The potential of synthetic aperture radar interferometry for assessing meltwater lake dynamics on Antarctic ice shelves
- Department of Geoscience and Remote Sensing, Delft University of Technology, Delft, the Netherlands
Correspondence: Weiran Li (firstname.lastname@example.org)
Surface meltwater drains on several Antarctic ice shelves, resulting in surface and sub-surface lakes that are potentially critical for the ice shelf collapse. Despite these phenomena, our understanding and assessment of the drainage and refreezing of these lakes is limited, mainly due to lack of field observations and to the limitations of optical satellite imagery during polar night and in cloudy conditions. This paper explores the potential of backscatter intensity and of interferometric coherence and phase from synthetic aperture radar (SAR) imagery as an alternative to assess the dynamics of meltwater lakes. In four case study regions over Amery and Roi Baudouin ice shelves, East Antarctica, we examine spatial and temporal variations in SAR backscatter intensity and interferometric (InSAR) coherence and phase over several lakes derived from Sentinel-1A/B C-band SAR imagery. Throughout the year, the lakes are observed in a completely frozen state, in a partially frozen state with a floating ice lid and as open-water lakes. Our analysis reveals that the meltwater lake delineation is challenging during the melting period when the contrast between melting snow and lakes is indistinguishable. Despite this finding, we show using a combination of backscatter and InSAR observations that lake dynamics can be effectively captured during other non-summertime months. Moreover, our findings highlight the utility of InSAR-based observations for discriminating between refrozen ice and sub-surface meltwater and indicate the potential for phase-based detection and monitoring of rapid meltwater drainage events. The potential of this technique to monitor these meltwater change events is, however, strongly determined by the satellite revisit interval and potential changes in scattering properties due to snowfall or melt events.
Widespread surface meltwater has been observed on Antarctic ice shelves over the past century (Kingslake et al., 2017). Through seasonal formation and draining of supraglacial lakes, which have the potential to fracture and weaken ice shelves through repeated compression and uplift, respectively (Banwell et al., 2013), such phenomena may have important implications for ice shelf hydrofracture and collapse (Bell et al., 2018). Therefore, accurately observing the spatial and temporal evolution (filling, drainage or refreezing) of such lakes is pertinent to elucidating the future stability and response of the Antarctic Ice Sheet to climate change.
Given the remote location, widespread area and harsh climatic conditions in which these lakes form, satellite remote sensing has become the primary method of observing their evolution and dynamics (Brucker et al., 2010; Dirscherl et al., 2021). Previous studies exploited various satellite remote sensing data sources to observe these phenomena; for example, Kingslake et al. (2017) presented an overview of the Antarctic-wide meltwater hydrological network by combining Landsat, WorldView and Aster optical satellite imagery together with historic (pre-satellite) aerial photography. Other work has combined both optical and synthetic aperture radar (hereafter SAR) imagery to detect meltwater features in both Greenland and Antarctica (Benedek and Willis, 2021; Dirscherl et al., 2021), including the detection of sub-surface meltwater across East Antarctica's Roi Baudouin Ice Shelf (RBIS; Lenaerts et al., 2016a). Such sub-surface melting is not detectable from optical-based imagery alone (Miles et al., 2017), emphasising the potential utility of SAR to better detect total surface meltwater presence.
Despite the potential of optical imagery and SAR imagery in observing surface meltwater, both sensor types have limitations over Antarctica. Polar nights and cloud cover, for example, limit data coverage in optical-based imagery (Williamson et al., 2017), whereas the operating frequencies and active-source configuration of SAR sensors allow for all-weather, day–night imaging (Miles et al., 2017). Relative to the intuitive representation of meltwater features detected by optical sensors, however, the interpretation of SAR imagery can be complex due to ambiguous backscatter returns and/or image geometry effects (e.g. Fahnestock et al., 1993; Miles et al., 2017; Rizzoli et al., 2017). While cross-polarised (horizontal transmit and vertical receive, HV, or vertical transmit and horizontal receive, VH) backscatter intensity SAR images generally provide a better contrast between water and ice than single polarisation (e.g. horizontal transmit and horizontal receive, HH) images (Miles et al., 2017), such images are not necessarily always available over Antarctica (Hillebrand et al., 2021).
A potential solution to these limitations is interferometric processing of the synthetic aperture radar data (InSAR), which provides complementary information on the geometric and dielectric properties of the meltwater features. InSAR processing uses pairs of images of the same area separated by a particular temporal baseline to derive coherence and interferometric-phase information. Coherence is an indicator of changes in the relative position of the scatterers between the two acquisitions, whereas the interferometric phase measures their range difference from the satellites with the precision of a fractional component of the measuring radar wavelength. For high-coherence areas, the phase can be related to a line-of-sight displacement without change in scattering properties (e.g. without intense regional precipitation and melts), whereas for low-coherence areas where surface melts typically occur, the phase becomes scarcely informative (Hanssen, 2001). We expect this combination of coherence and phase information from InSAR to facilitate the continuous monitoring of meltwater dynamics. The changes in InSAR coherence have been proven useful in X-band for monitoring the refreeze of thermokarst lakes in the Arctic region (Antonova et al., 2016). So far, however, no analysis has been conducted for C-band time series. Additionally, the interferometric phase might reveal information about the drainage and filling of lakes as these processes result in a vertical displacement of the surface (Banwell et al., 2013). However, the value added using InSAR for such applications has not yet been examined.
In this paper, we assess the potential of C-band InSAR data to quantify the dynamic behaviour of meltwater filling, drainage and refreezing. For this purpose, we use a combination of backscatter, coherence and phase information to monitor recent meltwater features over two East Antarctic locations – Amery and Roi Baudouin (RBIS) ice shelves – using data collected by Sentinel-1A/B in 2017/18. To supplement the interpretation of our (In)SAR-based analyses, we also utilise spatially and temporally collocated optical and passive microwave satellite data and climate data.
2.1 Study areas
Two ice shelves in East Antarctica with well-known meltwater dynamics (Kingslake et al., 2017) are used as case studies. The first case study is on the Roi Baudouin Ice Shelf (RBIS), where in situ research was conducted, and the exact locations of several lakes were mapped during field campaigns (Lenaerts et al., 2016a; Dunmire et al., 2020). We use the supraglacial and englacial lakes mapped by Lenaerts et al. (2016a) as delineated meltwater lake features and complement that dataset with manually delineated sample polygons of snow and ice surfaces based on Landsat imagery for studying the difference between meltwater lakes and the solid surrounding regions (Fig. 1).
For the second case study over Amery Ice Shelf, we use a similar approach based on sampled lake, snow and ice regions. For Amery, no previously published dataset from in situ studies is available. Therefore, samples of lakes are mapped manually based on available Landsat 8 imagery (introduced in Sect. 2.2) in summer 2017–2018. The goal of this sampling is not to map all possible lakes but to get a representative sample polygon for each snow, ice and lake class.
Two types of Level-1 Sentinel-1 Interferometric Wide (IW) products are used in this study: Single Look Complex (SLC) products, consisting of complex-valued data that preserve the phase information of the returned echoes, and Ground Range Detected (GRD) products, consisting of multi-looked backscatter intensity without phase information. For both products, HH polarisation is used as this is the only polarisation widely available over the studied ice shelves.
Sentinel-1 SLC data are available on Copernicus Open Access Hub (Copernicus, 2014) and are processed to derive phase information and σ0. SLC processing is carried out using the Delft Object-oriented Radar Interferometric Software (DORIS; http://doris.tudelft.nl, last access: 15 October 2021), whose processing chain is summarised in Fig. 2. The co-registration between images is performed using magnitude images of the complex data. Sentinel-1 IW operates in Terrain Observation by Progressive Scans (TOPS; De Zan and Monti Guarnieri, 2006) mode; therefore phase ramps are accounted for via deramp and reramp processes to ensure co-registration accuracy (Yague-Martinez et al., 2016). For the retrieval of the sub-pixel azimuth shift, enhanced spectral diversity (ESD) is also applied (Prats-Iraola et al., 2012; Yague-Martinez et al., 2017). Georeferencing is based on the TanDEM-X digital elevation model (DEM) for RBIS (Lenaerts et al., 2016a) and WGS84 geoid for Amery as it is the default DEM input of DORIS when the TanDEM-X DEM of the same quality is not available at the time of processing. The final SLC products have an azimuth resolution of 20 m and a ground range resolution of 5 m (Torres et al., 2012).
GRD products are used mainly as supplementary backscatter intensity information when specific SLC tracks are not available (i.e. data from ascending track 59 before July 2017 are not available on Copernicus Open Access Hub, as shown in Table 1). The GRD data are primarily acquired from Google Earth Engine (GEE; Gorelick et al., 2017), whose processing includes thermal noise removal, radiometric calibration and terrain correction. The final backscatter product has a 10 m×10 m resolution. When normalised by the area of the resolution cell on the ground, the calibrated backscatter intensities are usually termed sigma nought (σ0), and this is the term we use for the remainder of the paper for backscatter intensity.
Additionally, independent datasets are used to help interpret the Sentinel-1 SAR data. First, Landsat 8 images are used for visual interpretation; i.e. solid snow and ice surfaces are shown in the images in white, and ice and lakes as a result of intensive melt are shown in blue. Available calibrated top-of-atmosphere (TOA) Tier 1 Landsat surface reflectance data (Chander et al., 2009) of true colour bands (bands 4, 3 and 2) and panchromatic band (band 8) are acquired from GEE at their native pixel resolution (30 m for RGB bands and 15 m for panchromatic band) without any additional pre-processing steps. Detailed data type and acquisition dates of satellite imagery are provided in Table 1. Landsat 8 images are courtesy of the US Geological Survey.
To interpret temporal variations in Sentinel-1 backscatter intensity and coherence, it is moreover important to understand temporal melt extent and precipitation as these are the potential drivers of changes in scatterers. For estimating melt extent, multi-frequency radiometer observations – more specifically, brightness temperature (Tb) measurements from the Special Sensor Microwave Imager/Sounder (SSMIS) sensors (Kunkee et al., 2008) – are used. Brightness temperatures in polar stereographic projection are available from the National Snow and Ice Data Center (NSIDC) (Meier et al., 2021).
Precipitation from ERA5 Daily Aggregates (, ) over A2 and R1 (in Fig. 1) in 5 km resolution is averaged spatially and acquired from GEE. Acquisition dates of the brightness temperature observations and ERA5 data overlap with the SLC acquisition dates from ascending track 59 and descending track 3 in Table 1.
To assess meltwater lake dynamics, we analyse the spatial and the temporal variations in Sentinel-1 backscatter intensity and coherence over the lakes and control (snow and ice) sites. Therefore, we compare the spatial and temporal characteristics of the identified lakes with their surroundings to assess how well they can be distinguished in different seasons. For this purpose, the temporal variations in σ0 and coherence are compared per lake, snow and ice class by analysing their time series of the mean and standard deviation for each class (i.e. lakes, snow and ice). In this comparison, 10 samples of snow and 10 samples of ice on each ice shelf are used as shown in Fig. 1. Second, the spatio-temporal variation in σ0 is analysed along cross-sectional transects across the largest lake dimension to assess the seasonal differences between the lakes and their surrounding areas. This is a biennial analysis in order to show that the lakes may not behave identically every year. Subsequently, individual images are analysed, where changes in σ0 are compared to changes in coherence and phase to assess the added value of combining SAR backscatter intensity with InSAR information to improve the understanding of the melt–refreeze process of lakes.
Time series of backscatter intensity and coherence are interpreted with the assistance of melt extent and precipitation time series. As an approximation of melt extent, the cross-polarisation gradient ratio (XPGR) meltwater detection method proposed by Abdalati and Steffen (1995) is applied, where horizontally polarised 19 GHz (19H) and vertically polarised 37 GHz (37V) brightness temperatures are used to calculate the XPGR:
When XPGR ratio exceeds a specific threshold, the surface is assumed to experience melting. For SSMIS, this threshold is set as −0.0158 (Johnson et al., 2020); 19H and 37V observations used for the computation are measured daily and provided in 25 km resolution. In addition, time series of precipitation from ERA5 acquired from GEE are used directly.
3.1 Backscatter intensity analysis
The mean σ0 time series of lakes, snow and ice (Sect. 2.2) display strong seasonal variability, consistent with the changing nature of both surface snow and ice properties and the evolution of supraglacial lakes through time (Fig. 3). On Amery Ice Shelf, our observations reveal that σ0 has different values for snow (∼0 dB), lakes ( dB) and ice ( dB) and is relatively constant during the observed time span (fluctuations within ∼1 dB), with the exception of the summer melt seasons (January and February). In summer seasons, as a result of melting, the σ0 of (wet) snow and lakes shows a strong decrease due to the change in dielectric constant. The σ0 time series on RBIS show a similar pattern (i.e., ) except for December 2017 and January 2018, where drops below and . Both the Amery and RBIS time series show, however, that the discrimination of lakes based on σ0 alone is not straightforward as the σ0 of the lakes often resembles the σ0 of snow and ice.
A similar confusion between lakes and snow and ice samples is visible in the spatio-temporal analysis of selected cross-sectional transects. In the case of both RBIS a and Amery d (location shown in Fig. 1), for example, backscatter time series show significant inter-annual variation (Fig. 4). For RBIS a, this starts with high σ0 values (similar to snow) with limited spatial variation in June–November 2016, followed by a strong area-wide decrease in σ0 during the melting season (December 2016–February 2017). Subsequently, a clear spatial pattern emerges with borders of low σ0 at the edges and high σ0 in the central regions, which respectively refer to the edge and central regions of the lake. This pattern is followed again by a new area-wide decrease in σ0 in the December 2017–January 2018 melting season. This development is consistent with the description of ice lids in (Antonova et al., 2016) and the potential development of ice lids in winter on RBIS (Dunmire et al., 2020).
For Amery d, these spatio-temporal transect patterns of the lake are less distinguishable from the surrounding ice area as the σ0 of the lake closely resembles the σ0 of the surrounding ice, except for March–May 2018, when it shows a strong increase.
3.2 Coherence analysis
The coherence time series show a completely different behaviour than the σ0 time series (Fig. 3). On Amery Ice Shelf, for example, snow, ice and lakes all have low or null coherence in summer because of the altering scattering properties due to meltwater content. For the ice and snow zones, the coherence rises abruptly when the surface refreezes in spring, while the coherence over the lakes rises only gradually until winter, when the lakes reach coherence values that are similar to snow and ice. During winter, the coherence values of snow, ice and lakes show a similar behaviour with large temporal variations which fluctuate between 0.2 and 0.6 between successive (6 d) image acquisitions. These sudden drops likely result from short-term, weather-induced changes in scattering properties, including snowfall events (Fig. 5a). These drops are however sparse as the 6 d revisit cycle allows good overall coherence to be obtained. During summer, low coherence occurs when the surface melts. This can be seen in Fig. 6a and b, where XPGR exceeds the melting threshold in January 2017 and rises towards the melting threshold in January 2018.
On RBIS, the Sentinel-1 data are only available in a 12 d revisit cycle (as in Table 1), which reduces the overall coherence and makes interpretation more complicated as more weather-induced changes in scattering properties could occur. Figure 5b, for example, shows that region R1 (on RBIS) has a greater amount of total daily precipitation than region A2 (on Amery). Despite the overall lower coherence, the coherence time series on RBIS also show a relatively stable period from August to October, with coherence values above 0.35. Between October 2017 and January 2018, the coherence drops drastically, with an almost null coherence for all surveyed snow, ice and lake areas. The coherence then increases again in February. Overall, snow reaches the highest coherence (0.5–0.6), while the lakes show the lowest coherence.
To better understand the σ0 and coherence time series, some representative lake features in the Amery and RBIS zones are analysed in more detail in Figs. 7 and 8. The outlined lakes on Amery Ice Shelf in Fig. 7 are characterised by dominant blue ice cover with low backscatter intensities, as conveyed by the dark background in the σ0 panels. The blue ice region is intermittently covered by a shallow snow layer (e.g. Landsat true colour image of October 2017 in Fig. 7), which decreases in summer (e.g. Landsat true colour image of January 2018 in Fig. 7). This results in a stable ice surface with high coherence values. The lakes, on the other hand, show a more variable behaviour with lower coherence and strong changes in σ0 as a result of varying scattering properties. At the end of the summer (March 2017), both lakes show a low σ0, whereas it becomes substantially greater in the subsequent acquisitions from July to November 2017. Sigma nought (σ0) and coherence are moreover not uniform across each lake with the appearance of polygonal features that show large differences between the centre of the lake (with higher σ0 and coherence) and a thin strip at the edges (with lower σ0 and coherence). This is consistent with earlier observations based on optical satellite imagery, where the lakes show a circular appearance with a thick snow or ice lid in the centre and ice or water at the edges (e.g., Fig. S1 in Dunmire et al., 2020). This pattern often changes over time, for example, as in the lake Amery c (Fig. 7), where the coherence increases for only half of the lake and not for the other half, which could be an indicator of gradual, spatially non-uniform refreezing or drainage. One example of such a drainage event could be seen in the small circular feature in the coherence of Amery b in November 2017 (indicated by the arrow in the November 2017 coherence image of Fig. 7), which clearly corresponds to a collapsed circular feature in the January 2018 Landsat imagery. Moreover, between Amery b and c, a hydrological network that is clearly visible as high σ0 in the σ0 panels is present only in the March 2017 coherence panel as low coherence. This could suggest the surface refreezing between March and July 2017, similar to that discussed by Antonova et al. (2016).
On RBIS, the lakes are located in an area that contains both snow or firn and blue ice (Lenaerts et al., 2016a). In contrast to data acquired over Amery Ice Shelf, the Sentinel-1 SLC acquisition only started in July 2017, with a 12 d revisit (Fig. 8). Lake RBIS a shows a high σ0 in October and a low σ0 in February, which contrasts with the surroundings. The other lakes show a smaller contrast with their surroundings with only intermediate σ0 values. The whole area frequently undergoes coherence losses, especially between November 2017 and January 2018 (Fig. 3d). Figure 5b shows that precipitation may cause the drop in coherence as in October–November 2017 it is 2–5 times higher than in other times. Figure 6c shows that the low coherence between December 2017 and January 2018 may be caused by melt as the XPGR values during this period exceed the melting threshold. In October 2017 and February 2018, however, coherence is higher (>0.35; see both Figs. 3 and 8). In both coherence image pairs in Fig. 8, the meltwater features, with low or null coherence values, sharply emerge from the background. In February 2018, the coherence pairs moreover highlight a hydrological connection between the lakes, which is shown as dark curvilinear features between the highlighted lakes in the lower middle panel of Fig. 8. The patterns are clearly newly formed compared to the October 2017 coherence panel of Fig. 8. This feature is not visible in either σ0 or optical imagery, highlighting the benefit of InSAR-based coherence for the detection and monitoring of sub-surface lake networks.
3.3 Interferogram analysis
Interferometric-phase-difference maps (Fig. 7) emphasise the differences in spatial cover and melting patterns between the two lakes on Amery Ice Shelf. The centre of lake Amery b is associated with low-frequency fringes in all the acquisitions, even in March, despite the relatively low coherence. Between March 2017 and October 2017, the fringes in the centre of lake Amery b are disconnected from the high-frequency fringes of the surroundings, whereas they connect seamlessly in November 2017. This pattern of discontinuity is consistent with lower coherence at the edges of lake Amery b, which follows the orange delineation curve in the October 2017 coherence panel of Fig. 7. That both fringe discontinuity and coherence increase through time indicates the presence of the lake until October 2017, followed by a lake refreeze or drainage in November of that year. Consistent with our InSAR-based observations, Landsat images show a smooth snow-covered surface in October 2017 and a rough doline-like surface in January 2018 (labelled as lake collapse in the coherence panel of Fig. 7). This supports the hypothesis that the lake drained and the surface collapsed and highlights the potential of coherence and interferograms for analysing meltwater dynamics.
On the eastern part of RBIS, the interferogram shows a different potential for analysing meltwater dynamics (Fig. 9) as it shows a phase reversal from right to left of the December 2017 phase image (i.e. fringes change from red–blue–green–yellow to red–yellow–green–blue, forming a concentric pattern of deformation associated with a series of dense, closely spaced fringes) compared to a continuous phase from right to left of the April 2018 image (i.e. fringes are constantly red–yellow–green–blue). This phase reversal indicates that the lake has a displacement in the satellite line of sight which is opposite to the rest of the ice shelf. As the ice shelf background fringes correspond to the ice flow and presumably the tidal component, in this case moving away from the satellite line of sight, the lake fringes indicate an uplift as a result of ice shelf rebounce after lake collapse. This hypothesis is consistent with earlier observations, including the rebound effects described by Banwell et al. (2013). Indirect indicators of this lake collapse can also be observed in the Landsat 8 images before and after the collapse as the roughness of the surface strongly increased after the collapse. By counting the fringes, the feature consists of approximately seven fringes, each measuring 2.8 cm in the line of sight. Assuming a vertical movement, this corresponds to an uplift of approximately 24 cm (taking into account an incidence angle of approximately 35∘). However, this amount of uplift is only an approximation of a displacement relative to ice flow and tidal component and needs in situ observations to validate.
Another potential of interferogram time series is the detection of lake refreezing, as can be observed for the large lake feature in the middle of Amery Ice Shelf, labelled as Amery a in Fig. 1. Both Amery a and the surrounding ice shelf show an overall low σ0 on 4 January 2017 (Fig. 10). In subsequent weeks, the σ0 of the surrounding snow area increases. The σ0 of the lake gradually increases between 4 January and 17 March 2017 and gradually decreases between 17 March and 22 April 2017. The low σ0 on 4 January 2017 is likely a result of surface melt, while the subsequent rise in σ0 is likely due to refreezing. This pattern corresponds closely with the refreezing pattern identified by Spergel et al. (2021), who also identified a gradual refreezing towards the centre of the lake over 66 d based on transition from high to low backscatter intensity only. However, compared to interpreting the refreezing of the lake solely based on backscatter intensity, adding interferograms to the observation helps reduce ambiguities in the interpretation. The interferogram of both Amery a and the surroundings is completely incoherent on 4 January 2017, which can be interpreted as changing scattering properties due to intense surface melt. Since 28 January 2017, the coherence of the surrounding snow area increases due to refreezing, as can be seen from the visible regular fringes. For the lake, however, this increase in coherence lags behind and only recovers slowly as more portions of the lake start to refreeze. During the refreezing, the fringes' patterns over the lake gradually recover, while the incoherent noise gradually diminishes. The Landsat panels of both Figs. 10 and 5a show that January 2017 is a more intense melt season than January 2018, which is consistent with the observation from the fringes.
Using SAR-based observations acquired across two East Antarctic ice shelves, this study presents evidence of the utility of backscatter intensity and coherence to assess meltwater lake dynamics. Low backscatter intensities can indicate blue ice areas or strong absorption due to meltwater, while high backscatter intensities indicate rough surfaces or strong volume scattering due to larger refrozen snow grains. Moreover, the partly frozen lakes often show a bright centre (high σ0) that can be attributed to the single bounce mechanism at the rough ice–water boundary (Engram et al., 2013; Atwood et al., 2015; Antonova et al., 2016). Due to this contrasting behaviour, the identification and characterisation of the meltwater features based only on backscatter intensity are not straightforward. Several of the observed lakes, for example, show σ0 similar to their surroundings for long periods and even during the freezing and melting processes (e.g. Figs. 8 and 10).
Backscatter intensity may not therefore be sufficient to fully characterise meltwater processes. Interferometric coherence, however, provides additional dynamic information as it helps assess the degree of stability of the ice cover between two acquisitions. Coherence is an important property estimated from interferometric computation of SLC data. For repeat-pass acquisition, a loss of coherence mainly reveals the extent of a surface change (Zebker and Villasenor, 1992). However, with substantial microwave penetration depths in snow or firn, coherence variations can indicate changes in scattering properties. Coherence losses may consequently be due to changes in volume scattering (Zebker and Hoen, 2000) or sub-surface processes. Low coherence between interferometric images can therefore indicate altering scattering properties (e.g. a strong snowfall or an intense melt event) but also changes in the ice–water interface due to refreezing meltwater lakes (Antonova et al., 2016), where refreezing may result in a gradual increase in coherence. Ice and snow areas are typically characterised by a high coherence, while meltwater lakes show a low coherence due to the constantly changing ice–water interface and the increased attenuation due to the presence of water. This added value of coherence is shown, for example, in Figs. 7 and 8, where coherence provides more insight into the temporal dynamics of the lakes than the σ0 images alone. The change from complete polygonal low-coherence patterns to partly high coherence (Fig. 7), for example, provides an important indicator of the gradual refreezing patterns (i.e. more refreezing in the centre than at the edges). These results correspond to the study of Antonova et al. (2016), where the melting and refreezing of lake ice could be observed by using both backscatter intensity and coherence image time series.
Beyond coherence, we also demonstrate the potential of interferometric phase for assessing meltwater dynamics in areas of high coherence. For example, the deformation due to rapid meltwater events, such as drainage and collapse, may be captured if the fringe pattern in the lake area appears highly distinct to the surroundings affected by tidal and horizontal motion. Within this context, we identify two advantages of phase fringes over σ0 and coherence alone: (i) an easier detection of stable ice and lake refreezing than coherence and backscatter intensity and (ii) the detection of relative motion due to uplift and subsidence events as a result of lake drainage or lake filling. The first advantage is clear in Figs. 7–10, where the phase patterns allow additional interpretation of the refreezing patterns which cannot be imaged by coherence or backscatter intensity alone. The second advantage is shown clearly in Fig. 9, where the closely spaced fringes shown could be used to estimate the presence of an uplift event due to drainage.
While InSAR-based techniques show clear potential for monitoring meltwater lake evolution, there are several key limitations associated with this technique compared with conventional optically based and SAR-backscatter-based imaging. First, it requires high coherence between image pairs to allow a meaningful interpretation of meltwater lake dynamics (e.g. as in Fig. 10). When the revisit cycle for SLC data is long or when the surface changes due to other processes (e.g. strong snowfall events, as shown in Fig. 5) are frequent, the interpretation of coherence and phase changes can be limited. On Amery Ice Shelf, the Sentinel-1 mission has a 6 d revisit, whilst the revisit period on RBIS is 12 d. The amount of precipitation is also lower on Amery Ice Shelf compared to RBIS. Due to these differing imaging times and weather, the lake processes are better observed on Amery Ice Shelf than RBIS. Second, the interpretation of phase change should be performed relative to the displacement of the lake surroundings in the line of sight. For example, as the meltwater lakes typically develop in locations with strong ice and/or tidal displacement, interpretation should be done relative to that displacement. Therefore, to better derive the exact height change in lake ice lids, additional processing will likely be needed to cancel out, for example, the effects of ice shelf flow (Mohajerani et al., 2021) and to filter out signals due to tidal movements (McMillan et al., 2012). With SAR acquisitions from sensors in both ascending and descending orbits, it is however possible to better quantify the lake subsidence and uplift.
A potential improvement of lake monitoring using InSAR is the launch of new satellite missions. The launch of Sentinel-1C (Torres et al., 2017), for example, can provide < 6 d imaging capabilities to improve coherence of the ice and snow surface. The launch of the NASA-ISRO SAR (NISAR) mission, moreover, provides L-band and S-band repeat-pass interferometry with the repeat cycle of 12 d (Rosen et al., 2017). The long wavelength of this mission has the potential to measure deeper lake dynamics and to circumvent drifting snow and other atmospheric effects.
This study has provided insights into the utility of InSAR for monitoring meltwater lake dynamics on ice shelves. Four Antarctic ice shelf regions subject to intense summertime melt have been analysed using Sentinel-1A/B C-band SAR imagery, corresponding available Landsat 8 imagery, ERA5 precipitation data and SSMIS brightness temperature data. The spatial and temporal inspection of the meltwater features conveys that backscatter intensity allows identification of freezing and melting events as the lakes show an increase in the backscatter intensity due to the water–ice boundary when the lake is not completely frozen. The extent of such dynamics depends on the morphology of the lake and on the weather conditions. We show that meltwater detection using backscatter is, however, not straightforward as meltwater lakes often show similar backscatter intensity values to their surroundings. In such circumstances, InSAR information can be useful to increase the confidence of such delineation, especially during the freezing and melting period. In addition, we show that InSAR-derived information can also be used to observe meltwater lake evolution (and potential drainage) with high accuracy beyond that afforded by conventional backscatter or optical satellite imaging. Specifically, InSAR coherence information allows for the detection of changes in the ice–water interface, which shows clearer patterns than the backscatter intensity alone, while interferometric phase can effectively track the spatial and temporal evolution of ice refreezing. Maps of interferometric phase moreover allow for the detection of abrupt lake drainage (or filling) events via changes in the relative displacement of the surface between successive SAR passes.
Despite noted limitations to current Sentinel-1 InSAR imaging over parts of Antarctica, this study shows that InSAR provides promising potential for monitoring meltwater lake dynamics beyond that afforded by conventional, backscatter-only analyses. Such potential could pave the way for dedicated Sentinel-1 meltwater products that could facilitate the study of ice shelves in a changing climate.
SL developed the idea of this study and provided access to the mapped locations of the meltwater ponds on the RBIS and TanDEM-X data. PLD provided expertise in processing and interpreting InSAR data. WL was responsible for managing the data, processing the data with DORIS, generating melt extent and precipitation time series, processing and analysing the results, producing the figures, and providing the manuscript.
At least one of the (co-)authors is a member of the editorial board of The Cryosphere. The peer-review process was guided by an independent editor, and the authors also have no other competing interests to declare.
Publisher's note: Copernicus Publications remains neutral with regard to jurisdictional claims in published maps and institutional affiliations.
We are grateful for the DORIS development team at TU Delft. We acknowledge Copernicus Open Access Hub for providing Sentinel-1 SLC data, the National Snow and Ice Data Center (NSIDC) for providing the SSMIS brightness temperature data, and Google Earth Engine for providing Landsat 8 and Sentinel-1 GRD images. Landsat 8 images are courtesy of the US Geological Survey. This study contains modified Copernicus Climate Change Service information and Copernicus Sentinel data from 2018.
DEM for visualisation is provided by the Byrd Polar and Climate Research Center and the Polar Geospatial Center under NSF-OPP awards 1543501, 1810976, 1542736, 1559691, 1043681, 1541332, 0753663, 1548562 and 1238993 and NASA award NNX10AN61G. Computer time is provided through a Blue Waters Innovation initiative. The DEM is produced using data from DigitalGlobe, Inc.
We would also like to thank Lorenzo Iannini and Malte Manne for proof-reading and discussion. Additionally, we thank the referees for reviewing and Chris Derksen for editing the manuscript.
This paper was edited by Chris Derksen and reviewed by two anonymous referees.
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