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Lawrence et al. (2007) summarize that long-term changes of subsidence are expected to vary in a very repetitive way, that is, with plate-like deformation in the upper half of a tectonically deformed deformation band during the formation of the deformation—a behavior which may also be observed in the kinematic part of the megathrust realignment, particularly in the fore-arc ridges (see e.g., Esrada et al. 2015). In the case of a subsidence reduction (increase of the steepness of the horst subsidence) due to back-arc extension of the subduction zone, the deformation follows a more heterogeneous pattern, producing abrupt contraction and gradual extension to either side of the fault in a regular pattern (Lawrence et al. 2007).
The potential instability of the subduction zone might be identified and quantified by the distribution of the complex displacement map, which can be obtained using the knowledge of the weighted displacement field. The complexity of the subsidence pattern depends on the corrugation in the deformation boundaries, characterizing the solutions obtained with the InSAR/SBAS analysis. The role of the spatial and temporal baselines of the SAR instrument is clearly audible in the complex subsidence pattern; the longer the time series, the more stable the subsidence pattern is. Obviously, the optimal selection of the temporal and spatial baselines is an essential parameter in the InSAR/SBAS analysis.
Spearman’s rank correlation showed moderate congruence between SBAS estimates of subsidence and simulated values for scenario S2 with different runs (Table 3b; Supplementary Table S1). The median simulated and InSAR-derived subsidence values are 38 cm and 42 cm, respectively (see Fig. 6), with a median-to-mean ratio of 1.13 and an interquartile range of 0.39. The median simulated and InSAR-derived subsidence values are 39 cm and 42 cm, respectively (see Fig. 7), with a median-to-mean ratio of 1.15 and an interquartile range of 0.4.
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