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T h e p r o b l e m , from the geophysical viewpoint, is poorly constrained. As an example, we discuss in this section a possible significant change. T h e m a n t l e in the A r c h a e a n was a few h u n d r e d d e g r e e s h o t t e r than at present (see D u r r h e i m & M o o n e y 1994 for a discussion of the 34 G. 3 " ' 0 l (Tm"To=1300K) ] '

Since as a rule the creep strength of silicate rocks in the ductile field increases with decreasing silica content (see Table 1), the rheological structure of the lithosphere is layered, with one or more brittle layers separated by ductile layers. 'Type' profiles are shown in Fig. 5, for linearized geotherms and different types of lithosphere. ) Except for cold geotherms (corresponding to surface heat flows of the order of 40 mW m-2), the Moho is a strength discontinuity in the continental lithosphere (but not in the oceanic lithosphere).

1991. Middle and late Carboniferous extension in the Variscan belt: structural and petrological evidence from the Vosges massif (eastern France). Geodinamica Acta, 5, 17-36. Ru'VrER, E. H. & BRODIE, K. H. 1992. Rheology of the lower crust. In: FOUNTAIN,D. , ARCULUS,R. & KAY, R. W. (eds) Continental lower crust. Elsevier, Amsterdam, 201-267. ScnoLz, C. H. 1990. The mechanics of earthquakes and faulting. University Press, Cambridge. SHIMADA,M. 1993. Lithosphere strength inferred from fracture strength of rocks at high confining pressures and temperatures.

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