Aftershocks in a frictional earthquake model

Renormalization of earthquake aftershocks

Assume that each earthquake can produce a series of aftershock independently of its size according to its “local” Omori’s law with exponent 1+θ. Each aftershock can itself trigger other aftershocks and so on. The global observable Omori’s law is found to have two distinct power law regimes, the first one with exponent p− = 1− θ for time t < t ∗ ∼ κ−1/θ, where 0 < 1−κ < 1 measures the fraction o...

Modeling afterslip and aftershocks following the 1992 Landers earthquake

[1] One way to probe the rheology of the lithosphere and fault zones is to analyze the temporal evolution of deformation following a large earthquake. In such a case, the lithosphere responds to a known stress change that can be assessed from earthquake slip models constrained from seismology and geodesy. Here, we model the postseismic response of a fault zone that is assumed to obey a rate-str...

Foreshocks and Aftershocks of the Great 1857 California Earthquake

The San Andreas fault is the longest fault in California and one of the longest strike-slip faults anywhere in the world, yet we know little about many aspects of its behavior before, during, and after large earthquakes. We conducted a study to locate and to estimate magnitudes for the largest foreshocks and aftershocks of the 1857 M 7.9 Fort Tejon earthquake on the central and southern segment...

Aftershocks and Pore Fluid Diffusion Following the 1992 Landers Earthquake

Frictional weakening and slip complexity in earthquake faults

Previous work has shown that velocity-weakening friction produces slip complexity in simple dynamical models of earthquake faults ( Carlson and Langer, 1989). Rere I show that a different type of dynamical instability, caused by slipweakening friction, also produces slip complexity. The deterministically chaotic slip complexity produced by slip-weakening friction in a simple one dimensional mod...