Thinning of continental backarc lithosphere by flow-induced gravitational instability

Currie, Claire A.; Huismans, Ritske S.; Beaumont, Christopher

doi:10.1016/j.epsl.2008.02.037

Cited by 81 publications

(92 citation statements)

References 50 publications

Supporting

Mentioning

Contrasting

Order By: Relevance

“…Finally, we can increase the interplate friction and thus the shear traction acting on the interplate zone. In Experiment 2 the depth-averaged shear traction was 13 Pa (equivalent to ∼ 130 MPa in nature), which is very high and would therefore likely produce deformation of the thinner, hotter and hence weaker arc/back-arc (Currie and Hyndman, 2006;Currie et al, 2008). However, shear traction would have to be imposed on the upper shallow part of the plate boundary where the contact between the plates is seismogenic and thus frictional.…”

Section: Imposing a Subduction Regime In Non-cylindrical Thermo-mechamentioning

confidence: 98%

3-D thermo-mechanical laboratory modeling of plate-tectonics: modeling scheme, technique and first experiments

Boutelier

Oncken

2011

Solid Earth

View full text Add to dashboard Cite

Abstract. We present an experimental apparatus for 3-D thermo-mechanical analogue modeling of plate tectonic processes such as oceanic and continental subductions, arccontinent or continental collisions. The model lithosphere, made of temperature-sensitive elasto-plastic analogue materials with strain softening, is submitted to a constant temperature gradient causing a strength reduction with depth in each layer. The surface temperature is imposed using infrared emitters, which allows maintaining an unobstructed view of the model surface and the use of a high resolution optical strain monitoring technique (Particle Imaging Velocimetry). Subduction experiments illustrate how the stress conditions on the interplate zone can be estimated using a force sensor attached to the back of the upper plate and adjusted via the density and strength of the subducting lithosphere or the lubrication of the plate boundary. The first experimental results reveal the potential of the experimental set-up to investigate the three-dimensional solid-mechanics interactions of lithospheric plates in multiple natural situations.

show abstract

Section: Imposing a Subduction Regime In Non-cylindrical Thermo-mechamentioning

confidence: 98%

3-D thermo-mechanical laboratory modeling of plate-tectonics: modeling scheme, technique and first experiments

Boutelier

Oncken

2011

Solid Earth

View full text Add to dashboard Cite

show abstract

“…These areas have high heat flow for continental crust with average radiogenic heat production of 69-85 ± 16 mWm -2 (Hyndman et al 2005;Currie and Hyndman 2006;Currie et al 2008). Geophysical data summarised by Currie and Hyndman (2006) indicate Moho temperatures of 800-900°C in backarcs, uniformly high temperatures in the shallow mantle (~ 1200°C) and a thin lithosphere (~ 60 km thick over backarc widths of 250 to >900 km) in comparison with Moho temperatures of 400-500°C and lithosphere 200-300 km thick for cratons.…”

Section: Sources Of Heat For High-grade Crustal Metamorphism and Meltingmentioning

confidence: 98%

“…The reason subduction zone backarcs are hot may be principally due to thin lithosphere and shallow convection in the asthenosphere of the mantle wedge. Convection is inferred to result principally from a reduction in viscosity induced by water from the underlying subducting plate Hyndman 2006, 2007;Currie et al 2008;Schellart 2007). The high temperatures associated with circum-Pacific orogenic systems decay over a timescale of about 300 Ma following termination of subduction by collision (Currie and Hyndman 2006).…”

Section: Sources Of Heat For High-grade Crustal Metamorphism and Meltingmentioning

confidence: 99%

Some Remarks on Melting and Extreme Metamorphism of Crustal Rocks

Brown

Kothonen

2009

Physics and Chemistry of the Earth’s Interior

View full text Add to dashboard Cite

Abstract:Typically melting occurs during decompression in ultra-high-pressure terranes, along the evolution from peak pressure to peak temperature in medium-temperature eclogitehigh-pressure granulite terranes and by simple prograde heating in granulite facies and ultrahigh-temperature (UHT) metamorphic terranes. The source of heat must be due to one or more processes among thickening and radiogenic heating, viscous dissipation, and heat from asthenospheric mantle. Melt-bearing rocks become porous at a few vol% melt initiating an advective flow regime. As the melt volume approaches and exceeds the melt connectivity transition (~ 7 vol% melt), melt may be lost from the system in the first of several melt-loss events. In migmatites and residual granulites, a variety of microstructures indicates the former presence of melt at the grain scale and leucosome networks at outcrop scale record melt extraction pathways. This evidence supports a model of focused melt flow by dilatant shear failure at low melt volume as the crust weakens with increasing melt production. Melt ascent is initiated as ductile fractures but continues in dykes that propagate as brittle fractures. Crustal rocks undergo melting via a sequence of reactions beginning with minimal melt production at the wet solidus (generally < 1 vol% melt, unless there is influx of H 2 O-rich fluid). The major phase of melt production is related to hydrate-breakdown melting (perhaps > 50 vol% melt, depending on the fertility of the protolith composition and the intensive variables). At temperatures above the stability of the hydrate, assuming significant melt loss by this point, low-volume melt production continues by consumption of feldspar(s) and quartz at UHT conditions (generally < 10 vol% melt at peak UHTM conditions). Significant melt loss is a contributory factor to achieving UHTs because dehydration of the system limits the progress of heat-consuming melting reactions among the residual phases in the source.

show abstract

“…The high heat flow exists because the entire lithosphere is only 50-60 km thick (see also Currie & Hyndman 2006;Currie et al 2008). This hot, thin zone of lithospheric weakness becomes the focus of shortening during periods of increased compressive stress, and the heat is a natural consequence of shallow convection in the hydrous mantle wedge above the subducting plate (Hyndman et al 2005).…”

mentioning

confidence: 99%

Accretionary orogens through Earth history

et al. 2009

View full text Add to dashboard Cite

Accretionary orogens form at intraoceanic and continental margin convergent plate boundaries. They include the supra-subduction zone forearc, magmatic arc and back-arc components. Accretionary orogens can be grouped into retreating and advancing types, based on their kinematic framework and resulting geological character. Retreating orogens (e.g. modern western Pacific) are undergoing long-term extension in response to the site of subduction of the lower plate retreating with respect to the overriding plate and are characterized by back-arc basins. Advancing orogens (e.g. Andes) develop in an environment in which the overriding plate is advancing towards the downgoing plate, resulting in the development of foreland fold and thrust belts and crustal thickening. Cratonization of accretionary orogens occurs during continuing plate convergence and requires transient coupling across the plate boundary with strain concentrated in zones of mechanical and thermal weakening such as the magmatic arc and back-arc region. Potential driving mechanisms for coupling include accretion of buoyant lithosphere (terrane accretion), flat-slab subduction, and rapid absolute upper plate motion overriding the downgoing plate. Accretionary orogens have been active throughout Earth history, extending back until at least 3.2 Ga, and potentially earlier, and provide an important constraint on the initiation of horizontal motion of lithospheric plates on Earth. They have been responsible for major growth of the continental lithosphere through the addition of juvenile magmatic products but are also major sites of consumption and reworking of continental crust through time, through sediment subduction and subduction erosion. It is probable that the rates of crustal growth and destruction are roughly equal, implying that net growth since the Archaean is effectively zero.Classic models of orogens involve a Wilson cycle of ocean opening and closing with orogenesis related to continent-continent collision. These imply that mountain building occurs at the end of a cycle of ocean opening and closing, and marks the termination of subduction, and that the mountain belt should occupy an internal location within an assembled continent (supercontinent). The modern Alpine -Himalayan chain exemplifies the features of this model, lying between the Eurasian and colliding African and Indian plates (Fig.

show abstract

Thinning of continental backarc lithosphere by flow-induced gravitational instability

Cited by 81 publications

References 50 publications

3-D thermo-mechanical laboratory modeling of plate-tectonics: modeling scheme, technique and first experiments

3-D thermo-mechanical laboratory modeling of plate-tectonics: modeling scheme, technique and first experiments

Some Remarks on Melting and Extreme Metamorphism of Crustal Rocks

Accretionary orogens through Earth history

Contact Info

Product

Resources

About