By K. Shimazaki, W. Stuart (auth.), Kunihiko Shimazaki, William Stuart (eds.)

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Tejon event, which had a rupture length of about 350 km (SIEH, 1978). The approximate rupture ends are marked by the large brackets in Fig. 1. Based on 1) US Geological Survey, 525 S. , Pasadena, California 91106, USA. 794 William D. Stuart PAGEOPH, 0 N ~ PACIFIC OCEAN 0 KM 100 3 1° Figure 1 Map of southern California showing seismicity; geographic place names; and San Andreas, Imperial, Cerro Prieto, and San Jacinto fault traces. 0 during 1983. Seismicity data are from the California Institute of Technology - US Geological Survey Seismograph Network, courtesy of C.

For example, if Slau = 0, as with a horizontal rl(u) curve representing perfect plasticity, instability will not occur because there can be no stress drop. Similarly, the stiffness of the elastic surroundings, which depends on the elastic moduli and model geometry, may be high enough to preclude instability. In the present model, the average fault stress is also declining before instability, but some locations on the fault are slip hardening or at peak stress when instability starts. Figure 4a illustrates how the pre-instability stress state and amount of unstable slip might differ from one instability to the next at a fault location.

R. 792 Michele Dragoni, Maurizio Bonafede and Enzo Boschi PAGEOPH REFERENCES BIAGI, P. , and SPADEA, M. C. (1976), Le variazioni d'inclinazione e Ia sismicitd che hanno preceduto ilforte terremoto del Friuli de/6 maggio 1976, Annali Geofis. 29, 137-146. BILBY, B. , and EsHELBY, J. , Dislocations and the Theory of Fracture, in Fracture -An Advanced Treatise, vol. 1 (ed. H. Liebowitz) (Academic Press, New York 1968), pp. 99-182. , and DRAGONI, M. (1983), Viscoelastic Stress Relaxation on Deep Fault Sections as a Possible Source of Very Long Period Elastic Waves, J.

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