106:, are not widely accepted. Mineral assemblages, rather than single minerals, can also be used to identify UHP rocks; these assemblages include magnesite + aragonite. Because minerals change composition in response to changes in pressure and temperature, mineral compositions can be used to calculate pressure and temperature; for UHP eclogite the best geobarometers involve garnet + clinopyroxene + K-white mica and garnet + clinopyroxene + kyanite + coesite/quartz. Most UHP rocks were metamorphosed at peak conditions of 800 °C and 3
268:, Italy, in the Dabie orogen, and in the Himalaya. In addition it was demonstrated with analogue experiments. This mechanism is different from flow in a subduction channel in that the exhuming sheet is strong and remains undeformed. A variant of this mechanism, in which the exhuming material undergoes folding, but not wholescale disruption, was suggested for the Dabie orogen, where exhumation-related stretching lineations and gradients in metamorphic pressure indicate rotation of the exhuming block;
272:
slab to roll quickly back, making room for the UHP continental crust to exhume and driving back-arc extension. This model was developed to explain repeated cycles of subduction and exhumation documented in the Aegean and
Calabria–Apennine orogens. UHP exhumation by slab rollback has not yet been extensively explored numerically, but it has been reproduced in numerical experiments of Apennine-style collisions.
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305:
to form UHP terranes. Diapiric rise of a much larger subducted continental body has been invoked to explain the exhumation of the Papua New Guinea UHP terrain. This mechanism was alo used to explain the exhumation of UHP rocks in
Greenland. However, the mantle wedge above continental subduction zones
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If a plate undergoing subduction inversion begins to rotate in response to changing boundary conditions or body forces, the rotation may exhume UHP rocks toward crustal levels. This could occur if, for example, the plate is small enough that continental subduction markedly changes the orientation and
117:
Most felsic UHP rocks have undergone extensive retrograde metamorphism and preserve little or no UHP record. Commonly, only a few eclogite enclaves or UHP minerals reveal that the entire terrain was subducted to mantle depths. Many granulite terrains and even batholithic rocks may have undergone UHP
578:
Scholl, D. W., and von Huene, R., 2007, Crustal recycling at modern subduction zones applied to the past—Issues of growth and preservation of continental basement, mantle geochemistry, and supercontinent reconstruction, in Robert D. Hatcher, J., Carlson, M. P., McBride, J. H., and Catalán:, J. R.
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If continental material is subducted within a confined channel, the material tends to undergo circulation driven by tractions along the base of the channel and the relative buoyancy of rocks inside the channel; the flow can be complex, generating nappe-like or chaotically mixed bodies. The material
174:
UHP ultramafic xenoliths of mantle affinity provide information (e.g., mineralogy or deformation mechanisms) about processes active deep in Earth. UHP xenoliths of crustal affinity provide information about processes active deep in Earth, but also information about what kinds of crustal rocks reach
779:
Hacker, B. R., Ratschbacher, L., Webb, L. E., McWilliams, M., Ireland, T. R., Calvert, A., Dong, S., Wenk, H.-R., and
Chateigner, D., 2000, Exhumation of ultrahigh-pressure continental crust in east–central China: Late Triassic–Early Jurassic tectonic unroofing: Journal of Geophysical Research, v.
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If a subducting plate consists of a weak buoyant layer atop a stronger negatively buoyant layer, the former will detach at the depth where the buoyancy force exceeds slab pull, and extrude upward as a semi-coherent sheet. This type of delamination and stacking was proposed to explain exhumation of
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has provided considerable data on how the rocks deformed, the pressures and temperatures of metamorphism, and how the deformation and metamorphism varied as a function of space and time. It has been postulated that small UHP terrains that underwent short periods of metamorphism formed early during
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The buoyancy of a microcontinent locally slows the rollback of and steepens the dip of subducting mafic lithosphere. If the mafic lithosphere on either side of the microcontinent continues to roll back, a buoyant portion of the microcontinent may detach, allowing the retarded portion of the mafic
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UHP terrains vary greatly in size, from the >30,000 km2 giant UHP terrains in Norway and China, to small kilometer-scale bodies. The giant UHP terrains have a metamorphic history spanning tens of millions of years, whereas the small UHP terrains have a metamorphic history spanning millions of
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Eclogite-facies HP to UHP metamorphic rocks are produced by subduction of crustal rocks to the lower crust to mantle depths for extreme metamorphism at the low thermal gradients of less than 10°C/km. All of these rocks occur at convergent plate margins, and UHP rocks only occur in collisional
61:
or continental margins and the exhumation of all UHP terrains has been ascribed principally to buoyancy caused by the low density of continental crust—even at UHP—relative to Earth's mantle. While the subduction proceeds at low thermal gradients of less than 10°C/km, the exhumation proceeds at
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Hacker, B.R., 2007. Ascent of the ultrahigh-pressure
Western Gneiss Region, Norway. In Cloos, M., Carlson, W.D., Gilbert, M.C., Liou, J.G., and Sorenson, S.S., eds., Convergent Margin Terranes and Associated Regions: A Tribute to W.G. Ernst: Geological Society of America Special Paper 419, p.
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Yamato, P., Burov, E., Agard, P., Pourhiet, L. L., and
Jolivet, L., 2008, HP-UHP exhumation during slow continental subduction: Self-consistent thermodynamically and thermomechanically coupled model with application to the Western Alps: Earth and Planetary Science Letters, v. 271, p.
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Yin, A., Manning, C. E., Lovera, O., Menold, C. A., Chen, X., and
Gehrels, G. E., 2007, Early Paleozoic tectonic and thermomechanical evolution of ultrahigh-pressure (UHP) metamorphic rocks in the northern Tibetan Plateau, northwest China: International Geology Review, v. 49, p.
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Hacker, B. R., Luffi, P., Lutkov, V., Minaev, V., Ratschbacher, L., Plank, T., Ducea, M., Patiño-Douce, A., McWilliams, M., and
Metcalf, J., 2005, Near-ultrahigh pressure processing of continental crust: Miocene crustal xenoliths from the Pamir: Journal of Petrology, v. 46, p.
204:. Continental margin subduction is well documented in a number of collisional orogens, such as the Dabie orogen where South China Block passive-margin sedimentary and volcanic sequences are preserved, in the Arabian continental margin beneath the Samail ophiolite (in the
951:
Little, T. A., Hacker, B. R., Gordon, S. M., Baldwin, S. L., Fitzgerald, P. G., Ellis, S., and
Korchinski, M., 2011, Diapiric Exhumation of Earth's youngest (UHP) eclogites in the gneiss domes of the D'Entrecasteaux Islands, Papua New Guinea: Tectonophysics, v. 510, p.
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Li, Z., and Gerya, T. V., 2009, Polyphase formation and exhumation of high- to ultrahigh-pressure rocks in continental subduction zone; numerical modeling and application to the Sulu ultrahigh-pressure terrane in eastern China: Journal of
Geophysical Research, v.
528:
Hollocher, K., Robinson, P., Walsh, E., and Terry, M., 2007, The
Neoproterozoic Ottfjället dike swarm of the Middle Allochthon, traced geochemically into the Scandian hinterland, Western Gneiss region, Norway: American Journal of Science, v. 307, p.
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Warren, C. J., Beaumont, C., and Jamieson, R. A., 2008, Modelling tectonic styles and ultrahigh pressure (UHP) rock exhumation during the transition from oceanic subduction to continental collision: Earth and Planetary Science Letters, v. 267, p.
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Massonne, H.-J., 2003, A comparison of the evolution of diamondiferous quartz-rich rocks from the Saxonian Erzgebirge and the Kokchetav Massif: are so-called diamondiferous gneisses magmatic rocks?: Earth and Planetary Science Letters, v. 216, p.
50:, the composition and evolution of Earth's crust. The discovery of UHP metamorphic rocks in 1984 revolutionized our understanding of plate tectonics. Prior to 1984 there was little suspicion that continental rocks could reach such high pressures.
642:
Guo, Xiaoyu; Encarnacion, John; Xu, Xiao; Deino, Alan; Li, Zhiwu; Tian, Xiaobo (2012-10-01). "Collision and rotation of the South China block and their role in the formation and exhumation of ultrahigh pressure rocks in the Dabie Shan orogen".
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Klemd, R., Lifei, Z., Ellis, D., Williams, S., and Wenbo, J., 2003, Ultrahigh-pressure metamorphism in eclogites from the western Tianshan high-pressure belt (Xinjiang, western China); discussion and reply: American Mineralogist, v. 88, p.
294:(if the overlying plate is continental) is likely unless other forces are available to force the UHP rocks upward. Some UHP terrains might be coalesced material derived from subduction erosion. This model was suggested to explain the North
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belts; most occur in Eurasia. Coesite is relatively widespread, diamond less so, and majoritic garnet is known from only rare localities. The oldest UHP terrain is 620 Ma and is exposed in Mali; the youngest is 8 Ma and exposed in the
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Chemenda, A. I., Mattauer, M., Malavieille, J., and Bokun, A. N., 1995, A mechanism for syn-collisional rock exhumation and associated normal faulting: Results from physical modelling: Earth and Planetary Science Letters, v. 132, p.
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Burov, E., Jolivet, L., Le Pourhiet, L., and Poliakov, A., 2001, A thermomechanical model of exhumation of high pressure (HP) and ultrahigh pressure (UHP) metamorphic rocks in Alpine-type collision belts: Tectonophysics, v. 342, p.
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magnitude of slab pull or if the plate is being consumed by more than one subduction zone pulling in different directions. Such a model has also been proposed for the UHP terrain in eastern Papua New Guinea, where rotation of the
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Chopin, C., 1987, Very-high-pressure metamorphism in the western Alps: implications for subduction of continental crust: Philosophical Transactions of the Royal Society A-Mathematical Physical And Engineering Sciences, v. 321, p.
497:
Ernst, W. G., Hacker, B. R., and Liou, J. G., 2007, Petrotectonics of ultrahigh-pressure crustal and upper-mantle rocks: Implications for Phanerozoic collisional orogens: Geological Society of America Special Paper, v. 433, p.
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Searle, M. P., Waters, D. J., Martin, H. N., and Rex, D. C., 1994, Structure and metamorphism of blueschist-eclogite facies rocks from the northeastern Oman Mountains: Journal of the Geological Society of London, v. 151, p.
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Walsh, E. O., and Hacker, B. R., 2004, The fate of subducted continental margins: Two-stage exhumation of the high-pressure to ultrahigh-pressure Western Gneiss complex, Norway: Journal of Metamorphic Geology, v. 22, p.
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Gilotti, J. A., and McClelland, W. C., 2007, Characteristics of, and a Tectonic Model for, Ultrahigh-Pressure Metamorphism in the Overriding Plate of the Caledonian Orogen: International Geology Review, v. 49, p.
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Beaumont, C., Jamieson, R. A., Butler, J. P., and Warren, C. J., 2009, Crustal structure: A key constraint on the mechanism of ultrahigh-pressure rock exhumation: Earth and Planetary Science Letters, v. 287, p.
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Gerya, T. V., Perchuk, L. L., and Burg, J.-P., 2007, Transient hot channels: perpetrating and regurgitating ultrahigh-pressure, high temperature crust-mantle associations in collision belts: Lithos, v. 103, p.
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initiates. The positive buoyancy of the continental slab—in opposition principally to ridge push—can then drive exhumation of the subducting crust at a rate and mode determined by plate geometry and the
989:
Liou, J.G., and Ernst, W.G. (Editors), 2000. UltraHigh Pressure Metamorphism and Geodynamics in Collision-Type Orogenic Belts. Geological Society of America, International Book Series, volume 4, 293 pp.
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Gerya, T. V., and Stöckhert, B., 2006, Two-dimensional numerical modeling of tectonic and metamorphic histories at active continental margins: International Journal of Earth Sciences, v. 95, p. 250-274.
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Kylander-Clark, A., Hacker, B., and Mattinson, C., 2012, Size and exhumation rate of ultrahigh-pressure terrains linked to orogenic stage: Earth and Planetary Science Letters, v. 321-322, p. 115-120.
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Gerya, T. V., and Meilick, F. I., 2011, Geodynamic regimes of subduction under an active margin: effects of rheological weakening by fluids and melts: Journal of Metamorphic Geology, v. 29, p. 7-31.
458:, Tsujimori, T., Zhang, R. Y., Katayama, I., and Maruyama, S., 2004, Global UHP metamorphism and continental subduction/collision: The Himalayan model: International Geology Review, v. 46, p. 1-27.
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Brueckner, H. K., and van Roermund, H. L. M., 2004, Dunk tectonics: a multiple subduction/eduction model for the evolution of the Scandinavian Caledonides: Tectonics, v. doi: 10.1029/2003TC001502.
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Manning, C. E., and Bohlen, S. R., 1991, The reaction titanite + kyanite = anorthite + rutile and titanite-rutile barometry in eclogites: Contributions to Mineralogy and Petrology, v. 109, p. 1-9.
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Burtman, V. S., and Molnar, P., 1993, Geological and geophysical evidence for deep subduction of continental crust beneath the Pamir: Geological Society of America Special Paper, v. 281, p. 1-76.
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Hacker, B. R., 2006, Pressures and temperatures of ultrahigh-pressure metamorphism: Implications for UHP tectonics and H2O in subducting slabs.: International Geology Review, v. 48, p. 1053-1066.
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Schmid, R., Romer, R. L., Franz, L., Oberhänsli, R., and Martinotti, G., 2003, Basement-Cover Sequences within the UHP unit of the Dabie Shan: Journal of Metamorphic Geology, v. 21, p. 531-538.
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van Hunen, J., and Allen, M. B., 2011, Continental collision and slab break-off: A comparison of 3-D numerical models with observations: Earth and Planetary Science Letters, v. 302, p. 27-37.
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is cold like cratons, which do not allow for diapirically ascending of the crustal materials. Foundering of the gravitationally unstable portions of continental lithosphere locally carries
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Chopin, C., 1984, Coesite and pure pyrope in high-grade blueschists of the western Alps: a first record and some consequences: Contributions to Mineralogy and Petrology, v. 86, p. 107–118.
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Stöckhert, B., and Gerya, T. V., 2005, Pre-collisional high pressure metamorphism and nappe tectonics at active continental margins: a numerical simulation: Terra Nova, v. 17, p. 102-110.
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Masago, H., 2000, Metamorphic petrology of the Barchi-Kol metabasites, western Kokchetav ultrahigh-pressure–high-pressure massif, northern Kazakhstan: The Island Arc, v. 9, p. 358–378.
992:
Hacker, B.R., McClelland, W.C., and Liou, J.G. (Editors), 2006. Ultrahigh-Pressure Metamorphism: Deep Continental Subduction. Geological Society of America Special Paper 403, 206 pp.
807:
Zheng, Y.F., Zhao, Z.F., Chen, Y.X., 2013. Continental subduction channel processes: Plate interface interaction during continental collision. Chinese Science Bulletin 58, 4371-4377.
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Zheng, Y.-F., Chen, R.-X., 2017. Regional metamorphism at extreme conditions: Implications for orogeny at convergent plate margins. Journal of Asian Earth Sciences, v. 145, p. 46-73.
470:, Caby, R., and Monie, P., 2001, The oldest UHP eclogites of the World: age of UHP metamorphism, nature of protoliths and tectonic implications: Chemical Geology, v. 178, p. 143-158.
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Oberhänsli, R., Martinotti, G., Schmid, R., and Liu, X., 2002, Preservation of primary volcanic textures in the ultrahigh-pressure terrain of Dabie Shan: Geology, v. 30, p. 609–702.
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Massonne, H. J., and Nasdala, L., 2000, Microdiamonds from the Saxonian Erzgebirge, Germany: in situ micro-Raman characterisation: European Journal of Mineralogy, v. 12, p. 495-498.
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Faccenda, M., Gerya, T. V., and Burlini, L., 2009, Deep slab hydration induced by bending-related variations in tectonic pressure: Nature Geoscience, v. DOI: 10.1038/NGEO656.
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UHP rocks record pressures greater than those that prevail within Earth's crust. Earth's crust is a maximum of 70–80 km thickness, and pressures at the base are <2.7
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Andersen, T. B., Jamtveit, B., Dewey, J. F., and Swensson, E., 1991, Subduction and eduction of continental crust: major mechanism during continent-continent collision and
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orogens. There is general agreement that most well-exposed and well-studied UHP terrains were produced by the burial of crustal rocks to mantle depths of >80 km during
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is subducted because of its attachment to downgoing oceanic lithosphere, the downward slab pull force may exceed the strength of the slab at some time and location, and
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Hacker, B. R., Kelemen, P. B., and Behn, M. D., 2011, Differentiation of the continental crust by relamination: Earth and Planetary Science Letters, v. 307, p. 501-516.
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Okay, A. I., and Sengör, A. M. C., 1992, Evidence for intracontinental thrust-related exhumation of the ultrahigh-pressure rocks in China: Geology, v. 20, p. 411–414.
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Currie, C. A., Beaumont, C., and Huismans, R. S., 2007, The fate of subducted sediments: A case for backarc intrusion and underplating: Geology, v. 35, p. 1111-1114.
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Hacker, B.R., and Liou, J.G. (Editors), 1998. When Continents Collide: Geodynamics and Geochemistry of Ultrahigh-Pressure Rocks. Kluwer Academic Publishers, 323 pp.
82:, recognized by either the presence of a diagnostic mineral (e.g., coesite or diamond), mineral assemblage (e.g., magnesite + aragonite), or mineral compositions.
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Wilke, F. D. H. et al., 2010, Multi-stage reaction history in different eclogite types from the Pakistan Himalaya and implications for exhumation processes.
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Buoyancy alone is unlikely to drive exhumation of UHP rocks to Earth's surface, except in oceanic subduction zones. Arrest and spreading of UHP rocks at the
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Ravna, E. J. K., and Terry, M. P., 2004, Geothermobarometry of phengite-kyanite-quartz/coesite eclogites: Journal of Metamorphic Geology, v. 22, p. 579-592.
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buoyancy in the channel exceeds subduction-related traction and the channel is pushed upward by the asthenospheric mantle intruding between the plates; or
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Regional metamorphic UHP terrains exposed on Earth's surface provide considerable information that is not available from xenoliths. Integrated study by
933:, Hacker, B. R., and Massonne, H. J., 2011, Diapirs as the source of the sediment signature in arc lavas: Nature Geoscience, v. DOI: 10.1038/NGEO1214.
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Brun, J.-P., and Faccenna, C., 2008, Exhumation of high-pressure rocks driven by slab rollback: Earth and Planetary Science Letters, v. 272, p. 1-7.
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Plank, T., and Langmuir, C. H., 1993, Tracing trace elements from sediment input to volcanic output at subduction zones: Nature, v. 362, p. 739-742.
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Baldwin, S. L., Webb, L. E., and Monteleone, B. D., 2008, Late Miocene coesite-eclogite exhumed in the Woodlark Rift: Geology, v. 36, p. 735-738.
220:. Subduction erosion also occurs beneath volcanoplutonic arcs around the world, carrying continental rocks to mantle depths at least locally.
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UHP terrain in western China. Even subducted sediment may rise as diapirs from the subducting plate and accumulate to form UHP terrains.
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continuous introduction of new material into the channel driven by traction of the subducting plate pushes old channel material upward;
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continent subduction, whereas giant UHP terrains that underwent long periods of metamorphism formed late during continent collision.
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The specific processes by which UHP terrains were exhumed to Earth's surface appear to have been different in different locations.
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Smith, D. C., 1984, Coesite in clinopyroxene in the Caledonides and its implications for geodynamics: Nature, v. 310, p. 641–644.
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Studies of numerical geodynamics suggest that both subducted sediment and crystalline rocks may rise through the mantle wedge
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46:. It is important because the processes that form and exhume ultra-high-pressure (UHP) metamorphic rocks may strongly affect
151:). Some include sedimentary or rift-volcanic sequences that have been interpreted as passive margins prior to metamorphism.
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around the world and is recognized in the compositions of arc lavas. Continental subduction may be underway beneath the
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Hamilton, W., 1979, Tectonics of the Indonesian Region: U.S. Geological Survey Professional Paper, v. 1078, p. 1-345.
136:
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Coleman, R.G., and Wang, X. (Editors), 1995. Ultrahigh Pressure Metamorphism. Cambridge University Press, 528 pp.
167:. UHP rocks of a wide variety of compositions have been identified as both regional metamorphic terrains and
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Geologists have identified UHP terrains at more than twenty localities around the globe in most well-studied
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is the archetype for this exhumation mode, which has been termed 'eduction' or subduction inversion.
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of Papua New Guinea. A modest number of continental orogens have undergone multiple UHP episodes.
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M., eds., Geological Society of America, Memoir Boulder, Geological Society of America, p. 9-32.
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are diagnostic; other potential mineralogical indicators of UHP metamorphism, such as alpha-PbO
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for typical crustal densities. UHP rocks therefore come from depths within Earth's
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with a few percent mafic rock (eclogite) or ultramafic rock (garnet-bearing
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a strong indenter squeezes the channel and extrudes the material within.
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208:, Oman), and in the Australian margin presently subducting beneath the
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Webb, L. E.; Baldwin, S. L.; Little, T. A.; Fitzgerald, P. G. (2008).
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Petrological indicators of UHP metamorphism are usually preserved in
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Metamorphism of rocks at pressures ≥27kbar (2.7GPa) to stabilize
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The formation of many UHP terrains has been attributed to the
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High pressure terranes along the Bangong-Nujiang Suture Zone
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rocks into the mantle and may be ongoing beneath the Pamir.
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reached 1000–1200 °C at pressures of at least 4 GPa.
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great depth in Earth and how profound those depths are.
696:"Can microplate rotation drive subduction inversion?"
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94:. The presence of metamorphic coesite, diamond, or
34:processes at pressures high enough to stabilize
143:years. All are dominated by quartzofeldspathic
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1047:Ultra-high-temperature metamorphism
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1108:Dynamic quartz recrystallization
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665:10.1111/j.1365-3121.2012.01072.x
28:Ultra-high-pressure metamorphism
18:Ultrahigh-pressure metamorphism
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929:Behn, M. D., Kelemen, P. B.,
630:orogenic extensional collapse
330:Subduction zone metamorphism
155:Implications and importance
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256:is causing a rift in the
224:Exhumation of UHP rocks
137:D'Entrecasteaux Islands
195:Formation of UHP rocks
1156:Metamorphic petrology
1101:Metamorphic processes
1035:Types of metamorphism
246:Western Gneiss Region
180:structural geologists
780:105, p. 13339–13364.
214:volcanoplutonic arcs
74:, the high-pressure
38:, the high-pressure
1113:Foliation (geology)
760:, v. 114, p. 70-85.
715:2008Geo....36..823W
657:2012TeNov..24..339G
254:Woodlark microplate
237:necking of the slab
122:Global distribution
308:quartzofeldspathic
206:Al Hajar Mountains
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1065:Metamorphic rocks
723:10.1130/G25134A.1
112:Kokchetav Massifs
16:(Redirected from
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821:
815:
811:
806:
802:
797:
793:
788:
784:
778:
774:
768:
764:
753:
749:
744:
740:
734:
730:
709:(10): 823–826.
698:
693:
692:
688:
641:
640:
636:
627:
623:
618:
614:
608:
604:
599:
592:
587:
583:
577:
570:
565:
561:
555:
551:
546:
542:
537:
533:
527:
523:
518:
514:
509:
502:
496:
492:
487:
483:
478:
474:
466:
462:
454:
450:
444:
437:
432:
428:
423:
419:
414:
410:
404:
400:
395:
391:
386:
382:
376:
369:
364:
360:
355:
351:
346:
342:
338:
316:
231:If continental
226:
197:
157:
124:
105:
101:
88:
81:
68:
59:microcontinents
48:plate tectonics
45:
23:
22:
15:
12:
11:
5:
1169:
1167:
1159:
1158:
1148:
1147:
1141:
1140:
1138:
1137:
1130:
1122:
1119:
1118:
1116:
1115:
1110:
1104:
1102:
1098:
1097:
1095:
1094:
1089:
1084:
1079:
1074:
1068:
1066:
1062:
1061:
1054:
1052:
1050:
1049:
1044:
1038:
1036:
1032:
1031:
1025:
1023:
1022:
1015:
1008:
1000:
994:
993:
990:
987:
984:
979:
976:
974:
973:
964:
954:
944:
935:
919:
906:
897:
885:
875:
865:
855:
845:
832:
819:
809:
800:
791:
782:
772:
762:
747:
738:
728:
686:
651:(5): 339–350.
634:
621:
612:
602:
590:
581:
568:
559:
549:
540:
531:
521:
512:
500:
490:
481:
472:
460:
448:
435:
426:
417:
408:
398:
389:
380:
367:
358:
349:
339:
337:
334:
333:
332:
327:
325:Eclogitization
322:
315:
312:
288:
287:
284:
281:
258:Woodlark Basin
225:
222:
196:
193:
156:
153:
123:
120:
103:
102:structured TiO
99:
87:
86:Identification
84:
79:
67:
64:
43:
24:
14:
13:
10:
9:
6:
4:
3:
2:
1168:
1157:
1154:
1153:
1151:
1136:
1135:
1131:
1129:
1128:
1124:
1123:
1120:
1114:
1111:
1109:
1106:
1105:
1103:
1099:
1093:
1090:
1088:
1085:
1083:
1080:
1078:
1075:
1073:
1070:
1069:
1067:
1063:
1058:
1048:
1045:
1043:
1040:
1039:
1037:
1033:
1028:
1021:
1016:
1014:
1009:
1007:
1002:
1001:
998:
991:
988:
985:
982:
981:
977:
968:
965:
958:
955:
948:
945:
939:
936:
932:
926:
924:
920:
913:
911:
907:
901:
898:
892:
890:
886:
879:
876:
869:
866:
859:
856:
849:
846:
839:
837:
833:
826:
824:
820:
813:
810:
804:
801:
795:
792:
786:
783:
776:
773:
766:
763:
759:
758:
751:
748:
742:
739:
732:
729:
724:
720:
716:
712:
708:
704:
697:
690:
687:
682:
678:
674:
670:
666:
662:
658:
654:
650:
646:
638:
635:
631:
625:
622:
616:
613:
606:
603:
597:
595:
591:
585:
582:
575:
573:
569:
563:
560:
553:
550:
544:
541:
535:
532:
525:
522:
516:
513:
507:
505:
501:
494:
491:
485:
482:
476:
473:
469:
464:
461:
457:
452:
449:
442:
440:
436:
430:
427:
421:
418:
412:
409:
402:
399:
393:
390:
384:
381:
374:
372:
368:
362:
359:
353:
350:
344:
341:
335:
331:
328:
326:
323:
321:
318:
317:
313:
311:
309:
304:
299:
297:
293:
285:
282:
279:
278:
277:
273:
269:
267:
261:
259:
255:
249:
247:
243:
238:
234:
229:
223:
221:
219:
215:
211:
207:
203:
194:
192:
189:
185:
181:
176:
172:
170:
166:
162:
154:
152:
150:
146:
140:
138:
133:
129:
121:
119:
115:
113:
109:
97:
93:
85:
83:
77:
73:
65:
63:
60:
56:
51:
49:
41:
37:
33:
29:
19:
1132:
1125:
1041:
967:
957:
947:
938:
900:
878:
868:
858:
848:
812:
803:
794:
785:
775:
765:
755:
750:
741:
731:
706:
702:
689:
648:
644:
637:
624:
615:
605:
584:
562:
552:
543:
534:
524:
515:
493:
484:
475:
463:
451:
429:
420:
411:
401:
392:
383:
361:
352:
343:
303:diapirically
300:
289:
274:
270:
262:
250:
230:
227:
198:
184:petrologists
177:
173:
158:
141:
130:continental
125:
116:
89:
69:
52:
27:
26:
1077:Amphibolite
1027:Metamorphic
468:Jahn, B. M.
456:Liou, J. G.
233:lithosphere
128:Phanerozoic
32:metamorphic
645:Terra Nova
610:1661-1687.
336:References
202:subduction
149:peridotite
66:Definition
55:subduction
30:refers to
1029:petrology
931:Hirth, G.
681:128133726
673:1365-3121
378:1153-1160
210:Banda Arc
169:xenoliths
76:polymorph
40:polymorph
1150:Category
1127:Category
1082:Anatexis
962:777-797.
917:681-716.
883:171–184.
863:116-129.
843:129-145.
830:236-256.
817:113-136.
770:225-232.
736:183-197.
557:555-576.
529:901-953.
446:671-689.
406:347–364.
314:See also
266:Piedmont
242:rheology
132:orogenic
92:eclogite
711:Bibcode
703:Geology
653:Bibcode
72:coesite
36:coesite
1134:Portal
1092:Schist
952:39-68.
853:63-74.
757:Lithos
679:
671:
498:27-49.
296:Qaidam
186:, and
165:mantle
145:gneiss
78:of SiO
42:of SiO
1087:Augen
699:(PDF)
677:S2CID
218:Pamir
873:114.
669:ISSN
292:Moho
719:doi
661:doi
260:).
161:GPa
108:GPa
57:of
1152::
922:^
909:^
888:^
835:^
822:^
717:.
707:36
705:.
701:.
675:.
667:.
659:.
649:24
647:.
593:^
571:^
503:^
438:^
370:^
182:,
171:.
1019:e
1012:t
1005:v
725:.
721::
713::
683:.
663::
655::
104:2
100:2
80:2
44:2
20:)
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