Since the tidal bulge is misplaced relative to the gravitational Earth-Moon alignment, being about 0.3-2.4 degrees eastward of it [11; 12] due to the delay in reaction for the anelastic component of the Earth as a response to the tidal pull, a westerly-directed horizontal drag acts on the lithosphere and the continuously slows down Earth rotation [13]. The crux of the matter is that, besides the symmetric oscillatory motions, the nonlinear response of the low velocity zone (LVZ) breaks the symmetry of the tidal traveling wave on the Earth surface: the small asymmetry produces a net drift motion of any material point interacting with the gravitational wave force, in the direction following the rotation of the Moon. Therefore, detailed properties of the combined tidal oscillation and tidal drift depend on the degree of deformability of the lithosphere (a.k.a. Love and Shida numbers) due to its local temperature and geochemistry. These modulations act through two different mechanisms on the outer layers of the Solid Earth: the brittle and outermost part of the crust is elastically affected by tidal waves, which induce a stress variation in rocks that, depending on the local geodynamics, promotes or, on the contrary, can prevent the achievement of the critical breaking point, so that it plays a statistically significant role in fault activation [14; 15; 16], while solid tides actively modulate plate motion at low frequencies over geological periods [17; 18] due to a heterogeneous dissipation of the tidal torque at the LVZ level. The issue of the tidal triggering of seismicity is not trivial, since it is necessary to take into account not only of the effect of Earth tides, but also variations in pore and confinement pressure, the orientation of the DC (Double Couple contribution) in relation with focal mechanism, and CLVD (Compensated Linear Vector Dipole) of earthquakes and local geophysical heterogeneities. To make matters even more complicated, a further difficulty must be considered: the observed seismicity spans up to 11 orders of magnitude over time (from 10 s typical of microseismicity up to 10\({}^{12}\) s for earthquakes recurrence time intervals), and 14 concerning to energy (if one considers events ranging from M\({}_{w}\) 0 to 9.5) and seven in space (a M\({}_{w}\) 9.0 can breaks crust up to 1000 km); this creates an enormous obstacle of both resolution and saturation, catalog incompleteness [19], and unreliability of statistical data. Finally, to the technical complexity of measuring real stress, we add the estimation of uncertainties of seismic parameters such as magnitude and depth. Beyond the triggering mechanism, in this work we focus on the possibility of highlighting the growth of critical states in the crust induced by stress accumulation in rocks through the measurement of correlations between some features of the tidal perturbation and seismic activity. There is a flurry of scientific articles devoted to understand how tides influence seismic activity, but only a few of them (e.g., [20]) so far extensively studied whether tidal perturbation might somehow provide information about the stability of faults close to rupture, with a few exceptions regarding some particular case studies (e.g., [21; 22]). The novelty of this article with respect to previous scientific literature consists in highlighting not only the variations in responsiveness of faults to stress while reaching the critical point, i.e., before a large earthquake, but it also shows how seismic response of faults changes over time as a function of their instability.