Despite previous observations that aftershocks lie preferentially along the fault planes of mainshocks, many branching models for earthquake occurrences do not directly incorporate information on the moment tensors of mainshocks in forecasting the spatial distribution of aftershocks, or do so in a very simplistic way using spatial kernels which have not been rigorously tested on earthquake data...

A detailed 3-D P-wave velocity structure of the crust in the epicentral area of the 17 January, 1994 Northridge earthquake is determined by using 104,709 arrival times from 1673 Northridge aftershocks and 2948 other local earthquakes. A test performed using the data from the nearby portable stations suggests that the aftershock hypocenters relocated with the obtained 3-D model are accurate to a...

We developed a sliding-window cross-correlation (SCC) detection technique and applied the technique to continuous waveforms recorded by the Cooperative New Madrid Seismic Network stations following the 18 April 2008 Illinois earthquake. The technique detected more than 120 aftershocks down to ML 1.0 in the 2 week time window following the mainshock, which is three times more than the number of ...

An earthquake of M, = 5.3 occurred at 32°58.7'N, 117°51.5'W southwest of Oceanside in San Diego County at 13:47 13 July 1986 (UT). This main shock was followed by an extensive aftershock sequence, with 55 events of ML > 3.0 during July 1986. The epicenters of the main shock and aftershocks are located at the northern end of the San Diego Trough-Bahia Soledad fault zone (SDT-BS) where it changes...

[1] Aftershocks follow a well‐defined spatial decay pattern in the intermediate field. Here I investigate the same pattern for foreshocks. Foreshock linear density decays as r over distances r of 0.1–30 km for 15 minutes before magnitude 3–4 mainshocks. This trend is the same as that of the aftershocks within the error of the measurement. This consistency of spatial decay can be explained by th...

A measure of the correlation between two earthquakes is used to link events to their aftershocks, generating a growing network structure. In this framework one can quantify whether an aftershock is close or far, from main shocks of all magnitudes. We find that simple network motifs involving links to far aftershocks appear frequently before the three biggest earthquakes of the last 16 years in ...

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...