By Richard D. Miller, John H. Bradford, Klaus Holliger
Published by means of the yank Geophysical Union as a part of the Geophysical improvement sequence, quantity 15.
Advances in Near-surface Seismology and Ground-penetrating Radar (SEG Geophysical advancements sequence No. 15) is a suite of unique papers via well known and revered authors from world wide. applied sciences utilized in the appliance of near-surface seismology and ground-penetrating radar have visible major advances within the final a number of years. either tools have benefited from new processing instruments, elevated desktop speeds, and an increased number of applications.
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Additional resources for Advances in Near-surface Seismology and Ground-penetrating Radar, Volume 15
El Sorady, 2006, Joint inversion of gravity and geoelectrical data for groundwater and structural investigation: Application to the northwestern part of Sinai, Egypt: Geophysical Journal International, 165, 705–718. , H. R. Maurer, and A. G. Green, 2003, Discrete tomography and joint inversion for loosely connected or unconnected physical properties: Application to crosshole seismic and georadar data sets: Geophysical Journal International, 153, 389–402. , and J. Tronicke, 2007, Cooperative inversion of 2D geophysical data sets: A zonal approach based on fuzzy c-means cluster analysis: Geophysics, 72, no.
50. 2 b) 4 IRLS individual IRLS joint L2 individual L2 joint (19) 5 where ks and kw are the dielectric permittivities of the solid and water phases. It is then possible to determine the lower and upper bounds for radar wave speed using 6 7 8 c ¼ pﬃﬃﬃﬃﬃﬃﬃﬃﬃﬃ , kHSU (20) c vHSU ¼ pﬃﬃﬃﬃﬃﬃﬃﬃﬃﬃ , kHSL (21) vHSL 9 9 10 74 76 78 80 82 where c ¼ 3 Â 108 m/s is the vacuum speed of light. Figure 6. 09 GPa, ms ¼ inversions. 5, kw ¼ 84, rs ¼ 2605 kg . m23, and rw ¼ 1000 kg . m23. These values are representative robust descriptions of the system than the tomograms values of a-quartz (Scho¨n, 1996) and water at 108C themselves.
From equation 9, S-wave velocities (Figure 5b) can be calculated using the ﬁnal estimates of S-wave velocity at the surface VS0 and the measure of inhomogeneity m. , 2002c) are shown in Figure 5b (squares). Xia et al. (2006b) also estimated S-wave velocities by inverting only three data points ( f ¼ 12, 15, and 20 Hz) and keeping all other conditions and parameters the same as in the previous case. 274) was obtained (Figure 5b). Compared with the suspension-log results (Figure 5b), the Gibson half-space model (“Nonlayered”) does a good job from the subsurface down to 12 m.