## 3 Results and Discussion
### The Geodynamic Model Examples
#### 3.2.2 Model of the Quasi-Plastic Deformation of Rocks
Let us next consider the case of interlayering of anisotropic strata. Each layer of this model is characterized by the electrical conductivities \(\sigma_{11}^{i}\), \(\sigma_{22}^{i}\) (in the case of electric conductivity tensor reduction to a diagonal form), and \(\alpha_{i}\) by the rotation angle of the anisotropy tensor relative to the selected coordinate system:  
\[\sigma_{i}= \begin{pmatrix}\sigma_{11}^{i}\cos^{2}a_{i}+\sigma_{22}^{i}\sin^{ 2}\alpha_{i}&(\sigma_{22}^{i}-\sigma_{11}^{i})\cos\alpha_{i}\sin\alpha_{i}\\ (\sigma_{22}^{i}-\sigma_{11}^{i})\cos\alpha_{i}\sin\alpha_{i}&\sigma_{11}^{i} \sin^{2}\alpha_{i}+\sigma_{22}^{i}\cos^{2}\alpha_{i}\end{pmatrix} .\]  
Each layer has a thickness of \(h_{i}\). The described model is consistent with model (Appendix A, Equation (A9)). We will next consider the dependence of the effective tensor of resistivity's macroscale anisotropy on changes in the anisotropic characteristics of the intermediate layer. For this purpose, calculations were carried out for a three-layer model with the following parameters:  
\(\sigma_{1}=0.1,\ h_{1}=0.01,\)  
\(\sigma_{11}^{2}=0.1,\ \sigma_{22}^{2}=0.2,\ \alpha_{2}=[0.2\pi],\ h_{2}=0.01,\)  
\(\sigma_{11}^{3}=0.1,h_{3}=0.01.\)In this model, the angle of rotation of the anisotropy tensor of the second layer was changed from 0 to \(2\pi\). Graphs of changes in the coefficients of macroscale anisotropy, \(k_{11}^{12}=\sqrt{\frac{\rho_{12}}{\rho_{11}}}\) and \(k_{11}^{22}=\sqrt{\frac{\rho_{22}}{\rho_{11}}}\) depending on the angle, are shown in Figure 11. From the behavior of these graphs, we observe that the diagonal elements of the macroscale anisotropy tensor change slightly depending on the angle rotation, while the off-diagonal elements change very significantly. The absolute value of the off-diagonal elements is changed to the measurable value. A similar approach to calculating the effective parameters is valid in any other orthogonal coordinate system where the coordinate planes coincide with the planes of discontinuity in the electromagnetic parameters. In other words, when the representation in a certain coordinate system is valid, the description of the microstructure takes the form of a product of isolated functions of coordinates in a given coordinate system. As an example, consider a cylindrical coordinate system, which is important for studying the dynamics of physico-electric parameters associated with the destruction of rocks near production boreholes. Thus, in the examples considered for a Cartesian coordinate system and for a cylindrical one the macro anisotropic electrical parameters became gradient anisotropic media when passing from one coordinate system to another. Obtaining such information is associated with some methodological difficulties. The known technique of azimuthal resistivity sounding (ARS) is aimed at measuring the apparent anisotropy in direct current methods. However, there are no grounds to unambiguously recognize this setup as the only possible option for measuring the anisotropy of the electric conductivity of the media, since other installations also carry information about the anisotropy of the media.