Report

Tributaries of West Antarctic Ice Streams Revealed by RADARSAT Interferometry

See allHide authors and affiliations

Science  08 Oct 1999:
Vol. 286, Issue 5438, pp. 283-286
DOI: 10.1126/science.286.5438.283

Abstract

Interferometric RADARSAT data are used to map ice motion in the source areas of four West Antarctic ice streams. The data reveal that tributaries, coincident with subglacial valleys, provide a spatially extensive transition between slow inland flow and rapid ice stream flow and that adjacent ice streams draw from shared source regions. Two tributaries flow into the stagnant ice stream C, creating an extensive region that is thickening at an average rate of 0.49 meters per year. This is one of the largest rates of thickening ever reported in Antarctica.

The West Antarctic Ice Sheet, which would raise sea level by 5 to 6 m if it melted, has been a subject of intense glaciological study since doubts about its stability were first raised (1). Unlike the Greenland Ice Sheet and most of the East Antarctic Ice Sheet, much of the West Antarctic Ice Sheet is grounded below sea level and underlain by marine sediments. When saturated with water (2), these sediments may affect the dynamics of ice motion by allowing fast movement. Although the possibility of a catastrophic collapse of the ice sheet is under debate (3), field and satellite observations have established that substantial changes are occurring in West Antarctica (4–6), particularly in the ice streams.

Theoretical arguments (7) and inferred results (8) predict that the onsets of the ice streams feeding the Ross Ice Shelf are migrating inland at rates of several hundred meters per year. Regions inland of the onsets, from which ice streams draw mass and inherit thermal and mechanical signatures, are largely unexplored. In our study, we used satellite radar interferometry to provide a broad-scale view of inland ice flow feeding into four West Antarctic ice streams.

Satellite radar interferometry (9) has become a well-established method for measuring ice motion. Unfortunately for Antarctic studies, all past and present civilian synthetic aperture radars were designed to fly with the instrument pointed north, so that areas south of 79°S, including much of West Antarctica, are not imaged. In September 1997, however, the Canadian RADARSAT satellite (10) was maneuvered to point toward the south for a period of 30 days in order to perform high-resolution mapping of the complete Antarctic continent (11).

The 24-day repeat period of RADARSAT provides an interferometric data set that is well suited for measuring the relatively slow (<100 m/year) motion of ice flowing toward the ice streams. Direct interferometric measurements in the faster moving areas, such as the main trunks of the ice streams, are more difficult because the large displacements occurring over the 24-day repeat period cause phase aliasing and decorrelation. In faster areas, vector ice displacements occurring between a pair of precisely coregistered radar images were determined through “speckle tracking,” although with lower resolution and poorer accuracy (12). In addition, a combination of interferometry and speckle tracking was used to achieve vector estimates in areas where observations from only a single direction were available.

We used data from the RADARSAT Antarctic Mapping Mission to produce a surface velocity map (13) of most of the region flowing into ice streams B, C, D, and E in West Antarctica (Fig. 1). Most of the area mapped in Fig. 1 lacks visible features, such as crevasses, required for feature tracking with optical imagery (14); interferometric methods are free of such requirements. In situ velocity measurements (Fig. 1) are sparse and irregularly spaced (15), so that, with the exception of the regular grid in the upstream region of ice stream D (16), they do not reveal spatial patterns of flow. These data, however, provide an important source of control for our velocity field. Our interferometric velocity data increase the number of velocity measurements in regions upstream of the ice streams by several orders of magnitude.

Figure 1

Ice flow speed determined from multiple swaths of RADARSAT Antarctic Mapping Mission data (13) coregistered with a mosaic of advanced very high resolution radiometer imagery. Ice flow is generally from top left to bottom right. The red dots show the locations of in situ velocity measurements used for control, with small red dots corresponding to the survey grid mentioned in the text (16). The red box indicates the locations of data shown inFig. 4. Blue lines show previously mapped ice stream margins (ice streams are indicated by letter). m/yr; meters per year.

The data (Fig. 1) show that individual ice streams are fed by multiple tributaries and that source areas are shared. Ice stream E receives ice from two tributaries that share the same upstream reservoir as a major tributary to ice stream D. The other major tributary that feeds D, previously identified and mapped through a field campaign (16), originates from the same source area as a previously unknown major tributary leading to ice stream C. Much of the southern tributary of ice stream C draws ice from close to the head of ice stream B.

Previous calculations of ice stream mass balance assigned distinct catchment basins to individual ice streams (17, 18). Shared source regions complicate the delineation of adjacent ice stream catchment areas and the calculation of individual ice stream mass balances. Moreover, shared source regions make it more likely that the relative contributions to neighboring ice streams change over time.

Ice streams have been mapped by a combination of visible and radar imagery and by radio echo sounding (18–20). Our results show that, upstream of the previously mapped ice streams, there exists a network of tributaries extending far into the ice sheet interior. Tributary speeds are faster than that of the surrounding ice, yet the speed contrast is too small to generate crevassed margins. The transition to an ice stream with crevassed margins takes place at a speed of ∼100 m/year. Short isolated sections of this network have been identified before (21, 22), but Fig. 1 shows the intricate nature of the flow network inland of the ice streams. Speeds within the tributaries are nearly an order of magnitude faster than that of the surrounding ice. It is probable that the distinct dynamics of ice streams coincides roughly with the formation of crevassed margins and that the dynamics within the tributary network upstream of the ice streams represents a combination of internal deformation and basal sliding.

The tributary network coincides with valleys in the subglacial topography (Fig. 2), with the correspondence being much stronger for the tributaries than for the ice streams (23). The tributaries are guided by and contained within subglacial valleys, and only rarely does ice flow cross a ridge between valleys. The deepest subglacial valley, called the Bentley Subglacial Trench (Fig. 2), is over 2500 m below sea level. Within this trench, a long wide tributary begins that feeds the northern tributary of ice stream C and the southern tributary of ice stream D. The faster flow in this trench is probably due to the fact that this ice is nearly twice as thick as the adjacent ice (24).

Figure 2

Ice speeds up to 100 m/year contoured over bed topography. The area shown is approximately the same as in Fig 1. Basal topography is the difference between ice sheet surface elevation (30) and ice thickness from a number of sources (29–31), resulting in a bed map with spatially varying resolution.

Relative differences in ice thickness in and adjacent to other subglacial valleys are not as large as those for the Bentley Trench. Thus, other processes are likely involved in the flow of those tributaries. In a region where accumulation and geothermal heat flux are constant, thicker ice will be warmer near the base, making the ice softer and more deformable, but this effect in combination with the larger ice thickness may not be sufficient to explain the larger speeds in other tributaries. Subglacial valleys are also expected to have collected sediment during times when the ice was absent, as well as the subglacial water formed from geothermal heating and basal friction. Because subglacial water and sediment are necessary for streaming flow, it is possible that they also contribute in some measure to tributary flow (21).

Ice streams D and E form in a broad low-relief basin (Fig. 3) and are fed by a network of narrow tributaries 10 to 20 km wide. Several features of the D and E regions stand out. First, most of the basin feeds ice stream E (18). Second, the southern tributaries of E and the northern tributaries of D diverge from one upstream source to become a network of features narrower than the coalescing tributaries seen elsewhere. Figure 2shows that this network conforms to relatively narrow valleys in the subglacial topography. Although these tributaries and the downstream portions of D and E are clearly separated from each other by bedrock ridges, they are joined in the tributary region. Third, the pattern of speed (Figs. 1 and 3) shows alternating acceleration and deceleration as tributary ice flows toward ice streams D and E.

Figure 3

Ice speed superimposed on surface elevation. View is upstream from the Ross Ice Shelf toward the inland ice divide. A section of the Transantarctic Mountains appears on the right. The origin is at the South Pole.

In contrast to ice streams D and E, observations and modeling studies have suggested that ice streams B and C are linked (19, 25), possibly because the bedrock topography between the two ice streams is relatively subdued (Fig. 2). Although ice stream B currently discharges ∼50% more ice than it accumulates over its catchment area (17, 18) and discharge from neighboring ice stream C is negligible (18), their combined discharges approximately balance their combined accumulation. Figures 1 and 3 show that the southern tributary to ice stream C cuts across the heads of the much shorter northern tributaries feeding ice stream B. This suggests that there is a limited area from which ice stream B can continue to draw ice without interacting with the northern tributary now flowing into ice stream C.

Although there are two active tributaries flowing into the head of ice stream C, the main body of the ice stream is known to have ceased rapid motion ∼140 years ago (26). Thus, the boundary region between the active tributaries and the formerly streaming portion of the ice stream must be thickening over time. The mean thickening rate over the red box in Fig. 1 is 0.49 ± 0.02 m/year (Fig. 4, bottom) (27). This thickening rate agrees well with an independent in situ measurement of 0.56 m/year obtained at the Upstream C camp (Fig. 4, bottom) (28).

Figure 4

(Top) Surface elevation along profile line A–B. (Bottom) Rate of ice thickness change (colors), surface elevation (contour lines), and flow direction over the box outlined in Fig. 1 (right edge corresponds to downstream edge in Fig. 1). Elevation contour interval is 25 m. Vector length is proportional to ice speed. Location of the Upstream C (UpC) camp is marked. White area at the right-hand edge of the bottom panel is due to a small gap in velocity data that is enlarged through subsequent calculations.

The thickening in this region is probably responsible for the formation of the 70-km-wide bulge discernible in the surface elevations (Fig. 4, top). Slightly higher thickening rates at the bulge's perimeter (approximately delineated by the 575-m elevation contour inFig. 4, bottom), suggest that the bulge is spreading slowly. Because active ice streams generally have lower surface elevations than the adjacent ice, this bulge probably has thickened more than its average height of 25 m above a horizontal datum. If the area now occupied by the bulge was depressed by a mean of 45 m below the adjacent ice when ice stream C stopped, the present flow field and the associated thickening rates would have formed a bulge with the observed volume. A depression of this magnitude is feasible on the basis of a comparison with active ice streams [for example, tributary B2, adjacent to the thickening portion of ice stream C (29)]. Thus, it is possible that the tributary flow of ice stream C has persisted despite the stagnation of the ice stream.

In the blue area of Fig. 4 (bottom) is an area thinning at a mean rate of 1 m/year. Examination of the flow pattern shows that ice in this region is diverging strongly as some ice continues to flow along ice stream C, and neighboring ice turns nearly 90° to flow into the northernmost branch of ice stream B (Fig. 4). This appears to be an evolving encroachment of ice stream B on C. Despite the high thinning rate, no expression of this pattern is seen in the surface elevations, suggesting that this encroachment is more recent than the stagnation of ice stream C.

Overall, the data show that long tributaries, flowing much faster than the surrounding ice, form an extensive network, delivering ice to the ice streams. These tributaries coincide with valleys in the subglacial floor where sediments, subglacial water, and warmer ice are expected to concentrate. Many tributaries emanate from common source areas, complicating the notion of distinct catchments. The discovery of this tributary network and its speeds establishes that the transition from slow inland flow to fast ice stream flow occurs gradually, over an extended distance.

  • * To whom correspondence should be addressed. E-mail: ian{at}radar-sci.jpl.nasa.gov

REFERENCES AND NOTES

View Abstract

Navigate This Article