Tectonic evolution of SE Asia: introduction

Hall, Robert; Blundell, D. J.

doi:10.1144/gsl.sp.1996.106.01.01

Cited by 95 publications

(93 citation statements)

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“…It is possible that the massive tectonic changes that led to the formation of the Indo-Australian Arc and resultant separation of the Indian and Pacific Oceans caused a barrier to gene flow between these populations during the Miocene (25,26). The proposed Mindanao-Sulawesi land bridge, in conjunction with various proposed closures͞constrictions of the Makassar Strait between Borneo and Sulawesi, may have resulted in isolation of a north Sulawesi coelacanth population in a Sulawesi͞Sulu Sea basin during the Miocene and Pliocene (27,28).…”

Section: Resultsmentioning

confidence: 99%

Two living species of coelacanths?

Holder

Erdmann

Wilcox

et al. 1999

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

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During the period of September 1997 through July 1998, two coelacanth fishes were captured off Manado Tua Island, Sulawesi, Indonesia. These specimens were caught almost 10,000 km from the only other known population of living coelacanths, Latimeria chalumnae, near the Comores. The Indonesian fish was described recently as a new species, Latimeria menadoensis, based on morphological differentiation and DNA sequence divergence in fragments of the cytochrome b and 12S rRNA genes. We have obtained the sequence of 4,823 bp of mitochondrial DNA from the same specimen, including the entire genes for cytochrome b, 12S rRNA, 16S rRNA, four tRNAs, and the control region. The sequence is 4.1% different from the published sequence of an animal captured from the Comores, indicating substantial divergence between the Indonesian and Comorean populations. Nine morphological and meristic differences are purported to distinguish L. menadoensis and L. chalumnae, based on comparison of a single specimen of L. menadoensis to a description of five individuals of L. chalumnae from the Comores. A survey of the literature provided data on 4 of the characters used to distinguish L. menadoensis from L. chalumnae from an additional 16 African coelacanths; for all 4 characters, the Indonesian sample was within the range of variation reported for the African specimens. Nonetheless, L. chalumnae and L. menadoensis appear to be separate species based on divergence of mitochondrial DNA.

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Section: Resultsmentioning

confidence: 99%

Two living species of coelacanths?

Holder

Erdmann

Wilcox

et al. 1999

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

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“…Blow-ups of seismic image (a) along strike-slip fault shown in Figure 13.4a, (b) large fold along profile PGS08-12 and (c) along profile PGS08-06 near the subduction front. Hall & Blundell 1996;Hall 2002).…”

Section: Accretionary Wedgementioning

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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“…Karig [3] , Ben-Avraham [4] and Guo et al [5] proposed that the South China Sea is the back-arc basin of the Philippine arc, it is the result of paleo-Pacific ridge subducting toward Eurasia. Holloway [6] , Taylor and Hayes [7] and Hall [8] proposed that the slab pull caused by the subduction of the proto-South China Sea beneath the Borneo led to continental rifting of the South China margin and the opening of the South China Sea. Tapponnier et al [9,10] , Briais et al [11] and Leloup et al [12] believe that the India-Eurasia collision led to southeastward extrusion of the Indochina peninsula and the pulled apart South China Sea left-laterally at the end of the Red River Fault Zone.…”

Section: Introductionmentioning

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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Tectonic evolution of SE Asia: introduction

Cited by 95 publications

References 0 publications

Two living species of coelacanths?

Two living species of coelacanths?

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

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

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