Introduction

The work of the United States Antarctic Research Program party who wintered at Scott Base during 1959, preparing for the 1959–60 Victoria Land traverse, included glaciological observations on the part of the Ross Ice Shelf near Scott Base. Observations were made between January and September 1959 and in the month following the traverse party’s return to Scott Base on 10 February 1960.

Because no glaciological program for the winter had been formulated and the investigators were inexperienced, much time was spent in developing techniques. The observations were not distributed areally in the optimum manner and the data are incomplete, but this report illustrates some of the glaciological problems of the area and indicates the field work which is still required.

Most of the observations were made by A. W. Stuart, assisted by Mr. A. J. Heine of the New Zealand Geological Survey. Mr. Heine, in addition, measured the movement of the markers close to Scott Base and also assisted in the reduction of the data at this Institute.

Physiographic Setting

Scott Base (lat. 77° 51′ S., long. 166° 45′ E.) is at Pram Point, at the south-eastern extremity of the Hut Point peninsula of Ross Island (Fig. 1).

Fig. 1. Map of the north-western part of the Ross Ice Shelf, showing location of outlying movement stations. (Based on New Zealand Lands and Survey Department map N.Z.M.S. 135)

The Ross Ice Shelf occupies the approximately triangular area between the points lat. 78° S., long. 164° E., lat. 77° S., long. 158° W., and lat. 85° S., long. 160° W., although its northern limit, in McMurdo Sound and the Ross Sea, varies from year to year. In the north-west the northward flow of the ice shelf is hindered by Minna Bluff, Brown Peninsula and White, Black and Ross Islands.

It is convenient to divide the part of the Ross Ice Shelf north of Minna Bluff and west of long. 171° E. into three areas (Fig. 2) : (i) the north-western margin of the main Ross Ice Shelf, from about long. 171° E. to roughly a line from station 89 to Cape Crozier, where the ice movement is northwards; (ii) a transition zone, bounded in the east by the line from station 89 to Cape Crozier and in the west by the line from the north end of White Island to Cape MacKay; and (iii) the area bounded in the east by the White Island–Cape MacKay line, on the south by White and Black Islands, and in the north and west by Ross Island and McMurdo Sound, where the ice movement is predominantly westwards. For this third area the name “McMurdo Ice Shelf” is used. Significant differences exist in the regime of the eastern and the western parts of the “McMurdo Ice Shelf”; most of the present observations and discussion refer to the eastern part.

(Photograph 262 F-31 VX-6 USN 3/12 5 December 1956 0626Z; courtesy of U.S. Navy)

Fig. 2. Aerial photograph of Ross Island and part of the Ross Ice Shelf, looking northwards from above station 89.

Snow Accumulation on the Ice Shelf

Movement of the Ice Shelf

The movement of the ice shelf over various periods was determined at 40 points within 30 km. of Scott Base. The stake positions are shown in Figures 1, 3 and 4. and the movement. vectors, extrapolated or interpolated to a one-year period, are listed in Table II.

The positions of most of the stakes close to land were determined by triangulation from well-surveyed points on land, whereas those of stakes on the trail to the Skelton Glacier and near White Island were determined by resection.

The probable errors in the calculated velocity and in the direction of motion are about 5 m.yr. ⁻¹ and 5° for triangulated stations, and up to 30 m.yr.⁻¹ and 10° for the resected stations.

In the area east of the line from station 89 to Cape Crozier (stations 86, 86A, 87 and 89; Fig. 1) the ice movement is northward. The velocities at the neighboring stations 86 and 86A average 844 m.yr.⁻¹, the highest yet measured on the Ross Ice Shelf. (However, Reference CraryCrary (1961 [a]) has estimated an ice velocity west of Roosevelt Island as high as 1,400 m.yr.⁻¹.) To the north-west of station 86 the velocity decreases, and at station 89 it is 505 m.yr.⁻¹.

The conditions in the transition zone appear to be complex and unfortunately only one value for the movement is available, namely that at station 91. This gives an apparently anomalous velocity of 688 m.yr.⁻¹ in a southerly direction. Reference CraryCrary (unpublished) reported that the ice thickness in the transition zone varies; for example, it is greater at station 92 than at stations 90 or 91. Series of pressure ridges in this zone converge on Cape Crozier (Fig. 2) and crevasses are present.

At the measured points in the eastern part of the “McMurdo Ice Shelf” the ice movement is westward or north-westwards. Twenty kilometers from Scott Base the velocity is about 200 m.yr.⁻¹ (stations 93, 101 and 104; Fig. 3), but closer to Scott Base it drops to about 100 m.yr.⁻¹ (in good agreement with velocities between 67.5 and 89.1 m.yr.⁻¹ measured at 7 points by Reference Macdonald and HathertonMacdonald and Hatherton (1961)). This velocity is maintained to the edge of the ice shelf except where it abuts Ross Island and the old sea ice between Cape Armitage and Pram Point. In the area of the pressure ridges, very close to Scott Base (Fig. 4), the velocity decreases rapidly westwards. At stations 39, 40, 42 and 43, east of the pressure ridges, the velocity is about 85 m.yr.⁻¹ while at stations 38, 37 and 36 in the pressure ridges the velocity is much less, and is decreasing westwards, to 4 m.yr.⁻¹ at station 36. Furthermore, the direction of movement progressively changes from westwards, east of the ridges, to south-westwards at the closest station (36) to Pram Point.

The nature of the transition zone has not been fully determined. If the “McMurdo Ice Shelf” is merely a distributary of the main Ross Ice Shelf, then the transition zone is a shear zone associated with the blocking of the northward flow by Ross Island and the complex stress conditions which produce the change in flow direction. However, if a considerable part of the ice in the “McMurdo Ice Shelf” is obtained from Ross Island, the ridges in the transition zone may be largely the result of normal compression. The existing observations show southward movement at station 91, thinner ice in the transition zone on a line south-west from Scott Base, and ice thicker near Ross Island than 20 km. farther south (Reference Macdonald and HathertonMacdonald and Hatherton, 1961), but additional information is required on ice movement in the eastern part of “McMurdo Ice Shelf” and in the transition zone.

Horizontal Strain of the Ice Shelf and its Effect on Density

Measurements of the surface horizontal strain rate were made near the thermohm site (Fig. 4) . An L-shaped line was orientated so that one leg was parallel to the direction of movement (and of maximum strain) while the other was normal to it. Each Ieg was 1.5 km. long and was double-chained three times over a 12-month period. Parallel to the direction of movement the strain-rate was −0.0076 yr.⁻¹, while perpendicular to it the measured change in length was less than the measuring errors.

A second but less accurate value of the strain-rate is obtained by comparing the surface velocities at the thermohm station and at station 93. Between these points the mean strain-rate is −0.0071 ± 0.0010 yr.⁻¹.

The sub-surface snow density at the 7 m. pit site is higher than that reported at most polar sites having comparable values of accumulation and mean annual air temperature. Some representative density values (in g.cm.⁻³) are as follows:

Values for “Little America V” are from Reference RagleRagle and others (1960) and the remainder, except for Scott Base, are from Reference ZumbergeZumberge and others (1960). Densities at “South Ice” and Charcot are similar to those at “Eismitte” (Reference LoriusLorius, 1962).

The high values at “Camp Michigan” have been attributed to horizontal compaction (Reference ZumbergeZumberge and others, 1960) but the stress pattern there is very complex and produces intensive folding. Theoretical treatment has not been attempted yet. Near the Scott Base 7 m. pit the stress pattern appears to be simple and does not produce folding in the area of the pit. On glaciers a similar phenomenon can occur; Reference Crary and WilsonCrary and Wilson (1961) have shown that high densities on part of the Skelton Glacier are associated with negative horizontal strain-rates.

The effect of horizontal compression on the variation of density with depth is best shown by comparing the Scott Base and “Little America V” data. The mean annual temperatures and snow accumulations are nearly the same at the two places, but the horizontal strain at “Little America V” is much Less than that at Scott Base. Reference CraryCrary (1961 [b]) reported horizontal extensive strain-rates of 0.00129 and 0.00081 yr.⁻¹ normal and parallel to the direction of ice flow. The density values at Scott Base have been “corrected” for the effect of horizontal compression as follows. The effects of horizontal strain at “Little America” are ignored. It is assumed that the distribution of horizontal velocities on the ice shelf at Scott Base has remained unchanged for about 50 yr. The snow now at a depth of 15 m. in the pit was deposited 45 yr. ago on the surface east of the present station 93. Since then it has been subjected to a mean strain-rate of −0.00735 yr.⁻¹. The snow near the surface in the pit has been subjected to a strain-rate of −0.0076 yr.⁻¹ since it was deposited. It is assumed that the mean strain-rate to which the snow in the pit has been subjected varies linearly with its age beween these limits. Starting with a surface density of 0.391 g.cm.⁻³, the density increase per year due to the horizontal strain has been calculated and has been subtracted from the measured values. The original densities, the densities corrected in this way, and the densities at “Little America V” are compared in Figure 7. In view of the approximations involved, the agreement is good between the “corrected” Scott Base densities and those at “Little America”. The discrepancies at depth may indicate that the strain-rate in the past was less than now, or that the decrease in strain-rate eastwards is greater than that given by the comparison of velocity at the pit with that at station 93. (See also the section below.) It is also possible that positive vertical strain-rates exist, with consequent vertical thickening of the ice shelf. Since no data are available, this possibility has not been considered further, but any thickening must be at a rate less than that of bottom melting.

Fig. 7 Variation of snow densities with depth at Scott Base 7 m. pit and at “Little America V”

Infiltration of Brine into the Ice Shelf

In addition to the core to 15.42 m. at the 7 m. pit, another was drilled to 13.7 m. at the thermohm station and shallower ones at stations 36 and 2 (Fig. 4). In all of the cores the firn was brine-soaked below a certain level; the slush in the two deeper holes prevented deeper drilling by hand. Measurements of salinity were made at intervals along the cores.

At stations 36 and 2 brine was encountered approximately at sea-level; at the thermohm site at a depth of 5.26 m. (approximately 0.7 m. below sea-level) and at the 7 m. pit at a depth of 15.10 m. (4.1 m. below sea-level). Brine-soaking continued from these depths to the bottom of all the holes. Figure 8 represents the situation.

Fig. 8

It is clear that the material near the bottom of these holes is brine-soaked firn and not sea ice. At a depth of 15.18–15.30 m. at the 7 m. pit site the density is 0.71 g.cm.⁻³ and the salinity is 20‰. These values would be most unusual for sea ice. Furthermore, no difference in the fabric is found between the soaked and the neighboring dry firn.

Brine is also found in the Ward Hunt Ice Shelf (Ellesmere Island) (Reference Marshall and BushnellMarshall, 1960; Reference Lyons and LeavittLyons and Leavitt, 1961) and in the Lazarev Ice Shelf, but not at “Little America V”, Maudheim (Reference SchyttSchytt, 1958 [a], Reference Schytt[b], Reference Schytt1960) or “EIlsworth” (Reference NeubergNeuberg and others, 1959).

The mechanisms by which brine-soaking of the ice shelf can occur appear to be (a) vertical infiltration from the bottom, (b) lateral infiltration from the seaward edge, and (c) diffusion along crystal boundaries.

The diffusion method has been suggested for the Ward Hunt Ice Shelf by Reference Marshall and BushnellMarshall (1960), but the vertical transport of salt may be assisted by surface ablation and freezing at the bottom of the ice shelf. However, the absence of brine at all depths in the ice shelves at Maudheim, “Little America” and “Ellsworth” indicate that this is not a widespread process in Antarctica. Diffusion of salt solution is likely to be a slow process; bottom melting may proceed faster. At “Little America” bottom melting removes annually about 80 cm. of ice (73 g.cm.⁻²). Near Scott Base the bottom melting is comparable, so that the soaking there is not likely to be due to diffusion.

Because lateral and vertical infiltration can occur only in firn with interconnected pore spaces, the firn at sea-level at the ice shelf edge or at the bottom of the ice shelf must be permeable. For air the transition from permeable (firn) to impermeable (ice) occurs at a density of about 0.81 g.cm.⁻³, and in the absence of specific data it is assumed that the same critical density applies for permeability to brine.

At “Little America V” and at Maudheim this initial condition is met for lateral infiltration. At both places the density at sea-level is about 0.76 g.cm.⁻³ (Schytt, Reference Schytt1958 [a], Reference Schytt[b], Reference Schytt1960; Reference RagleRagle and others, 1960; Reference CraryCrary, 1961 [a]). In both areas the elevation of the ice shelf edge is less than it is at the drill site, so that the densities at sea-level at the edge should be less than 0.76 g.cm.⁻³.

Two other factors influence lateral infiltration: (a) the temperature, and (b) the forward velocity of the ice shelf. In the hole at “Little America V” the temperature at 7 m. below sea-level is −22.3° C., which is lower than the cryohydric point of salt water. At Maudheim the temperature at all depths is higher than −18° C. but the ice shelf is estimated to be breaking away at about 280 m.yr.⁻¹ (Reference SwithinbankSwithinbank, 1957 [a], Reference Swithinbank[b], Reference Swithinbank1958) which may be greater than the velocity of lateral infiltration.

The density at the ice shelf bottom is the controlling factor in the vertical infiltration mechanism; the horizontal movement of the ice shelf and the temperature in the ice shelf can only limit the vertical extent of infiltration. Because the ice-water contact must be at about −2° C., some penetration occurs even in fast-moving ice as long as the bottom is permeable.

At “Little America V”, Maudheim and “Ellsworth”, the density at the ice shelf bottom is more than 0.81 g.cm.⁻³, which should preclude vertical infiltration. Near Scott Base the bottom densities have not been measured directly and it is difficult to estimate them accurately because the densities in the upper layers are abnormally high.

An estimate of the bottom density at the 7 m. pit site is obtained as follows: the difference between the densities at “Little America V” and at Scott Base for given depths is listed in Table III as a percentage of the density at that depth at “Little America V”. In the 0–5 m. range the Scott Base density is 9.3 per cent higher, in the 5–10 m. range 15.0 per cent and in the 10–15 m. range 17.7 per cent higher than the corresponding densities at “Little America”. More annual layers (19) occur between 10 and 15 m. depth than between 5 and 10 m. (15) or between 0 and 5 m. (13). If the increase in density due to horizontal compaction were independent of density, the disparity between the Scott Base and “Little America V” densities would increase with depth faster than linearly. In fact, the disparity increases only from 15 per cent in the 5–10 m. range to 17.7 per cent at 10–15 m. It is therefore reasonable to assume that at greater depths the per cent density difference between the two profiles asymptotically approaches a constant value of about 20 per cent. (If the ice shelves were of greater thickness, so that the densities approached more closely that of pure ice, the percentage difference between the two profiles would decrease with depth and eventually disappear, since the densities at both places would reach the same value asymptotically.) With this assumption, of constant percentage difference between the densities at a given depth at “Little America” and Scott Base, the densities at the Scott Base site at depths greater than 15 m. have been estimated from the “Little America” data. The density should reach the critical value of 0.81 g.cm.⁻³ at between 33 and 34 m. The thickness of the ice shelf at the pit site is 32 ± 2 m. (see p. 412) ; therefore, the bottom density should be low enough to permit vertical brine infiltration.

East of the pit site where the ice shelf thickens appreciably the bottom density should exceed 0.81 g.cm.⁻³. A critical evaluation of the possible mechanisms of soaking could easily be made by examining cores from sites east of the 7 m. pit. If these cores were found to be brine-soaked, lateral infiltration would have to be the mechanism responsible. At present we can only report that at Maudheim, where lateral infiltration could have occurred, it has not, while at Scott Base, where either lateral or vertical infiltration could have occurred, the firn is soaked. The evidence, though not conclusive, strongly suggests that vertical infiltration is responsible for the soaking at Scott Base.

Apart from the “McMurdo Ice Shelf” and a small “ice shelf” near Wilkes Station, mentioned below, the only reported occurrence of brine soaking in shelf ice in Antarctica is near “Lazarev Station” (Reference DubrovinDubrovin, 1960). At a position 1.3 km. from the edge of the ice shelf brine was found at a depth of 41 m., 18 m. below sea-level, at a temperature of −13.5° C. Pumping tests show that the brine in the hole was part of a larger supply which could move readily through the firn. Vertical infiltration is unlikely here because the ice shelf is about 140 m. thick and must have a bottom density greater than 0.81 g.cm.⁻³. Apparently this situation contradicts the postulates given above. Horizontal ice velocities were not reported.

The Thickness of the Ice Shelf

Because it was not possible to drill by hand to the bottom of the ice shelf at the pit site and because the ice is too thin to permit the use of seismic methods, the thickness can be determined only approximately.

The surface elevation, determined by carefully controlled altimetry, was 11.0 ± 0.5 m. and the density of sea-water at the ice edge was 1.0260 g.cm.⁻³ (Reference Van der HoevenVan der Hoeven, unpublished). With an 11 m. surface elevation, freely floating ice shelves of the following thicknesses would have the stated mean densities: 34 m., 0.692 g.cm.⁻³; 32 m., 0.673 g.cm.⁻³; 30 m., 0.650 g.cm.⁻³; 28 m., 0.623 g.cm.⁻³. With an 11.5 m. surface elevation the mean density for a 32 m. thickness is 0.657 g.cm.⁻³. Accepting the densities at depth obtained by the extrapolation method given above, the mean density of a 32 m. thick shelf is 0.667 g.cm.⁻³.

The mean annual temperature is known to 15 m. depth and the ice-sea-water contact may be assumed to be −1.9° C. Assuming that the temperature gradient varies with proportion of total distance through the ice shelf as it does at “Little America V” or at Maudheim, the extrapolated temperature reaches −1.9° C. at about 32 m. It is appreciated that an accurate treatment of temperature distribution, taking the bottom melting into account, should be possible by the method outlined by Reference CraryCrary (1961 [b]) but this requires a knowledge of the thermal diffusivity at all depths. The effect of freely moving brine on the thermal diffusivity of firn is not known. (Crary used this method to estimate bottom melting. Since the amount of bottom melting near Scott Base can be estimated from the surface profile, a temperature profile through the brine-soaked ice shelf would be valuable chiefly in determining diffusivities.)

Bottom Melting

The “McMurdo Ice Shelf” thins towards its seaward edge. Of the three possible mechanisms, surface ablation, lateral spreading and bottom ablation, the first two disagree with the observations quoted.

Between stations 93 and 94 (where the bottom is impermeable ice) the ice shelf thins at about 44 g.cm.⁻² yr.⁻¹. Between the 7 m. pit and thermohm sites the rate is 73 g.cm.⁻² yr.⁻¹ (Reference Macdonald and HathertonMacdonald and Hatherton (1961) obtained a rate of 0.7 m. of ice per year, from limited data). Nearer the edge, and in the bay ice between Cape Armitage and Pram Point, the rate of bottom melting must be less, and in the bay it is probably nearly equal to the annual surface accumulation.

The brine soaking of the firn greatly assists the bottom ablation process. The brine probably loosens the ice crystals by solution until the firn forms a slush which can be removed even by a weak water current. The lower strength of the brine-soaked firn at Scott Base has been noted, and is in agreement with the observations on a small static “ice shelf” near Wilkes Station (Reference HollinHollin and others, 1961) where it was found that the soaked firn became less competent with increasing depth. To substantiate this conjecture, rates of bottom melting are required in dense sea ice of comparable thickness.

Observations during the winter of 1959 by Van der Hoeven (unpublished) at a site 5 km. south-west of Scott Base (Fig. 4) show (a) that sea currents averaging about 20 cm.sec.⁻¹ change direction diurnally with a mean current from the east of 7.5 cm.sec.⁻¹, in contrast to the anti-clockwise current around Ross Island, previously postulated (Reference Macdonald and HathertonMacdonald and Hatherton, 1961), (b) that the water is isothermal to 275 m. (in a total depth of 580 m.), and (c) that the temperature and salinity changed from −1.76° C. and 34.6‰ in May to −1.90° C. and 34.8‰ in August. Order of magnitude calculations show that to account for the bottom melting and the heat flow through the ice shelf, each vertical column of water of 1 cm.² cross-section must lose about 100 cal. between its introduction under the ice shelf, assumed to be east of Cape Crozier, and its emergence in McMurdo Sound. The corresponding decrease in temperature in the well-mixed isothermal layer would be much less than 0.01 ° C. It thus seems entirely reasonable to attribute the thinning of the “McMurdo Ice Shelf” to this westward-flowing current.

The Western Part of the “McMurdo Ice Shelf”

West of a line between the summit of White Island and Cape Armitage the ice shelf surface is ablating. The easternmost evidence of surface ablation was found in March 1959, a few kilometers south-west of station 101, where small surface melt holes appeared. These increased in size westwards and 7 km. west of station 101 many were 2 m. deep and up to 10 m. long. In the walls of these holes the stratigraphy was composed largely of superimposed ice interlayered with dirt bands. In September 1959 all of the holes had filled with drifting snow.

Several observations of surface ablation farther west have been recorded in the area of the Dailey Islands (lat. 77° 52′ S., long. 165° 18′ E.) (Reference DebenhamDebenham, 1920; Reference SwithinbankSwithinbank and others, 1961). It has been suggested that in this area the “McMurdo Ice Shelf” is maintained by freezing of sea-water onto its bottom, while the surface is ablating. Recent observations on the Ward Hunt Ice Shelf (personal communication from H. Lister, May 1962) confirm earlier suggestions that this ice shelf is nourished by bottom freezing. Nevertheless, the data given above and by Crary show that the main part of the Ross Ice Shelf is maintained by surface accumulation, and that bottom melting occurs, certainly near its northern edge and almost certainly over the rest of its area.

The reason for the change in conditions from surface accumulation near Scott Base to surface ablation near White Island is not known with certainty but it is now generally believed to be due to the presence of dust and moraine on the surface (from the land immediately to the south) which lowers the albedo. However, the figures given above (Fig. 6) show that even the winter surface accumulation is much less near White Island than near Pram Point.

It may be significant that the surface velocity in the ablating area (B-1, B-2 and B-3) is 18 m.yr.⁻¹ to the west, while nearby in the accumulating area (station 101) it is 71 m.yr.⁻¹ to the north-west (Fig. 3). Temperature profiles, salinity and density values through the ice shelf here are required for comparison with those on the Ward Hunt Ice Shelf of Ellesmere Island and in the bottom-melting areas of the “McMurdo Ice Shelf”.

Acknowledgements

It is a pleasure to thank Mr. A. J. Heine for his assistance in the field and in the office. Mr. F. G. Van der Hoeven also assisted with the field work. Members of the Institute have helped in various ways. In particular, thanks are extended to Dr. F. Loewe for reading the manuscript. This work has been supported by National Science Foundation grants G-14818 and G-20473.