Introduction
The ice streams of the Siple Coast of the West Antarctic ice sheet (WAIS) are bands of rapidly moving ice that play a crucial role in the discharge of ice to the ocean and the mass balance of the ice sheet (Reference Alley and WhillansAlley and Whillans, 1991). The margins of these ice streams are sharp, dynamic boundaries separating fast- and slow-moving ice. One of the important enigmas is what determines the location of the margins and how they may shift or not (Reference Raymond, Echelmeyer, Whillans, Doake, Alley and BindschadlerRaymond and others, 2001). High icestream speed and localization of marginal shearing indicates a fairly sharp mechanical transition from good basal lubrication underneath the streaming flow to a locked basal condition in the slow-moving ice to the side, with much of the downslope weight of the ice stream supported by the bed near its edges (Reference Echelmeyer, Harrison, Larsen and MitchellEchelmeyer and others, 1994; Reference Scambos, Echelmeyer, Fahnestock and BindschadlerScambos and others, 1994; Reference Whillans and van der VeenWhillans and Van der Veen, 1997). An important question is: what could maintain a locked condition in these zones of mechanical support in the face of concentration of stress and associated mechanical heating into them (Reference Jacobson and RaymondJacobson and Raymond, 1998; Reference SchoofSchoof, 2004)? This question bears on the potential for large discharge increases through ice streams by widening discharge gates and associated speed-up.
Water plays a crucial role in the basal lubrication of these ice streams. Differences in the amount and ionic content of liquid water important in the lubrication process affect electrical properties of the base, and should be detectable using radar (Reference Peters, Blankenship and MorsePeters and others, 2005). Indeed, available radar observations indicate generally higher basal reflectivity under ice streams compared to inter-ice-stream ridges (Reference Bentley, Lord and LiuBentley and others, 1998; Reference Gades, Raymond, Conway and JacobelGades and others, 2000; Reference Catania, Conway, Gades, C.F. Raymond and EngelhardtCatania and others, 2003).
Characteristics of the transition in basal reflectivity and its relation to shearing marked by marginal crevasses on the upper surface have barely been explored. Airborne radioecho sounders are typically unable to clearly image internal layers or the bed beneath ice-stream margins because of strong scattering from the crevasses (e.g. Reference Shabtaie, Whillans and BentleyShabtaie and others, 1987). While imaging of the bed can be improved using synthetic aperture radar (SAR) methods (e.g. Reference Peters, Blankenship and MorsePeters and others, 2005), quantitative assessment of the bed reflectivity remains difficult. Ground deployment and low frequency allows better penetration through the near-surface fractures. Profiling is relatively easy across buried inactive margins of dormant ice streams, and a number of profiles traversing from an inactive ice stream to an adjacent ridge have revealed spatial features of high to low basal reflectivity transitions (Reference Gades, Raymond, Conway and JacobelGades and others, 2000; Reference Catania, Conway, Gades, C.F. Raymond and EngelhardtCatania and others, 2003). A common feature is that transitions in bed reflectivity lie several kilometers inside the outer edges of the marginal crevasse bands. This discordance raises questions about the mechanics of margins. Is the lubrication under a margin of an ice stream different than in its interior? Or are there mechanical processes in the ice that enable concentration of shear straining remote from the edge of lubrication of the ice-stream base? With regard to active ice-stream mechanics, interpretation of the radar data from these dormant margins is complicated by the dormant condition during observation and over several centuries before, during which drainage and/or freezing of the bed could have occurred. Unfortunately, the active shear margins are not straightforward to traverse, because the crevasses are actively forming and are not buried.
This paper presents the first radar measurements revealing bed reflectivity trends in an active ice-stream margin. It examines the north margin (called the Snake) of the upper part of Whillans Ice Stream (WIS) (formerly known as Ice Stream B, branch B2; Fig. 1). The Snake is one of the most spectacular shear margins of the WAIS. The observations begin to place some constraints on the characteristics of the locked to lubricated boundary associated with the present position of this margin.
(a) Location of field area in Antarctica. (b) SAR image of Engelhardt Ridge (ER) and bounding Whillans and Kamb Ice Streams taken from the RADARSAT-1 Antarctic Mapping Project (RAMP) mosaic (Reference JezekJezek, 1999). Lines indicate the approximate paths of ground-based, low-frequency radar profiles collected on parts of ER in the last decade (Reference Nereson and RaymondNereson and Raymond, 2001; Reference Catania, Conway, Gades, C.F. Raymond and EngelhardtCatania and others, 2003 and unpublished information; this paper). White lines show profiles at approximately 2 MHz used in this paper. Black lines show other profiles not used because of higher frequency (nominally 5–7 MHz) over rough bed areas or instrumental artifacts complicating analysis of power return. Dashed lines are specific profiles from Reference Catania, Conway, Gades, C.F. Raymond and EngelhardtCatania and others (2003) mentioned in the text. White box shows the location of (c). (c) Large-scale image of the WIS margin (Snake) with precise locations (white lines) of three profiles shown in Figure 2. Coordinates are polar stereographic projection in units of km. Horizontal axis is polar stereographic x, and vertical is polar stereographic y
Radar Profiles
Radar profiles were made across the Snake at three locations spaced about 8 km along the margin (Fig. 1). Each profile covered a substantial distance on Engelhardt Ridge (ER) and penetrated through the most chaotic zone of the Snake to less disturbed ice toward the interior of the ice stream. This paper is concerned primarily with basal reflection strength from those parts of the profiles lying near and in the margin. The profile Camp extending into ER and across its divide (Fig. 1b) gives information about the large-scale spatial pattern of accumulation on ER and its recent history of flow, as discussed by Reference Nereson and RaymondNereson and Raymond (2001).
The radar profiling system utilized a high-voltage, impulse transmitter (±2000 V step with 15 ns rise time) driving a low-frequency dipole antenna with tapered resistive loading to give a transmitted pulse length of about 1.5 period. Returns were received by an identical antenna fed to a digital oscilloscope with internal stacks (typically on the order of 102–103) downloaded to a small computer. The basic features of the radar system are described in more detail by Reference WeertmanWeertman (1993), Reference MorseMorse (1997) and Reference Gades, Raymond, Conway and JacobelGades and others (2000). We used antennae with length corresponding to frequency of about 2 MHz. The effective center frequency is somewhat higher. The antennae were dragged end-to-end over the firn surface with a center-to-center spacing of about 118 m. On the smooth terrain of ER, the system was drawn by a snowmobile, but it was hauled on foot (with great difficulty) in the crevassed zone of the Snake. Soundings were taken typically every 5 m in horizontal distance along the profile paths in the Snake as determined by a bicycle wheel. Barometric altimetry was used to determine elevation of the surface at the horizontal position of each record. Both horizontal and vertical positions on the surface were controlled by differential global positioning system spaced at several hundred meters along the profile.
Recorded returns of voltage vs time were de-trended and bandpass filtered (phase-preserving, forward–reverse Butterworth filter with corner frequencies of 1 and 10 MHz). Depths of returns from beneath the surface were computed from the two-way travel time accounting for velocity of radio waves in the firn and ice, refraction in the firn and antenna geometry (Reference WeertmanWeertman, 1993) using the vertical variation of density found nearby on ER by Reference Alley and BentleyAlley and Bentley (1988). To produce images of the geometry of the surface, layers and bed, the voltage return from each horizontal and vertical position sampled in a profile was mapped to grayscale with results shown in Figure 2.
Radar profiles across the Snake at three locations (Fig. 1b) separated by about 8 km along the direction of flow of WIS: (a) East profile (83.3042° S, 138.3697° W to 83.2667° S, 138.4764° W); (b) Camp profile (83.318° S, 138.976° W to 83.2831 º S, 139.0662° W); and (c) West profile (83.345° S, 139.547° W to 83.2883° S, 139.6608° W). Profiles are aligned with 0 distance at the approximate outer edge of the zone of arcuate crevasses. Shaded vertical bar indicates the possible range in location of maximum strain rate. The disturbance at +1 km in the Camp profile results from scattering from a radio antenna and other objects in the camp. The panel beneath each profile shows relative power return from the bed (BRPR; heavy curve) and interior (IRPN; light curve) as described in the text. Curves of BRPR and IRPN are not smoothed. Curve for IRPN is shifted by 1 to separate it from BRPR.
Bed Reflectivity
Power returned from bed and interior
The power returned from the bed (abbreviated below as BRP) is related to the reflectivity of the bed. However, the system characteristics, near-field interaction with the firn, loss along the propagation path and environmental electromagnetic noise also affect the return power. By using methods similar to those described by Reference Gades, Raymond, Conway and JacobelGades and others (2000), power returned from bright internal layers below the zone of crevasses (abbreviated below as IRP) is used to calibrate these additional effects to allow definition of the spatial variation of relative reflectivity from the bed.
The average returned power from within any two-way travel time window tt1–tt2 is defined as half the mean square voltage v over the interval. In practice, this is evaluated in terms of a sum over the discrete samples n(tt1 to n(tt2) in the time window
which gives the mean power per sample.
BRP is defined as RP evaluated on the time window of length T b starting at T b/4 before the maximum of the wavelet returning from the bed, where T b is roughly one period of the bed wavelet defined as two times the time difference from the maximum to the first minimum following it. (The typical sampling interval of 10 ns gives about 20 samples in T b of about 0.2 μs.)
IRP is defined on a fixed time window starting at tt1 = 2 μs and ending at tt2 = 5.24 μs. (It includes 324 samples with the typical sampling interval of 10 ns.) This time window for IRP corresponds to a depth range of about 202–480m and includes only the zone where internal layers are clearly imaged (Fig. 2), thereby excluding effects unrelated to internal scattering at short time from the direct wave along the surface and at long time from noise obscuring dim returns from deep ice. It also excludes the strong bed reflection in all profiles and a variable and sometimes strong disturbance (glitch) associated with the transmitter at about 6 μs appearing in some profiles.
Some of the power in any time window comes from noise. We use an approximately 1 μs time window in the last part of the recording interval well below the bed to gauge the noise power level (NP).
Figure 3 shows BRP and IRP displayed according to ttb for the local profiles (Fig. 1c) and the extension of the Camp profile across the ER divide (Fig. 1b). For our profiles (on about 0.9 km thickness) IRP is one to two orders of magnitude smaller than BRP. NP is scattered about 1 mv2 per sample. (We do not show NP because it is much less than IRP (more than one order of magnitude), and its inclusion stretches the vertical scale with loss of detail in BRP and IRP.)
Power returned from bed BRP and interior IRP vs two-way travel time to the bed, ttb, for local profiles East, Camp and West (Fig. 1c) including the extension of Camp profile across the divide of ER (Fig. 1b). Different symbols distinguish measurements from ER and those from the Snake. The solid curve represents a function BRP = Ғ(ttb) fit to data from the ER parts of profiles.
BRP is distinctly correlated with ttb as a result of path losses from geometrical spreading and attenuation (absorption and scattering). As expected from their definitions, IRP and NP are not correlated with ttb. There is no clear separation for any of BRP or IRP found under the Snake parts of the profiles (circles in Fig. 3) compared to under ER (points in Fig. 3), although the Snake shows more scatter than ER.
Spatial variation along profiles
To highlight possible spatial anomalies in bed reflection and compare with internal scattering, it is convenient to de-trend BRP and to normalize IRP.
To approximate the trend in BRP vs ttb, we define a smooth empirical function F(ttb) = 0.5a exp (bttb) (straight line on the log-linear plot of Fig. 3) by a least-squares fit to BRP vs ttb. We use the data in Figure 3 excluding those parts of the profiles in the Snake, where we want to investigate the possibility that BRP does not conform to the pattern in the adjacent ER. The resulting least-squares fit gives a = 7.713 (5.434, 9.993) × 109 mV2 and b = –1.293 (–1.323, –1.264)μs–1, where the range in parentheses shows 95% confidence bounds. Because of the scatter, the data do not tightly constrain choice of F(ttb) (Fig. 3). In fact, there is no correct F(ttb), given that there could be some degree of spatial variation in ice temperature and chemistry affecting attenuation. However, these are not major problems in our search for a large change in bed reflectivity. The ice thickness (and ttb) varies smoothly without steep gradients along the profiles. Furthermore, the continuity of internal layers suggests no reason to expect discontinuities in the thickness-averaged internal ice temperature or chemistry. Thus, F(ttb) provides a useful model to identify differences in BRP that are not easily explained solely by ttb trends.
We define a relative bed reflection power BRPR = BRP/F(ttb). The detailed spatial variation of BRPR for each profile across the Snake is shown below its image in Figure 2. Table 1 gives quantitative statistical information about the spatial variability of BRPR for the full profile distances and separately for the parts in ER and in the Snake.
Statistics of relative bed return power variations
To display the spatial variation of IRP, we define a normalized IRP as 
where 
is the average over the full distance along a profile. IRPN is shown below the corresponding profile image in Figure 2 shifted by 1 to separate it from BRPR. Table 2 gives quantitative statistical information about the spatial variability of IRPN for the full distance and separately for the parts in ER and in the Snake.
Statistics of normalized internal return power variations
Both BRPR and IRPN show variation along the profile tracks. They appear to vary independently (Fig. 2). The visual impression is supported by relatively low linear correlation coefficients calculated for the different profiles (East, Camp, West) and segments (ice stream or ridge), which fall in the range 0.1–0.4. Examination of each profile individually in the order East, Camp, West shows that correlation is slightly higher in the ice-stream segments (0.44, 0.29, 0.37) compared to the ridge segments (0.26, 0.28, 0.10). The lack of negative correlation indicates that backscattering from layers is not a prevailing factor in attenuating BPR as would also be expected from the low IRP. The small positive correlation suggests some variability in the transmission of radar power to and through the near surface. The somewhat more positive correlation together with a very slightly lower mean for both BRPR and IRP and larger spread for IRPN in the ice stream compared to the ridge (Tables 1 and 2) suggests a detectable but small extra loss by scattering from nearsurface crevasses.
Examination of the more detailed spatial variation of both BRPR and IRPN shown in Figure 2 does not reveal any distinct shift in either BRP or IRP across the edge of the ice stream or any boundary inward that would suggest large jumps in radar penetration through the upper surface, column ice properties or bed reflectivity. We have also examined the reflection power from individual internal layers, which like IRP do not show any spatial trends associated with the margin position. BRPR is slightly larger than is typical just inside the margin on the West profile and just outside the margin on the Camp profile. However, anomalies of similar or larger size are found for both BRPR and IRPN away from the margin, thus calling into question any significance to the near-margin patterns. In general, the largest anomalies in BRPR appear to be associated with locations of high bed curvature that could cause focusing or defocusing or locations of roughness elements as indicated by diffraction hyperbola (e.g. West profile at –0.5 km and 3.0 km).
The conclusion is that the radar sees no significant difference in bed reflection properties in the Snake compared to ER. The difference in average basal reflectivity between the sampled parts of the ridge and of the Snake is less than about ±20% (Table1). This is much smaller than the reflectivity contrast up to about a factor of 6 from ridge to ice stream known in some places as discussed below.
Magnitude along profiles
The procedure that we have followed reveals only (lack of) relative changes in reflectivity but not absolute values, which would also be useful to know. To obtain some constraints for this part of ER and the adjacent Snake, we examine already published data from other WAIS locations together with ours. Interpretation is not straightforward, since the available data were not all gathered with identical configuration or calibrated radar systems. We follow related paths ultimately based on the constraint that 1 is an upper reflectivity limit.
First, we compare our local area of ER to Siple Dome (SDM). Reference Gades, Raymond, Conway and JacobelGades and others (2000) deduced a relatively low bed power reflectivity (less than about 0.14) under SDM, because it was substantially lower there (by a factor of 1/7) than in the adjacent ‘Siple Ice Stream’. Radar at SDM and ER both used similar low frequency but different antenna loading, transmitter and receiver. As above, we use IRP to inter-calibrate the systems by examining BRP/IRP in Figure 4. Both BRP and IRP found on Siple Dome are about one order of magnitude smaller than the corresponding quantity in our area of ER (Fig. 3), but BRP/IRP is nearly the same. The parallel behavior of BRP and IRP is most simply explained by different system characteristics (and possibly different near-surface coupling) interacting with nearly the same internal scattering and bed reflection under SDM and our local area of ER.
Power returned from the bed BRP scaled to power from the interior IRP vs the corresponding two-way travel time to the bed, ttb, for profiles collected with approximately 2MHz impulse radar. Different symbols indicate source of data. ER local and Snake are from BRP and IRP in Figure 3. SDM are from Siple Dome (Fig. 1b) using data from Reference Jacobel, Scambos, Raymond and GadesJacobel and others (1996) and Reference Gades, Raymond, Conway and JacobelGades and others (2000).
Second, we compare other areas of ER where measured profiles span both ridge and ice-stream environments. Nominally 5MHz profiles pass from the lower (west) part of ER into a stagnated part of WIS and from the upper (east) part of ER into a now dormant connection from WIS to Kamb Ice Stream (Fig. 1b). Both show distinctly higher bed power reflectivity (by up to an order of magnitude) in parts of the former streaming areas compared to ER (Reference Catania, Conway, Gades, C.F. Raymond and EngelhardtCatania and others, 2003, figs 3 and 4), thus capping the power reflectivity beneath these areas of ER at low values (less than roughly 0.1). Airborne 50MHz radar analyzed by Reference Bentley, Lord and LiuBentley and others (1998) indicates a similar upper limit for power reflectivity beneath wide areas of the western part of ER, as shown by substantially lower values than in the interiors of both Kamb Ice Stream (larger by about one order of magnitude) and WIS (larger by about a factor of 3). We do not attempt to directly compare these data from other ER locations with our local ER data, because of differences in frequency and related antennae configuration that could affect BRP and IRP differently. Nevertheless, these data from other ER locations support low power reflectivity (<0.1) under broad areas of ER.
Collectively, the published data indicate bed power reflectivity beneath our local ER area that is substantially lower than in some ice-stream areas and does not exceed 0.1–0.2. Our local results also show that low reflectivity extends beneath the Snake.
Context for Interpretation
Margin mechanics
The presence of a narrow, chaotic shear zone at the Snake indicates that it is underlain by a large, sharp transition in the lubrication of the bed going from locked under ER to well lubricated under WIS. Flow models provide some constraints on the spatial relationship between the shear zone on the upper surface and the lubrication transition at the bed causing it.
With homogeneous mechanical properties of the ice, the maximum shear strain rate on the surface is predicted to lie almost directly over the lubrication jump on the bed, when it is very sharp (Reference RaymondRaymond, 1996). If the transition in lubrication is spread out (e.g. Reference SchoofSchoof, 2004), the location of maximum shear strain rate on the surface lies toward the ice-stream center from the outer edge of enhanced basal slip, which is driven by a combination of elevated basal shear stress and heightened lubrication. Modeling shows that some of the fast motion in the outer margin results from high internal deformation near the bed induced by high stress transmitted laterally in the relatively cold, stiff upper part of the ice column (e.g. Reference Whillans and van der VeenWhillans and Van der Veen, 2001). Accounting for a temperature effect on ice deformation predicts an inward shift of the strain-rate maximum toward the ice-stream center (Reference Jacobson and RaymondJacobson and Raymond, 1998), but only by a small amount (a few hundred meters) probably because the effective viscosity stratification caused by temperature variation introduces dominantly vertical gradients. Large outward shifts of the peak in surface strain rate from the outer edge of basal lubrication would require a basal zone of very soft ice connecting to a similarly soft vertical band guiding high strain rate upward to the surface. Although we contrive this rather complex structure here, it is not expected. Correspondingly, it has not been explored in models. It is not clear what size of displacement of strain-rate peak would be possible within the constraint of no more than one order of magnitude softening associated with strong singlemaximum c-axis fabric (Reference Budd and JackaBudd and Jacka, 1989). Furthermore, maintaining this structure in the face of inflow of ice from the ridge is problematic.
The balance of theoretical understanding indicates that the bed inward from the location of maximum shear strain rate on the surface should be well lubricated. The location of maximum strain rate is known for each profile from measurements on displacement of poles set along the profile (Van der Veen and others, unpublished information). The location is shown in Figure 2 (shading).
On this basis, the radar profiles would be expected to have extended into the ice stream sufficiently far to be sampling well-lubricated parts of the bed under the Snake. Thus, our observation above means that the bed can pass from lubricated to locked without a significant change in bed reflectivity. In the remainder of this paper, our central question is what implication that has for lubrication conditions under the Snake.
Basal conditions
Subglacial till plays a central role in the basal lubrication of the Siple Coast ice streams (Reference Kamb, Alley and BindschadlerKamb, 2001). Seismic methods (Reference Blankenship, Bentley, Rooney and AlleyBlankenship and others, 1987) and extensive basal sampling through boreholes (Reference Engelhardt, Humphrey, Kamb and FahnestockEngelhardt and others, 1990; Reference Kamb, Alley and BindschadlerKamb, 2001) show that a multi-meter thick layer of dilated, water-saturated basal till lies beneath the central zone of WIS close to the area of the Snake examined here. Electrical conductivity of pore water was found to be 2.5 × 10–2 Sm–1 by direct sampling in boreholes (Reference Engelhardt, Humphrey, Kamb and FahnestockEngelhardt and others, 1990).
Information about bed conditions beneath inter-ice-stream ridges is still very limited. Reference Anandakrishnan and WinberryAnandakrishnan and Winberry (2004) have identified 300m of sediments beneath Siple Dome, based on seismic measurements. However, basal till with morphology like that found under ice streams was not found in boreholes penetrating to the bed under the summit of Siple Dome (Reference EngelhardtEngelhardt, 2003). Basal till has been found in boreholes on the Unicorn (Fig. 1) outside of the shear margin known as the Dragon on the other (south) side of WIS (Reference Kamb, Alley and BindschadlerKamb, 2001). Since streaming is known to have occurred in this area when the Dragon was further to the south in the past, it is actually stagnant ice stream. Unfortunately, there has not been any basal sampling in ER to provide direct information to guide interpretation of our radar results.
With regard to the thermal regime, heat-flow modeling together with borehole measurements indicate basal temperatures close to the melting point are pervasive in both ice streams and inter-ice-stream areas (Reference Hulbe, Payne, Alley and BindschadlerHulbe and Payne, 2001; Reference Joughin, Tulaczyk, MacAyeal and EngelhardtJoughin and others, 2004). The abundant water beneath WIS and other ice streams shows that basal temperature is at the melting point. The available data give basal temperature within 1–2 K of the melting point beneath ridges (Reference Kamb, Alley and BindschadlerKamb, 2001; Reference EngelhardtEngelhardt, 2003). Specifically with regard to this area of ER, downward extrapolation of temperature measurements over part of the ice thickness using thermal modeling indicates basal temperature close to the melting point (Reference Alley and BentleyAlley and Bentley, 1988).
Implications for Margin Processes
One expects relatively high (>0.2) power reflectivity from thick till dilated with conductive pore water (Reference Peters, Blankenship and MorsePeters and others, 2005, table I) as found beneath the central parts of WIS (Reference Engelhardt, Humphrey, Kamb and FahnestockEngelhardt and others, 1990). The bed reflectivity of this area of WIS has not been measured to directly confirm this expectation. However, the high bed reflectivity found under other ice-stream locations including parts of WIS further downstream (Reference Bentley, Lord and LiuBentley and others, 1998; Reference Gades, Raymond, Conway and JacobelGades and others, 2000; Reference Catania, Conway, Gades, C.F. Raymond and EngelhardtCatania and others, 2003) is probably associated with wet basal till. On this basis, we argue that the thick, dilated basal till known to be present in the center of WIS does not extend under the Snake (or exist under this local area of ER). A corollary is that the lubrication under the Snake occurs without thick, wet, dilated till.
Although we exclude any bed morphology with high reflectivity under the Snake, it is problematic to say what is there. One potential model to focus discussion is a smooth bed surface of low reflectivity lubricated by small amounts of water. If the lubricating water were thin (several mm or less) with electrical conductivity found under WIS, it would not be detected in comparison to a dry bed by the radar (Reference Gades, Raymond, Conway and JacobelGades and others, 2000). With cleaner water, thicker amounts of water could go undetected. Most probably the water would be fragmented into linked gaps or dispersed in pores of a thin, dilated till slurry.
An obvious, and probably unanswerable, question in this characterization is the composition and structure of the relatively non-reflective substrate. Some combination of low porosity and clean pore water is probably an essential feature. Till or other sediment that has been consolidated over considerable thickness, for example as a result of desiccation through removal of pore water to a freezing interface (Reference TulaczykTulaczyk, 1997) sometime in the past, is one possibility.
Partially frozen pore water in the substrate is another consideration. However, it is less compelling. Partially frozen till within a few degrees of bulk pressure-melting point can retain fairly high basal reflectivity (Reference JiracekJiracek, 1967; Reference Hoekstra and DelaneyHoekstra and Delaney, 1974) because of residual pore water with high electrical conductivity maintained by surface interactions and concentrated impurities. In any case, partially frozen till beneath a wet lubricated bed surface as under the Snake would imply transient thermal conditions, with the wet bed condition being recently established by water injection along the bed or dynamic heating associated with recent outward migration.
Discussion
The spatial pattern of reflectivity associated with the Snake is consistent with the findings in the margins of dormant ice streams where jumps in bed reflectivity can be several kilometers (4–10 km) inside the outer edge of buried crevasses (Reference Catania, Conway, Gades, C.F. Raymond and EngelhardtCatania and others, 2003). Evidently this feature of stagnant margins may not be just a consequence of basal drainage or freezing after shutdown, but may have been present even during active motion. Correspondingly, it could be common for active margins. Consideration of till continuity suggests a partial explanation. Since flow of ice from an adjacent ridge toward an ice stream is dominated by internal deformation without significant basal motion, the ice flow across the margin is not accompanied by advection of basal till. Basal motion in the margin itself would tend to sweep deforming till away into the ice-stream flow. Any dilated till layer would have to be built up by activation of local substrate material and would likely remain thin and not reflective.
While our data from the Snake provide a snapshot in 1998/99 and our discussion concerns bed conditions at that time, the recent history of this part of the Snake may have involved recent rapid outward migration. Reference Stearns, Jezek and van der Veen.Stearns and others (2005) compared aerial photography in 1987 with satellite-based SAR in 1997 and found evidence for approximately a 2 km outward (northward) jump of the Snake upstream from our measurements. Such a rapid jump of the Snake into the slope of ER would have implications for surface topography and internal layer geometry that we do not take up here. Accepting that such a jump may have happened, it is enticing to interpret the low bed reflectivity under the Snake to be a consequence of the recent initiation of lubrication with small amounts of clean meltwater and newly activated substrate that are not yet detectable. Correspondingly, the radar provides no evidence for any substantial difference in bed morphology going from the present Snake position into ER. Therefore, the possibility of (further) outward migration and that such migration could happen without dilation of a thick packet of till cannot be discounted. With regard to past margin positions, the lack of major disturbance in the internal layers outside the present margin indicates that it has not been further out in the recent past.
The present Dragon shear margin just across from these measurements appears to present a different situation. The Dragon has been migrating outward at slow speed on the order 101 ma–1 (Reference Harrison, Echelmeyer and LarsenHarrison and others, 1998; Reference Echelmeyer and HarrisonEchelmeyer and Harrison, 1999) toward a former margin identified by a lineation on the surface (called the Fishhook) from which it earlier migrated inward at higher speed of order 102ma–1 for about 200 years (Reference Clarke, Liu, Lord and BentleyClarke and others, 2000). As mentioned above, borehole measurements determine that basal till is present under this transient ice-stream area. It is plausible that the ongoing expansion is associated with reactivation of that basal till. Similar circumstances are likely to hold for other now or earlier active margins that are known to be inside former areas of active streaming motion, such as the most recent north margin of Kamb Ice Stream (Reference Jacobel, Scambos, Nereson and RaymondJacobel and others, 2000) and the present Snake further to the west close to where it reaches the Ross Ice Shelf (Reference Catania, Conway, Gades, C.F. Raymond and EngelhardtCatania and others, 2003).
Conclusion
Ground deployment of a low-frequency radar system allows imaging of the subsurface beneath the chaotic zone of ice-stream margins. Internal layers of ER extend without disruption beneath the active north margin of WIS. Radar returns from internal layers enable calibration of propagation losses through the fractured near surface and evaluation of spatial changes in relative reflectivity of the bed. Large contrasts in basal reflectivity between the adjacent ER and the active margin were not detected. An expected jump in reflectivity from low values beneath the ridge to high values in the central parts of WIS associated with wet, dilated till must lie inboard of the Snake. Lubrication under the Snake must have different character than in the central parts of the ice stream relying on relatively small amounts of water with at most sub-meter thickness of dilated till.
Acknowledgements
This research was supported by US National Science Foundation grant Nos. OPP-9725882 and OPP-9909469. The expertise of M. Conway contributed immeasurably to our field operations within the fractured terrain of the Snake. Collaboration with a field team concurrently measuring strain distribution in the Snake, led by the late I. Whillans, with support from OPP-9615127, provided much collegial encouragement and essential back-up for safe work of our three-member field team. C.J.v.d.V. acknowledges support from NASA through NAG5-11383. L. Stearns provided information about the location of maximum strain rate in the margin that enabled our discussion of the bed reflectivity pattern. Comments from two reviewers (R. Jacobel and anonymous) led to substantial improvements in the manuscript.
