Rifting of the northern margin of the Australian continent and the origin of some microcontinents in Eastern Indonesia

Pigram, C. J.; Panggabean, Hermes

doi:10.1016/0040-1951(84)90257-9

Cited by 165 publications

(77 citation statements)

References 7 publications

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“…Similar arc and ophiolitic rocks now found in Bacan, Obi, Halmahera and Waigeo remained part of the Philippine Sea Plate and have rotated clockwise and moved westwards approximately 1500 km at an average rate of ~ 6 cm/yr. The small continental areas of east Indonesia appear to have their origin in a single micro-continent which separated early from Australia by rifting as suggested by Pigram and Panggabean (1984) and which has been fragmented in the Neogene by splays of the Sorong Fault.…”

Section: Discussionmentioning

confidence: 89%

Evolution of the boundary between the Philippine Sea Plate and Australia: palaeomagnetic evidence from eastern Indonesia

Ali¹,

Hall

1995

Tectonophysics

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Section: Discussionmentioning

confidence: 89%

Evolution of the boundary between the Philippine Sea Plate and Australia: palaeomagnetic evidence from eastern Indonesia

Ali¹,

Hall

1995

Tectonophysics

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“…In the Permian, the Tethys Ocean started to form to the north (Pigram and Panggabean, 1984;§engör, 1985;Scotese, 1986;Audley-Charles, 1988;Görür and §engör, this volume) and there was considerable stretching and thinning of the Exmouth Plateau crust (Mutter et al, 1989;Williamson et al, 1990). This led to rapid subsidence, and the deposition of a thick section of largely fluviodeltaic Triassic sediments.…”

Section: Overall Tectonic Evolutionmentioning

confidence: 97%

Mesozoic Seismic Stratigraphy and Tectonic Evolution of the Western Exmouth Plateau

Exon¹,

Buffler²

1992

Proceedings of the Ocean Drilling Program

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The western comer of the continental Exmouth Plateau is bounded by Early Cretaceous (ValanginianHauterivian) abyssal plains on two sides. A study of a regional grid of reflection seismic profiles, in conjunction with the results from ODP Sites 762, 763, and 766, has helped us elucidate the Triassic to Late Cretaceous history of the region.Before late Mesozoic continental breakup, this area was part of northern Gondwana facing Tethys, and was subject to detrital, largely fluviodeltaic sedimentation. Several thousand meters of Triassic fluviodeltaic sediments were cut by strike-slip and normal faults in latest Triassic to Late Jurassic times. Near the western margin the Triassic sediments give way to a volcanic sequence, of inferred latest Triassic to earliest Jurassic age, parts of which were planated near sea level in and before the early Neocomian. The detritus from the early Neocomian erosion formed a shallow-marine sediment body in the west, 90 km long and up to 500 m thick, equivalent to the Barrow Group in the east. In the southeast in the Berriasian, the top Triassic unconformity was overlain by up to 1500 m of prodelta muds of the Barrow delta (deposited in 6 m.y.) prograding northward. These were derived largely from an uplifted area, formed by Neocomian thermal doming along the Cape Range Fracture Zone, and also along the zone of later rifting farther southeast.Late Valanginian breakup led to the movement of Greater India away to the west, by rifting on the northwestern side of the plateau and by shearing along the Cape Range Fracture Zone on the southwestern side. On the plateau, after a Valanginian hiatus, there was slow detrital sedimentation as the plateau sank, and by Late Cretaceous times bathyal carbonates were being deposited. Postbreakup sediments are generally less than 1000 m thick. On the new abyssal plains sedimentation was in increasingly deep water. During the late Valanginian to Hauterivian, grain-flow sands and silts were deposited on oceanic basalt close to the plateau, while abyssal muds were deposited farther away. In the mid-Cretaceous, pelagic sediments and carbonate turbidites replaced the grain-flow sands, silts, and muds. The postbreakup sediments on the abyssal plain are 400-500 m thick.

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“…According to Pigram and Panggabean (1984) the Birds Head consists of two microcontinents, Kemum (which forms the nucleus of its northern half) and Misool (consisting of Misool island and the Onin and Kumaua peninsulas), of which the first one became detached from near central Papua New Guinea and the second one probably from an area east of Queensland. These microcontinents collided and moved as a single block westward, just north of the continent, by the same process that moved other microcontinents into the Moluccan area, and they collided again with the continent (about 10 m.y.…”

Section: Geological Historymentioning

confidence: 99%

Historical biogeography of the cicadas of Wallacea, New Guinea and the West Pacific: a geotectonic explanation

Boer

Duffels

1996

Palaeogeography, Palaeoclimatology, Palaeoecology

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The present-day distribution patterns of the cicadas of Wallacea, New Guinea, and the West Pacific reflect the extremely complex geotectonic history of that area. The patterns found in two unrelated monophyletic groups of cicadas (Insecta, Homoptera, Cicadoidea), the subtribe Cosmopsaltriaria and the tribe Chlorocystini with its sister tribe Prasiini, are analysed and related to data from the geological literature. The two groups have a comparable distributional range over Sulawesi, Maluku, New Guinea, the Bismarck Archipelago, and the East-Melanesian archipelagos, to Tonga and Samoa. The occurrence of endemic species, species groups, and genera in congruently delimited parts of this range made us recognize 14 areas of endemism. The areas of endemism coincide with geological entities, which have been isolated during a considerable period of time. Most of the areas originated from oceanic island arcs, which developed as a result of subduction along the southern and western edges of the Pacific tectonic plate, others are rifted microcontinents. Concentrations of species and especially endemic species of the various cicada genera in different areas of endemism suggest that each of these genera evolved in isolation on one of the afore mentioned geological entities. These entities can therefore be regarded as source areas for the genera. The island arc fragmented as a result of collisions first with the Asian-and later with the Australian tectonic plate and several of its parts reamalgamated at the northern craton of the Australian plate, where they now form the greater part of the island of New Guinea. After reamalgamation of the arc fragments the cicadas of the respective genera that had evolved on these fragments could disperse into adjoining areas, but since cicadas are poor dispersers the source areas of the genera can still be recognized in present-day distribution patterns. The generic relationships in the two groups of cicadas under study indicate area relationships that comply with the latest palaeogeographic reconstructions. The main vicariant speciation events in the cicada cladograms correspond with the presumed sequences of fragmentation of the island arc. Cicada phylogeny and distribution combined reflect the historic area relationships rather than the present ones.

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Rifting of the northern margin of the Australian continent and the origin of some microcontinents in Eastern Indonesia

Cited by 165 publications

References 7 publications

Evolution of the boundary between the Philippine Sea Plate and Australia: palaeomagnetic evidence from eastern Indonesia

Evolution of the boundary between the Philippine Sea Plate and Australia: palaeomagnetic evidence from eastern Indonesia

Mesozoic Seismic Stratigraphy and Tectonic Evolution of the Western Exmouth Plateau

Historical biogeography of the cicadas of Wallacea, New Guinea and the West Pacific: a geotectonic explanation

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