By Renata Dmowska
A transparent exposition of the new release T waves by means of earthquakes, the tension accumulation version, and seismic ray tracing and wavefront monitoring in laterally heterogeneous media.
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Extra info for Advances in Geophysics, Vol. 49
They were able to associate those records featuring positive D with sources in the immediate vicinity of steep conversion zones, which provide an efficient conversion resulting in high amplitudes and short durations. By contrast, Talandier and Okal (2004b) studied 10 records from true intraplate earthquakes, located in abyssal areas where no significant bathymetry is documented. They all feature negative values of D, and are thus unequivocally identified as earthquakes (Fig. 20b). These include some of the most negative D 46 OKAL F IG .
The combined effect of the finite strain release on a 2-dimensional fault and of the limited velocity of the actual slip between the fault walls leads to a total saturation of spectral amplitudes once the source corner frequencies recess below the frequency f of interest in the wave group under study. 8 × 1026 dyn cm) when properly measured on P waves at 1 second (larger values of mb reported in bulletins usually stem from measurements taken at longer periods, or on S waves, or relate to deep events allowing greater strain release).
Note the streaks of epicenters along great circles radiating from the array, which express the loss of range resolution for very distant events. The location of the new hydrophone station at Juan Fernandez Island (JF) is shown by the large circle and that of the Polynesian Seismic Network (RSP) by the open box. Adapted (re-labeled) from Fox et al. (2001). 5 Hz), otherwise poorly sampled due to anelastic attenuation of conventional teleseismic waves. However and as detailed below, for larger earthquakes, T waves are strongly affected by interference resulting from source finiteness, and their amplitude alone cannot be a good proxy for source size.
Advances in Geophysics, Vol. 49 by Renata Dmowska