Surface Wave Data

Figure 3
[11]  As mentioned above, additional observational data are required to stabilize the receiver function inversion results. Phase velocities of surface waves have recently been utilized for this purpose [Julia et al., 2000]. Such data are unavailable from RUKSA records due to the overly small aperture. However, the phase velocities were determined from SVEKALAPKO (without RUKSA) broadband records of many earthquakes [Bruneton et al., 2004]. The method consists in the measurement of traveltimes of the Rayleigh wave fundamental mode between their curvilinear fronts within the SVEKALAPKO array and the inversion of the measured data into the phase velocity field. These data in the form of dispersion curves of the Rayleigh phase velocity at grid nodes covering the SVEKALAPKO array were afforded by M. Bruneton, who used them for the construction of the SVEKALAPKO tomography model [Bruneton et al., 2004]. A phase velocity curve in the range of periods from 10.5 s to 190 s was constructed at each grid point. We used the dispersion curve that was obtained by extrapolating the set of these curves (Figure 3) to the point with the RUKSA coordinates by the kriging method [Isaacs and Srivastava, 1989]. In our opinion, this procedure is reliable because the spread of the dispersion curves in the region about 500 km across is small (Figure 3) and the distance from the RUKSA array to the nearest SVEKALAPKO stations does not exceed 100 km. The inversion interval of periods was 10.5-110 s.


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