## 6 Discussion
### Triads
Threshold tension \(\tau_{*}\) at which destruction occurs, i.e., the sides of the fault shift and a rupture occurs, generally speaking, is the lower, the larger the linear dimensions of the fault \(l\):  
\[\tau_{*}=Cl^{-m}. \tag{26}\]  
\[N_{-}<N_{+}. \tag{24}\]0 Time dependence of the properties of symmetric triads. From top to bottom: earthquake frequency, activation (blue), and deactivation (red) factors. Here \(C\) is the dimensional coefficient of proportionality, depending on the properties of rocks in the selected volume, \(m>0\). Then, the largest fault reaches the threshold first. Its destruction is manifested in the form of the main shock of an earthquake with a magnitude \(M_{0}\). If the \(C\) parameter is uniformly distributed over the source volume, then foreshocks do not arise. Aftershocks appear due to the fact that after the main shock, the general external stress is partially removed, and the remaining stress is redistributed in a complex way throughout the volume. The local over-tensions arise, in such a way that smaller faults than the one that generated the main shock can be activated and give repeated tremors. This is how we can imagine the emergence of a shortened classical triad. In some cases, the specific distribution of faults in terms of \(l\) and the distribution of local stresses may turn out to be such that not a single aftershock occurs. It is possible that such a situation occurs when the GTS is excited. The appearance of the mirror triad can be understood if we assume that the parameter \(C\) is not uniformly distributed over the volume, or rather, that there is a strong scatter in the \(C(l)\) values. Then a situation is possible when, before the largest fault is destroyed, smaller faults are activated, and foreshocks appear. A triad of tectonic earthquakes will appear. Whether it will be classical or mirror-like depends on the distribution of faults by the value of \(l\), on the dispersion of the \(C(l)\) coefficient, and on the mosaic of local stresses that arose after the main shock. As a summary, we point out that classical (normal) triads make up approximately 85% of all triads. Anomalous triads account for 15%, with mirrored, 10% and symmetrical, 5%. In this calculation, we excluded the GTS, which seem to form a special set of earthquakes. In the class of tectonic earthquakes, we found a subclass of the so-called mirror triads. A specific property of mirror triads is that, in contrast to classical triads, in which the number of aftershocks is greater than the number of foreshocks, in mirror triads the number of aftershocks is less than the number of foreshocks in the interval 24 h before and 24 h after the main shock. In many cases, there are no aftershocks at all. In addition to this, strong solitary earthquakes were discovered, which are not preceded by foreshocks, and after which there are no aftershocks. The mirror triads, these ghosts of the classical triads, are not only curious in themselves, but can most decisively influence our understanding of the alternative possibilities of the dynamics of lithosphere, leading to catastrophic earthquakes. In particular, we face a fundamental problem, the essence of which is to find the physical and geotectonic reasons for the apparent predominance of truncated classical triads in the seismic activity of the Earth. Concluding the discussion, we want to make a judgment, perhaps controversial, that [PERSON]'s law, like no other, gives us the opportunity to realize the uncertainty, incompleteness, and, in a certain sense, immaturity of the physics of earthquakes. So far, it is still possible and, in reality, there is a wide range of opinions on the unresolved issues of the Earth's seismicity. So far, everyone, in accordance with their idea of the nature of cognition, can see in the Omori law either an empirical formula convenient for approximating observations, or an indication of the deep physical meaning of hyperbolicity in the frequency of aftershocks after a strong earthquake.