrections have been applied. where « obs are corrections to the observations of relative sea level and δζ esl ðtÞ is a corrective term to Δζ 0 esl ðtÞ, parameterized in the first instance as mean values in time bins of 1,000 y from present to 22 ka BP, with larger bins for the data-sparse intervals 22-26 ka BP, 26-31 ka BP, and 31-36 ka BP (Fig.…”

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.

1,919

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.

1,919

1,613

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“…The NeoceneeQuaternary post-rift subsidence stage can further be divided into thermal subsidence and accelerated subsidence sub-stages. The sediment layers are mainly composed of neritic shelf sandstones and neriticesemipelagicepelagic calcareous mudstones, which act as excellent reservoirs and seals for hydrocarbon fluid (Huang et al, 2003;Xie et al, 2006;Zhu et al, 2009). The study area is characterized by high sedimentation rates (up to 1.2 mm/yr) and high geothermal gradients (39e41 C/km) (Zhu et al, 2009).…”

Section: Geological Settingmentioning

confidence: 99%

Pockmark activity inferred from pore water geochemistry in shallow sediments of the pockmark field in southwestern Xisha Uplift, northwestern South China Sea

Luo

Chen

Wang

et al. 2013

Marine and Petroleum Geology

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“…However, the specific time and location of the accelerated subsidence are still in debate. Lei et al (2011) and Song et al (2011) argued that the accelerated subsidence occurred since Pliocene (5.3 Ma); In contrast, Li et al (1998), Xie et al (2006), Tian (2010), Li et al (2012) proposed that it happened during and after the late Miocene (10.5 Ma); Yuan et al (2008) believed that it took place since late Miocene (10.5 Ma) in the west but since the Pliocene (5.3 Ma) in the east. New data and methods are employed to explore when, where and how the accelerated subsidence happened.…”

Section: Introductionmentioning

confidence: 99%

The dynamic mechanism of post-rift accelerated subsidence in Qiongdongnan Basin, northern South China Sea

Zhao

Sun

Wang³

et al. 2013

Mar Geophys Res

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A 1-D unloaded tectonic subsidence (air-loaded tectonic subsidence) model is proposed and applied to the Qiongdongnan Basin. Results show that three episodes of subsidence exist in Cenozoic, that is, syn-rift rapid subsidence (Eocene-Oligocene) with subsidence rate at 20-100 m/m.y., post-rift slow thermal subsidence (early-middle Miocene) around 40 m/m.y., and post-rift accelerated subsidence (since late Miocene) 40-140 m/m.y., which is substantially deviated from the exponentially decayed thermal subsidence model. For exploring the mechanism of post-rift accelerated subsidence, the faulting analyses are conducted and results show that there is a dramatically decrease in the numbers of active faults and fault growth rate since 21 Ma, which indicates that no active brittle crust extension occurred during post-rift period. Furthermore, previous studies have demonstrated that the stretching of the upper crust is far less than that affecting the whole crust. Therefore, we infer that the lower crust thinned during the post-rift period and a new model of basin development and evolution is put forward to explain the post-rift accelerated subsidence and depth-dependent crust thinning in the Qiongdongnan Basin, which is supported by gravity data.

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Origin of anomalous subsidence along the Northern South China Sea margin and its relationship to dynamic topography

Cited by 254 publications

References 40 publications

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

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

Pockmark activity inferred from pore water geochemistry in shallow sediments of the pockmark field in southwestern Xisha Uplift, northwestern South China Sea

The dynamic mechanism of post-rift accelerated subsidence in Qiongdongnan Basin, northern South China Sea

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