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Geological Society, London, Special Publications; 2000; v. 179; p. 387-399;
DOI: 10.1144/GSL.SP.2000.179.01.23
© 2000 Geological Society of London

Syn-convergent high-temperature metamorphism and magmatism in the Variscides: a discussion of potential heat sources

A. Henk1, F. von Blanckenburg2, F. Finger3, U. Schaltegger4 & G. Zulauf5

1 Institut für Geologie, Universität Würzburg, Pleicherwall 1, D-97070 Würzburg, Germany andreas.henk{at}mail.uni-wuerzburg.de
2 Mineralogisch-Petrographisches Institut, Abt. für Isotopengeologie, Universität Bern, Erlachstr. 9a, CH-3012 Bern, Switzerland
3 Institut für Mineralogie, Universität Salzburg, Hellbrunnerstr. 34, A-5020 Salzburg, Austria
4 Institut für Isotopengeochemie und Mineralische Rohstoffe, ETH-Zentrum NO, Sonneggstr. 5, CH-8092 Zürich, Switzerland
5 Institut für Geologie und Mineralogie, Universität Erlangen-Nürnberg, Schloßgarten 5, D-91054 Erlangen, Germany

A period of pervasive high-temperature metamorphism and igneous activity from 340 to 325 Ma is a well-established characteristic of the Variscan Orogen of Central Europe. During this stage, the internal zone of the orogen was virtually soaked by granitic to granodioritic magmas. Petrological data point to temperatures of 600–850 °C at upper- to mid-crustal levels. These elevated temperatures occurred during the final convergence stage and may be comparable with similar processes inferred from geophysical evidence for the present-day Tibetan Plateau, in both regional extent and significance for the orogen’s evolution. We review various geodynamic scenarios that may have provided the heat for melting and metamorphism, and compare model predictions with field data from the Variscides. All lines of evidence point to a geodynamic scenario that led to thickening of the continental crust with increased internal radiogenic heating, but without simultaneous thickening of the mantle lithosphere. Possible mechanisms include convective removal of the thermal boundary layer, delamination of part of the lithospheric mantle, and subduction of the mantle lithosphere of the downgoing plate. However, with the present stage of knowledge it is virtually impossible to single out one of these three mechanisms, as their geological consequences are so similar.





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