Late Miocene obduction and microplate migration around the southern Banda Sea and the closure of the Indonesian Seaway

Linthout, K.; Helmers, H.; Sopaheluwakan, Jan

doi:10.1016/s0040-1951(97)00156-x

Cited by 62 publications

(34 citation statements)

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“…Lavas also display a variety of compositions, including high-Mg IAT and Mg-rich BABB with sub-alkaline affinities. Both IAT and BABB display high Th/Nb ratios which support an origin close to a continental crust environment.Our 20 to 15 Ma 40 K/ 40 Ar ages calculated for the BABB and 15-9 Ma for the IAT show that the basin and arc formed in a very short span of time, before their obduction 9-7 Ma ago [Linthout et al, 1997]. Considering the paleogeographic situation in the Miocene [Haile, 1979 ;Haile, 1981] and our data, we propose that the Seram-Ambon ophiolites formed during the early Miocene in a small, short-lived (10 Ma), transtensive basin bordered on its east by an active margin and on its western part by a passive continental margin over which it was later obducted towards the SW direction.…”

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confidence: 66%

“…IV) obtenus sur les basaltes arrière-arc (20-15 Ma) montrent bien que le bassin marginal s'est ouvert au cours des premiers stades de l'édification d'un arc volcanique dont seulement des jeunes témoins ont pu être datés (15-9 Ma). Ce dernier âge (9 Ma) est contemporain de celui de l'exhumation de l'ophiolite sur l'île de Seram qui aurait débuté vers 9,5 Ma pour s'achever vers 7 Ma [Linthout et al, 1996[Linthout et al, , 1997. Ceci indique un contexte géotectonique particulièrement rapide pour la formation et l'exhumation de l'ophiolite.…”

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Dynamics and age of formation of the Seram-Ambon ophiolites (Central Indonesia)

Monnier

Girardeau

Permana

et al. 2003

Bulletin De La Société Géologique De France

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Abstract. -The Seram-Ambon ophiolitic series comprise peridotites, websterites, gabbros and lavas. Petro-geochemical data show that the peridotites are weakly depleted rocks, except for the rare Cpx-free harzburgites. They underwent a sub-solidus metamorphic re-equilibration in the plagioclase field. The associated websterites and gabbros display various chemical features, allowing to define 3 types of websterites and 2 groups of gabbros. They have mostly BAB characteristics (presence of negative anomalies in Nb, Zr, Ti and Y), except the group 2 gabbros which have N-MORB features and the type 3 websterites which bear adakitic affinities. Lavas also display a variety of compositions, including high-Mg IAT and Mg-rich BABB with sub-alkaline affinities. Both IAT and BABB display high Th/Nb ratios which support an origin close to a continental crust environment.Our 20 to 15 Ma 40 K/ 40 Ar ages calculated for the BABB and 15-9 Ma for the IAT show that the basin and arc formed in a very short span of time, before their obduction 9-7 Ma ago [Linthout et al., 1997]. Considering the paleogeographic situation in the Miocene [Haile, 1979 ;Haile, 1981] and our data, we propose that the Seram-Ambon ophiolites formed during the early Miocene in a small, short-lived (10 Ma), transtensive basin bordered on its east by an active margin and on its western part by a passive continental margin over which it was later obducted towards the SW direction. Dynamique et âge de formation des ophiolites de Seram-Ambon (Indonésie centrale)Mots-clés. -Asie du Sud-Est, ophiolite, tholéiites riches en MgO, basaltes arrière-arc, rifting transtensif.Résumé. -L'île de Seram-Ambon est située au nord de la mer de Banda entre les îles de Sulawesi et de Nouvelle Guinée (fig. 1A). Sa position actuelle montre que son évolution géotectonique est et a été fortement liée, depuis le milieu du Cé-nozoïque, aux mouvements respectifs de la plaque Australienne qui remonte vers le NNW à raison de 7 cm.an -1 et de la plaque Philippine qui se déplace vers l'ouest à une vitesse d'environ 10 cm.an -1 [Minster et Jordan, 1978 ;De Mets et al., 1990].Plusieurs fragments d'ophiolites y sont présents. Ils sont pour l'essentiel localisés dans la partie ouest de l'île de Seram ( fig. 1B), sur les petites îles de Kelang situées à l'ouest et sur l'île d'Ambon présente au sud-est [Tjokrosapoetro et Budhitrisna, 1982] (fig. 1C). Ces trois secteurs réunis présentent tous les termes classiques d'une séquence ophiolitique, avec des péridotites, pyroxénites, gabbros et basaltes, mais aucun d'entre eux ne présente la totalité des termes d'une série ophiolitique complète. Les péridotites sont essentiellement des lherzolites à plagioclase, des harzburgites à spinelle riches en Cpx (3-3,5 %) pouvant contenir jusqu'à 2,2 % de plagioclase, et plus rarement des harzburgites sans Cpx qui contiennent quelques rubannements d'orthopyroxénites. Ces péridotites sont localement recoupées par des filonnets de chromitites, par des filons ou poches de webstérites de compositions chimiques variée...

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confidence: 66%

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Dynamics and age of formation of the Seram-Ambon ophiolites (Central Indonesia)

Monnier

Girardeau

Permana

et al. 2003

Bulletin De La Société Géologique De France

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“…Red triangles represent volcanoes. (de Smet, 1989;de Smet et al, 1989a, b;van Hinte and Hartono, 1989;Helmers et al, 1989;Linthout et al, 1989Linthout et al, , 1991Linthout et al, , 1996Linthout et al, , 1997Linthout and Helmers, 1994), and by oil companies working in eastern Seram and the Seram Trough (Zillman and Paten, 1975;O'Sullivan et al, 1985;Price et al, 1987;Kemp and Mogg, 1992;Pairault et al, 2003a, b;Charlton, 2004;Teas et al, 2009;Darman and Reemst, 2012) represents the bulk of previous research carried out on and around the islands. More than ten different stratigraphic schemes have been proposed for Seram, with names for equivalent units changing from publication to publication (Fig.…”

Section: The Geology Of Seram and Ambon: A Synopsis Of Previous Workmentioning

confidence: 99%

Extreme extension across Seram and Ambon, eastern Indonesia: evidence for Banda slab rollback

2013

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Abstract. The island of Seram, which lies in the northern part of the 180 • -curved Banda Arc, has previously been interpreted as a fold-and-thrust belt formed during arc-continent collision, which incorporates ophiolites intruded by granites thought to have been produced by anatexis within a metamorphic sole. However, new geological mapping and a re-examination of the field relations cause us to question this model. We instead propose that there is evidence for recent and rapid N-S extension that has caused the hightemperature exhumation of lherzolites beneath low-angle lithospheric detachment faults that induced high-temperature metamorphism and melting in overlying crustal rocks. These "Kobipoto Complex" migmatites include highly residual AlMg-rich garnet + cordierite + sillimanite + spinel + corundum granulites (exposed in the Kobipoto Mountains) which contain coexisting spinel + quartz, indicating that peak metamorphic temperatures likely approached 900 • C. Associated with these residual granulites are voluminous MioPliocene granitic diatexites, or "cordierite granites", which crop out on Ambon, western Seram, and in the Kobipoto Mountains and incorporate abundant schlieren of spineland sillimanite-bearing residuum. Quaternary "ambonites" (cordierite + garnet dacites) emplaced on Ambon were also evidently sourced from the Kobipoto Complex migmatites as demonstrated by granulite-inherited xenoliths. Exhumation of the hot peridotites and granulite-facies Kobipoto Complex migmatites to shallower structural levels caused greenschistto lower-amphibolite facies metapelites and amphibolites of the Tehoru Formation to be overprinted by sillimanite-grade metamorphism, migmatisation, and limited localised anatexis to form the Taunusa Complex. The extreme extension required to have driven Kobipoto Complex exhumation evidently occurred throughout Seram and along much of the northern Banda Arc. The lherzolites must have been juxtaposed against the crust at typical lithospheric mantle temperatures in order to account for such high-temperature metamorphism and therefore could not have been part of a cooled ophiolite. In central Seram, lenses of peridotites are incorporated with a major left-lateral strike-slip shear zone (the "Kawa Shear Zone"), demonstrating that strike-slip motions likely initiated shortly after the mantle had been partly exhumed by detachment faulting and that the main strike-slip faults may themselves be reactivated and steepened lowangle detachments. The geodynamic driver for mantle exhumation along the detachment faults and strike-slip faulting in central Seram is very likely the same; we interpret the extreme extension to be the result of eastward slab rollback into the Banda Embayment as outlined by the latest plate reconstructions for Banda Arc evolution.

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“…Acceleration of the Australian plate in the Late Miocene is indirectly supported by independent geologic data, such as: (1) ophiolite obduction in the Banda Arc region starting ca. 9.5 Ma and collision of the Banda Arc with the Australian margin 8-3 Ma (Linthout et al, 1997); (2) regional uplift across the southeast Australian margin in the Late Miocene (Dickinson et al, 2000); and, (3) the apparent termination of tectonic rotation of terranes along the Australia-Philippine Sea plate margin (e.g. Fuller et al, 1999;Ali and Hall, 1995).…”

Section: -Irmmentioning

confidence: 99%

Paleolatitudes and magnetostratigraphy for Cenozoic sediments, ODP Leg 182: The Great Australian Bight

Molina-Garza¹,

Fuller

2014

Earth Planet Sp

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Cenozoic northward drift of the Australian plate was determined from paleomagnetism of Middle Eocene through Pleistocene sediment cores from ODP Leg 182 (Sites 1126(Sites , 1128(Sites , and 1134 in the Great Australian Bight. Paleolatitude estimates are based on stepwise AF and thermal demagnetization of ∼400 discrete samples, of which ∼250 provided reliable data. The characteristic magnetization of the sediments resides in magnetite and magnetic sulfides. Middle Eocene through Lower Oligocene (∼36 Ma) paleolatitudes of ∼52• (±2 • ) change gradually to Late Miocene (∼9 Ma) paleolatitudes of ∼48• (±2 • ). These data, combined with Australian paleomagnetic pole data, indicate a slow rate of northward motion through much of the Cenozoic (∼28 mm/yr). These data also indicate an abrupt acceleration in the Late Miocene (drift rate ∼115 mm/yr), coinciding with tectonic events in Southeast Asia. Paleolatitude estimates support Miocene versions of the Australian apparent polar wander path that place the Oligocene-Miocene pole (∼25 Ma) at ∼70• S-125• E and the Late Miocene pole at ∼70 • S-105• E (e.g., Idnurm, 1985Idnurm, , 1994. Inclination data for discrete samples also provide a refined magnetostratigraphy for portions of the Miocene, Oligocene, and Eocene carbonate and siliciclastic section of the Great Australian Bight.

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Late Miocene obduction and microplate migration around the southern Banda Sea and the closure of the Indonesian Seaway

Cited by 62 publications

References 27 publications

Dynamics and age of formation of the Seram-Ambon ophiolites (Central Indonesia)

Dynamics and age of formation of the Seram-Ambon ophiolites (Central Indonesia)

Extreme extension across Seram and Ambon, eastern Indonesia: evidence for Banda slab rollback

Paleolatitudes and magnetostratigraphy for Cenozoic sediments, ODP Leg 182: The Great Australian Bight

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