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Article

Temporal Variations in Ice Thickness of the Shirase Glacier Derived from Cryosat-2/SIRAL Data

by
Yurina Satake
1 and
Kazuki Nakamura
2,*
1
Graduate School of Engineering, Nihon University, Fukushima 963-8642, Japan
2
College of Engineering, Nihon University, Fukushima 963-8642, Japan
*
Author to whom correspondence should be addressed.
Remote Sens. 2023, 15(5), 1205; https://doi.org/10.3390/rs15051205
Submission received: 30 December 2022 / Revised: 9 February 2023 / Accepted: 14 February 2023 / Published: 22 February 2023
(This article belongs to the Special Issue Selected Papers from the “International Symposium on Remote Sensing 2022”)
Browse Figures
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Abstract

:
This study presents the feasibility of estimating the ice thickness of the Shirase Glacier using the synthetic aperture interferometric radar altimeter (SIRAL) on board the CryoSat-2 and the interannual variation of the ice thickness of the Shirase Glacier in 2011–2020. The SIRAL data were converted to ice thickness by assuming hydrostatic equilibrium, and the results showed that the ice thickness decreased from the grounding line to the terminus of the glacier. Furthermore, the ice thickness decreased 30 km downstream from the grounding line of the glacier in 2012 and 2017, and decreased 55 km and 60 km downstream from the grounding line of the glacier at other times, which was attributed to the discharge of landfast ice and the retreat of the glacier terminus. When the flow of glacial ice can be reasonably approximated as an incompressible fluid, and the law of conservation of mass can be applied to the ice stream, the multiple of the velocity and the underlying ice thickness under a constant ice density can be shown to correspond to the equation of continuity. Consequently, this study revealed that the ice thickness decreases with accelerating flow velocity, which is coincident with past outflow events.

Graphical Abstract

1. Introduction

The Antarctic ice sheet accounts for approximately 90% of the ice on Earth. When the ice sheet melts and flows out into the ocean, the sea level will rise by approximately 58 m [1]. The bottom water in the vicinity of Antarctica, which is cold seawater that is highly salinized by sea ice formation, sinks into the deeper layers of the ocean, driving the general circulation of the ocean. This general circulation plays a role in transporting heat to the entire globe. Therefore, quantitatively understanding the ice discharge from the Antarctic ice sheet is important for understanding global changes.
In recent years, glacier flow velocity has increased rapidly in West Antarctica due to basal melting of the ice shelf, and the current ice mass balance, which is the sum of snow accumulation and ice mass discharge, indicates that discharge exceeds accumulation [2]. It has been reported that the ice flow in the Pine Island Glacier in West Antarctica has accelerated, and its ice thickness has decreased [3]. While the ice mass balance in East Antarctica is considered to be almost balanced [4,5], the ice mass balance of the Shirase Drainage Basin, which includes the fastest flowing glacier, the Shirase Glacier, has been estimated to be −1.9 Gt a−1 [6]. As in West Antarctica, it was observed that the basal melting beneath the tongue of the Shirase Glacier caused an inflow of southward-flowing warm water from offshore [7], but the interannual variability of the inflow of warm water needs to be considered. Therefore, it is important to accurately measure the ice thickness of the glacier in order to continuously monitor the trend of the ice mass balance.
The Antarctic region has a severe weather environment, as well as polar nights and crevasses that make field observation hazardous and difficult. Satellite remote sensing techniques are capable of performing continuous spatiotemporal observation of an area and are effective for studying target areas in the cryosphere. The ice flow estimation of the Shirase Glacier using remote sensing techniques began with the use of two aerial photographs of the floating tongue taken at different times [8,9], enabling the assessment of the ice flow. The results obtained using the interferometric synthetic aperture radar (interferometric SAR or InSAR) technique showed that the velocity distribution around the same floating ice tongue ranged from 2.2 to 2.6 km a−1 [10]; furthermore, the flow velocity at the grounding line of the Shirase Glacier, which was 2.3 km a−1, made it one of the fastest flowing glaciers, and extremely fast compared to most other known glaciers, since the mean flow velocity of the 9 glaciers in East Antarctica is 1.0 km a−1 [11]. The application of the offset tracking method to intensity images derived from SAR has been shown to be effective for fast-flowing glaciers such as the Shirase Glacier (e.g., [12]), and the flow velocity at the grounding line has shown no significant changes in the last 24 years [13], while interannual variation in ice thickness remains insufficiently studied.
Although optical sensors are affected by clouds, microwave sensors can be used in polar regions because of their high atmospheric transparency, making observations possible under any weather condition. The estimation of ice thickness in cases where the ice shelves are covered by several thousand kilometers of ice in Antarctica can be accomplished by applying hydrostatic equilibrium to radar altimeter (RA) data obtained from the ERS-1, launched by the European Space Agency (ESA), with results as reported in [14]. Most recently, in 2010, CryoSat-2 was launched by the ESA, and the estimation of sea ice thickness has revealed a decrease in sea ice volume in the Arctic Ocean [15]. In the Antarctic region, CryoSat-2 is capable of greater coverage than conventional satellite altimeters, and it was able to show that mean elevation has decreased across the entire Antarctic ice sheet [16]. Furthermore, ice thicknesses were obtained for ice shelves by applying hydrostatic equilibrium to CryoSat-2 data [17]. As CryoSat-2 has also been used to observe the area around the Shirase Glacier, we were able to obtain the ice thickness of the glacier.
This study presents the possibility of estimating the ice thickness of the Shirase Glacier using microwave radar altimeter data obtained from CryoSat-2, as well as the interannual variation derived from the estimated ice thickness.

2. Materials and Methods

2.1. Estimation of the Area of the Shirase Glacier

The Shirase Glacier is located approximately 150 km south of Syowa Station (Figure 1a). The drainage basin of the Shirase Glacier is located in Dronning Maud Land, and forms part of the Mizuho Plateau [18,19]. The drainage basin of the Shirase Glacier is also the terminus of the ice stream of the Shirase Glacier, which reaches Lützow-Holm Bay in the form of a floating ice tongue (Figure 1a). Given that the floating ice tongue is surrounded by the landfast ice that covers most of Lützow-Holm Bay, the glacier mass has no direct outlet from the bay [20].
Focusing on the interannual variation in ice thickness in the calving area of the Shirase Glacier, the grounding line of the glacier is the boundary between the bedrock under the ice sheet and the ocean; the glacier ice in the region downstream from the grounding line floats into the ocean as an ice tongue. Hence, the ice thickness can be estimated by applying hydrostatic equilibrium to the calving area of the Shirase Glacier. This study used CryoSat-2/SIRAL data, which was obtained by observing the downstream region of the Shirase Glacier from its grounding line. The grounding line was determined on the basis of the detailed detection results obtained using the InSAR technique [21]. To estimate the ice thickness, the central streamline of the glacier had to be determined, and it was derived from the image acquired by the Landsat-8 in 2016 in the middle of the analysis period of this study. Then, the area to be analyzed was set to a width of ±3 km from the central streamline. The true-color composite Landsat-8 image used in this study is shown in Figure 1.
The elevation of the exposed rock area is unaffected by ice sheet fluctuations, since that area is not covered by the ice sheet. Hence, the accuracy of the CryoSat-2/SIRAL data can be validated by examining the long-term change in elevation in the exposed rock area. However, as described in Section 2.2, the measured position was dispersed in the exposed rock area, and then the measured position was nonuniform along the track of the satellite. This made it difficult to obtain the elevation at the desired measurement position, because the surface of the exposed rock was characterized by large undulations, which caused a deviation from the original measurement position of the CryoSat-2.
Consequently, the accuracy of the SIRAL observation performed in this study was examined on the basis of temporal changes in elevation on a pond in the exposed rock area, because it is difficult to validate the accuracy of elevation obtained by examining temporal changes in SIRAL data at the exposed rock itself. Three exposed rock areas, Rundvågshetta, Skallevikshalsen and Skallen, are located approximately 10 km east of the terminus of the Shirase Glacier. In each exposed rock area, there are three ponds, Maruwan O-ike, Dairi Ike and Skallen O-ike (Figure 1b). The ponds are 200–300 m wide and 600–800 m long, and there are more than a dozen data of SIRAL datasets obtained from the ponds during the period analyzed in this study. Skallen O-ike originates from drift melt water, while Dairi Ike originates from glacial melt water [23]. Maruwan O-ike is a depression surrounded by hills and filled with water, which can be observed from the 1:25,000 topographic map published by the GSI. Hence, Maruwan O-ike can be regarded as being similar to Dairi Ike and Skallen O-ike. In addition to these geographical features, the three ponds are always filled with fresh water, and the ponds’ surfaces can be considered to remain at a constant height. Therefore, the accuracy of the SIRAL data in this study was validated by examining long-term changes in the elevations of the three ponds.

2.2. CryoSat-2/SIRAL Data

Cryosat-2 was launched by ESA in 2010. The SAR interferometric radar altimeter (SIRAL) on board is a microwave altimeter operating in the Ku band (13.6 GHz). The SIRAL has three different observation modes, depending on the features of what is being observed: low-resolution mode, SAR mode, and SAR interferometric (SIN) mode. The low-resolution mode is used to perform observations over ice sheet interiors and oceans. The SAR mode is used to perform observations over sea ice and ocean areas, and the SIN mode is used to perform observations around ice sheet margins and mountain glaciers. The specifications of CryoSat-2/SIRAL are shown in Table 1.
The Shirase Glacier was observed using the SIN mode because of its location in the coastal part of the ice sheet, connected to the southern part of Lützow-Holm Bay. Therefore, the SIN mode data used in this study were of level 2, with ice baseline D products. The products covering the Shirase Glacier, in which atmospheric and tidal corrections are applied, are available from 2011 to 2020. The amounts of CryoSat-2/SIRAL data are summarized in Table 2 (details regarding acquisition day are listed in Table A1).
Conventional radar altimeters have a high degree of error in the form of slope-induced error in elevations as a result of its large footprint [24,25]. The radar altimeter measures the closest point within this footprint, which is not the same as the subsatellite location in the case of irregular terrain with slopes. This leads to problems in accurately determining elevation using a radar altimeter, which performs measurements within a footprint that includes large slopes such as the ice sheet margin [26]. To solve this problem, the CryoSat-2/SIRAL employs the SIN mode. Based on the Delay/Doppler RA principle [27], the resolution of the SIN mode is improved to approximately 300 m in the along-track direction as a result of the segmentalized footprint in low-resolution mode. Because the footprint size is improved only in the along-track direction, the resolution in the across-track direction remains approximately 1.6 km, the same as in low-resolution mode [28].
Furthermore, SIN mode uses the phase difference between the reflected waves received by the two antennas on the CryoSat-2/SIRAL equipment in order to determine the arrival angle of the former reflected wave, to improve the accuracy of elevation measurement. In SIN mode, there is an offset in the across-track direction in the ground track projected from the satellite location, because the measurement position in SIN mode does not correspond to the location of the subsatellite in the case of irregular terrain with slopes. Hence, the measurement position when using SIN mode is ambiguous, as shown in Figure 2. Therefore, in this study, gridding was applied to the observation results obtained using SIN mode, as described in Section S3, in order to be able to analyze the data.
Previous research has shown that performing backscatter correction on radar altimeter data can reduce spurious changes in elevation [29,30]. The snowfall on the Shirase Glacier was difficult to observe in situ due to the fast-flowing nature of the glacier; therefore, we were unable to obtain snowfall data. Through personal communication with one of the co-authors of [7], a snow depth on the glacier of 3.1 m at a location approximately 20 km downstream from the grounding line in January 2020, determined via helicopter transfer onto the glacier, was obtained. The microwave penetration depth of the CryoSat-2/SIRAL (Ku-band: 13.575 GHz) for the snow layer was calculated to be 42.6 m, assuming a density and dielectric constant of 0.3 g cm−3 and 1.47–j0.0001 [31], respectively. Since the penetration depth was one order larger than the measured snow depth, we considered the snow on the glacier to make a negligible contribution to the backscatter of CryoSat-2/SIRAL. Therefore, we did not apply backscatter correction to the CryoSat-2/SIRAL data used in this study.

2.3. ALOS World 3D Data

The accuracy of the CryoSat-2/SIRAL data was validated by comparing, for the ponds in the exposed rock area described in Section 2.1, the elevations obtained from the SIRAL data with those obtained using another digital elevation model (DEM) and from ground-based control point data. In this section, the data used for the DEM comparison are described. The results obtained using the ground-based control point data are described in Section 2.4.
The Advanced Land Observing Satellite (ALOS) was launched by the Japan Aerospace Exploration Agency (JAXA) on an H-IIA booster in January 2006. The ALOS has three remote sensing instruments: the Panchromatic Remote-sensing Instrument for Stereo Mapping (PRISM) for digital elevation mapping, the Advanced Visible and Near Infrared Radiometer type 2 (AVNIR-2) for precise land coverage observation, and the Phased Array type L-band Synthetic Aperture Radar (PALSAR) for day-and-night and all-weather land observation. ALOS World 3D (AW3D), a digital surface model (DSM), was compiled from images of approximately 3 million scenes acquired by the ALOS/PRISM in 2006–2011, and a product corresponding to a resolution of 30 m (AW3D30) was released in an open and free data format by the JAXA [32].
Since AW3D30 data were available for the exposed rock area, including the ponds, this study examined the accuracy of the CryoSat-2/SIRAL data by performing a comparison with the AW3D30 height. In addition, AW3D30 data were not only available for the ice shelves, but also for the floating ice tongue of the Shirase Glacier. Hence, this study also used AW3D30 height as the reference height to screen ice thickness estimation results to remove outliers (described in detail in Section S2). A color-coded map derived from AW3D30 height data is shown in Figure 3.

2.4. Control Point Survey Results

The leveling results obtained at the spot height in the exposed rock area used in this study were available via the topographic map provided by the Geospatial Information Authority of Japan (GSI). The 1:25,000 topographic map was compiled from aerial photographs and the results of control point surveys implemented by the Japanese Antarctic Research Expedition.
In this study, the leveling results at the spot height of Dairi Ike (hereafter referred to as the GSI height), corresponding to a height of 50 m, were found to be available for use. Therefore, the height obtained on the basis of CryoSat-2/SIRAL data was compared not only to that obtained using AW3D30 data, but also to the GSI height.

2.5. Conversion of CryoSat-2/SIRAL Data into Ice Thickness

In this study, the acquired CryoSat-2/SIRAL data were converted into the ice thickness of the Shirase Glacier using the following procedure: firstly, the CryoSat-2/SIRAL data were converted into height; then, the CryoSat-2 height results were screened for outlier data; and finally, the CryoSat-2 heights were gridded and converted into ice thickness. These procedures are described in detail in the Supplementary Materials. The percentage of CryoSat-2/SIRAL data that were excluded as outliers when performing the conversion to ice thickness using the above procedures is summarized in Table 3 as quality control data.

3. Results

3.1. Comparison of CryoSat-2 Height with AW3D30 DSM

Table 4 shows the means and standard deviations of the CryoSat-2 height and the AW3D30 height, calculated for each of the ponds in the exposed rock areas, as described in Section 2.1. The standard deviations of the CryoSat-2 height and the AW3D30 height were 1.19 m and 0.63 m, respectively. When the GSI height was used as the true value, the RMSEs of the CryoSat-2 height and the AW3D30 height were 1.6 m and 1.1 m, respectively. This can be attributed to the differences in pixel spacing between the CryoSat-2 height and the AW3D30 height, while the standard deviations are comparable when considering the size of pixel spacing for both heights.
Furthermore, an absolute validation of AW3D has been performed on the basis of 5121 ground-based checkpoints all over the world, resulting in an RMSE of 4.40 m [32]. The RMSE of the CryoSat-2 height was 4.04 m when the AW3D30 height was used as the true value, suggesting that the accuracy of the obtained CryoSat-2 height is similar to the accuracy of the AW3D30 height.
Therefore, the accuracy of ice thickness estimation δ H , determined on the basis of the CryoSat-2 height, can be approximated as δ H = 7.92 × δ h using Equation (S5), with a resultant δ H of ±9.5 m, where δ h is substituted by the standard deviation of ±1.2 m. Likewise, the accuracy of the estimation determined on the basis of AW3D30 is ±4.8 m.

3.2. Estimate of Ice Thickness

A color-coded map of the estimated ice thickness distribution for the Shirase Glacier, as derived from the AW3D30 height and the annual CryoSat-2 height, is presented in Figure 4. In addition, Figure 5 shows the profile of the mean ice thickness between 2011 and 2020, extracted at 5 km intervals along the central streamline of the glacier. In this figure, the line indicates the mean ice thickness and the error bar indicates the accuracy of the estimated ice thickness obtained in Section 3.1.
In Figure 5a, the mean ice thickness derived from the CryoSat-2 height was 529.6 ± 9.5 m at the location 10 km downstream from the grounding line and 299.4 ± 9.5 m at the location 60 km downstream from the grounding line. In Figure 5b, the mean ice thickness derived from the AW3D30 height was 629.0 ± 4.8 m at the location 5 km downstream from the grounding line and 302.3 ± 4.8 m at the location 40 km downstream from the grounding line. These results show that the ice thickness decreased between its periphery at the grounding line and the terminus of the Shirase Glacier. In addition, Figure 6 shows the relationship between the ice thickness estimated on the basis of the AW3D30 height and that estimated on the basis of the CryoSat-2 height in the range of 10–40 km downstream from the grounding line. The ice thicknesses estimated on the basis of the AW3D30 height and the CryoSat-2 height were positively correlated and in good agreement, with a correlation coefficient of 0.97.

4. Discussion

4.1. Decline of Ice Thickness with Distance from Grounding Line

It can be seen from Figure 5a that the estimated ice thickness decreased from the grounding line to the terminus of the Shirase Glacier, but that this trend between the grounding line and 30 km downstream differed from that between 35 km downstream from the grounding line and the terminus of the glacier. This decline H d e c is expressed as a function of distance D from the grounding line, as follows:
H d e c = { − 8.60 × D + 640.92         ( D < 35   km ) − 0.03 × D + 312.56         ( D ≥ 35   km ) .
An annual H d e c in D < 35 km of 19.8 m was obtained on the basis of a flow velocity of 2.3 km a−1 [13]. This is comparable to the decline in estimated ice thickness obtained using the ice radar, which was 7–16 m, resulting from basal melting, located approximately 20 km downstream from the grounding line [7]; however, it is possible that there are other factors at play, as discussed in Section 4.2. Meanwhile, an annual H d e c of 0.1 m was obtained in D ≥ 35 km, suggesting that the contribution of basal melting to the difference in ice thickness was minimal.

4.2. Fluctuation of Ice Thickness with the Breaking Away of Glacier and Landfast Ice

In 1998 [12], 2005 [33] and 2018 [34], events occurred in which ice belonging to the floating ice tongue and the landfast ice surrounding it broke up and flowed out into Lützow-Holm Bay, resulting in an acceleration of the flow velocities of the Shirase Glacier. The volume of ice discharge V can be determined as follows:
V = H × v × w ,
where H is the ice thickness, v is the flow velocity and w is the flow width. Since there has been no significant change in the ice flow velocity at the grounding line over the past 20 years [13], w can be regarded as being constant. Hence, the ice thickness and the flow velocity are the dominant factors influencing the ice discharge from the glacier.
The flow of glacial ice can be reasonably approximated as an incompressible fluid, and the law of conservation of mass can be applied to the ice stream. The multiplication of the velocity v by the underlying ice thickness H under constant ice density corresponds to the equation of continuity, as shown in the following relation:
( H + Δ H ) v = H ( v + Δ v ) ,
where Δ H is the decline from H and Δ v is the acceleration from v . This is shown schematically in Figure 7. Rearranging Equation (3) for H gives the following:
H = Δ H Δ v v .
Equation (4) states that the ice thickness decreases with the acceleration of flow velocity.
To clarify the decreases in ice thickness on the Shirase Glacier that coincided with past outflow events, we investigated the relationship between ice thickness and flow velocity. Changes in the ice thickness of the glacier were recorded with temporal changes such as the occurrence of basal melting and past events. To investigate whether the changes in ice thickness controlled those events, we focused on the significant change in ice thickness at a location 30 km downstream from the grounding line in Figure 5a. To examine the association between changes in ice thickness at the location 30 km downstream from the grounding line and past events, we also examined changes in ice thickness at a location 25 km downstream from the grounding line. This is because the ice thickness profile at 30 km downstream should have experienced the same past changes in ice thickness as those at 25 km downstream. The annual mean values of ice thicknesses at 25 km and 30 km downstream from the grounding line are shown in Figure 8.
Although the ice thickness in 1998 was not determined in this study, the glacier would have advanced approximately 30 km in 14 years when assuming a flow velocity of 2.3 km a−1 at the grounding line of Shirase Glacier [13]. In the profile at 30 km in Figure 8, the ice thickness in 2012 (14 years after 1998) was 330.0 m, while the mean thickness for 2012–2020 was 356.5 m; therefore, the difference from the mean was 26.5 m. Hence, the profile at 30 km downstream in 2012 showed a lesser value than in other years. The change in ice thickness 30 km downstream from the grounding line in 2012 should be compared with that at 25 km downstream from the grounding line in 2010 (as there was less than a 5 km advance between 2010 and 2012); however, the ice thickness in 2010 was obtained in this study due to insufficient stacking for the analysis. Consequently, the ice thickness at 25 km downstream from the grounding line in 2011 was verified, and the profile at 25 km in 2011 presented in Figure 8 was the lesser, at 426.4 m (where the mean for 2012–2020 was 449.3 m). This was attributed to the acceleration in the glacier flow associated with the retreat of the terminus of the Shirase Glacier in 1998 [12]. Similarly, the ice thickness in 2005 was not determined, but the glacier would have advanced approximately 30 km in 12 years, and the profile at 30 km in 2017, presented in Figure 8, can be regarded as indicating the change 12 years after 2005. In this figure, the profile at 30 km in 2017 was 314.3 m, corresponding to a difference from the mean of 42.2 m and showing a lesser value compared to other years. The ice thickness 30 km downstream from the grounding line in 2017 was compared with that 25 km downstream from the grounding line in 2015. The profile 25 km downstream in 2015, presented in Figure 8, was 451.5 m, which was the smallest value between 2013 and 2016. This was attributed to the breaking up and flowing out of the southernmost landfast ice into Lützow-Holm Bay, which surrounds the terminus of the Shirase Glacier, in 2005 [33].
Since the Shirase Glacier has advanced since the retreat of its terminus in 2018 [35], it is expected that the terminus will indicate the change in ice thickness associated with the discharge of the floating ice tongue and its surrounding landfast ice occurring in March–April 2018. With the glacier advancing approximately 5 km in 2 years, the difference in ice thickness between 55 km and the 60 km downstream from the grounding line presented in Figure 5a was 26.0 m. If the same intensity of basal melting [7] is applied near the terminus of the Shirase Glacier, it is not clear whether the difference in ice thickness can be attributed to the event in 2018 or to basal melting. However, there was no significant change in ice thickness between 35 km downstream from the grounding line and the terminus of the glacier, whereby the change in ice thickness was determined to be 0.2 m per 5 km on the basis of a simple linear regression analysis. In other words, there might be no significant effect of the basal melting between 35 km downstream from the grounding line and the terminus of the glacier. Hence, the difference of ice thickness was attributed to the discharge of the floating ice tongue and its surrounding landfast ice in 2018.
Therefore, the decrease in ice thicknesses observed 30 km downstream from the grounding line in 2012 and 2017 and the mean ice thickness in the terminus of the Shirase Glacier during the analysis period were revealed to be a result of the acceleration of the glacier flow occurring as a result of the discharge of landfast ice and the terminus of the glacier.

5. Conclusions

This study demonstrated the estimation of the ice thickness of the Shirase Glacier by applying an assumption of hydrostatic equilibrium in the calving region of the glacier on the basis of CryoSat-2/SIRAL data from 2011 to 2020. To validate the accuracy of the CryoSat-2/SIRAL data, temporal changes in the elevation of ponds in exposed rock areas were investigated via a DSM of the AW3D30 and ground survey by means of GSI. The accuracy of the ice thickness estimation performed on the basis of the CryoSat-2 height was determined to be ±9.5 m, which was applied as a standard deviation.
The mean ice thickness profile along the central streamline of the Shirase Glacier indicates that the ice thickness decreases from the grounding line to the terminus of the glacier. In addition, the trend differed between (1) the range from the grounding line to 30 km downstream and (2) the range from 35 km downstream from the grounding line to the terminus of the glacier. An annual decline in ice thickness of 19.8 m was identified in (1), which is comparable to the estimated decline in ice thickness occurring due to basal melting. Meanwhile, a decline of 0.1 m was identified in (2), which suggests that basal melting makes little contribution to the ice thickness.
When the flow of glacial ice can be reasonably approximated as an incompressible fluid and the law of conservation of mass can be applied to the ice stream, the multiple of the velocity and the underlying ice thickness under a constant ice density corresponds to the equation of continuity. Changes in the ice thickness of the glacier occur as a result of temporal changes, such as basal melting, and past events, such as the breaking up and discharge of floating ice tongues and their surrounding landfast ice in Lützow-Holm Bay. To investigate the changes in ice thickness changes occurring as a result of such events in 1998, 2005 and 2018, we focused on the significant ice thickness change 30 km downstream from the grounding line.
Consequently, this study revealed that ice thickness decreases with increasing flow velocity, coinciding with past outflow events. In summary, the estimation of ice thickness performed using the CryoSat-2 height in this study is expected to contribute to accurate mass balance estimation of the Shirase Drainage Basin, since the results take into account interannual changes and discharge events of the Shirase Glacier and its surrounding landfast ice in Lützow-Holm Bay.

Supplementary Materials

The following supporting information can be downloaded at: https://www.mdpi.com/article/10.3390/rs15051205/s1. These materials describe the pre-processing steps referred to in Section 2.5. References [36,37] are cited in the Supplementary Materials.

Author Contributions

Conceptualization, Y.S. and K.N.; methodology, Y.S. and K.N.; software, Y.S. and K.N.; validation, Y.S. and K.N.; formal analysis, Y.S. and K.N.; investigation, Y.S. and K.N.; resources, Y.S. and K.N.; data curation, Y.S. and K.N.; writing—original draft preparation, Y.S.; writing—review and editing, K.N.; visualization, Y.S.; supervision, K.N.; project administration, K.N.; funding acquisition, K.N. All authors have read and agreed to the published version of the manuscript.

Funding

This work was funded in part by the Japan Society for the Promotion of Science Grant-in-Aid Scientific Research (C), under Grant 21K12214, in part by the Joint Research Program of the Institute of Low Temperature Science, Hokkaido University, under Grant 22G023, and in part by the National Institute of Polar Research through General Collaboration Project (2–25).

Data Availability Statement

The CryoSat-2/SIRAL data are available at https://cs2eo.org/ (accessed on 1 December 2022). The AW3D30 dataset is available at https://www.eorc.jaxa.jp/ALOS/en/dataset/aw3d30/aw3d30_e.htm (accessed on 1 December 2022). The Antarctica geospatial data are available at https://www.gsi.go.jp/antarctic/index-e.html (accessed on 1 December 2022).

Acknowledgments

This work was supported in part by the Japan Society for the Promotion of Science Grant-in-Aid Scientific Research (C), under Grant 21K12214, in part by the Joint Research Program of the Institute of Low Temperature Science, Hokkaido University, under Grant 22G023, and in part by the National Institute of Polar Research through General Collaboration Project (2–25).

Conflicts of Interest

The authors declare no conflict of interest.

Appendix A

Table A1 and Table A2 list the CryoSat-2/SIRAL data that we used to estimate the ice thickness of the Shirase Glacier and to validate the accuracy of the measured height, respectively.
Table
Table A1. The CryoSat-2/SIRAL data acquisition dates for the estimation of ice thickness.
Table A1. The CryoSat-2/SIRAL data acquisition dates for the estimation of ice thickness.
Date/OrbitDate/OrbitDate/OrbitDate/Orbit
06 Jan 2011/Descending11 Jan 2011/Ascending04 Feb 2011/Descending07 Feb 2011/Ascending
02 Mar 2011/Descending08 Mar 2011/Ascending31 Mar 2011/Descending06 Apr 2011/Ascending
29 Apr 2011/Descending05 May 2011/Ascending26 May 2011/Descending24 Jun 2011/Descending
30 Jun 2011/Ascending23 Jul 2011/Descending29 Jul 2011/Ascending19 Aug 2011/Descending
21 Aug 2011/Descending25 Aug 2011/Ascending15 Sep 2011/Descending17 Sep 2011/Descending
23 Sep 2011/Ascending16 Oct 2011/Descending21 Oct 2011/Ascending12 Nov 2011/Descending
14 Nov 2011/Descending17 Nov 2011/Ascending11 Dec 2011/Descending16 Dec 2011/Ascending
09 Jan 2012/Descending14 Jan 2012/Ascending07 Feb 2012/Descending10 Feb 2012/Ascending
05 Mar 2012/Descending07 Mar 2012/Descending10 Mar 2012/Ascending03 Apr 2012/Descending
08 Apr 2012/Ascending02 May 2012/Descending05 May 2012/Ascending07 May 2012/Ascending
29 May 2012/Descending31 May 2012/Descending03 Jun 2012/Ascending26 Jun 2012/Descending
02 Jul 2012/Ascending25 Jul 2012/Descending31 Jul 2012/Ascending21 Aug 2012/Descending
23 Aug 2012/Descending27 Aug 2012/Ascending19 Sep 2012/Descending25 Sep 2012/Ascending
18 Oct 2012/Descending24 Oct 2012/Ascending14 Nov 2012/Descending16 Nov 2012/Descending
20 Nov 2012/Ascending22 Nov 2012/Ascending13 Dec 2012/Descending19 Dec 2012/Ascending
11 Jan 2013/Descending17 Jan 2013/Ascending07 Feb 2013/Descending09 Feb 2013/Descending
13 Feb 2013/Ascending08 Mar 2013/Descending13 Mar 2013/Ascending06 Apr 2013/Descending
11 Apr 2013/Ascending05 May 2013/Descending08 May 2013/Ascending01 Jun 2013/Descending
06 Jun 2013/Descending30 Jun 2013/Descending05 Jul 2013/Ascending29 Jul 2013/Descending
03 Aug 2013/Ascending25 Aug 2013/Descending27 Aug 2013/Descending30 Aug 2013/Ascending
23 Sep 2013/Descending28 Sep 2013/Ascending02 Oct 2013/Ascending21 Oct 2013/Descending
27 Oct 2013/Ascending17 Nov 2013/Descending19 Nov 2013/Descending23 Nov 2013/Ascending
16 Dec 2013/Descending22 Dec 2013/Ascending14 Jan 2014/Descending20 Jan 2014/Ascending
10 Feb 2014/Descending12 Feb 2014/Descending16 Feb 2014/Ascending11 Mar 2014/Descending
15 Mar 2014/Ascending17 Mar 2014/Ascending09 Apr 2014/Descending15 Apr 2014/Ascending
08 May 2014/Descending04 Jun 2014/Descending06 Jun 2014/Descending08 Jun 2014/Ascending
10 Jun 2014/Ascending12 Jun 2014/Ascending03 Jul 2014/Descending08 Jul 2014/Ascending
01 Aug 2014/Descending06 Aug 2014/Ascending28 Aug 2014/Descending30 Aug 2014/Descending
02 Sep 2014/Ascending22 Sep 2014/Descending26 Sep 2014/Descending01 Oct 2014/Ascending
25 Oct 2014/Descending30 Oct 2014/Ascending21 Nov 2014/Descending23 Nov 2014/Descending
26 Nov 2014/Ascending20 Dec 2014/Descending25 Dec 2014/Ascending27 Dec 2014/Ascending
18 Jan 2015/Descending20 Jan 2015/Descending23 Jan 2015/Ascending15 Feb 2015/Descending
19 Feb 2015/Ascending14 Mar 2015/Descending20 Mar 2015/Ascending12 Apr 2015/Descending
18 Apr 2015/Ascending11 May 2015/Descending17 May 2015/Ascending07 Jun 2015/Descending
13 Jun 2015/Ascending06 Jul 2015/Descending12 Jul 2015/Ascending04 Aug 2015/Descending
10 Aug 2015/Ascending31 Aug 2015/Descending02 Sep 2015/Descending06 Sep 2015/Ascending
29 Sep 2015/Descending05 Oct 2015/Ascending28 Oct 2015/Descending02 Nov 2015/Ascending
22 Nov 2015/Descending24 Nov 2015/Descending26 Nov 2015/Descending29 Nov 2015/Ascending
30 Nov 2015/Descending23 Dec 2015/Descending28 Dec 2015/Ascending21 Jan 2016/Descending
26 Jan 2016/Ascending19 Feb 2016/Descending22 Feb 2016/Ascending17 Mar 2016/Descending
19 Mar 2016/Descending22 Mar 2016/Ascending15 Apr 2016/Descending20 Apr 2016/Ascending
14 May 2016/Descending19 May 2016/Ascending09 Jun 2016/Descending11 Jun 2016/Descending
15 Jun 2016/Ascending08 Jul 2016/Descending14 Jul 2016/Ascending06 Aug 2016/Descending
12 Aug 2016/Ascending29 Aug 2016/Descending02 Sep 2016/Descending04 Sep 2016/Descending
08 Sep 2016/Ascending01 Oct 2016/Descending07 Oct 2016/Ascending30 Oct 2016/Descending
05 Nov 2016/Ascending26 Nov 2016/Descending28 Nov 2016/Descending02 Dec 2016/Ascending
25 Dec 2016/Descending31 Dec 2016/Ascending23 Jan 2017/Descending25 Jan 2017/Descending
29 Jan 2017/Ascending21 Feb 2017/Descending24 Feb 2017/Ascending20 Mar 2017/Descending
25 Mar 2017/Ascending18 Apr 2017/Descending23 Apr 2017/Ascending17 May 2017/Descending
20 May 2017/Ascending22 May 2017/Ascending13 Jun 2017/Descending18 Jun 2017/Ascending
12 Jul 2017/Descending17 Jul 2017/Ascending10 Aug 2017/Descending15 Aug 2017/Ascending
06 Sep 2017/Descending08 Sep 2017/Descending11 Sep 2017/Ascending04 Oct 2017/Descending
10 Oct 2017/Ascending31 Oct 2017/Descending02 Nov 2017/Descending08 Nov 2017/Ascending
29 Nov 2017/Descending01 Dec 2017/Descending03 Dec 2017/Ascending05 Dec 2017/Ascending
28 Dec 2017/Descending03 Jan 2018/Ascending26 Jan 2018/Descending01 Feb 2018/Ascending
24 Feb 2018/Descending28 Feb 2018/Ascending29 Mar 2018/Ascending21 Apr 2018/Descending
27 Apr 2018/Ascending20 May 2018/Descending24 May 2018/Ascending16 Jun 2018/Descending
18 Jun 2018/Descending21 Jun 2018/Ascending15 Jul 2018/Descending18 Jul 2018/Ascending
20 Jul 2018/Ascending13 Aug 2018/Descending18 Aug 2018/Ascending09 Sep 2018/Descending
12 Sep 2018/Ascending14 Sep 2018/Ascending08 Oct 2018/Descending11 Oct 2018/Ascending
13 Oct 2018/Ascending04 Nov 2018/Descending06 Nov 2018/Descending11 Nov 2018/Ascending
03 Dec 2018/Descending05 Dec 2018/Descending08 Dec 2018/Ascending01 Jan 2019/Descending
06 Jan 2019/Ascending29 Jan 2019/Descending04 Feb 2019/Ascending27 Feb 2019/Descending
03 Mar 2019/Ascending26 Mar 2019/Descending01 Apr 2019/Ascending05 Apr 2019/Ascending
24 Apr 2019/Descending30 Apr 2019/Ascending23 May 2019/Descending29 May 2019/Ascending
19 Jun 2019/Descending25 Jun 2019/Ascending18 Jul 2019/Descending24 Jul 2019/Ascending
16 Aug 2019/Descending22 Aug 2019/Ascending12 Sep 2019/Descending14 Sep 2019/Descending
18 Sep 2019/Ascending20 Sep 2019/Ascending09 Oct 2019/Descending11 Oct 2019/Descending
14 Oct 2019/Ascending16 Oct 2019/Ascending09 Nov 2019/Descending14 Nov 2019/Ascending
06 Dec 2019/Descending08 Dec 2019/Descending11 Dec 2019/Ascending04 Jan 2020/Descending
09 Jan 2020/Ascending02 Feb 2020/Descending07 Feb 2020/Ascending02 Mar 2020/Descending
05 Mar 2020/Ascending27 Mar 2020/Descending29 Mar 2020/Descending31 Mar 2020/Descending
03 Apr 2020/Ascending27 Apr 2020/Descending02 May 2020/Ascending25 May 2020/Descending
29 May 2020/Descending31 May 2020/Ascending21 Jun 2020/Descending23 Jun 2020/Descending
25 Jun 2020/Ascending27 Jun 2020/Ascending20 Jul 2020/Descending22 Jul 2020/Descending
26 Jul 2020/Ascending12 Aug 2020/Descending14 Aug 2020/Descending18 Aug 2020/Descending
08 Sep 2020/Descending12 Sep 2020/Ascending14 Sep 2020/Ascending03 Oct 2020/Descending
07 Oct 2020/Ascending24 Oct 2020/Descending26 Oct 2020/Descending01 Nov 2020/Ascending
20 Nov 2020/Descending26 Nov 2020/Ascending15 Dec 2020/Descending
Table
Table A2. The CryoSat-2/SIRAL data acquisition dates for the validation of height accuracy.
Table A2. The CryoSat-2/SIRAL data acquisition dates for the validation of height accuracy.
Date/OrbitDate/OrbitDate/OrbitDate/Orbit
31 Mar 2011/Descending04 Apr 2011/Ascending26 May 2011/Descending19 Aug 2011/Descending
12 Nov 2011/Descending12 Jan 2012/Ascending05 Mar 2012/Descending29 May 2012/Descending
30 Jun 2012/Ascending23 Sep 2012/Ascending09 Apr 2013/Ascending01 Jun 2013/Descending
30 Jun 2013/Descending25 Aug 2013/Descending04 Jun 2014/Descending03 Jul 2014/Descending
06 Jul 2014/Ascending28 Aug 2014/Descending21 Nov 2014/Descending12 Apr 2015/Descending
16 Apr 2015/Ascending13 Jun 2015/Ascending06 Jul 2015/Descending10 Jul 2015/Ascending
31 Aug 2015/Descending03 Oct 2015/Ascending31 Oct 2015/Ascending24 Nov 2015/Descending
22 Feb 2016/Ascending18 Apr 2016/Ascending09 Jun 2016/Descending08 Jul 2016/Descending
12 Jul 2016/Ascending02 Sep 2016/Descending05 Oct 2016/Ascending20 Mar 2017/Descending
13 Jun 2017/Descending12 Jul 2017/Descending06 Sep 2017/Descending08 Oct 2017/Ascending
25 Apr 2018/Ascending18 Jul 2018/Ascending09 Sep 2018/Descending03 Dec 2018/Descending
02 Feb 2019/Ascending28 Apr 2019/Ascending19 Jun 2019/Descending18 Jul 2019/Descending
22 Jul 2019/Ascending12 Sep 2019/Descending11 Dec 2019/Ascending05 Feb 2020/Ascending
30 Apr 2020/Ascending23 May 2020/Descending21 Jun 2020/Descending27 Jun 2020/Ascending
24 Jul 2020/Ascending26 Oct 2020/Descending30 Oct 2020/Ascending

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Figure 1. (a) Map of Lützow-Holm Bay, East Antarctica; the red line indicates the grounding line of the Shirase Glacier [21] and the green line indicates the grounding line of other glaciers and the coastline [22]. The blue rectangle defines the area of the Shirase Glacier analyzed in the present study. (b) Locations of ponds in exposed rock area for the height validation in this study.
Figure 1. (a) Map of Lützow-Holm Bay, East Antarctica; the red line indicates the grounding line of the Shirase Glacier [21] and the green line indicates the grounding line of other glaciers and the coastline [22]. The blue rectangle defines the area of the Shirase Glacier analyzed in the present study. (b) Locations of ponds in exposed rock area for the height validation in this study.
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Figure 2. Schematic diagram of measurement performed using CryoSat-2/SIRAL over irregular terrain with slope.
Figure 2. Schematic diagram of measurement performed using CryoSat-2/SIRAL over irregular terrain with slope.
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Figure 3. Color-coded map derived from AW3D30 height data; the red line indicates the grounding line of the Shirase Glacier [21] and the green line indicates the grounding line of other glaciers and the coastline [22].
Figure 3. Color-coded map derived from AW3D30 height data; the red line indicates the grounding line of the Shirase Glacier [21] and the green line indicates the grounding line of other glaciers and the coastline [22].
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Remotesensing 15 01205 g004a 550Remotesensing 15 01205 g004b 550Remotesensing 15 01205 g004c 550Remotesensing 15 01205 g004d 550
Figure 4. Color-coded map of the estimated ice thickness distribution for the Shirase Glacier, as derived from (a) the AW3D30 height and the CryoSat-2 height in (b) 2011, (c) 2012, (d) 2013, (e) 2014, (f) 2015, (g) 2016, (h) 2017, (i) 2018, (j) 2019 and (k) 2020. The red line indicates the grounding line of the Shirase Glacier [21] and the black line indicates the grounding line of other glaciers and the coastline [22].
Figure 4. Color-coded map of the estimated ice thickness distribution for the Shirase Glacier, as derived from (a) the AW3D30 height and the CryoSat-2 height in (b) 2011, (c) 2012, (d) 2013, (e) 2014, (f) 2015, (g) 2016, (h) 2017, (i) 2018, (j) 2019 and (k) 2020. The red line indicates the grounding line of the Shirase Glacier [21] and the black line indicates the grounding line of other glaciers and the coastline [22].
Remotesensing 15 01205 g004aRemotesensing 15 01205 g004bRemotesensing 15 01205 g004cRemotesensing 15 01205 g004d
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Figure 5. Mean ice thickness profile from 2011 to 2020, extracted at 5 km intervals along the central streamline of the glacier. Ice thickness derived from (a) the CryoSat-2 height and (b) the AW3D30 height.
Figure 5. Mean ice thickness profile from 2011 to 2020, extracted at 5 km intervals along the central streamline of the glacier. Ice thickness derived from (a) the CryoSat-2 height and (b) the AW3D30 height.
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Figure 6. The relationship between ice thickness estimated on the basis of the AW3D30 height and that estimated on the basis of the CryoSat-2 height in the range of 10–40 km downstream from the grounding line.
Figure 6. The relationship between ice thickness estimated on the basis of the AW3D30 height and that estimated on the basis of the CryoSat-2 height in the range of 10–40 km downstream from the grounding line.
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Figure 7. The relationship between the ice thickness and the ice flow velocity assuming an incompressible fluid and the law of conservation of mass. The schematic diagram illustrates (a) that there is no change in the ice thickness, while (b) the ice thickness decrease Δ H is associated with the acceleration in flow velocity Δ v .
Figure 7. The relationship between the ice thickness and the ice flow velocity assuming an incompressible fluid and the law of conservation of mass. The schematic diagram illustrates (a) that there is no change in the ice thickness, while (b) the ice thickness decrease Δ H is associated with the acceleration in flow velocity Δ v .
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Figure 8. The annual mean of ice thickness at 25 km and 30 km downstream from the grounding line of the Shirase Glacier.
Figure 8. The annual mean of ice thickness at 25 km and 30 km downstream from the grounding line of the Shirase Glacier.
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Table
Table 1. The specifications of CryoSat-2/SIRAL.
Table 1. The specifications of CryoSat-2/SIRAL.
SpecificationValue
AgencyESA
Launch date8 April 2010
Satellite altitude717 km
Repeat cycle
(Sub-cycle)		369 days
(30 days)
SensorSIRAL
Frequency13.575 GHz
(Ku band)
Footprint
(SIN mode)		0.25 km (Along track)
1.60 km (Across track)
Table
Table 2. The amount of CryoSat-2/SIRAL data used in this study. Data for the Shirase Glacier are indicated without parentheses, and those used for validation are indicated with parentheses.
Table 2. The amount of CryoSat-2/SIRAL data used in this study. Data for the Shirase Glacier are indicated without parentheses, and those used for validation are indicated with parentheses.
YearAmt DataYearAmt DataYearAmt DataYearAmt DataYearAmt Data
201128 (5)201232 (5)201330 (4)201434 (5)201531 (9)
201631 (7)201731 (5)201830 (4)201932 (7)202036 (8)
Table
Table 3. Quality control (QC) data for CryoSat-2 height.
Table 3. Quality control (QC) data for CryoSat-2 height.
YearMeasuring PointsRemoved RatioYearMeasuring PointsRemoved Ratio
OriginalAfter QCOriginalAfter QC
2011103226274.6%201298921378.5%
201386916081.6%201485320775.7%
201592717581.1%201696924874.4%
201784115781.3%2018100827273.0%
2019101825275.2%202098520679.1%
Table
Table 4. The mean and standard deviation of the CryoSat-2 height and the AW3D30 height for each of the ponds in the exposed rock areas, as described in Section 2.1.
Table 4. The mean and standard deviation of the CryoSat-2 height and the AW3D30 height for each of the ponds in the exposed rock areas, as described in Section 2.1.
Pond NameCryoSat-2 (m)AW3D30 (m)
Maruwan O-ike6.33 ± 1.6110.38 ± 0.52
Dairi Ike48.57 ± 0.7150.97 ± 0.44
Skallen O-ike7.83 ± 1.2612.87 ± 0.92
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Satake, Y.; Nakamura, K. Temporal Variations in Ice Thickness of the Shirase Glacier Derived from Cryosat-2/SIRAL Data. Remote Sens. 2023, 15, 1205. https://doi.org/10.3390/rs15051205

AMA Style

Satake Y, Nakamura K. Temporal Variations in Ice Thickness of the Shirase Glacier Derived from Cryosat-2/SIRAL Data. Remote Sensing. 2023; 15(5):1205. https://doi.org/10.3390/rs15051205

Chicago/Turabian Style

Satake, Yurina, and Kazuki Nakamura. 2023. "Temporal Variations in Ice Thickness of the Shirase Glacier Derived from Cryosat-2/SIRAL Data" Remote Sensing 15, no. 5: 1205. https://doi.org/10.3390/rs15051205

APA Style

Satake, Y., & Nakamura, K. (2023). Temporal Variations in Ice Thickness of the Shirase Glacier Derived from Cryosat-2/SIRAL Data. Remote Sensing, 15(5), 1205. https://doi.org/10.3390/rs15051205

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