Can microplate rotation drive subduction inversion

Webb, Laura E.; Baldwin, Suzanne L.; Little, Timothy A.; Fitzgerald, Paul G.

doi:10.1130/g25134a.1

Cited by 72 publications

(94 citation statements)

References 23 publications

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“…The orogen's geology documents a history of convergence and extension between the Australian plate and microplates including the Woodlark and Solomon plates during arcÀcontinent collision (Davies & Smith 1971;Smith & Milsom 1984;Hall 2002;Webb et al 2008;Whattam et al 2008;Whattam 2009;Daczko et al 2011;Little et al 2011;Baldwin et al 2012;Fitz & Mann 2013). Elevations in excess of 2000 m are present on Goodenough and Fergusson islands and on the Papuan Peninsula (Mt Suckling-3676 m-is the highest mountain in Papua, and for comparison, is only 48 m below Aoraki/Mt Cook, South Island, New Zealand).…”

Section: Tectonic Setting Of Eastern Papua Papuan Orogenmentioning

confidence: 98%

Suckling Dome and the Australian–Woodlark plate boundary in eastern Papua: the geology of the Keveri and Ada'u Valleys

Lindley¹

2014

Australian Journal of Earth Sciences

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Section: Tectonic Setting Of Eastern Papua Papuan Orogenmentioning

confidence: 98%

Suckling Dome and the Australian–Woodlark plate boundary in eastern Papua: the geology of the Keveri and Ada'u Valleys

Lindley¹

2014

Australian Journal of Earth Sciences

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“…Most of these microplates are rotating rapidly about nearby vertical axes as a result of localized collisions. Webb et al. (2008) have proposed that these rotations have led to a process of ‘subduction inversion’ in which previously subducted material including the core complexes are now being exhumed along active microplate boundaries.…”

Section: Regional Geology Of Metamorphic Core Complexes In Eastern Pngmentioning

confidence: 99%

Exhumation of the Dayman dome metamorphic core complex, eastern Papua New Guinea

Daczko

Caffi

Halpin

et al. 2009

Journal Metamorphic Geology

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The 750 km 2 Dayman dome of the Late Cretaceous Suckling-Dayman massif, eastern Papua New Guinea, is a domed landform that rises to an elevation of 2850 m. The northern edge of the dome is a fault scarp >1000 m high that is now part of an active microplate boundary separating continental crust of the New Guinea highlands from continental and oceanic crust of the Woodlark microplate. Previous work has shown that a parallel belt of eclogite-bearing core complexes north-east of the Dayman dome were exhumed from up to 24-28 kbar in the last few millions of years. The remarkably fresh and lightly eroded scarp of the Dayman dome exposes shallowly-dipping mylonitic (S1) metabasite rocks (500 m thick) on the northern flank of Mount Dayman. Field relationships near the base of this scarp show a cross cutting suite of ductile and brittle meso-structures that includes: (i) rare ductile S2 folia with a shallowly ESE-plunging mineral elongation lineation defined by sodic-calcic blue amphibole; (ii) narrow steeply-dipping ductile D2 shear zones; and (iii) semi-brittle to brittle fault zones. Pumpellyite-actinolite facies assemblages reported by previous workers to contain local aragonite, lawsonite and ⁄ or glaucophane are found in the core of the complex at elevations greater than 2000 m. These assemblages indicate peak metamorphic pressures of 6-9.5 kbar, demonstrating exhumation of the core of the Dayman dome from depths of 20-30 km. The S1 metamorphic mineral assemblage in metabasite includes actinolite-chlorite-epidote-albite-quartz-calcite-titanite, indicative of greenschist facies conditions for the main deformation. New mineral equilibria modelling suggests that this S1 assemblage evolved at 5.9-7.2 kbar at 425°C. Modelling variable Fe 3+ indicates that the sodic-calcic blue amphibole (D2) formed under a higher oxidation state compared with the S1 assemblage, probably at <4.5 kbar. A SE-dipping, Mio-Pliocene sedimentary sequence (Gwoira Conglomerate) forms a hangingwall block juxtaposed by low-angle fault contact with the metabasite footwall. Prehnite-bearing D3 brittle fault zones separate the two blocks and likely accommodated the final exhumation of the S1 greenschist facies assemblage in the footwall. These results indicate that the extensive Mt Dayman fault surface coincides with a domed S1 greenschist facies foliation that was last active at >20 km depth. Exhumation of this foliation must therefore be controlled by brittle faults of the active microplate boundary that are largely not observed in the study area. The structural record of the final exhumation of the Dayman dome to the surface was likely lost as a result of erosion, poor exposure or wide spacing of semi-brittle to brittle fault zones.

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“…High-grade lower-crustal metamorphic core complexes have been studied in eastern Papua New Guinea on the D'Entrecasteaux Islands (Fig. 1B), where rocks that formed under a large range of depth and temperature conditions have been uplifted (Davies and Smith, 1971;Ollier and Pain, 1981;Davies and Warren, 1988;Hill et al, 1992Hill et al, , 1995Baldwin et al, 1993Baldwin et al, , 2004Baldwin et al, , 2005Baldwin and Ireland, 1995;Little et al, 2007;Monteleone et al, 2007;Webb et al, 2008). However, studies of emergent, late Quaternary coral reefs and Neogene sedimentary sections in eastern Papua New Guinea suggest that the D'Entrecasteaux Islands have been stable or subsiding for the past 0.5 m.y.…”

Section: Introductionmentioning

confidence: 99%

Structural evolution of the Dayman dome metamorphic core complex, eastern Papua New Guinea

Daczko

Caffi

Mann

2011

Geological Society of America Bulletin

100

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Can microplate rotation drive subduction inversion

Cited by 72 publications

References 23 publications

Suckling Dome and the Australian–Woodlark plate boundary in eastern Papua: the geology of the Keveri and Ada'u Valleys

Suckling Dome and the Australian–Woodlark plate boundary in eastern Papua: the geology of the Keveri and Ada'u Valleys

Exhumation of the Dayman dome metamorphic core complex, eastern Papua New Guinea

Structural evolution of the Dayman dome metamorphic core complex, eastern Papua New Guinea

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