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I believe Kusumoto (2015, 2016a, 2016b) was able to obtain results that coincided with seismic surveys since he estimated the fault dip in normal fault regions by the maximum eigenvector of the tensor.
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As to why the dip of normal fault was given by the dip of the maximum eigenvector of the gravity gradient tensor, I considered that the lower part of the boundary structure (fault) exists inside the low-density area more than its upper part.
We estimated the dip distribution of Oita Kumamoto Tectonic Line located in central Kyushu, Japan, by using the dip of the maximum eigenvector of the gravity gradient tensor.
As indicated by Beiki and Pedersen (2010), the maximum eigenvector of the gravity gradient tensor points to the causative body of the gravity anomaly (Fig. 1a).
When the sedimentary layer is in contact with the basement by normal fault, the dip of the maximum eigenvector follows the dip of the normal fault.
Therefore, because the gravity gradient tensor is most sensitive to the subsurface structures near the surface, the structure shown in Fig. 5a was considered a high-density body that intruded into the low-density layer, and the dip of the normal fault was given by the dip of the maximum eigenvector.
ID is dominated by the maximum compressive strain and CS by the maximum shear strain.
Deconvolution was performed by the Maximum Likelihood Estimation (MLE) algorithm.
Maximum speed (mm/second), defined by the maximum speed reached by the hand movement.
Regions are ranked by the maximum of the enrichment values.
Regression coefficients were estimated by the maximum likelihood method.
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