By Renata Dmowska
A transparent exposition of the new release T waves via earthquakes, the tension accumulation version, and seismic ray tracing and wavefront monitoring in laterally heterogeneous media.
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The fundamental framework of this approach was developed by Pekeris (1948). Given a flat-layered structure featuring translational symmetry along the horizontal x and y directions, the potential φ of the elastic wave in the water is sought at each angular frequency ω as a cylindrical wave radiating out of the polar axis r = 0: φ(r, z, t) = (z)H0(1) (kr) e−iωt , (1) 20 OKAL (1) where H0 is the Hankel function of first kind and order 0, and d2 (z) ω2 − k2 + dz2 v 2 (z) (z) = 0, satisfies (2) v being the local velocity of sound, which can be a priori a function of depth z.
2001). The latter have much shorter durations, which probably reflects the difference in the nature of the slide (the simple collapse of a cohesive block) and the shorter length of its total underwater path. Finally, in Fig. 24, we compare on a dataset of eight South American earthquakes the performance of the three parameters D, γ , and , introduced by Talandier and Okal (2001), Okal et al. (2003) and Newman and Okal (1998) to detect any possible slowness in the rupture characteristics of seismic sources.
8 between TS and Ms in (4)) for a very homogeneous dataset of 24 East Pacific Rise earthquakes at regional distances. 49 similarly expresses that T -wave amplitudes do suffer from interference effects in a range of magnitudes (Ms 5) where 20-second waves are immune from them. Walker et al. (1992) later investigated the correlation of T -phase strength (which they restricted to the frequency range 10–35 Hz) with seismic moment M0 for a dataset of 25 Pacific-rim earthquakes recorded at the Wake hydrophone array.