The thermal structure of collisional orogens as a response to accretion, erosion, and radiogenic heating

Huerta, A. D.; Royden, L.; Hodges, K. V.

doi:10.1029/98jb00593

Cited by 135 publications

(120 citation statements)

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“…11a), from 340 to at most 314 Ma, developed at temperatures above the water-saturated quartz -feldspar solidus and was coeval with crustal thickening characterized by (a) thrusting of the Upper Gneiss Unit at the roof and margin of the dome, (b) decoupling and stacking of the Lower Gneiss Unit preserved within the migmatites, and (c) metamorphic paragenese of the Cévennes micaschists (Arnaud, 1997). At this stage, thermal relaxation and heat production within the thickened crust were probably the main causes of temperature increase (England and Thompson, 1984;Huerta et al, 1998). The emplacement of the peri-Velay precursor granites and high-K magnesian monzodiorite magmatism of mantle origin constitute an additional heat source.…”

Section: Discussion: the Significance Of Crustal Anatexis In The Velamentioning

confidence: 99%

“…According to current petrological and thermal numerical models (Thompson and Connolly, 1995;Huerta et al, 1998), a simple crustal thickening event followed by erosion can hardly account for the generation of large volumes of granite. Results from experimental petrology show that high melt fractions require conditions well above 800°C, above the destabilization curves of hydrous minerals (Clemens and Vielzeuf, 1987;Patiño Douce and Johnston, 1990;Gardien et al, 1995).…”

Section: Discussion: the Significance Of Crustal Anatexis In The Velamentioning

confidence: 99%

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The Velay dome (French Massif Central): melt generation and granite emplacement during orogenic evolution

Ledru

Courrioux

Dallain³

et al. 2001

Tectonophysics

164

101

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This paper is a synthesis of available data on the Velay dome that include both small-and large-scale lithologic and structural mapping, strain analysis, isotope geochemistry, geochronology and pressure -temperature estimates. The Velay dome, one of the largest granite -migmatite domes of the Variscan Belt, formed during orogenic collapse at around 300 Ma. Its study allows an assessment of the thermal and geodynamic context leading to voluminous crustal anatexis of the Variscan orogenic crust. A first melting stage developed in connection with south-verging thrust zones during the Early Carboniferous, leading to a crustal thickening estimated at 20 km minimum. The involvement of fertile lithologies and the intrusion of plutons of deep origin contributed to the development of water-saturated melts. The volume of biotite granite extracted from melt during this period was limited. The second phase of melting, corresponded to generalized melting of gneiss achieved by biotite-dehydration melting reactions and accompanied by the generation of cordierite-bearing granites. At this stage, crustal-scale detachment faults were active and partially obliterated the earlier structures. The new structures were progressively tilted to the vertical at the margin of the Velay dome due to the southward and lateral ballooning of the granitic dome. The reconstructed P, T path indicate that the large volume of melt produced was a consequence of a significant increase in temperature at the onset of biotite dehydration melting. At the base of the crust, this melting event is coeval with granulite facies metamorphism associated to underplating of mantle-derived magmas as suggested by the geochemical signature of Late Paleozoic lower crustal xenoliths sampled by Cenozoic volcanoes and with the isotopic signature of the late granitic intrusions. Accordingly, it is proposed that asthenospheric upwelling was responsible for the temperature increase favoring melting of hydrous minerals.

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Section: Discussion: the Significance Of Crustal Anatexis In The Velamentioning

confidence: 99%

Section: Discussion: the Significance Of Crustal Anatexis In The Velamentioning

confidence: 99%

The Velay dome (French Massif Central): melt generation and granite emplacement during orogenic evolution

Ledru

Courrioux

Dallain³

et al. 2001

Tectonophysics

164

101

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“…(3) Advective heat transfer to the upper crust by exhumation of hot eclogitic slices within a subduction channel (becker 1993; Engi et al 2001), or alternatively, by extension-related exhumation of hot high-pressure rocks (Platt 1986;ballèvre et al 1990). (4) Accretion of continental crustal rocks characterised by high radioactive heat production (chamberlain & sonder 1990;bousquet et al 1997;Huerta et al 1998;roselle et al 2002;Goffé et al 2003).…”

Section: Discussion Of Potential Heat Sources Of Barrow-type Overprinmentioning

confidence: 99%

From subduction to collision: Thermal overprint of HP/LT meta-sediments in the north-eastern Lepontine Dome (Swiss Alps) and consequences regarding the tectono-metamorphic evolution of the Alpine orogenic wedge

et al. 2008

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the cenozoic-age metamorphic structure of the Alps consists of a throughgoing pressure-dominated belt (blueschists and eclogites) that strikes parallel to the orogen and was later truncated by two thermal domes characterised by barrow-type metamorphism (Lepontine dome and tauern window). this study documents for the first time that relics of Fe-Mg carpholite occur also within meta-sedimentary units that are part of the north-eastern Lepontine structural and metamorphic dome, where so far exclusively barrovian assemblages were found. they occur in meta-sediments of both Valais Oceanderived Lower Penninic bündnerschiefer and structurally lower Europe-derived sub-Penninic cover nappes and slices. these high-pressure units were subsequently overprinted by a thermal event, as is documented by the growth of new minerals typical for barrovian metamorphism.We present evidence for a two-stage metamorphic evolution in the northern part of the Lepontine dome: (1) Early subduction-related syn-D1 (safien phase) HP/Lt metamorphism under blueschist facies conditions (350-400 °c and 1.2-1.4 GPa) was immediately followed by "cold" isothermal (or cooling) decompression during D2 nappe-stacking (Ferrera phase). (2) collisionrelated barrovian overprint (500-570 °c and 0.5-0.8 GPa) postdates the D3 nappe-refolding event (Domleschg phase) and represents a late heating pulse, separated by D2 and D3 from the D1 high-pressure event. It occurred before and/or during the initial stages of D4 (chièra phase) representing a second nappe-refolding event.In discussing possible heat sources for the late barrow-type heating pulse it is argued that heat release from radioactive decay of accreted material may play an important role in contributing much to heat production. based on the field evidence, we conclude that heat transfer was essentially conductive during these latest stages of the thermal evolution. Introductionthe zoning of Alpine metamorphism is rather complex, evolving over a very long period of time before, during and after the collision of Europe with Adria, i.e. from Late cretaceous to Late cenozoic times. Mapping of metamorphic facies in the Alps started with early pioneering studies based on the spatial distribution of index minerals and mineral assemblages (Wenk 1962;Niggli & Niggli 1965;trommsdorff 1966;Frey 1969; Fox 1975;Frey et al. 1980). Metamorphic maps at the scale of the Alpine orogen, showing the spatial arrangement of the different metamorphic facies types, were repeatedly synthesised and improved (Ernst 1971;Niggli & Zwart 1973;Oberhänsli et al. 2004). the cenozoic-age metamorphic pattern is characterised by a pressure-dominated belt (blueschists and eclogites) that strikes orogen-parallel but is interrupted by two thermal domes, the Lepontine dome in the central Alps and the tauern window in the Eastern Alps (Oberhänsli et al. 2004).Our area of investigation is located at the NE border of the Lepontine thermal dome. there, along strike of the tectonic units, a remarkable metamorphic field gradient that rang...

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“…However, using realistic crustal properties, it has also been suggested that thrusting could not be responsible for inverted gradient beneath thrusts (e.g. Jaupart and Provost, 1985;Ruppel and Hodges, 1994;Huerta et al, 1996Huerta et al, , 1998 but only induces low thermal perturbations (Shi and Wang, 1987;Endignoux and Wolf, 1990).…”

Section: Thrust Propagationmentioning

confidence: 99%

Thermal regime of fold and thrust belts—an application to the Bolivian sub Andean zone

Husson

Moretti

2002

Tectonophysics

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The thermal structure of collisional orogens as a response to accretion, erosion, and radiogenic heating

Cited by 135 publications

References 51 publications

The Velay dome (French Massif Central): melt generation and granite emplacement during orogenic evolution

The Velay dome (French Massif Central): melt generation and granite emplacement during orogenic evolution

From subduction to collision: Thermal overprint of HP/LT meta-sediments in the north-eastern Lepontine Dome (Swiss Alps) and consequences regarding the tectono-metamorphic evolution of the Alpine orogenic wedge

Thermal regime of fold and thrust belts—an application to the Bolivian sub Andean zone

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