A Miocene collisional belt in north Borneo: uplift mechanism and isostatic adjustment quantified by thermochronology

Hutchison, Charles S.; Bergman, Steven C.; Swauger, David A.; Graves, John E.

doi:10.1144/jgs.157.4.783

Cited by 168 publications

(144 citation statements)

References 25 publications

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“…Furthermore, rifting was terminated during active propagation as result of the collision of the southern Dangerous Grounds margin with Borneo (Hutchison et al 2000;Clift et al 2008;Hinz et al 1989). This basin was formed as a result of extension starting in the Late Cretaceous and accelerating during the Eocene, culminating in breakup and the onset of seafloor spreading likely around 30 Ma, at least offshore of southern China (Su et al 1989;Briais et al 1993;Ru and Pigott 1986;Franke et al 2014;Barckhausen et al 2014).…”

Section: South China Seamentioning

confidence: 99%

Coupled onshore erosion and offshore sediment loading as causes of lower crust flow on the margins of South China Sea

Clift

2015

Geosci. Lett.

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Hot, thick continental crust is susceptible to ductile flow within the middle and lower crust where quartz controls mechanical behavior. Reconstruction of subsidence in several sedimentary basins around the South China Sea, most notably the Baiyun Sag, suggests that accelerated phases of basement subsidence are associated with phases of fast erosion onshore and deposition of thick sediments offshore. Working together these two processes induce pressure gradients that drive flow of the ductile crust from offshore towards the continental interior after the end of active extension, partly reversing the flow that occurs during continental breakup. This has the effect of thinning the continental crust under super-deep basins along these continental margins after active extension has finished. This is a newly recognized form of climate-tectonic coupling, similar to that recognized in orogenic belts, especially the Himalaya. Climatically modulated surface processes, especially involving the monsoon in Southeast Asia, affects the crustal structure offshore passive margins, resulting in these "load-flow basins". This further suggests that reorganization of continental drainage systems may also have a role in governing margin structure. If some crustal thinning occurs after the end of active extension this has implications for the thermal history of hydrocarbon-bearing basins throughout the area where application of classical models results in over predictions of heatflow based on observed accommodation space.

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Section: South China Seamentioning

confidence: 99%

Coupled onshore erosion and offshore sediment loading as causes of lower crust flow on the margins of South China Sea

Clift

2015

Geosci. Lett.

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“…Following seafloor spreading in the Middle Oligocene, Reed Bank moved southwards, together with the Dangerous Grounds (Taylor and Hayes 1980;Briais et al 1993;Sun et al 2009), and finally collided with Palawan and Borneo continents during the Middle Miocene (Hutchison et al 2000; b Fig. 1 Franke et al (2013).…”

Section: Regional Geological Settingmentioning

confidence: 99%

Oligocene–Miocene carbonates in the Reed Bank area, South China Sea, and their tectono-sedimentary evolution

Ding

Dong

et al. 2014

Mar Geophys Res

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We have analyzed two recently acquired multichannel seismic profiles across the Reed Bank area, South China Sea. A detailed seismic interpretation coupled with drilling data has proved the occurrence of a wide carbonate platform, developed between the Late Oligocene and the Early Miocene (32-20 Ma). The top of these carbonates is an important regional unconformity, corresponding to a strong and continuous seismic reflector. An age of about 20 Ma is inferred for this reflector, acting as a regional unconformity marking the cessation of seafloor spreading with an erosional/non-depositional hiatus, spanning 3 or 4 m.y. The time interval during which the carbonate platforms formed is concurrent with the opening of the South China Sea. The reconstruction of the tectonic subsidence in this area has shown a decrease in rate of subsidence during the drifting stage (32-17 Ma), indicating that the whole Reed Bank area was in a tectonically stable and shallow water environment for more than 10 m.y., favoring the development of shallow water carbonates. With a sharply increased subsidence rate after the end of spreading (17 Ma) and a continuously increased sea level, the carbonate platforms were drowned and died, except some structural highs with reef buildups, where the carbonate sedimentation continued to Middle Miocene. We suggest that delayed tectonic subsidence in Reed Bank area might have been related to a secondary mantle convection under the rift lasting more than about 10 m.y.

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“…The NW-to N-verging structures in the Rajang and Crocker accretionary prism complex, magmatic and uplift history of Borneo suggest that there should be a subduction zone of the proto-South China Sea slab [35][36][37] . Roughly west of the Baram Line (the west divergent boundary of the Nansha block), only early Cretaceous to late Eocene Rajang flysch belt is revealed, which is bounded by the Bukit Mersing Line ophiolite in the north and the Lupar line Ophiolite in the south [38] , it is believed that the sea plate subduction beneath Borneo should have finished around late Eocene here.…”

Section: Evidence For the Proto-south China Seamentioning

confidence: 99%

Research on the dynamics of the South China Sea opening: Evidence from analogue modeling

Sun

Zhou

Zeng³

et al. 2006

SCI CHINA SER D

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Independent of Indochina extrusion, the South China Sea experienced a process from passive continental rifting to marginal sea drifting. According to the fault patterns in the Beibu Gulf basin and the Pearl River Mouth basin, the continental rifting and early spreading stage from 32 to 26 Ma were controlled by extensional stress field, which shifted clockwise from southeastward to south southeastward. From 24 Ma on, the sea spread in NW-SE direction and ceased spreading at around 15.5 Ma. Integrated geological information with the assumption that the South China Sea developed along a pre-Cenozoic weakness zone, we did analogue experiments on the South China Sea evolution. Experiments revealed that the pre-existing weakness zone goes roughly along the uplift zone between the present Zhu-1 and Zhu-2 depression. The pre-existing weakness zone is composed of three segments trending NNE, roughly EW and NEE, respectively. The early opening of the South China Sea is accompanied with roughly 15° clockwise rotation, while the SE sub-sea basin opened with SE extension. Tinjar fault was the western boundary of the Nansha block (Dangerous Ground), while Lupar fault was the eastern boundary of the Indochina, NW-trending rift belt known as Zengmu basin developed between above two faults due to block divergent of Indochina from Nansha. In the experiment, transtensional flower structures along NW-trending faults are seen, and slight inversion occurs along some NE-dipping faults. The existence of rigid massifs changed the orientations of some faults and rift belt, and also led to deformation concentrate around the massifs. The rifting and drifting of the South China Sea might be caused by slab pull from the proto South China Sea subducting toward Borneo and/or mantle flow caused by India-Asia collision.

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A Miocene collisional belt in north Borneo: uplift mechanism and isostatic adjustment quantified by thermochronology

Cited by 168 publications

References 25 publications

Coupled onshore erosion and offshore sediment loading as causes of lower crust flow on the margins of South China Sea

Coupled onshore erosion and offshore sediment loading as causes of lower crust flow on the margins of South China Sea

Oligocene–Miocene carbonates in the Reed Bank area, South China Sea, and their tectono-sedimentary evolution

Research on the dynamics of the South China Sea opening: Evidence from analogue modeling

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