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d c is large enough in conditional asperity to become conditionally stable (e.g., Boatwright and Cocco, 1996).
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However, large d c in the conditional asperity results in a lower weakening rate, and hence in slower rupture propagation than in ordinal events.
On the other hand, in the conditional asperity (x = 100, 300, 500 in Fig. 2), nearly constant aseismic slip and af-terslip appear, as well as large coseismic slip and a locked state, depending upon the stage in the M 9 earthquake cycle.
In such cases, d c in the regular asperity should be one order or more smaller than it is in the conditional asperity.
The source area outside the regular asperities is called a conditional asperity, since in this area both aseismic sliding and seismic slip occur, depending on the stress and fault strength conditions.
Although the weakening rate during the coseismic rupture has not yet been estimated, our model predicts a higher and lower weakening rate in the regular and conditional asperities, respectively.
There are substantial differences in conditional rates.
Upper right: Observed in conditional distribution.
During the running-in process, asperities experience both elastic and plastic contact and as a result of the plastic deformation, the asperity heights change.
In this work, the asperities used in asperity model are extracted from the surface generated above.
In the asperity of early winter, he seemed grossly overfed.
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