Age, Character and Provenance of The Tipuma Formation, West Papua: New Insights From Detrital Zircon Dating

Gunawan, Indra; Hall, Robert; Sevastjanova, Inga

doi:10.29118/ipa.0.12.g.027

Cited by 13 publications

(17 citation statements)

References 19 publications

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“…The Triassic rift setting R 1 is limited eastward to the Gulf of Papua in the Coral Sea ( Formation I , Figure ). Unconformities (BR 1 in the Kutubu Basin) and correlative disconformities in other places (Figure ) bound various correlatable clastic sequences (e.g., Jimi Formation in the Aure Fold Belt, Bain et al, ; Home et al, , Tipuma Formation in the Lengguru and Central Papuan fold and thrust belts, Fraser et al, ; Gunawan et al, , Cape Londondery Formation and Malita Formation along the NW Shelf, Ahmad & Munson, , ). These are grouped into a regional synrift megasequence, called Megasequence EM 1 , which the definition is broadly equivalent to the Gondwana Synrift Megasequence A of Home et al () or the Tipuma Formation of Visser and Hermes () and Pieters et al ().…”

Section: Discussionmentioning

confidence: 95%

Successive Rifting Events in Marginal Basins: The Example of the Coral Sea Region (Papua New Guinea)

et al. 2018

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Reactivation of extensional structures is commonly inferred during rift evolution. In that context, we present original seismic interpretation to explore the geometry and interactions of three successive rifting events in the Coral Sea region, Papua New Guinea. The first event (R1), poorly documented, occurred during the Triassic along an older N‐S Permian structural fabric. During the Jurassic, extensional faults were reactivated through a second extensional episode (R2), which formed small (~10/20 km) basins bounded by N‐S, NE‐SW, and E‐W listric faults. Extension prolonged during the Lower Cretaceous with seafloor spreading in the Owen Stanley Oceanic Basin, now incorporated in the Papuan fold and thrust belts. A third Late Cretaceous extensional phase (R3) gently reactivated some of the faults with very limited landward tilt in most basins and deformation located along the present continent‐ocean transition. Seafloor spreading in the Coral Sea followed from Danian to Ypresian. This extensional system is sealed by unequally preserved Eocene strata that mark the onset of postrift thermal subsidence prior to the margin inversion from Oligocene onward. This overall evolution suggests various extensional systems that are geographically and temporarily defined the one another. The early rifting of the crust is controlled by preexisting continental features resulting in the local Pangaea breakup. In contrast, the Coral Sea propagator cuts through the rifted margin and is controlled by a subduction complex in accordance with the Tasman Sea opening. This evolution underlines the interactions existing between two extension modes in agreement with variations of the regional geodynamical setting around Australia.

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Section: Discussionmentioning

confidence: 95%

Successive Rifting Events in Marginal Basins: The Example of the Coral Sea Region (Papua New Guinea)

et al. 2018

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“…Most of these samples contain Devonian to earliest Jurassic zircons (dominated by Devonian, Carboniferous, and Triassic zircon). These zircons are interpreted to have been derived from the erosion and transport of material sourced locally (e.g., Gunawan et al, ). Recent geochronology studies have dated Triassic igneous rocks to the south, east, and northwest of the Wandamen Peninsula (Decker et al, ; Jost et al, ).…”

Section: Discussionmentioning

confidence: 99%

“…North‐western New Guinea currently marks a section of the boundary between the Australian, Caroline, and Pacific plates (Figure ). A plate boundary has existed north of New Guinea since the Devonian where New Guinea represented the northern edge of eastern Gondwana (e.g., Baldwin et al, ; Davies, ; Gunawan et al, ; Jost et al, ; Webb & White, ). However, widespread deposition of carbonate sequences along the northern margin of New Guinea during the Cretaceous to early Eocene indicates that there was a period of relative tectonic quiescence on the southern (“Australian”) side of the plate boundary during this time (e.g., Gold, White, et al, ; Pieters et al, ; Visser & Hermes, ).…”

Section: Geologic Settingmentioning

confidence: 99%

Tectonic Mode Switches Recorded at the Northern Edge of the Australian Plate During the Pliocene and Pleistocene

et al. 2019

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We report new data from medium-high grade metamorphic rocks found at the northern margin of the Lengguru Fold Belt in West Papua. The study involved a systematic analysis of cross-cutting structures to establish the relative timing of deformation, together with isotopic dating to define when these tectono-thermal events occurred. These data show that the region underwent multiple episodes of deformation within the last six million years. Metamorphic mineral growth was associated with the development of ductile shear zones. This episode occurred during a phase of crustal stretching associated with the formation of a metamorphic core complex. Metamorphic zircon growth at 4.9 to 5.3 Ma was documented in two of the dated samples. These data are interpreted to postdate the peak pressure and temperature conditions of the phase of regional crustal stretching. The shear fabrics associated with the metamorphic core complex were later overprinted by at least two generations of folds. The change in mode from crustal extension to shortening reflects a tectonic mode switch. A subsequent mode switch is documented by numerous brittle extensional faults that cross-cut the earlier formed ductile fabrics. We interpret ca. 0.75-1.51 Ma (U-Th)/He age data to reflect cooling associated with the later stages of crustal shortening (marked by folds) or the later extensional unroofing of the peninsula. This work demonstrates that an orogen can record multiple tectonic mode switches within several million years. These outcomes should be considered in studies of ancient orogens where analytical uncertainties associated with isotopic dating may mask short-lived mode switches.Plain Language Summary How much time is required for a mountain belt to develop? Our knowledge of mountain building is somewhat limited because many of the best-studied mountain belts are quite old and our ability to date tectonic events is less precise the farther back we look through time. The work presented here investigates a mountainous peninsula that developed at the northern margin of the Australian Plate within the last six million years. This region records multiple episodes of deformation-we show that the relatively young rocks have been stretched, then pushed together and then stretched again (much like an accordion). These cycles must occur over a period of one to two million years, which is very fast compared to numerous studies of ancient mountain belts that consider the same processes occur over tens of millions of years.

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“…During the Permian-Triassic, the Bird's Head Peninsula was largely exposed above sea level, likely due to uplift associated with the development of a continental arc (Gold et al, 2017, Gunawan et al, 20122014; Webb and White 2016). One product of this arc is the Netoni Intrusive Complex, a granitoid complex entirely fault-bounded by the Sorong Fault System to the north of the Kemum Basement High (Fig.…”

Section: Geological Background and Previous Workmentioning

confidence: 99%

The Mesozoic and Palaeozoic granitoids of north-western New Guinea

Jost¹,

Webb²,

White³

2018

Preprint

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A large portion of the Bird's Head Peninsula of NW New Guinea is an inlier that reveals the pre-Cenozoic geological history of the northern margin of eastern Gondwana. The peninsula is dominated by a regional basement high exposing Gondwanan ('Australian') Palaeozoic metasediments intruded by Palaeozoic and Mesozoic granitoids. Here, we present the first comprehensive study of these granitoids, including field and petrographic descriptions, bulk rock geochemistry, and U-Pb zircon age data. We further revise and update previous subdivisions ofgranitoids in the area. Most granitoids were emplaced as small to medium scale intrusions during two episodes in the Devonian-Carboniferous and the Late Permian-Triassic, separated by a period of apparent magmatic quiescence. The oldest rocks went unrecognised until this study, likelydue to the younger intrusive events resetting the K¬-Ar isotopic system used in previous studies. Most of the Palaeozoic and Mesozoic granitoids are peraluminous and in large parts derived from partial melts of the country rock. This is corroborated by local migmatites and country rockxenoliths. Although rare, the metaluminous and mafic rocks show that partial melts of mantle-derived material played a minor role in granitoid petrogenesis, especially during the Permian-Triassic. The Devonian-Carboniferous granitoids and associated volcanics are locally restricted, whereas the Permian-Triassic intrusions are found across NW New Guinea and further afield. The latter were likely part of an extensive active continental margin above a subduction system spanning the length of what is now New Guinea and likely extending southward through easternAustralia and Antarctica.

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Age, Character and Provenance of The Tipuma Formation, West Papua: New Insights From Detrital Zircon Dating

Cited by 13 publications

References 19 publications

Successive Rifting Events in Marginal Basins: The Example of the Coral Sea Region (Papua New Guinea)

Successive Rifting Events in Marginal Basins: The Example of the Coral Sea Region (Papua New Guinea)

Tectonic Mode Switches Recorded at the Northern Edge of the Australian Plate During the Pliocene and Pleistocene

The Mesozoic and Palaeozoic granitoids of north-western New Guinea

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