1. Introduction
Ice-shelf flow is resisted by ice rises, ice rumples and by shear friction along the side margins (e.g. Reference ThomasThomas, 1973). For ice rises, where flow is diverted around the perimeter of grounded ice, and ice rumples, where flow is diverted over the grounded region, resistance occurs at all phases of the ocean tide (i.e. at high tide as well as at low tide).
In this study, we present observational evidence of a new kind of ice rumple in which grounding occurs only during low tide (i.e. the ice shelf floats freely at high tide), and where the associated resistance must therefore vary with the tidal cycle. We call this new ice-shelf feature an ephemeral grounding zone and use differential interferometric synthetic aperture radar (InSAR) data to display various examples found in the Antarctic. Differential InSAR is a technique which combines two interferograms spanning the same time interval and acquired from the same orbit configuration, as is discussed in more detail elsewhere (e.g. Reference Rignot, Padman, MacAyeal and SchmeltzRignot and others, 2000). One of the hallmark features of differential interferometry is its ability to display with great precision and spatial clarity areas where the ice shelf is grounded (Reference RignotRignot, 1998b). Our objectives are to determine (a) how significantly these features contribute to the overall resistance of ice-shelf flow and (b) whether changes in ephemeral grounding over time may be used to monitor ice-shelf thickness and grounding-line location.
The creep flow of an ice shelf and its tidal deformation are both measured on a single SAR interferogram because InSAR measures the overall displacement of the reflecting surface in the radar line of sight. The line of sight is 23° away from the vertical direction in the case of European Remote-sensing Satellites 1 and 2 (ERS-1 and -2). Assuming that the ice-shelf flow is continuous and steady with time, a combination of two interferograms spanning the same time interval permits the elimination of the signal associated with creep deformation. The residual measurement contains only the change in vertical displacement of the ice-shell surface in response to changes in oceanic tides (Reference RignotRignot, 1996). The converse, which is to eliminate the tidal motion from the ice-shelf velocity field, is possible but more difficult to achieve, especially with the same degree of precision, because it requires a precise knowledge of oceanic tides underneath the ice shelf (which is typically not available) or the examination of a longer time period of creep-flow deformation. As a result, the effect of ephemeral grounding on the tidal regime of an ice shelf is detected with great precision in ERS interferograms, while the same data procure little information on its influence on ice-shelf creep rates.
To address the importance of the influence of ephemeral grounding on ice-shelf flow, we use a finite-element model designed to simulate ice-shelf flow in realistic geometries. The model design and application is similar to that described by Reference Hulbe, Rignot and MacAyealHulbe and others (1998). Model simulations of ephemeral grounding at the mouth of Rutford Ice Stream and on the ice shelf in front of Pine Island Glacier, both areas of West Antarctica, are used to quantitatively estimate the role of ephemeral grounding in resistance to ice-shelf flow.
The usefulness of ephemeral grounding as a means of monitoring subtle changes in ice-shelf thickness is evaluated for two examples. First, we present a time series of InSAR observations of the grounding zone of Thwaites Glacier, West Antarctica, collected in 1992, 1994 and 1996. This glacier appears to be in a state of retreat (Reference RignotRignot, in press). Second, we discuss the case of Rutford Ice Stream for which knowledge of oceanic tides (personal communication from D. G. Vaughan, 1997) is combined with InSAR results to infer the water-column thickness underneath areas of ephemeral grounding.
2. Study Areas (Glaciological Setting)
Differential InSAR enables grounded parts of an ice shelf to be detected with spectacular precision (mm) compared to what could be achieved in the field even with modern technology (cm precision with global positioning system traverses (e.g. Reference RignotRignot, 1998b)). Areas of ephemeral grounding, as defined earlier, are observed in numerous interferograms of Antarctic ice shelves. In this paper, we focus our discussion on three selected areas of ephemeral grounding which cover a spectrum of ice-shelf morphology and flow style. The location and orientation of the InSAR imagery used in this study is displayed in Figure 1.
Fig. 1. Location map indicating the studied areas: Rutford Ice Stream, Pine Island Glacier and Thwaites Glacier, plotted on the United States Geological Survey Advanced Very High Resolution Radiometer mosaic of Antarctica (Reference MersonMerson, 1989).
Rutford Ice Stream (Fig. 1) flows into the Ronne Ice Shelf from its extreme inland boundary, approximately 1000 km from the ice front. Ice-shelf flow in the grounding zone of this glacier is thus highly constrained by the coastal geometry and the presence of ice rises downstream. The 30 km wide ice stream enters the ice shelf with a velocity of about 0. 4 km a−1 (Reference Frolich and DoakeFrolich and Doake, 1988) and an ice thickness of about 1650 m (Reference Smith and DoakeSmith and Doake, 1994). Seismic surveys conducted in the region suggest that the seabed underneath the floating portion of Rutford Ice Stream is hummocky (Reference Smith and DoakeSmith and Doake, 1994), and the tidal range in the region is large (e.g. Reference Robertson, Padman, Egbert, Jacobs and WeissRobertson and others, 1998). The hummocky bottom and large tidal range combine to produce ephemeral grounding downstream of the permanent (constrained by a bedrock knoll) grounding line of the ice stream.
In contrast to the grounding zone of Rutford Ice Stream, Pine Island Glacier and Thwaites Glacier (Fig. 1) flow into short, virtually unconstrained ice shelves of limited size. Ephemeral grounding areas are also found in these ice regions, which we deem to be distinct in both morphology and flow style from that of the Rutford Ice Stream region.
Pine Island Glacier is a fast-moving outlet glacier which flows into the Amundsen sea at about 2.4 km a−1 (e.g. Reference Ferrigno, Williams, Rosanova, Lucchitta and SwithinbankFerrigno and others, 1998). It enters a small ice shelf 70 km long by 40 km wide that appears to provide some buttressing influence on the flow at the grounding line (personal communication from T. K. Dupont and M. Schmeltz, 1999). The ice-shelf thickness decreases from about 1400 m at the grounding line to 400 m at the calving front (Reference Crabtree and DoakeCrabtree and Doake, 1982). That extraordinary amount of ice thinning has been attributed to basal melting (Reference Jenkins, Vaughan, Jacobs, Hellmer and KeysJenkins and others, 1997; Reference RignotRignot, 1998a). The flow of Pine Island Glacier appears to be impeded by several small-size ice rises, mainly located near the ice front (Reference RignotRignot, 1998a).
Thwaites Glacier enters the Amundsen Sea directly west of Pine Island Glacier. Flowing at approximately 3 km a−1, the ice tongue of Thwaites Glacier ranks among the fastest moving ice masses in Antarctica. The ice-shelf section of interest to us, located east of the main fast-moving ice tongue, is the smallest ice shelf discussed in this study. About 40 km by 30 km in size, it flows at about 0.5 km a−1 (interferometric estimation) and abuts a large, prominent ice rise.
3. Interferometric Observations
The fringe pattern observed in a typical SAR interferogram of an ice-shelf region reveals displacements caused by both creep flow and vertical tidal motion of the ice shelf (Reference Hartl, Thiel, Wu, Doake and SieversHartl and others, 1994). In circumstances where ice-shelf flow is continuous and relatively steady with time, it is possible to eliminate the creep-flow signal using differential interferometry, which is described in detail by Reference Rignot, Padman, MacAyeal and SchmeltzRignot and others (2000). Tide-only interferograms (i.e. double-difference interferograms) reveal narrow bands of elastic tidal flexure surrounding regions of permanent and ephemeral grounding (e.g. Reference RignotRignot, 1996, Reference Rignot1998a). The nature of this flexure is discussed by Reference HoldsworthHoldsworth (1969, Reference Holdsworth1977).
What is of primary interest in this study is the fringe patterns found in differential interferograms which signify elastic tidal flexure along the coast, around ice rises and around zones of ephemeral grounding. Examples of such fringe-line patterns are shown in Figures 2–5. In those figures, each interferometric fringe, represented by a full color cycle, corresponds to a different number of radians change in interferometric phase. For reference, a 2π rad change in phase corresponds to a 31 mm displacement of the ice-shelf surface in the vertical direction (31 mm is λ/2/sin (23°), where the radar wavelength λ is 56 mm). The displacement is measured between several epochs and as such does not represent an absolute tidal displacement in reference to mean sea level, but a change in vertical displacement of the ice shelf over a combination of time periods. For more details, we refer to appendix A of Reference Rignot, Padman, MacAyeal and SchmeltzRignot and others (2000).
Fig. 2. Cartoon showing the differences between permanent and ephemeral grounding. Ephemeral grounding is distinguished from permanent grounding by whether or not the number of fringes in the “bull’s-eye” is less than or equal to the number of fringes which define the grounding line.
The important aspect of fringe-pattern analysis is the method by which we distinguish zones of permanent grounding from zones of ephemeral grounding. This task requires that the ocean tide be relatively uniform in both amplitude and phase throughout the region covered by the differential interferometry. Under most circumstances, as indicated by models of sub-ice-shelf tide (e.g. Reference Robertson, Padman, Egbert, Jacobs and WeissRobertson and others, 1998), this assumption is valid. The method we use for discrimination is shown schematically in Figure 2. First, we examine the differential interferogram for two generic types of fringe patterns: (a) the closely spaced “bull’s-eye” patterns that signify local islands of grounding, and (b) the closely spaced “ribbon” patterns that signify the main grounding line (where the shelf starts to float). Next, we count the number of fringes in all of the examples of the two patterns seen in the differential interferogram. Finally, using the number of fringe lines identified at the main grounding line as the critical reference, we are able to say whether regions of local “island-type” grounding are permanent or ephemeral. Where the fringe count is equal to the critical reference count, permanent grounding is indicated, because the ice is shown to have the same response to tidal uplift as the main grounded ice body. Where the fringe count is less than the critical reference count, ice must have become ungrounded during the tidal cycle, and ephemeral grounding is indicated.
A conceptual explanation of why this method works can be provided succinctly as follows. For the difference in tidal-flexure displacement between two pairs of satellite passes to vary from one tidal-flexure zone to another, there must be a difference in the range of tidal motion. This can happen where there is an unusual and unlike y variation in the ocean-tide amplitude, which we reject by assumption (e.g. Reference Robertson, Padman, Egbert, Jacobs and WeissRobertson and others, 1998); or where a part of the ice shelf rises at high tide, but does not settle fully at low tide because it is grounded.
For the example provided in Figure 2, the grounding line and permanent ice rise both have three fringes. The ephemeral grounding, i.e. grounding which occurs only at low tide, has only one fringe. The fact that the fringe count for the ephemeral grounding zone is less than for either the grounding line or the permanently grounded ice rise distinguishes the ephemeral grounding from the other two cases.
3.1. Rutford Ice Stream
The tidal interferogram of Rutford Ice Stream (Fig. 3) combines three separate passes of the ERS-1 satellite, collected at a 3 day time interval in 1992. Two interferograms were constructed by differencing the phase between the second and first passes for one, and the third and second passes for the other. The two interferograms were then differenced to obtain the differential interferogram shown in Figure 3.
Fig. 3. Tidal interferogram of Rutford Ice Stream in 1992. The area of ephemeral grounding is located at 78.65° S, 82.5° W. The scale of 25 rad per cycle represents a 123 mm vertical displacement of the glacier surface induced by tidal motion from blue to blue. The white masked areas denote where phase could not be unwrapped. The cross-section AA′ is from Reference Smith and DoakeSmith and Doake (1994, fig. 4). The orientation of the box is the same as in Figure 1.
Downstream of the grounding line, there is an area where the number of fringes between the center of the presumed ice rise and the ice shelf is less than the number of fringes counted across the grounding line. We count 26 fringes across the grounding line but only four fringes in the bull’s-eye pattern. This signifies ephemeral grounding.
Seismic surveys conducted in the area do not reveal an isolated peak at the location of ephemeral grounding on Rutford Ice Stream (Reference Smith and DoakeSmith and Doake, 1994). The density of InSAR data observations is, however, higher than that of the seismic survey; thus the lack of seismic data indicating a seabed hummock capable of causing ephemeral grounding is not necessarily incompatible with the results of the InSAR data. Furthermore, figure 4 in Reference Smith and DoakeSmith and Doake (1994) showing the water column and seabed across section AA′ (shown here in Fig. 3) illustrates the rough character of the bed in this region, which would be consistent with ephemeral grounding revealed by the InSAR data.
Fig. 4. Tidal interferogram of the ice shelfat the outlet of Pine Island Glacier in 1996. The scale of 12 rad per cycle represents 59.2 mm vertical displacement. The orientation of the box is the same as in Figure 1.
3.2. Pine Island Glacier
The differential interferogram of the small ice shelf in front of Pine Island Glacier is shown in Figure 4. The fringe count across the grounding line is five. Near the ice front, several features have been labelled as ice rises because the bull’s-eye patterns are formed with the same number of fringes as across the grounding line. Several examples of ephemeral grounding are also apparent, the most prominent of which is near the grounding line at approximately 75.31° S, 100.5° W, as labeled on the figure. The close proximity of this zone to the grounding line suggests a rather flat seabed, so there is a possibility for sea water to infiltrate over a long distance underneath grounded ice at high tide, which is consistent with the identification of an ice plain in this region by Reference Corr, Vaughan, Doake and JenkinsCorr and others (2000).
3.3. Thwaites Glacier
Ephemeral grounding is also evident on Thwaites Glacier, as shown in a series of three tidal interferograms obtained in 1992, 1994 and 1996 (Fig. 5). Two areas of ephemeral grounding labeled in the 1992 differential interferogram (those near the grounding line in Figure 5a) deserve particular attention. They are not detected in the 1994 or 1996 differential interferograms. This means that the ice shelf was not able to establish contact with the seabed at low tide in 1994 and 1996, probably because the shelf is thinning.
Fig. 5. Tidal interferograms of the ice shelf at the outlet of Thwaites Glacier in (a) 1992, (b) 1994 and (c) 1996. The scale of 8 rad per cycle represents a 39.5 mm vertical displacement. The orientation of the boxes is the same as in Figure 1.
Another feature seen in the 1992 differential interferogram shows a remarkable evolution. The ice rise located at 75.1 °S, 105.25° W, in the 1992 differential interferogram becomes an area of ephemeral grounding in the 1994 differential interferogram and is no longer visible in the 1996 differential interferogram. In the 1992 interferogram, the number of fringes surrounding the ice rise is the same as across the grounding line (seven fringes). In 1994, we see only a little more than one fringe, whereas eleven are counted across the grounding line. The zone of contact completely disappears in the 1996 interferogram, while we count four to five fringes across the flexure zone.
We interpret the changes in the ice rise and ephemeral grounding zone discussed above as indicating ice-shelf thinning over the period of observation (1992–96). Because the glacier bed is unlikely to be flat, such areas of ephemeral grounding are likely to be present over an area where an ice shelf is thinning. This suggests that the observation of ephemeral grounding could be used to monitor ongoing ice-shelf thickness change.
The ephemeral grounding area in the center of the ice shelf evolves differently from the two examples discussed above. On the 1994 differential interferogram (Fig. 5b) we see a twin bull’s-eye pattern where the ice-shelf displacement is of opposite sign compared to other areas of ephemeral grounding (hence the color cycle of the bull’s-eye pattern is reversed compared to other areas). In 1992 and 1996, there seems to be only one bull’s-eye pattern at this location. This area of ephemeral grounding therefore evolves differently from the others. Since this portion of the ice shelf is influenced by a large ice rise located downstream (numerous compression ridges are seen in the imagery between the ice rise and the zone of ephemeral grounding), the ice-shelf thickness is most likely not uniform in this area, which complicates the interaction of the ice-shelf bottom with the sea floor during a tidal cycle, especially as irregularities in ice-shelf thickness are advected downstream. Without further knowledge of oceanic tides, ice-shelf thickness and ocean depth, it is not possible to explain the observed evolution of the twin-bull’s-eye fringe pattern.
3.4. Ice-thickness change: example of Rutford Ice Stream
Ice-thickness changes may also be detected from a combination of tide predictions and a time series of InSAR data. First, we estimate the water-column thickness underneath the ice shelf at one epoch. Second, we differentiate estimates obtained at different epochs to measure the rate of thinning or thickening. We study the case of Rutford Ice Stream for which tidal predictions are available.
As mentioned earlier, the 1992 tidal interferogram of Rutford Ice Stream results from the combination of three passes, which we label t 1, t 2 and t 3. For these three passes, the oceanic tide, at the location of the ephemeral grounding, is respectively −1.826, −0.030 and −1.204 m, referenced to mean sea level (personal communication from D. G. Vaughan, 1997, reported in Reference RignotRignot, 1998a, table 2). The differential interferogram shown in Figure 3 is the difference (t 2 − t 1) − (t 3 − t 2). We therefore expect to measure a difference in tidal displacement across the grounding zone of 2.97 m in the radar interferogram. We measure 26 fringes, which corresponds to a 3.2 m displacement. The difference between the two estimates is within the uncertainty of the tidal predictions (±10 cm).
The area of ephemeral grounding yields four fringes or a 0. 5 m displacement between the center of the ephemeral grounding and the freely floating ice shelf. The area of ephemeral grounding must have been in contact with the sea floor at the lowest tide, which is t 1, and not in contact with the sea floor at the highest tide, which is t 2. Since (t 1 − t 3) is >0.5 m, there was no contact at t 3 either. Hence, the 0.5 m displacement is the vertical displacement from the lower tide t 1. The water-column thickness is therefore |t 1| − 0.5 or 1.33 m at the location of the ephemeral grounding. If we assume a tidal amplitude of 2 m (the tidal amplitude must be > |t 1|), this means that the ice is in contact with the bedrock during less than one-third of a tidal cycle over the area of ephemeral grounding.
A similar calculation was made for the 1996 tidal interferogram of Rutford Ice Stream (Reference RignotRignot, 1998b). We obtained a mean water-column thickness of 1.42 m at the location of the ephemeral grounding. The difference between this estimate and the 1992 estimate (+9 cm) is within the uncertainty of the tidal predictions. We may conclude from this analysis that there is no detectable change in ice thickness on Rutford Ice Stream between 1992 and 1996. This result is consistent with the stable grounding-line position of this glacier, discussed in Reference RignotRignot (1998b).
4. Model Study
We investigate how ephemeral grounding influences the velocity by simulating the ice-shelf flow at the mouth of Rutford Ice Stream and Pine Island Glacier using a numerical model of ice-shell stress balance. Thwaites Glacier is not modelled because reliable ice-thickness data are not available in the area. The model used here is described by Reference MacAyeal, Bindschadler and ScambosMacAyeal and others (1995, Reference MacAyeal, Rommelaere, Huybrechts, Hulbe, Determann and Ritz1996) and has been used in other applications of InSAR interpretation (e.g. Reference Hulbe, Rignot and MacAyealHulbe and others, 1998). A finite-element method is used to solve the “reduced” stressbalance equations appropriate for ice-shelf flow on a mesh of triangular elements covering realistic ice-shelf geometries. Grounded ice upstream of the grounding line is not included in the model domains, and grounded ice downstream of the grounding line is treated through the introduction of variable basal stress as described below.
Figures 6 and 7 show the two model domains of Rutford Ice Stream and Pine Island Glacier. Ice thickness is required as input to the model. For Rutford Ice Stream, we use a constant thickness of 1650 m (an average from Reference Smith and DoakeSmith and Doake, 1994). For Pine Island Glacier, we calculate ice thickness from Reference Bamber and BindschadlerBamber and Bindschadler’s (1997) digital elevation model of Antarctica referenced to mean sea level, assuming an ice shelf in hydrostatic equilibrium.
Fig. 6. Model mesh covering the entire Filchner–Ronne Ice Shelf Rutford Ice Stream is at the bottom center of the mesh. The mesh comprises 3752 elements with 2056 nodes. The inset shows an expanded view of the mesh near the outlet of Rutford Ice Stream, where we use a higher mesh resolution. The projection is polar stereographic. Black areas denote open or sea-ice-covered water; gray areas denote grounded ice. The red line identifies the grounding line of Rutford Ice Stream; the blue line identifies the ice-shelf front.
Fig. 7. Model mesh of the ice shelf of Pine Island Glacier. The mesh comprises 2703 elements with 1469 nodes. The projection is polar stereographic. Black areas denote open or sea-ice-covered water; gray areas denote grounded ice. The red line identifies the grounding line; the blue line identifies the ice front.
Both kinematic and dynamic boundary conditions are needed to solve the stress-balance equations. The kinematic boundary condition is the velocity at the model domain boundary. At the glacier grounding line, velocity is prescribed according to InSAR velocity estimates (Reference RignotRignot 1998a, b). Where the ice shelf flows past grounded ice coasts and around well-established ice rises (e.g. Henry, Korff and Berkner Island on the Ronne Ice Shelf), the velocity is prescribed to be zero, i.e. a no-slip condition. A dynamic boundary condition is also applied at the seaward ice front where ice-shelf flow is resisted by sea-water pressure alone.
Small ice rises in the Pine Island Glacier simulation and ephemeral grounding zones in both simulations are considered in the mesh design and treated by specification of a basal friction coefficient β (in Pa s m−1) at specified mesh elements, independently of the rest of the mesh. This approach allows the ice to potentially flow over the seabed on which it is grounded. While not entirely consistent with the simplifying assumptions of the model equations, this approach represents a logical first step in evaluating the degree of resistance provided by small areas of grounding. The basal stress τ b generated by the flow over the seabed is determined by the model, and is given by β · u b where u b is the ice velocity at the bed (assumed to be the same as the vertically constant ice-shelf velocity). The coefficient β is zero in the absence of ice rise or ephemeral grounding, so the basal stress is zero. We explored a range of β values to determine the sensitivity of the ice-shelf flow to increasing seabed contact in ephemeral grounding zones. This range is 109 to 1010 Pa s m−1 (as in Reference MacAyeal, Bindschadler and ScambosMacAyeal and others, 1995). To simulate an ice rise in which the ice shelf can no longer flow over the seabed, β should be infinite, so in practice we use β = 1040 Pa s m−1.
We first simulate ice flow for both Rutford Ice Stream and Pine Island Glacier using a basal friction coefficient of zero on all grounded regions (ice rises and ephemeral grounding). This establishes a reference velocity field which we then compare to the results obtained using different values of β: 1010 Pa s m−1 for the ephemeral grounding zone of Rutford Ice Stream, and 1040 Pa s m−1 for the ice rise in Pine Island Bay. The grounding on Rutford Ice Stream occurs during less than one-third of a tidal cycle. Therefore, the mean velocity with grounding is the sum of two-thirds of the reference velocity and one-third of the velocity simulated with β = 1010 Pa s m−1.
We assess the influence of ephemeral grounding and small ice rises in the case of Pine Island Glacier by comparing the velocity fields in the β = 0 and β ≠ 0 scenarios.
5. Results and Discussion
The presence of ephemeral grounding downstream of Rutford Ice Stream reduces the modelled surface velocity by <0.5% in the central region of the ice (Fig. 8). A maximum decrease of 2% is reached at the location of ephemeral grounding. Significant changes in velocity (>5% in the center) are induced when the basal friction coefficient is > 1012 Pa s m−1, but such a large value is unlikely.
Fig. 8. (a) Modeled velocity of the floating ice downstream of Rutford Ice Stream, including the whole Filchner−Ronne Ice Shelf, with a zero basal friction coefficient (contour interval is 100 m a−1). (b) Percentage difference between model without ephemeral grounding and model with ephemeral grounding, for the region near the outlet of Rutford Ice Stream only (contour interval is 0.2%). The dots mark the location of ephemeral grounding
The ice rises in the ice shelf in front of Pine Island Glacier have a significant influence on the shelf’s flow (Fig. 9). The main flow velocity (in the central region of fast-moving ice) typically decreases by 8% with the introduction of ice rises. Away from the ice rises, the decrease in velocity is proportional to the inverse of the distance to the ice rise as calculated by Reference ThomasThomas (1973). The decrease calculated away from the ice rise located at 74.85° S, 100.9° W (the one indicated by the second arrow pointing towards ice rises in Figure 4) follows approximately the curve 160/r, where r is the distance from the ice rise.
Fig. 9. (a) Modeled velocity of Pine Island Glacier with a zero basal friction coefficient (no grounding). (b) Modeled velocity with a β value equal to 1040 Pa m s−1 (i.e. a value selected to stop flow over the seabed). Contour intervals are 200 m a−1 from 2500 to 2100, and400 m a−1 thereafter. (c) Percentage difference between model without ice rises and model with ice rises (contour interval is 1% from 5% to 10%, and 10% thereafter). The small dots mark the location of the ice rises.
We conclude from these experiments that despite the detectable influence of ephemeral grounding on the tidal deformation of an ice shelf, these features have no influence on the ice-shelf flow that would be of major significance to the overall stability and mass balance of the ice shelf. In the case of ice rises, it is good to notice that the model works as well and that it confirms what we expect, i.e. that they do exert a significant restraint on ice-shelf flow.
The importance of ephemeral grounding lies therefore in its potential to reveal subtle changes in ice-shelf thickness. As demonstrated in the case of the floating ice shelf in front of Thwaites Glacier, the evolution of areas of ephemeral grounding may reveal ongoing changes in ice-shelf thickness. If an ice shelf thickens, it becomes grounded over a larger area, and areas of ephemeral grounding may develop as the water column underneath the ice shelf decreases to within the tidal range. Conversely, when an ice shelf thins and retreats, areas of ephemeral grounding may remain for some period of time in the wake of the retreat. These retreats or advances may be quantitatively measured if InSAR observations are combined with tidal predictions.
Acknowledgements
This work was performed at the Jet Propulsion Laboratory, California Institute of Technology, under a contract with the NASA Polar Research Program. Funding at the University of Chicago was provided by the U.S. National Science Foundation (OPP-9818622). We thank C. Werner for use of his SAR processor. We especially thank C. Hulbe who made numerous and very helpful comments on the text as well as on the figures, and an anonymous reviewer who also gave very constructive comments to improve the manuscript. Lastly, we would like to thank the Scientific Editor, R. Greve, for his thorough and expeditious handling of the paper.
