Collisional delamination in New Guinea: The geotectonics of subducting slab breakoff

Cloos, Mark; Sapiie, Benyamin; Ufford, Andrew Quarles van; Weiland, Richard J.; Warren, Paul Q.; McMahon, Timothy P.

doi:10.1130/2005.2400

Cited by 105 publications

(124 citation statements)

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“…This is because the buoyancy forces resisting the subduction of continental lithosphere are as large as those pulling oceanic lithosphere downward (Cloos et al 2005). Eventually, the greater density of the oceanic lithosphere causes the lower plate to break, predominantly by viscous necking (Duretz et al 2012) at its weakest point, and sink into the mantle.…”

Section: Discussionmentioning

confidence: 99%

“…The resulting magmas, which form linear arrays above tears in the descending slab, are linear upwellings flowing through the breach in the slab, but are compositionally heterogeneous as they reflect differences within both the mantle and crust and well as variable amounts of melting and mixing. They commonly overlap the terminal stages of deformation and are highly metalliferous (Solomon 1990;Cloos et al 2005;Hildebrand 2009Hildebrand , 2013.…”

Section: Discussionmentioning

confidence: 99%

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Arc and Slab-Failure Magmatism in Cordilleran Batholiths I – The Cretaceous Coastal Batholith of Peru and its Role in South American Orogenesis and Hemispheric Subduction Flip

Hildebrand¹,

Whalen

2014

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We examined the temporal and spatial relations of rock units within the Western Cordillera of Peru where two Cretaceous basins, the Huarmey-Cañete and the West Peruvian Trough, were considered by previous workers to represent western and eastern parts respectively of the same marginal basin. The Huarmey-Cañete Trough, which sits on Mesoproterozoic basement of the Arequipa block, was filled with up to 9 km of Tithonian to Albian tholeiitic–calc-alkaline volcanic and volcaniclastic rocks. It shoaled to subaerial eastward. At 105–101 Ma the rocks were tightly folded and intruded during and just after the deformation by a suite of 103 ± 2 Ma mafic intrusions, and later in the interval 94–82 Ma by probable subduction-related plutons of the Coastal batholith. The West Peruvian Trough, which sits on Paleozoic metamorphic basement, comprised a west-facing siliciclastic-carbonate platform and adjacent basin filled with up to 5 km of sandstone, shale, marl and thinly bedded limestone deposited continuously throughout the Cretaceous. Rocks of the West Peruvian Trough were detached from their basement, folded and thrust eastward during the Late Cretaceous–Early Tertiary. Because the facies and facing directions of the two basins are incompatible, and their development and subjacent basements also distinct, the two basins could not have developed adjacent to one another. Based on thickness, composition and magmatic style, we interpret the magmatism of the Huarmey-Cañete Trough to represent a magmatic arc that shut down at about 105 Ma when the arc collided with an unknown terrane. We relate subsequent magmatism of the early 103 ± 2 Ma syntectonic mafic intrusions and dyke swarms to slab failure. The Huarmey-Cañete-Coastal batholithic block and its Mesoproterozoic basement remained offshore until 77 ± 5 Ma when it collided with, and was emplaced upon, the partially subducted western margin of South America to form the east-vergent Marañon fold–thrust belt. A major pulse of 73–62 Ma plutonism and dyke emplacement followed terminal collision and is interpreted to have been related to slab failure of the west-dipping South American lithosphere. Magmatism, 53 Ma and younger, followed terminal collision and was generated by eastward subduction of Pacific oceanic lithosphere beneath South America. Similar spatial and temporal relations exist over the length of both Americas and represent the terminal collision of an arc-bearing ribbon continent with the Americas during the Late Cretaceous–Early Tertiary Laramide event. It thus separated long-standing westward subduction from the younger period of eastward subduction characteristic of today. We speculate that the Cordilleran Ribbon Continent formed during the Mesozoic over a major zone of downwelling between Tuzo and Jason along the boundary of Panthalassic and Pacific oceanic plates.SOMMAIRENous avons étudié les relations spatiales et temporales des unités de roches dans la portion ouest de la Cordillère du Pérou, où deux bassins crétacés, la fosse d’accumulation de Huarmey-Cañete et la fosse d’accumulation péruvienne de l’ouest, ont été perçues par des auteurs précédents comme les portions ouest et est d’un même bassin de marge. La fosse de Huarmey-Cañete, qui repose sur le socle mésoprotérozoïque du bloc d’Arequipa, a été comblée par des couches de roches volcaniques tholéitiques – calco-alcalines de l’Albien au Thithonien atteignant 9 km d’épaisseur. Vers l’est, l’ensemble a fini par former des hauts fonds. Vers 105 à 101 Ma, les roches ont été plissées fortement puis recoupées par une suite d’intrusions vers 103 ± 2 Ma, durant et juste après la déformation, et plus tard dans l’intervalle 94 – 82 Ma, probablement par des plutons de subduction du batholite côtier. Quant à la fosse d’accumulation péruvienne de l’ouest, elle repose sur un socle métamorphique paléozoïque, et elle est constituée d’une plateforme silicoclastique – carbonate à pente ouest et d’un bassin contigu comblé par des grès, des schistes, des marnes et des calcaires finement laminés atteignant 5 km d’épaisseur et qui se sont déposés en continu durant tout le Crétacé. Les roches de la fosse d’accumulation péruvienne de l’ouest ont été décollées de leur socle, plissées et charriées vers l’est durant la fin du Crétacé et le début du Tertiaire. Parce que les facies et les profondeurs de sédimentation de ces deux fosses d’accumulation dont incompatibles, et que leur développement et leur socle sont différents, ces deux fosses ne peuvent pas s’être développées côte à côte. À cause de l’épaisseur accumulée, de sa composition et du style de son magmatisme, nous pensons que la fosse d’accumulation de Huarmey-Cañete représente un arc magmatique qui s’est éteinte vers 105 Ma, lorsque l’arc est entré en collision avec un terrane inconnu. Nous pensons que le magmatisme subséquent aux premières intrusions mafiques syntectoniques et aux réseaux de dykes de 103 ± 2 Ma sont à mettre au compte d’une rupture de plaque. Le bloc Huarmey-Cañete-batholitique côtier et son socle mésoprotérozoïque sont demeurés au large jusqu’à 77 ± 5 Ma, moment où il est entré en collision et a été poussé par-dessus la marge ouest sud-américaine partiellement subduite, pour ainsi former la zone de chevauchement de vergence est de Marañon. Nous croyons que la séquence majeure de plutonisme et d’intrusion de dykes qui a succédé à la collision finale à 73–62 Ma doit être reliée à une rupture de la plaque lithosphérique sud-américaine à pendage ouest. Le magmatisme de 53 Ma et plus récent qui a succédé à la collision finale, a été généré par la subduction vers l’est de la lithosphère océanique du Pacifique sous l’Amérique du Sud. Des relations temporelles et spatiales similaires qui existent tout le long des deux Amériques représentent la collision terminale d’un ruban continental d’arcs avec les Amériques durant la phase tectonique laramienne de la fin du Crétacé–début du Tertiaire. Elle a donc séparé la subduction vers l’ouest de longue date de la période de subduction vers l’est plus jeune caractérisant la situation actuelle. Nous considérons que le ruban continental de la Cordillère s’est constitué durant le Mésozoïque au-dessus d’une zone majeure de convection descendante entre Tuzo et Jason, le long de la limite entre les plaques océaniques Panthalassique et Pacifique.

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Section: Discussionmentioning

confidence: 99%

Section: Discussionmentioning

confidence: 99%

Arc and Slab-Failure Magmatism in Cordilleran Batholiths I – The Cretaceous Coastal Batholith of Peru and its Role in South American Orogenesis and Hemispheric Subduction Flip

Hildebrand¹,

Whalen

2014

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“…4), which were joined between 260-253 Ma (Beranek and Mortensen 2011). Slab failure magmatism commonly overlaps the terminal stages of deformation and is highly metalliferous (Solomon 1990;McDowell et al 1996;de Boorder et al 1998;Cloos et al 2005;Hildebrand 2009Hildebrand , 2013. Within Selwyn basin and Yukon-Tanana terrane the slab failure magmatism led to a swarm of small 99-92 Ma, post-kinematic, plutons with associated Au, Cu, Bi, W, Zn, Sn, Mo, and Sb mineralization -known variously as the Tombstone-Mayo-Tungsten-Livengood suites (Fig.…”

Section: Sevier Eventmentioning

confidence: 99%

Geology, Mantle Tomography, and Inclination Corrected Paleogeographic Trajectories Support Westward Subduction During Cretaceous Orogenesis in the North American Cordillera

Hildebrand

2014

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Geological evidence, including the presence of two passive margin platforms, juxtaposed and mismatched deformation between North America and more outboard terranes, as well as the lack of rift deposits, suggest that North America was the lower plate during both the Sevier and Laramide events and that subduction dipped westward beneath the Cordilleran Ribbon Continent (Rubia). Terranes within the composite ribbon continent, now present in the Canadian Cordillera, collided with western North America during the 125–105 Ma Sevier event and were transported northward during the ~80–58 Ma Laramide event, which affected the Cordillera from South America to Alaska. New high-resolution mantle tomography beneath North America reveals a huge slab wall that extends vertically for over 1000 km, marks the site of long-lived subduction, and provides independent verification of the westward-dipping subduction model. Other workers analyzed paleogeographic trajectories and concluded that the initial collision took place in Canada at about 160 Ma – a time and place for which there is no deformational thickening on the North American platform – and later farther west where subduction was not likely westward, but eastward. However, by utilizing a meridionally corrected North American paleogeographic trajectory, coupled with the geologically most reasonable location for the initial deformation, the position of western North America with respect to the relict superslab parsimoniously accounts for the timing and extents of both the Sevier and Laramide events. SOMMAIRELes indications géologiques, en particulier la présence de deux marges de plateforme passives, de déformations adjacentes non-conformes entre l’Amérique du Nord et les terranes extérieurs, ainsi que l’absence de gisements de rift, permet de croire que l’Amérique du Nord était la plaque sous-jacente durant les événements de Sevier et de Laramide et que la subduction plongeait vers l’ouest sous le continent rubané de la Cordillères (Rubia). Les terranes du continent rubané composite, maintenant au sein de la Cordillère canadienne, sont entrés en collision avec l’ouest de l’Amérique du Nord durant l’événement Sevier (125-105 Ma), et ont été transportés vers le nord durant l’événement Laramide (~80–58 Ma), laquelle a affecté la Cordillère, de l’Amérique du Sud à l’Alaska. Une nouvelle tomographie haute résolution du manteau sous l’Amérique du Nord montre la présence d’un gigantesque mur de plaques vertical qui s’étend sur 1 000 km, marque le site d’une subduction de longue haleine, et offre une validation indépendante du modèle d’une subduction à pendage vers l’ouest. D’autres chercheurs ont analysé les trajectoires paléogéographiques et conclu que la collision initiale s’est produite au Canada vers 160 Ma – un moment et un endroit sans épaississement par déformation sur la plateforme d’Amérique du Nord – et plus tard plus à l’ouest, là où la subduction n’était vraisemblablement pas vers l’ouest, mais vers l’est. Cela dit, en considérant une trajectoire paléogéographique de l’Amérique du Nord corrigée longitudinalement, avec la position géologique la plus probable de la déformation initiale, la position de la portion ouest de l’Amérique du Nord par rapport aux restes de la super-plaque explique alors facilement la chronologie et l’étendue des épisodes Sevier et Laramide.

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“…Most of the deformation in the Central Range is a result of an oblique convergent motion that led to an arc-continent collision between the Australian and Pacific Plates (Sapiie, 1998;Cloos et al, 2005). The results of detailed structural mapping at the GBMD along a 15-km traverse of the Heavy Equipment Access Trail (HEAT) and the Grasberg mine access road have provided new information concerning the Late Cenozoic structural evolution of the Central Range of Papua (Sapiie, 1998;Sapiie and Cloos, 2004;and Cloos et al, 2005). The main purpose of this paper is to present the results of a detailed kinematic analysis using fault-slip data (fault plane and striation/slickensides) in the ramification deformation and tectonic evolution of the study area.…”

Section: Introductionmentioning

confidence: 99%

“…The Central Range is an orogenic belt that stretches 1300 km from West Papua to the Papuan Peninsula. The Ruffaer Metamorphic Belt (RMB) is a 1000 km long and 50 km wide zone of highlydeformed, generally low-temperature (<300°) metamorphic rocks which are bounded on the north by the Papua Ophiolite belt (IOB) and on the south by deformed, but unmetamorphosed, passive margin strata (Dow et al, 1988;Cloos et al, 2005). The most northern orogenic belt in Papua is a poorly exposed, complex zone involving oceanic rocks from a collided Melanesian island arc built into the Pacific Plate.…”

Section: Introductionmentioning

confidence: 99%

Kinematic Analysis of Fault-Slip Data in the Central Range of Papua, Indonesia

Sapiie¹

2016

Indonesian J. Geosci.

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-Most of the Cenozoic tectonic evolution in New Guinea is a result of obliquely convergent motion that led to an arc-continent collision between the Australian and Pacific Plates. The Gunung Bijih (Ertsberg) Mining District (GBMD) is located in the Central Range of Papua, in the western half of the island of New Guinea. This study presents the results of detailed structural mapping concentrated on analyzing fault-slip data along a 15-km traverse of the Heavy Equipment Access Trail (HEAT) and the Grasberg mine access road, providing new information concerning the deformation in the GBMD and the Cenozoic structural evolution of the Central Range. Structural analysis indicates that two distinct stages of deformation have occurred since ~12 Ma. The first stage generated a series of en-echelon NW-trending (π-fold axis = 300°) folds and a few reverse faults. The second stage resulted in a significant left-lateral strike-slip faulting sub-parallel to the regional strike of upturned bedding. Kinematic analysis reveals that the areas between the major strike-slip faults form structural domains that are remarkably uniform in character. The change in deformation styles from contractional to a strike-slip offset is explained as a result from a change in the relative plate motion between the Pacific and Australian Plates at ~4 Ma. From ~4 -2 Ma, transform motion along an ~ 270° trend caused a left-lateral strike-slip offset, and reactivated portions of pre-existing reverse faults. This action had a profound effect on magma emplacement and hydrothermal activity.

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Collisional delamination in New Guinea: The geotectonics of subducting slab breakoff

Cited by 105 publications

References 110 publications

Arc and Slab-Failure Magmatism in Cordilleran Batholiths I – The Cretaceous Coastal Batholith of Peru and its Role in South American Orogenesis and Hemispheric Subduction Flip

Arc and Slab-Failure Magmatism in Cordilleran Batholiths I – The Cretaceous Coastal Batholith of Peru and its Role in South American Orogenesis and Hemispheric Subduction Flip

Geology, Mantle Tomography, and Inclination Corrected Paleogeographic Trajectories Support Westward Subduction During Cretaceous Orogenesis in the North American Cordillera

Kinematic Analysis of Fault-Slip Data in the Central Range of Papua, Indonesia

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