By Renata Dmowska, Barry Saltzman

This sequence presents a venue for longer reports of present advances in geophysics. Written at a degree obtainable to graduate scholars, the articles serve to expand wisdom of assorted fields and will be invaluable in classes and seminars.

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In Fig. 18 we show the dynamic stress build up on the fault plane of the second subevent of the 1980 Irpinia earthquake (the fault geometry is illustrated in Fig. , 1999). The origin time is taken at the rupture initiation on the first subevent’s fault (also named master 0’s event). , 1997). After nearly 8 s the dynamic stress reached the maximum value at the NW edge of the fault plane (the closest to the rupturing 0’s subevent). After 13 s the dynamic stress reached the static configuration, as described in detail by Belardinelli et al.

1994). Aftershocks of the Campania-Lucania (Italy) earthquake of 23 November, 1980. Bull. Seismol. Soc. Am. 84, 935–953. Dieterich, J. H. (1972). Time dependence friction as a possible mechanism for aftershocks. J. Geophys. Res. 77, 3771–3781. Dieterich, J. H. (1978). Time dependent friction and the mechanics of stick-slip. Pure Appl. Geophys. 116, 790–806. Dieterich, J. H. (1979a). Modeling of rock friction, 1, experimental results and constitutive equations. J. Geophys. Res. 84, 2161–2168. Dieterich, J.

1995). Multifractal scaling properties of a growing fault population. Geophys. J. Int. 122, 457–469. Crider, J. , and Pollard, D. D. (1998). Fault linkage: Three-dimensional mechanical interaction between echelon normal faults. J. Geophys. Res. 103(10), 24,373–24,392. , and Scholz, C. (1981). Off-fault aftershock clusters caused by shear stress increase? Bull. Seismol. Soc. Am. 71, 1669–1675. , and Sykes, L. R. (1997a). Evolution of the stress field in southern California and triggering of moderate-size earthquakes: A 200-years perspective.

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