The spatial wave structure was k x = 10−3 km−1 and k y = 0.
The combination of the temporal and spatial wave information permits to obtain wave data, such as the wave spectrum, being related to sea state parameters [4, 6, 9].
In the calculation, we used Ĝ (x A, x B, ω)* = Ĝ (x A, x B, −ω), because G (x A, x B, t) is real, and Ŝ N = Ŝ N because S N = S N. In particular, for the noise spectrum, which is assumed to be white, given by Ŝ N = S0 and S N = S0δ, Eq. (15) becomes, (16) Equation (16) indicates the relation between the spatial correlation of continuous ocean waves and the tsunami Green's function.
Moreover, we examine the relation between the spatial distribution of coda Q, shear wave velocity, and seismicity.
This study investigates details of the spatial distribution of coda Q around the Atotsugawa fault zone and examines the relation between the spatial distributions of coda Q and shear wave velocity in the lower crust.
We focus here on the distribution of the S-wave velocity because coda waves consist mainly of S-waves. Figure 4f shows a plot of the correlation coefficients, between the spatial distribution of coda Q in each frequency band and the S-wave velocity, with depth.
In this study, we also observe a negative correlation between the spatial distribution of coda Q in the lower-frequency bands and the S-wave velocity in the upper crust (Fig. 4f).
If correct, then the spatial dynamics of wave propagation may shape the nature of information processing [ 44].
The effect of the spatial derivatives of the wave velocity on the wave surface kinematics is quantified and shown to determine the wave spectral cut-off frequency limit.
The spatial modeling of waves could also be improved.
