## 3 Results  
This section shows the results of data processing of DInSAR and DInSAR images and the profiles along the survey line and the valley line showing ice surface topography, ice bed topography, hydraulic head, and radargram. Figure 2 shows an example of a one-day DInSAR image generated from the SAR images obtained on 16 and 17 June 2010. Interferometric fringes are equi-displacement lines in every half wavelength LOS direction while the density of fringes represents strain rate. The yellow line connects the maximum ice velocity points across the ice flow at the center of the valley, while the blue line is one of the IPR survey routes close to the yellow line. Note that part of the yellow line is hidden under the blue line, but they share the same starting and ending nodes. Radargram can be observed along the blue survey line but not along the yellow line. Those lines are used to compare the ice surface and bottom topography. Figure 2: An example of one-day DInSAR images (the pair of [20100616_20100617]). The yellow line is the steepest ice-velocity gradient line at the center of the valley while the blue line is one of the IPR routes close to the white line. White boxes are image areas for Figure 4 (smaller one) and Figure 6 (bigger one), respectively. Note that part of the yellow line is hidden under the blue line, but they share the same starting and ending nodes. Figure 3 shows an example of DDInSAR image generated by subtracting the DInSAR pair [20100616,20100617] from the pair [20110502-20110503] (also shown in Figure 4e). Most of the constant glacial flow signal were deleted. Tidal deflection signal near the grounding line of Campbell Glacier and Priestley Glacier can be seen, of which tidal fringes over Campbell Glacier Tongue were analyzed by [PERSON] and [PERSON] [19]. Fringes over landfast sea ice near Campbell Glacier Tongue have also been reported by [PERSON] and [PERSON] [22] as a combination of tidal and glacial stress. Possible grounding lines and a hinge line were drawn in black and white lines near the Campbell Glacier Tongue. Apart from them, there are two velocity anomalies at 11-15 km inland from the grounding line of the Campbell Glacier, which is the main focus of this study. Denoted as A and B in Figure 3, the anomalies are in circular shapes with radii of \(\sim\)800 m. The centers of the circles are located 14.7 km (A) and 11.3 km (B) upstream from the grounding line. Velocity anomalies are \(-\)0.9 cm/day for the anomaly A and 2.7 cm/day for the anomaly B, both in LOS direction in this image. The two anomalies are in the central valley of the glacier along the profile lines. The IPR survey line (blue) crosses the center of A only but only a part of B. The intended profile line in yellow is drawn to cross the two centers of A and B to investigate the ice surface and bottom topography. A series of DDInSAR images in Figure 4 shows the change of anomalies in location, shape, and magnitude. Dotted circles are drawn based on Figure 4e and have the same location and size in all sub-images for comparison. The locations of two anomalies are almost identical even though the amplitude fluctuates. Exceptions are Figure 4b,c where there exists only one anomaly and the locations are between A and B. Particularly in Figure 4c, some a fluvial feature appears to be flowing out of the circular anomaly, implying the action of basal water. Figure 3: An example of DDInSAR image by subtracting the DInSAR pair [20100616-20100617] from the pair [20110502-20110503], also shown in Figure 4e. A and B are the velocity anomalies found in the central valley along the profile lines. Note that dense fringes are tidal deflection at the hinge zones of Priestly Glacier (bottom) and Campbell Glacier (top). The possible grounding lines and hinge line were drawn in black and white lines near the Campbell Ice Tongue.