## 4 Results
### Analysis of the Spatial Structural Model  
The \(p\)-value resulting from the analysis of variance (ANOVA) -<2.2e\(-\)16-, indicates significant differences between the mean elevations per basin, confirming the influence of the basin factor (Figure 5A).  
Global trend analysis in the structural model was carried out through graphic analysis. Figure 3 discretely shows a growing trend of rock glacier elevation toward the east. This analysis has been complemented with a dispersion diagram of the elevation with respect to the geographical position (latitude and longitude) (Figure 5B). This diagram allows us to assume the shape of an inclined plane determined by a polynomial equation for the global trend, whose greatest slope is found in the west-east direction.  
For the second stochastic component of the structural model 8(s), the omnidirectional and directional semivariograms were calculated at 0\({}^{\circ}\), 45\({}^{\circ}\), 90\({}^{\circ}\), and 135\({}^{\circ}\) (Figure 6).  
Spatial autocorrelation at elevations up to an approximate distance of 1.0 (approximately 100 Km) has been confirmed in the omnidirectional semivariogram, with a significant micro-variability at minimum distances of the order of \(\pm\) 200 m. The directional semivariograms reveal the direction 90\({}^{\circ}\) as the lowest micro-variability (178 m). This is of greater autocorrelation or less variability between the elevations of the rock glaciers (Figure 6).  
Figure 4: Results of different criteria applied to DInSAR and Optical data to determine the degree of activity. The rock glaciers identified as active in both techniques (DInSAR and Optical) are represented by red polygons, while light blue and black polygons indicate active and inactive rock glaciers according to the geomorphological or DInSAR technique, respectively. The results of both criteria were plotted in an optical image (A-upper left) and in five (ascending and descending) interferograms (B–F). No phase changes are observed in some rock glaciers classified as active according to geomorphological criteria. Interferograms B and D (late spring to early summer) show the highest degree of activity, while C and E interferograms (late summer to early autumn) have a lower degree of activity. The interferogram with the shortest temporal baseline (F) is the one with the least amount of creeping rock glaciers.  
The directional semivariograms per basin show some differences with respect to general behavior, since not all basins have spatial autocorrelation in the four main directions. This is the case of the Tupungato, Patos, Choapa, and Castano basins which, in at least one direction, do not have anisotropy. The directions where there is autocorrelation vary according to the basin and have a maximum range of 0.1 to 0.2 (10 to 20 Km). In addition, some basins display lower microvariability, reaching values of up to 130 m (Figure 6).  
Figure 5: **(A)** Box and whisker plot considering the elevations of rock glaciers by basin. The width of the boxes is proportional to the amount of rock glaciers per basin. **(B)** Scatter diagram of elevation with respect to latitude and longitude.  
Figure 6: Omnidirectional and directional semivariograms of the whole study area and differentiated according to the basin. The x-axis in all the graphs indicates the distance expressed in decimal degrees. Note that in the latitudinal direction, one-degree represents 111.3 Km, while in the longitudinal direction, this relationship changes. At 30\({}^{\circ}\) and 35\({}^{\circ}\) south latitude, one-degree represents 96.4 and 91.2 Km, respectively.