Receiver functions at the stations of the German Regional Seismic Network (GRSN)

Abstract

S U M M A R YSeveral years of broad-band teleseismic data from the GRSN stations have been analysed for crustal structure using P -t o 4 converted waves at the crustal discontinuities. An inversion technique was developed which applies the ThomsonHaskell formalism for plane waves without slowness integration. The main phases observed are Moho conversions, their multiples in the crust, and conversions at the base of the sediments. The crustal thickness derived from these data is in good agreement with results from other studies. For the Grafenberg stations, we have made a more detailed comparison of our model with a previously published model obtained from refraction seismic experiments. The refraction seismic model contains boundaries with strong velocity contrasts and a significant low-velocity zone, resulting in teleseismic waveforms that are too complicated as compared to the observed simple waveforms. The comparison suggests that a significant low-velocity zone is not required and that internal crustal boundaries are rather smooth.

Elevation of the 410 km discontinuity beneath the central Tien Shan: Evidence for a detached lithospheric root

“…The method used to detect upper mantle discontinuities is a P-SV stacking technique described in detail elsewhere [e.g., Vinnik, 1977;Kind et al, 1995]. Briefly, each seismogram is rotated into a "ray system" (Longitudinal (L), SV and SH components), using the theoretical backazimuth and an angle of incidence determined from the radial-vertical covariance matrix of the P-wave.…”

Seismic signature of the collision between the east Tibetan escape flow and the Sichuan Basin

“…Techniques exist for inverting receiver function waveforms into velocity-depth models (e.g. Kind et al 1995).…”

Crustal structure of Northwest Zagros (Kermanshah) and Central Iran (Yazd and Isfahan) using teleseismic Ps converted phases

“…We used the method, which was described by Kind et al (1995). The theoretical seismograms are computed for the starting model using the method of Haskell (1962), and then the components are rotated and deconvolved in the same manner as done for the observed traces.…”