Seismic Images of Modern Convergent Margin Tectonic Structure

Huene, Roland von; Vath, Susan; Sperber, Christine M.; Fulop, Bridgett; Bailey, Lee W.; Martin, M.

doi:10.1306/st26461

Cited by 8 publications

(4 citation statements)

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“…A number of exceptions occur to these two end members. For example, Japan has low elevation and other characteristics of W-directed subduction zones, such as the backarc basin and an accretionary prism mostly composed of shallow rocks (von Huene, 1986). However the slab has low dip of the subduction plane (Jarrard, 1986) and there is no active hangingwall extension, in spite of an onshore morphology suggesting widely distributed structural depressions.…”

Section: Subduction Zones Asymmetrymentioning

confidence: 99%

Subduction kinematics and dynamic constraints

Doglioni

Carminati

Cuffaro

et al. 2007

Earth-Science Reviews

292

177

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Section: Subduction Zones Asymmetrymentioning

confidence: 99%

Subduction kinematics and dynamic constraints

Doglioni

Carminati

Cuffaro

et al. 2007

Earth-Science Reviews

292

177

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“…The pro-side of the orogen is an arc-trench system, with a forebelt of variable width cored by basement rocks (von Huene 1986). The retro-side is a thick-skinned thrust belt also involving basement, but frequently propagating foreland-ward in thin-skinned mode (e.g., Rocky Mountains; Bally et al 1966).…”

Section: F) Eastward Subduction Of Oceanic Beneath Continental Lithosmentioning

confidence: 99%

Orogenic Belts and Orogenic Sediment Provenance

Garzanti

Doglioni²,

Vezzoli

et al. 2007

The Journal of Geology

224

111

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By selecting a limited number of variables (westward vs. eastward subduction polarity; oceanic vs. continental origin of downgoing and overriding plates), we identify eight end-member scenarios of plate convergence and orogeny. These are characterized by five different types of composite orogenic prisms uplifted above subduction zones to become sources of terrigenous sediments (Indo-Burman-type subduction complexes, Apennine-type thinskinned orogens, Oman-type obduction orogens, Andean-type cordilleras, and Alpine-type collision orogens). Each type of composite orogen is envisaged here as the tectonic assembly of sub-parallel geological domains consisting of genetically associated rock complexes. Five types of such elongated orogenic domains are identified as the primary building blocks of composite orogens: 1) magmatic arcs; 2) obducted or accreted ophiolites; 3) neometamorphic axial belts; 4) accreted paleomargin remnants; and 5) accreted orogenic clastic wedges. Detailed provenance studies on modern convergent-margin settings from the Mediterranean Sea to the Indian Ocean show that erosion of each single orogenic domain produces peculiar detrital modes, heavy-mineral assemblages and unroofing trends that can be tentatively predicted and modelled. Five corresponding primary types of sediment provenances ("Magmatic Arc", "Ophiolite", "Axial-Belt", "Continental-Block", and "Clastic-Wedge" provenances) are thus identified, which reproduce, redefine, or integrate provenance types and variants originally recognized by Dickinson and Suczek (1979). These five primary provenances may be variously recombined in order to describe the full complexities of mixed detrital signatures produced by erosion of different types of composite orogenic prisms. Our provenance model represents a flexible and valuable conceptual tool to predict the evolutionary trends of detrital modes and heavy-mineral assemblages produced by uplift and progressive erosional unroofing of various types of orogenic belts, and to interpret petrofacies from arc-related, foreland-basin, foredeep, and remnant-ocean clastic wedges.

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“…But, as Davis and Hyndman [1989] infer, some of the truly massive accretionary bodies may achieve their exceptional size because factors that favor efficient offscraping operate at these margins, for example, slow convergence speeds and thick ( Huene [1986] as well as numerous other authors. øthe solid-and fluid-fraction thicknesses for type 1 margins are based on the porosity-depth curve of Figure 6.…”

Section: Differing With the Implications Of The Data Onmentioning

confidence: 99%

Observations at convergent margins concerning sediment subduction, subduction erosion, and the growth of continental crust

Huene¹,

Scholl²

1991

Reviews of Geophysics

1,172

777

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At ocean margins where two plates converge, the oceanic plate sinks or is subducted beneath an upper one topped by a layer of terrestrial crust. This crust is constructed of continental or island arc material. The subduction process either builds juvenile masses of terrestrial crust through arc volcanism or new areas of crust through the piling up of accretionary masses (prisms) of sedimentary deposits and fragments of thicker crustal bodies scraped off the subducting lower plate. At convergent margins, terrestrial material can also bypass the accretionary prism as a result of sediment subduction, and terrestrial matter can be removed from the upper plate by processes of subduction erosion. Sediment subduction occurs where sediment remains attached to the subducting oceanic plate and underthrusts the seaward position of the upper plate's resistive buttress (backstop) of consolidated sediment and rock. Sediment subduction occurs at two types of convergent margins: type 1 margins where accretionary prisms form and type 2 margins where little net accretion takes place. At type 2 margins (∼19,000 km in global length), effectively all incoming sediment is subducted beneath the massif of basement or framework rocks forming the landward trench slope. At accreting or type 1 margins, sediment subduction begins at the seaward position of an active buttress of consolidated accretionary material that accumulated in front of a starting or core buttress of framework rocks. Where small‐to‐medium‐sized prisms have formed (∼16,300 km), approximately 20% of the incoming sediment is skimmed off a detachment surface or decollement and frontally accreted to the active buttress. The remaining 80% subducts beneath the buttress and may either underplate older parts of the frontal body or bypass the prism entirely and underthrust the leading edge of the margin's rock framework. At margins bordered by large prisms (∼8,200 km), roughly 70% of the incoming trench floor section is subducted beneath the frontal accretionary body and its active buttress. In rounded figures the contemporary rate of solid‐volume sediment subduction at convergent ocean margins (∼43,500 km) is calculated to be 1.5 km³/yr. Correcting type 1 margins for high rates of terrigenous seafloor sedimentation during the past 30 m.y. or so sets the long‐term rate of sediment subduction at 1.0 km³/yr. The bulk of the subducted material is derived directly or indirectly from continental denudation. Interstitial water currently expulsed from accreted and deeply subducted sediment and recycled to the ocean basins is estimated at 0.9 km³/yr. The thinning and truncation caused by subduction erosion of the margin's framework rock and overlying sedimentary deposits have been demonstrated at many convergent margins but only off northern Japan, central Peru, and northern Chile has sufficient information been collected to determine average or long‐term rates, which range from 25 to 50 km³/m.y. per kilometer of margin. A conservative long‐term rate applicable to many sectors of converge...

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Seismic Images of Modern Convergent Margin Tectonic Structure

Cited by 8 publications

References 0 publications

Subduction kinematics and dynamic constraints

Subduction kinematics and dynamic constraints

Orogenic Belts and Orogenic Sediment Provenance

Observations at convergent margins concerning sediment subduction, subduction erosion, and the growth of continental crust

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