Introduction
The few studies which have been made on shapes of crystals from crystalline aggregates in a glacier include the following: Reference BaderBader (1951) observed that crystals collected from a glacier had markedly complicated shapes. Rigsby (1968) proposed a quantitative method of analysing the shape of crystals. Reference KizakiKizaki (1969) showed that polygonal ice crystals located up-stream in a glacier grew and underwent deformation to have irregular shapes as it moved down-glacier. Reference Narita, Kusunoki and SuzukiNarita and others (1979) introduced a stereological method in their analysis of a core from Antarctica. Most of these studies were concerned, however, with the crystal shape itself, devoting little attention to the discussion of any correlation between the orientations of crystallographic axes and the shape of a single crystal. The present study aims to look into the existence of such a correlation.
Method of measurement and results
Single crystals of ice were brought back by HU-AGE ‘75 (Hokkaido University Alaska Glacier Expedition 1975) from Mendenhall Glacier, Alaska, U.S.A. (Reference HigashiHigashi and others, unpublished), after collection from veins of large crystals in icebergs which had been calved from the terminus of the glacier floating on the glacier lake. The icebergs were exposed to the Sun, which melted the grain boundaries of individual single crystals, making it easy to identify each of them. Consequently, large-sized single crystals could be identified and collected with hardly any damage to their exterior surface, thus enabling them to preserve their original shape. Meanwhile, an aggregate of single crystals, which constituted a block, was also collected from a vein of an iceberg; thin sections of this block, which are shown in Figure 1, had the fabric pattern of the typical four-maxima type (Higashi and others, unpublished). Crystallographic orientations of the large-sized single crystal were determined to within ±3° by the method of optical reflection by crystallographic surfaces namely the {1010} and {0001} planes, utilizing a piece of hoar which was condensed on the surface of the ice sample. Figure 2 shows one of the single crystals with the crystallographic axes indicated. As shown here, most of them had both the flattened and the elongated shape. Though the crystals had a somewhat interlocked shape as indicated in Figure 2, the correlation between the orientation of crystallographic axes and the shape of a single crystal was investigated by approximating the crystal shape to an ellipsoid in order to obtain a quantitative expression of the orientation of its elongation. That is, the orientation of three axes of the ellipsoid was estimated by fitting an ellipsoid by eye to the shape of the crystal within an error of ± 10°; then the lengths of the three axes and their misorientations relative to the crystallographic axes of the crystal (i.e. c-axis and a-axis) were measured. Figure 3 gives a correlation between the axes of the ellipsoid and the crystallographic axes of the crystal in a stereographic projection with the shortest axis of the ellipsoid at the centre of the projection circle. Solid circles and open circles of the figure show c-axes and a-axes of the crystal respectively. It appears from the figure that most of them had a flattened shape in directions close to the c-axis and an elongated shape in the direction of one of the a-axes. The mean ratio of the length of the shortest axis of the ellipsoid to that of the longest axis was 0.44, and the mean ratio of the length of the middle axis to the longest axis was 0.63.
Meanwhile, ice-core samples were drilled at Amery Ice Shelf and Cape Folger by ANARE as part of its project led by Dr W. F. Budd of the Antarctic Division, Australia. Reference BuddBudd (1966) and Reference Wakahama and KuroiwaWakahama (1974) reported the results of dynamical and textural studies using the data obtained from the ice-core samples. The present authors also analysed a core from a depth of 324 m at Cape Folger by preparing serial thin sections made at an interval of 5 mm to obtain shapes and sizes of randomly selected crystals. According to Reference Wakahama and KuroiwaWakahama (1974) the mean crystal size at this depth is the largest of all the core samples from Cape Folger. Figure 4 shows photographs of horizontal and vertical thin sections taken under crossed polaroids. Crystallographic orientation was determined by the transmission Laue technique. The fabric pattern of the core sample also showed the typical four-maxima type (Reference Wakahama and KuroiwaWakahama, 1974). The individual single crystals of the crystalline aggregate from the Cape Folger core were approximated to an ellipsoid in the same way as for the single crystals from Mendenhall Glacier. A similar result was obtained for them as for the Mendenhall Glacier ice as given in Figure 5; that is, the individual crystals were flattened in a direction close to the c-axis and elongated to the direction of one of the a-axes. The mean ratio of the length of the shortest axis of the ellipsoid to that of the longest axis was 0.46, and the mean ratio of the length of the middle axis to the longest axis was 0.64.
A stereological analysis was made following the method of Reference UnderwoodUnderwood (1970, p. 48–79) to examine a possible relation between the flow direction of a glacier and the shape of its single crystals. Two sections intersecting at right angles in each of Figures 1 and 4 have been used to obtain rose diagrams, as shown in Figure 6. A rose diagram gives a visible indication of a stereologically oriented structure by recording on a polar plot the number of intersections between grain boundaries in the thin section and the constant length of a test line which is rotated around its centre. The diagrams reveal that the Mendenhall Glacier sample has no preferred elongations in any specific direction in space since the diagrams are rather isometric (Fig. 6a, b). In the case of the Cape Folger sample the horizontal section also shows a stereologically randomly oriented structure in the horizontal section (Fig. 6c). However, the rose diagram for the vertical section shows that the shapes of the crystals are elongated in the direction x–y (Fig. 6d) since there is a decrease in the number of intersections in this direction. This implies that the shapes are preferentially elongated in a specific plane with an inclination of 30° to the horizontal as given in Figure 6d. Since the sample is derived from a core whose horizontal orientation is unknown, the relation between this direction x–y and the flow direction is unknown.
Concluding remarks
As shown by these two results, single crystals in glaciers which had the four-maxima type of fabric pattern, showed a correlation between the crystallographic axes and the shape. This correlation is thought to originate from anisotropy in growth rate in the glacier, since both samples analysed in this study had large crystals, as mentioned above.
Acknowledgement
Some portions of this research derive from work forming part of the Hokkaido University Alaska Glacier Expedition 1975 (leader: Professor A. Higashi). The present authors wish to express thanks to Dr W. F. Budd for kindly supplying them with ice-core samples.