Location and description of ice shelf

The northernmost edge of the Ward Hunt Ice Shelf borders on the Arctic Ocean approximately along the lat. 83° 12′ N. parallel. The east and west extremes of the shelf are bounded by meridians long. 72° 00′ W. and long. 78° 30′ W. respectively. Three mountain ranges with peaks over 3,000 m. high lie to the south in nearly parallel arrangement: the Challenger Mountains, the British Empire Range, and the United States Range, the most formidable of the three. Glaciers from these mountains flow into three bays: Markham Bay at the east end of the shelf; Disraeli Bay in about the center; and M’Clintock Bay at the west end of the shelf (Fig. 1). No doubt at one time these glaciers fed the main glaciers which occupied the fiords leading into the bays. This, however, is no longer true for during the height of the summer melt there is open water in the fiords.

Fig. 1. Index map of Ellesmere Island with the Ward Hunt Ice Shelf and locations of ice cores drilled in 1960

The shelf is composed of two parts: the inner, older shelf (south of Ward Hunt Island and up to 7 km. wide) described by Reference MarshallMarshall (1955), Reference CraryCrary (1960), and Reference Lyons and LeavittLyons and Leavitt (1961, p. 36), and the outer, younger shelf (north of the Ward Hunt Island and 12–15 km. wide) from which the ice cores were obtained. According to Crary, the older portion of the shelf is probably 1,600 to 3,000 yr. old, whereas the younger portion is only 1,600 yr. old or less.

Ward Hunt Island lies just outside of Disraeli Bay about 5 km. north of the nearest shore of Ellesmere Island. It is identified by an unnamed hill on the east end of the island and by Walker Hill (500 m. a.s.l.) on the west end. The hills are separated by a saddle occupied in part by a small lake. The main camp of the four-man drilling party was located on the north slope of this island near the shore (Fig. 1).

The Ward Hunt Ice Shelf is composed of three primary physiographic features: the floating shelf, the grounded ice rises,Footnote * and a re-entrant.Footnote † The single dominating characteristic of the floating shelf is the ridge and trough system running east–west and superimposed upon the sea-ice platform. Equally interesting is the ice rise contiguous to Ward Hunt Island and the Markham Bay re-entrant that is believed to have formed since 1947 (Fig. 2a, b).

Photograph: R.C.A.F. Scale 1:128,000

Fig. 2a. Ward Hunt Island and grounded ice rise. Note also the ridge and trough system running generally east-west and the lakes occupying the troughs.

Photograph: R.C.A.F. Scale 1:128,000

Fig. 2b. Markham Bay re-entrant with ridge and trough system of the ice shelf on the west and pack ice to the north.

Core drilling

Ice cores were taken from each of the three physiographic features of the ice shelf and thermal profiles from each hole were recorded for study of sub-surface morphology (Reference Lyons and LeavittLyons and Leavitt, 1961) and thermal history (Reference Lyons and RagleLyons and Ragle, 1962). Approximately 130 m. of a core 7.5 cm. in diameter was packed and shipped to Dartmouth College Polar Studies Cold Laboratory in Hanover, New Hampshire, for study.

Hole No. 1 (Fig. 1) was drilled on a ridge and provided about 35 m. of core before slush in the hole threatened freezing in and possible loss of the auger. Seismic records indicate a depth to water of about 41 m. (Reference Crowley, Rigsby and BushnellCrowley, 1961). Core from hole No. 4, drilled in the trough immediately north of the ridge hole, yielded 34 m. before slush again prevented further drilling. The third core (Fig. 1, No. 5) was taken through the ice rise to a depth of 55 m., where the auger grounded in glacial till. Only the uppermost 36 m. were recovered in time for transport to Dartmouth. The remaining 19 m. were drilled and examined in the field by J. B. Lyons of the Department of Geology, Dartmouth College.

Two cores (Fig. 1, Nos. 2 and 3) taken from the Markham Bay re-entrant showed it to about 11 m. thick and to consist principally of sea ice. The lithologic complexity of this ice suggests that it did not form in place but was more likely a re-entry of rafted and hummocked pack ice which had become fast ice and an integral part of the shelf. This same lithologic complexity is also found in the transition ice at the interface between the easily identifiable glacier ice and sea ice in the cores taken from the ridge, trough, and rise.

Glacier ice

Glacier iceFootnote * is clear to bubbly, somewhat cloudy ice exhibiting a variety of structures and a rather constant texture. Etched by infrared light or viewed in plane polarized light, glacier ice has a homogeneous, medium-grained texture of equant-shaped grains, i.e. euhedral.Footnote †

The criteria for identifying glacier ice were its density, chemistry, generally medium-grained texture, equidimensional grains in thin section, variable transparency, and large number of bubbles.

The texture of glacier ice is generally medium and granular. Most of the grains are 0.5–1.5 cm. in size but may range from fine to coarse (Figs. 3, 4, 5). The equidimensional or equant shape is characteristic of this ice type except along a healed fracture or fault where many of the grains become elongated.

Fig. 3. Horizontal thin section of fine and medium texture glacier ice (trough core; depth 23.96 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Fig. 4. Horizontal thin section of medium texture glacier ice (trough core; depth 2.03 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Fig. 5. Vertical thin section of medium and coarse texture glacier ice (trough core; depth 22.28 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Lake ice

Lake ice on the Ward Hunt Ice Shelf forms in transitory bodies of water which coexist with the ice forming their basins (Lake Type 23c, Reference HutchinsonHutchinson, 1957); i.e. it forms when summer melt water freezes in troughs of the ridge and trough topography and in puddles or incipient troughs of the re-entrant. It is easily recognized by its medium to very coarse grain texture, the long columnar crystals with straight grain boundaries, and the long, linear, well-oriented bubbles which terminate at a boundary defined by 1–2 cm. of crystal-clear ice (Figs. 6, 7, 18, 19, 20). The greatest percentage of columnar grains observed in vertical thin section are larger than 3.0 cm.

Fig. 6. Horizontal thin section of medium to very coarse texture lake ice (re-entrant core; depth 2.77 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Fig. 7. Vertical thin section of lake ice (trough core; depth 10.25–10.40 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

In natural light, the lake-ice zones of the core could be determined, but more positive identification was made between crossed polaroids. Research by Lyons and Persson (personal communication) indicates that oxygen analysis can also be used as a reliable parameter in identifying lake ice.

Medium grains form close to or in contact with the air and cold ice along the sides and bottom of the trough. These grains are more granular and tabular than columnar. This same general growth pattern was observed in a temperate lake by Reference RagleRagle (in press) when a very cold, calm night produced a surface of granular and tabular texture underlain by columnar crystals. Lake ice for the most part is euhedral and subhedral.

Sea ice

Most sea ice viewed in natural light is cloudy and homogeneous. The cloudiness is caused by the presence of very small bubbles, generally less than 500 μ; the homogeneity probably results from infrequent fluctuations at the interface of the physical and chemical environment of growing saline crystals. This megascopic characteristic usually was sufficient to distinguish this ice type from other types.

Grain-boundary relationships of old sea ice are distinctly different from those of other ice types. Over natural light, characteristic sutured and irregular grain boundaries became evident after a warm iron had been passed over the ice followed by a rapid and light sponging. This interdigitating growth assemblage was composed of a wide range of textures. There were instances where large grains, themselves intergrown, were penetrated and surrounded by medium-grained to very fine-grained crystals. When this type of sea ice, which can be called “porphyritic”, was found, it usually alternated with a homogeneous texture of fine-grained, subhedral crystals.

The grain sizes in sea ice range from fine to coarse and the crystals are mostly tabular (Figs. 8, 9, 10). Areas of fine-grained sea-ice crystals up to 0.3 cm. in diameter were fairly homogeneous in texture (Fig. 11), but areas of crystals from 0.3–3.0 cm. were inhomogeneous in size or shape (Figs. 12, 13). Within their size range, most grains were tabular or columnar with many interesting assemblages of needlelike or thinly tapered crystals. Boundaries are irregular and texture may be said to be anhedral.

Fig. 8. Horizontal thin section of very fine and fine texture homogeneous sea ice (re-entrant core; depth 9.40 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Fig. 9. Horizontal thin section of medium to coarse texture inhomogeneous sea ice (re-entrant core; bottom; photographed between crossed polaroids, grid lines are 1 cm. apart)

Fig. 10. Vertical thin section of sea ice showing typical sutured crystal boundaries, brine pockets, and also healed fractures indicated by the two light colored diagonal lines of bubble concentrations (ridge core; depth 27.26–27.46 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Fig. 11. Vertical thin section of the bottom 20 cm. of re-entrant core showing evidence of annual increments of crystal growth (photographed between crossed polaroids, grid lines are 1 cm. apart)

Fig. 12. Vertical thin section of transition ice indicating chaotic appearance and mylonitic texture caused by milling action along a fault (trough core; depth 28.87–29.03 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Fig. 13. Horizontal thin section of sea ice in the transition zone with rounded crystal edges (trough core; depth 25.69 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

The texture of old sea ice is generally coarse and tabular, yet there are zones of granular texture. Both Reference MarshallMarshall (1955) and Schwarzacher (personal communication) have identified the sequence of granular texture followed by columnar texture to be an annual increment of growth. In Marshall’s case, this increment was identified in old sea ice south of Ward Hunt Island. However, Schwarzacher measured and identified this increment in new sea ice forming on the bottom of a floe. Figure 11 shows a vertical thin section between crossed polaroids from the bottom 20 cm. of the re-entrant core. Indicated in the photograph is the break between two growth periods, the break occurring approximately 12 cm. from the bottom of the section. Of interest are the much more regular grain boundaries exhibited by the recent coarse-grained crystals in comparison with the irregular boundaries of the older generation of sea ice above. It is possible that the fine-grained ice may represent slush-like saline aggregates which are rafted along the bottom of the sea ice until they become fused to the ice undersurface. Also it may be possible that this fine-grained component is fresh-water ice from melt water flowing under the shelf and freezing (Reference SchwarzacherSchwarzacher, 1959; Reference Lyons and LeavittLyons and Leavitt, 1961). This would explain the abrupt change apparent between the fine and coarse textures. During his studies on Drifting Station A, Schwarzacher (personal communication) found that the break between crystal generations is more commonly identified as a slight dislocation but continuation of former crystal growth. This dislocation can be seen only after etching a vertical thin section.

An empirical criterion for identifying sea ice was encountered during the coring operation. A marked increase in the length of unbroken core occurs as soon as the auger penetrates sea ice. Sea ice, because of its greater plasticity, yielded sections of core up to 90 cm. in length; this was in striking contrast to the glacier-ice core which broke by glassy, often conchoidal fractures, and was rarely recovered in pieces longer than 30 cm.

Transition ice

Transition iceFootnote * has the characteristics of the three other ice types and is believed to be the buried former edge of the ice shelf. This ice type was first seen in thin section between crossed polaroids near the anticipated glacier ice-sea ice contact. A zone of mixed typical glacier and sea-ice grains 2 to 3 m. thick and a thin but unmistakable lens of lake-ice type was identified in the ridge, trough, and ice-rise cores. The faulted, chaotic appearance of this ice suggests one of the mechanisms by which the shelf grows.

In the zone of accumulation along the shelf edge, sea-ice floes, blocks, and cakes with a veneer of firn become rafted, fragmented, and disoriented by wind, wave, and tidal forces. The result is a mixture of ice types which, after becoming fast ice, is gradually sandwiched and buried in a landward direction by firn accumulating above and the sea ice accumulating below.

Evidence to support this thesis (personal communication from Moira Dunbar) was found in the re-entrant cores (Fig. 1, Nos. 2 and 3) and strengthened by interpretation of aerial photographs taken by the U.S. Air Force in July 1947, which show that the re-entrant was jammed with much broken-up sea ice quite indistinguishable from the rest of the pack off the edge of the shelf. There were even small open patches in the area. Trimetrogon photographs taken in 1950 by the Royal Canadian Air Force show the ice to have become unquestionable fast ice and an integral part of the shelf.

The structural history of the Ward Hunt Ice Shelf is an important consideration in accounting for the inhomogeneily of the textures found in transition ice. Ice of every origin so far identified in the structure of the shelf can be identified in the transition ice of each core. Within the section are glacier ice, lake ice, and sea ice as well as zones of brecciated ice which indicates rafting or faulting. This similarity in disorder led to the conclusion that the mechanisms which contributed to the formation of the Markham Bay re-entrant most likely were analogous to those which established the original platform upon which snow was deposited and below which sea ice accreted. An almost “mylonitic” texture can be observed along fractures within this chaotic zone (Fig. 12).

In several horizontal and vertical thin sections of transition ice (Figs. 13, 14, 15), the sharp corners and edges of granular, “needle” (tabular) and columnar crystals have been blunted and rounded. A “jigsaw” pattern of interdigitating crystals, each with one or more rounded projections, suggests that brines, migrating through the boundaries of “youthful” ice, melt the crystal edges until enough dilution occurs to allow the brine to freeze at the existing temperature.

Fig. 14. Vertical thin section of iced firn or glacier ice in transition zone showing a marked rounding of grains (trough core; depth 24.85–24.95 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Fig. 15. Vertical thin section of chaotic ice in transition zone showing rsunded “needles”. Note also the recrystallization along a fracture (trough core; depth 25.48–25.63 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Fractures and faults

Fractures were common in all cores. All of the fractures showed evidence of healing either by the formation of new crystal assemblages (recrystallization) of different textures and orientation than the bordering grains (Fig. 15), or by the planar orientation of sheets of bubbles marking the “ghost” fracture (Figs. 10, 16).

Fig. 16. Bubble plane in lake ice marking a healed fracture (trough core; depth 5.93–6.03 m.)

It was observed in the field that overthrusting (rafting) of ice was clearly active at the edge of the shelf. Thin sections from the Markham Bay re-entrant core showed repeated truncation of crystals by obliquely oriented overlying crystals (Figs. 12, 17). In 34.94 m. of trough core (Fig. 1, No. 4), one normal fault was logged with a displacement of approximately 1 cm. The ridge core (Fig. 1, No. 1) also exhibited one normal fault of about 1.5 cm. displacement. Both faults occurred in glacier ice, the former at a depth of 4 m., the latter at a depth of 18 m. Most of the fractures and both faults were subvertical; very few of the fractures had a dip less than 45 degrees.

Fig. 17. Orerthrusting (rafting) in re-entrant core (depth 1.73–1.84 m.; photographed between crossed polaroids, grid lines are 1 cm. apart)

Bubbles

Bubbles constitute the most common structure in the cores. Theoretically their shape, composition, pressure and frequency should be distinct in all ice types and genetically related to the ice in which they occur, as well as having a quantitative relationship with the strength properties of ice. The size of the bubbles ranged from microscopic in glacier and sea ice to more than 10 cm. long in lake ice. The most frequent shape in glacier ice was approximately spherical, and in sea ice predominantly teardrop. In general, sea-ice bubbles were smaller and more numerous than those in glacier or lake ice, although long tubular bubbles similar to those in non-saline ice do occur. The cloudy appearance of much of the sea ice is consistent with the abundance of microscopic bubbles.

The occurrence of bubble clusters was nearly as common as that of single bubbles not in a cluster. Their shapes ranged from spherical to subspherical, and, as in the case of individual bubbles, clusters gave evidence of migration. Glacier ice contained more bubble clusters than lake ice, although lake ice exhibited many clusters in ice nearest to the freezing surfaces. Figure 18 is a section taken from the trough core. The break in the core is 5.6 m. below the present surface of the shelf. The photograph, taken in natural light, illustrates a typical pattern of lake-ice origin. At both ends of the section there are bubble clusters, which show evidence of migration, and dense lenticular bubble layers. These regions are followed by a confused zone of bubbles of many shapes and sizes displaying no apparent order or orientation. Finally, as a band of clear ice is approached, the bubbles become fistular and in most cases terminate abruptly at both top and bottom (Fig. 19).

Fig. 18. Section of lake ice showing the typical bubble pattern observed in all lake-ice increments of the core (trough core; depth 5.19–5.98 m.). The top of the core is at the to right; the bottom at the bottom left

Fig. 19. Long tubular bubbles terminating where last liquid water freezes in formation of lake ice. Note vapor figures (inclined disks) at top of photograph (trough core; depth 10.80–10.94 m.)

This clear band is believed to be the last liquid water to freeze. This opinion is substantiated by the following observation. During late September and October 1959, personnel from the U.S. Naval Civil Engineering Laboratory formed an ice pad on a ridge by successive floodings of a confined area. The water froze quickly as a result of rapid loss of heat to the atmosphere and to the cold reserve of the solid base. The temperature of the water at the source was + 1° C., and at the discharge end of the hose the temperature was 0° C. At night temperatures fell well below −18° C., reaching a minimum of −46° C. on 21 October 1959. A core taken from this pad showed that the rapid cooling of the water mass from the top and bottom produced ice identical to increments found in the ridge, trough, and rise cores. Figure 20 is a sketch of a section of the core taken from the pad.

Fig. 20. Sketch of core through a man-made lake. Note migrating bubble clusters and similarities to Figures 18 and 19

Dirt layers

Dirt layers were recognized in the ridge, trough and ice-rise cores. Except for a notable concentration in frequency and density in or immediately adjacent to the transition zone, the distribution and densities of the layers are quite constant. Generally the layers are spread over 1–4 cm. of core. Up to the present time no stratigraphic correlations have been recognized between cores. A high density dirt layer also was noted on or just below the 1960 summer surface.

Brine pocket

Brine pockets are found in the sea ice from all four cores. The best developed, however, are found in the youngest ice, ice from the re-entrant core (Fig. 21, 22). In all cores the pockets or layers of brine are from 0.3–0.8 mm. in thickness separating planes of more pure ice 0.8–1.5 mm. thick. The maximum values in both cases appear to be confined to the re-entrant ice.

Fig. 21. Horizontal section. Cross-section of new sea ice in re-entrant core showing brine pockets (grid lines are 1 cm. apart)

Fig. 22. Horizontal section. Cross-section of re-entrant core about 2 m. from top showing well-developed brine pockets (grid lines are 1 cm. apart)

Vapor figures

Vapor-figure concentrations occur with great frequency and varying density in all the glacier ice above the transition zone in the ridge, trough and ice rise cores (Fig. 19). An extensive visual examination of vapor figures in the trough core showed no correlation between the frequency, position, and density of vapor figure zones and other structural features. Orientation was noted but no fabric pattern evolved since there were as many horizontal figures (vertical c-axes) as those inclined to either side of the horizontal. Evidence of migration is present and indicates that most movement was upward.

Micropolygons

Micropolygonal figures on the order of 0.5 mm. in their largest dimension were observed in sea ice using a compound microscope with a high-powered objective. They were usually hexagonal in shape but also occurred as 4- and 6-sided polygons. These features are similar to the strain figures which precede subboundary formation described by Reference KnightKnight (1962) as associated with internal stresses. It is also possible that they are relic features resulting from a temperature flux.

Chlorine and sulphate

Chlorine and sulphate analyses were made on the cores to obtain quantitative information on the amount of these salts in the different ice types. These data helped define another parameter for the positive identification of a transition zone or interface between easily identifiable glacier and sea ice.

The chlorine ion concentration of the core samples was measured by a standard titration method with silver nitrate. Potassium chromate was used as the indicator, and standard seawater from Denmark (Cl−, 13.970‰) was the standard against which the titrations were performed.

Sulphate ion analyses were computed by the turbidimetric method (American Health Association, Inc., 1960) which involves the precipitation of the sulphate ions as barium sulphate followed by a colorimetric measurement of the ion concentration.

No background salts were detectable in the de-ionized water used for dilution in both Cl⁻ and SO₄ ⁻⁻ determination. The limits of detestability for the chlorine and sulphate are 0.06‰ and 0.002‰ respectively. Standard deviations were calculated from four groups of data and are as follows: chlorine in glacier ice 0.026‰; chlorine in sea ice 0.060‰; sulphate in glacier ice 0.060‰; sulphate in sea ice 0.163‰.

The results of these chemical analyses show that the glacier ice-sea ice interface, even in very old sea ice, can be detected easily. In Figures 23 and 24 it can be seen that there is little difference between the brine content of the two older cores and the younger re-entrant core. The rise core, in comparison, shows a low brine content, indicating that brine within the sea-ice member of the grounded ice rise either has continued to drain from the bottom because of less proximity to the sea-water or that it is a remnant of a shelf older than the floating shelf of present day and has had a longer time for the brine to drain. The re-entrant, though a recent addition to the shelf, would not be expected to differ from the older floating ice because rapid loss of brine occurs in the first year after the initial freeze followed by a much less rapid drainage (leakage) (Reference Weeks and LeeWeeks and Lee, 1962).

Fig. 23. Depth—chlorinity relations of four ice cores, Ward Hunt Ice Shelf, northern Ellesmere Island

Fig. 24. Depth—sulphate relations of four ice cores, Ward Hunt Ice Shelf, northern Ellesmere Island

Density

In the field, ice densities were computed from measurements of weight and volume. In order to be more certain of the third-place figure, however, the immersion method for calculating densities of solids was employed in the laboratory, using 2,2,4-trimethylpentane at a controlled temperature.

The spread of values of eight samples processed two or more times was 0.002 g./cm.³.

Figure 25 is a plot of the depth-density data. The zero datum is present sea-level and the position of the glacier ice-sea ice interface is marked. A least-squares analysis shows no significant correlation between density and depth in either the glacier or sea ice portions of the plot. However, there is a significant difference in density between the two ice types. The glacier ice also shows a larger scatter in the density values and perhaps a slight correlation between the modal density at a given level and the depth.

Fig. 25. Depth—density relationship

The plot and Figure 26 also show that the interface in the rise core is above the level at which it occurs in the ridge and trough. It is conceivable that the difference may be a measure of post-glacial isostatic rebound, for sudden uplift of this magnitude perhaps could explain the unpredicted break-off of the shelf which has occurred since the 1960 field season.

Fig. 26. Core site elevations recorded from surface

Dielectric constant

The dielectric properties of two ice samples, one from a glacier-ice zone and the other from a sea-ice zone, are listed in Table II. The measurements were made at a frequency range of 150–1,000 Mc./sec., and at temperatures ranging from -1° C. to −60° C.

The dielectric data obtained from the two ice samples indicate a larger dielectric constant and larger loss tangent for the sea ice. The larger dielectric constant would be expected in view of the larger density of the sample, and the larger loss tangent would be expected in view of a greater percentage of conducting ions.

The dielectric data thus show a correlation with the other groups of parameters covered in this paper. The difference in dielectric constant suggests the possibility of detecting the glacier ice-sea ice interface by the reflections of electromagnetic waves. A quantitative discussion of such techniques, however, is beyond the scope of this paper.