## 2 Data and Methods
The generalization of results of lineament decoding in the form of a map of the lineament density distribution is an important operation for final interpretation. Since the methodological foundations of seismic hazard maps are based on a direct analogy between lineaments and fracture tectonics [14; 33], the increasing lineament density can be correctly interpreted as increasing the fragmentation in the upper part of the cross-section. Numerically, the procedure is based on counting the number of tips of selected lineaments per unit area of the integration interval (Figure 2d). Morphotectonic analysis is an independent operation that verifies the morphobstructural reconstructions described above and information about the position of areas of reduced stability in upper part of the cross-section. Here, the basic element includes the selection of geoblock boundaries, in which, firstly, the expert analysis of anomalies of the spatial stationarity parameter (entropy parameter) and, secondly, the optimal separation of this signal into long-wave and short-wave components are applied. The expert analysis of the scalar entropy field is performed visually with involvement of contour lines and half-tone images of entropy anomalies. The principal elements of morphobstructural zoning include the existence of isometric and/or elongated anomalies, fixation of their linear size, the dominant strike azimuth of axes of anomalies and/or local gradient zones, existence of zones of sharp space-related gradients, variation in general \"image\" of isolines, variation in space-related stationarity of the signal and the existence of a significant jog in the structure of individual isolines or a set of isolines. Separation of the signal into components is initially associated with a methodological element for identifying the base and erosion-active layers in the relief structure. In the considered case, it is enough to select the threshold wavelength (space-related frequency) of the signal, separating the spectrum of this signal into two areas with fundamentally different structures of harmonics. The distribution of the threshold wavelength along the coordinate axes can differ in remarkable anisotropy. This is marked by the azimuthal variation in the autocorrelation radius approximated by the elliptical contour. As a consequence, the signal separation by the wavelength is reduced to averaging in the sliding elliptical window, with semiaxes being equal to the autocorrelation radius in two mutually orthogonal directions. Finally, extended elements are traced in the structure of components with different wavelengths \(\lambda\), correlated with a priori known manifestations of fracture tectonics, manifested at different depths. The complex of areal estimations described above is completed by deep geostructural reconstructions based on the analysis of landforms of the Earth's surface. The physical foundations of the method and their correspondence to geological and engineering formulation of the problem are considered in [10]. The main idea is in the interpretation of the presence of periodic and quasiperiodic components in the structure of the spatial geological-geophysical signal by the standing wave, shaping  
\[K(x)=A\cos(kx)\cos(\omega t-\varphi)\]  
in the spatial structure of nonequilibrium geological media [34; 35]. Its wave dynamics are caused by periodic transgressive-regressive processes and regular tectonic-magmatic activations, covering both the entire Earth's crust and the particular small vicinity of the point within the considered geoblock. Since the geological environment is a spatially distributed system, the documented vibrations of its individual elements are able to propagate in the volume of rock complexes, forming the waves. In the volume of the layered mining massif, they are recorded, in particular, as an alternation of synforms and antiforms with a definite step in the relief of the interface between any pair of structural-constitutional complexes.