Late Jurassic–Cenozoic reconstructions of the Indonesian region and the Indian Ocean

Tectonic framework and Phanerozoic evolution of Sundaland

SE Asia comprises a collage of Gondwana-derived continental blocks assembled by the closure of multiple Tethyan and back-arc ocean basins now represented by suture zones. Two major biogeographical boundaries, the Late Palaeozoic Gondwana–Cathaysia divide and the Cenozoic-Recent Australia–Asia divide (Wallace Line) are present. Palaeozoic and Mesozoic evolution involved the rifting and separation of three collages of continental terranes from eastern Gondwana and the opening and closure of three successive ocean basins, the PalaeoTethys (Devonian–Triassic), Meso-Tethys (Permian–Cretaceous) and Ceno-Tethys (Late Triassic–Cenozoic). This led to the opening and closing of ocean gateways and provision of shallow-marine and terrestrial land bridges and stepping-stones for biotic migration. The SE Asia core (Sundaland) comprises a western Sibumasu block, an eastern Indochina–East Malaya block, and the Sukhothai Island Arc terrane between. The Jinghong, Nan-Uttaradit and Sra Kaeo sutures represent the Sukhothai closed back-arc basin. The Palaeo-Tethys is represented by the Changning-Menglian, Chiang Mai/Inthanon and Bentong-Raub suture zones. The West Sumatra and West Burma blocks were accreted to the Sundaland core in the Late Permian– Early Triassic. SW Borneo and/or East Java–West Sulawesi are now identified as the missing ‘Argoland’ that separated from NW Australia in the Jurassic and accreted to SE Sundaland in the Cretaceous. SE Asia is located at the zone of convergence between the ESE moving Eurasia Plate, the NE moving Indian and Australian Plates and the ENE moving Philippine Plate (Fig. 1). SE Asia and adjoining regions comprise a complex collage of continental blocks, volcanic arcs, and suture zones that represent the closed remnants of ocean basins (including back-arc basins). The continental blocks of the region were derived from the margin of eastern Gondwana as three successive continental strips or collages of continental blocks that separated in the Devonian, Early Permian and Triassic– Jurassic and which then assembled during the Late Palaeozoic to Cenozoic to form present day East and SE Asia (Metcalfe 2005). Global, regional and local Palaeozoic–Mesozoic tectonic evolution resulted in changes to continent– ocean configurations, dramatic changes in relief both on land and in the seas, and changes in palaeo-ocean currents, including the opening and closing of oceanic gateways. The significant effect on ocean circulation caused by ocean gateway closure/ opening is well documented (e.g. Von der Heydt & Dijkstra 2006, 2008). The changes in continent– ocean, land–sea, relief, and ocean current patterns are fundamental factors leading to both global and regional climate-change and to important changes in biogeographical patterns. Changes in biogeographical barriers and bridges caused by geological evolution and consequent climate-change have also influenced the course of migration, dispersal, isolation and evolution of biota, both globally and in SE Asia. This paper provides an overview of the tectonic framework, and Palaeozoic and Mesozoic geological evolution and palaeogeography of SE Asia and adjacent regions as a background to and to underpin studies of the Indonesian Throughflow Gateway and the distribution and evolution of biota in the region. Geological and tectonic framework of SE Asia and adjacent regions Mainland East and SE Asia comprises a giant ‘jigsaw puzzle’ of continental blocks, volcanic arc terranes, suture zones (remnants/sites of destroyed ocean basins) and accreted continental crust (Figs 2 & 3). From: Hall, R., Cottam, M. A. & Wilson, M. E. J. (eds) The SE Asian Gateway: History and Tectonics of the Australia–Asia Collision. Geological Society, London, Special Publications, 355, 7–35. DOI: 10.1144/SP355.2 0305-8719/11/$15.00 # The Geological Society of London 2011. Continental blocks of SE Asia The principal continental blocks located in mainland SE Asia (Fig. 2) have been identified and established over the last two decades (e.g. Metcalfe 1984, 1986, 1988, 1990, 1996a, 1998, 2002, 2006) and include the South China block, the Indochina–East Malaya block(s), the Sibumasu block, West Burma block and SW Borneo block (Fig. 3). More recently, the West Sumatra block has been established outboard of Sibumasu in SW Sumatra (Barber & Crow 2003, 2009; Barber et al. 2005) and a volcanic arc terrane is now identified, sandwiched between Sibumasu and Indochina–East Malaya (Sone & Metcalfe 2008). A series of smaller continental blocks are identified in eastern (maritime) SE Asia and these were accreted to the mainland core of SE Asia in the Mesozoic– Cenozoic. The continental terranes of SE Asia and adjacent regions are here categorized into six types based on their specific origins, times of rifting and separation from Gondwana, and amalgamation/ accretion to form SE Asia. These are discussed below and the suture zones between them are described separately. Continental blocks derived from Gondwana

/pdf/palaeozoic-mesozoic-history-of-se-asia-hdqnbqvgxj.pdf

Palaeozoic–Mesozoic history of SE Asia

Abstract The Sundaland core of SE Asia is a heterogeneous assemblage of Tethyan sutures and Gondwana fragments. Its complex basement structure was one major influence on Cenozoic tectonics; the rifting history of the north Australian margin was another. Fragments that rifted from Australia in the Jurassic collided with Sundaland in the Cretaceous and terminated subduction. From 90 to 45 Ma Sundaland was largely surrounded by inactive margins with localized strike-slip deformation, extension and subduction. At 45 Ma Australia began to move north, and subduction resumed beneath Sundaland. At 23 Ma the Sula Spur promontory collided with the Sundaland margin. From 15 Ma there was subduction hinge rollback into the Banda oceanic embayment, major extension, and later collision of the Banda volcanic arc with the southern margin of the embayment. However, this plate tectonic framework cannot be reduced to a microplate scale to explain Cenozoic deformation. Sundaland has a weak thin lithosphere, highly responsive to plate boundary forces and a hot weak deep crust has flowed in response to tectonic and topographic forces, and sedimentary loading. Gravity-driven movements of the upper crust, unusually rapid vertical motions, exceptionally high rates of erosion, and massive movements of sediment have characterized this region.

Australia–SE Asia collision: plate tectonics and crustal flow

SE Asia comprises a collage of continental terranes derived directly or indirectly from the India–Australian margin of eastern Gondwana The Late Palaeozoic and Mesozoic evolution of the region involved the rifting and separation of three elongate continental slivers from eastern Gondwana and the successive opening and closure of three ocean basins, the Palaeo-Tethys, Meso-Tethys and Ceno-Tethys The Sukhothai Island Arc System, including the Linchang, Sukhothai and Chanthaburi terranes, is identified between the Sibumasu and Indochina–East Malaya terranes in SE Asia and was formed by back-arc spreading in the Permian The Jinghong, Nan–Uttaradit and Sra Kaeo sutures represent the closed back-arc basin The Palaeo-Tethys is represented to the west by the Changning–Menglian, Chiang Mai/Inthanon and Bentong–Raub suture zones The West Sumatra and West Burma blocks rifted and separated from Gondwana, along with Indochina and East Malaya in the Devonian, and together with South China formed a composite terrane ‘Cathaysialand’ in the Permian They were translated westwards to their positions outboard of the Sibumasu Terrane by strike-slip tectonics in the Late Permian–Early Triassic at the zone of convergence between the Meso-Tethys and Palaeo-Pacific plates SW Borneo is tentatively identified as possibly being the missing ‘Argoland’ that separated from NW Australia in the Jurassic Palaeogeographical reconstructions for the Late Palaeozoic and Mesozoic illustrating the tectonic and palaeogeographical evolution of SE Asia are presented SE Asia is a unique natural laboratory for studying collisional plate tectonics, suture formation and mountain building (Hall 2002, 2009) The region is also one of the best for studying long-lived terrane dispersion and accretion processes (Metcalfe 1999) and the effects of rapid changes in continent– ocean configurations on biogeographical patterns and ecosystems (Hall & Holloway 1998; Kershaw et al 2001; Metcalfe et al 2001) The tectonic evolution, terrane accretion, and assembly of SE Asia during the Late Palaeozoic and Mesozoic has resulted in complex changes in the palaeogeography of SE Asia and in the juxtaposition of contrasting but temporally coincident palaeo-ecosystems in the region Changing continent–ocean configurations, palaeogeography and climate changes in the Late Palaeozoic and Mesozoic of what is now SE Asia have resulted in complex patterns of both marine and terrestrial ecosystems of SE Asia both in space and time This paper presents an overview of the tectonic and palaeogeographical evolution of SE Asia in the Late Palaeozoic and Mesozoic Tectonic framework of SE Asia SE Asia is located at the zone of convergence between the Eurasia, Pacific and Indo-Australian plates (Fig 1) The region comprises a complex assemblage of continental terranes (bounded by suture zones or other major tectonic features), island arcs and small ocean basins The older Palaeozoic and Mesozoic portions of the region comprise allochthonous continental terranes (small to medium-sized allochthonous continental blocks that have distinctive tectonostratigraphic histories) that were assembled prior to the current collision of Australia with the region The Cenozoic evolution of the region has been well studied, and the evolution and reconstruction models of Hall (2002) are considered the most reliable This paper focuses on the Late Palaeozoic and Mesozoic evolution Continental terranes and their origins The principal continental terranes and sutures of SE Asia are shown in Figures 2 and 3 Terranes are grouped according to their interpreted origins and are discussed briefly under these origin groupings below Descriptions of the terranes have been given by Metcalfe (2006) All the continental terranes of East and SE Asia are interpreted to have been directly or indirectly derived from the eastern Gondwana margin at different times and some small terranes were subsequently derived indirectly from larger Gondwana-derived terranes or composite terranes (see Metcalfe 1986, 1988, 1990, 1991, 1993, 1996a, b, 1998, 2001, 2002, 2005, 2006; Table 1) I have previously described the successive rifting and northwards drift of three From: BUFFETAUT, E, CUNY, G, LE LOEUFF, J & SUTEETHORN, V (eds) Late Palaeozoic and Mesozoic Ecosystems in SE Asia The Geological Society, London, Special Publications, 315, 7–23 DOI: 101144/SP3152 0305-8719/09/$1500 # The Geological Society of London 2009 Gondwana-derived continental slivers (now disrupted into various terranes), with the successive opening and closure of the Palaeo-Tethys, Meso-Tethys and Ceno-Tethys ocean basins This broad scenario is still advocated here (Fig 4), but recent new data demand modification of the terrane make-up of these continental slivers, and also reinterpretations of the origins and boundaries of some of the terranes in the region Terranes derived from Gondwana in the Devonian A group of East and SE Asian terranes are interpreted to have rifted and separated from Gondwana as an elongate continental sliver in the Devonian (Fig 4) and comprise North China, South China (including Hainan), Indochina–East Malaya (including the Qamdao–Simao/Simao and disrupted West Sumatra and West Burma terranes) and Tarim (including the disrupted Kunlun, Qaidam and Ala Shan terranes) The West Sumatra terrane was proposed by Hutchison (1994) and Barber & Crow (2003), and is interpreted to have been translated westwards from ‘Cathaysialand’ (combined South China–Indochina–East Malaya composite terrane in Permo-Triassic times) as suggested by Barber et al (2005) and Metcalfe (2005) A Devonian separation of these terranes from Gondwana is still advocated here based on palaeomagnetic and biogeographical data from the terranes themselves and also from Devonian age data for oceanic radiolarian cherts in the Palaeo-Tethys (for details, see Metcalfe 1988, 1990, 1998, 2005) Jablonski & Saitta (2004) have, however, on the basis of transgressive–regressive sequences in western Australian basins, argued for a later Early Carboniferous (Visean) separation of South China, Indochina and Simao terranes This timing seems too young in view of the fact that the Palaeo-Tethys suture zone includes oceanic sediments of Devonian age and no post-Devonian Gondwana biota is reported from the terranes in question Terranes derived from Gondwana in the Early Permian The second continental sliver that rifted and separated from Gondwana in the Early Permian (with opening of the Meso-Tethys) was the Cimmerian continent of Sengor (1979, 1984), which included the Sibumasu terrane (Metcalfe 1984) of SE Asia and the Baoshan and Tengchong terranes of Yunnan in western China I have presented evidence for the NW Australian origin and Early Permian rifting and separation of the Sibumasu portion of the Cimmerian continent from Gondwana in a series of papers (eg Metcalfe 1986, 1988, 1990, 1991, 1993, 1996a, b, 1998, 2001, 2002, 2005, 2006) and this will not be repeated here Recent studies (Sone & Metcalfe 2008) have led to the recognition of an island arc system, the Sukhothai Island Arc system, through SE Asia (Fig 5) situated between Sibumasu and Indochina–East Malaya (from which it was derived by back-arc spreading) This interpretation, Fig 1 Principal tectonic plates of SE Asia Arrows show plate motions relative to Eurasia I METCALFE 8

http://metcalfeian.com/web-data/PDF%20Files/Metcalfe%202009%20Geol%20Soc.pdf

Late Palaeozoic and Mesozoic tectonic and palaeogeographical evolution of SE Asia

Recent studies of the Tertiary tectonics of the Bawean area suggest that strain is regionally inhomogeneous and the area has been partitioned into several domains separated by major strike-slip faults and extensional zones. Major structural elements occurring from west to east are the Muriah Trough, the Bawean Arch, the Tuban-Camar Trough, the JS-1 Ridge, the Central Deep Depression, the Masalembo Basin and the North-Madura Shelf. Tectonic rotation of these domains, as well as their internal deformation, has occurred as a result of regional sinistral shear. Two major tectonic phases have been identified, one controlling the Paleogene rift-phase and the other the Neogene reactivation of the Bawean area. The sedimentary fill of the Paleogene basin is closely related to its tectonic history. Doming and fracturing of the entire region during the Eocene/Oligocene was followed by a period of regional subsidence and tectonic quiescence lasting into the Early Miocene. Northeast-southwest trending grabens formed during the Middle Eocene and were filled with alluvial clastics, lateritic clays and lacustrine shales. Organic rich shales in this sequence provide the source rock for hydrocarbons throughout the region. Basement onlap began in the Late Eocene to Early Oligocene with the deposition of transgressive basal marine sandstones and limestones including reefs. Facies distribution in the Neogene is controlled also by the positions of pre-existing highs and their intervening depressions. Generally, shallow marine shales, sandstones and limestones were deposited over the region with deeper marine sediments deposited to the south. A number of the Paleogene fault zones were reactivated during the Neogene, mainly as comparatively gentle flexures which were accentuated by minor faults. Wrench faulting, basin inversion or renewed basin subsidence starting in the Late Miocene appears to have continued into Recent times. In addition to imparting a strong northeast-southwest structural grain to the region with associated north-south oriented en-echelon structures, the later tectonic regime has apparently facilitated local magmatism. Increased heat flow during tectonic activity caused parts of the Paleogene source kitchens to reach maturity before the main pulse of inversion. Where renewed subsidence has occurred, these source rocks are now in the gas window or are overmature. Structures formed during the Late Miocene are readily identified on seismic data, however they are generally dry because their origin postdates the main phase of hydrocarbon generation. The size of hydrocarbon accumulations in these structures may also be limited by a lack of effective seal. Pre-Late Miocene structures, on the other hand, despite also having suffered a later inversion phase, are an attractive exploration target due to their existence before oil generation. Potential traps for hydrocarbon accumulation are extremely varied. Along the Madura-Kangean trend in the Early Tertiary basins, Oligocene to Early Miocene pinnacle reefs are surrounded and overlain by deep water shales. The Middle Miocene inversion led to the deposition of turbidite sandstones in some basins, with vertical migration of hydrocarbons through rejuvenated faults. On the shelfal areas, patch reefs and shallow marine sandstones of Oligocene to Middle Miocene age are the targets for exploration. Transgressive basal marine sandstones occur over regional palaeohighs. Reefal limestones of Pliocene age are also of interest where they are sealed by Recent mudstones.

Structural Control on Hydrocarbon Habitat in the Bawean Area, East Java Sea

Handle everyday research tasks with reliable, citation-backed results

Your personal Research Agent to handle research tasks with citation-backed results

Popular Tasks used by Researchers

How can I help with your research?

Meet SciSpace

Get more enhanced response by uploading the PDFs you want me to reference.

No relevant PDFs in your library

SciSpace is the AI research assistant for academics. Run systematic literature reviews on 280M+ papers, and write papers with cited sources. Trusted by 1M+ students, PhDs & researchers.

SciSpace | AI for Research

Analyze PDFs

Code & Manuscripts

Funding & Grants

Literature & Patents

Medical & Clinical Data

Systematic Review

Visualize & Present

Web & Data

Build a Google Scholar-like website for your research.

Build a website

Create charts and images for your research

Create a Chart

Write a paper for submission to a journal

Draft a manuscript

Patent Search

Design eye-catching scientific posters in minutes.

Scientific Poster Generation

Systematic Literature Review

One task is running at the moment. Your messages will be shown right after.

Drag and drop or click here to browse

Loved by <highlight>1 million+</highlight> researchers

Extract a list of specific topics and their sources from unstructured text

Topics

Compare and analyze relevant papers that matches with your search

Papers

Get insights from PDFs and bookmarked papers from your library

My library

Recent searches

Try searching for:

Catch AI-generated content in scholarly and non-scholarly content

{ai} Detector

Ai Writer

Get PDF Summaries, highlighted text explanations 

Chat with PDF

Effortlessly create in-text citations and bibliographies in APA and 2,500 other formats

Citation generator

Get explanations, summaries, and answers on academic papers

Ease up your research workflow with {scispace}'s cohort of exciting AI tools

Elevate your academic writing skills and convey your ideas the way you want

Paraphraser

Explore our range of reading and writing tools

Your file is being prepared and should be ready in a few minutes. If it's a large file, it might take a bit longer. You can close this window, and we'll email you the file when it's done.

You have reached a maximum limit of <strong>{limit}</strong> columns in the table. Remove at least <strong>1</strong> column to add or create another one.

Rob Barraclough

Author Tools

Chat about Author

Papers

Structural Control on Hydrocarbon Habitat in the Bawean Area, East Java Sea