INTRODUCTION

Law Dome, a local ice cap about 200 km in diameter with summit height of 1395 m a.s.l., is situated on the edge of the main East Antarctic ice sheet near the Australian Antarctic Station Casey. The snow stratigraphie studies on Law Dome started in the late 1950s and the investigation of the ice structure in the 1970s by American and Australian glaciologists. Main results of their studies are published in the papers of Cameron and others 1959; Hollin and Cameron 1961; Hollin and others 1961; Cameron and Bull 1962; Budd 1966; Budd 1972; Matsuda and others 1976; and Russell Head and Budd 1979.

As part of the cooperative programme of scientific studies in Antarctica under an agreement between Australia and China, the author was invited to participate in the 1982 Australian National Antarctic Research Expedition (ANARE) to Casey Station and had the opportunity to make a study of snow stratigraphy and ice structure on Law Dome.

ICE FORMATION ON LAW DOME

Determination of the characteristics of the ice formation and its distribution on Law Dome was the main aim of the author in his study of snow stratigraphy, in order to investigate the accumulation-ablation processes of snow on the surface of the polar ice sheet. Ordinary snow stratigraphie and crystallographic as well as oxygen isotope methods were used in more than 20 snow pits along the traverse routes at particular sites (Figure 1). The results of these studies affirmed the existence of a complete range of ice formation zones on Law Dome following the terminology of Shymskii (1955, 1962).

As shown in Figure 2, between the coast and the summit of Law Dome, the following progression was observed: ablation zone, infiltration-congelation (superimposed ice) zone, infiltration (wet snow) zone, cold infiltration (percolation) zone, regelation-recrystallization zone and recrystallization (dry snow) zone. It was hyphothesized that a warm infiltration-recrystallization zone existed on the northeast coast resulting from the high rate both of accumulation and ablation near the coast.

Fig. 1. Map of Law Dome with surface elevation contours, showing location of traverse routes, pit and sampling sites, and of borehole sites and other key points.

Fig. 2. Map showing the geographical distributions of ice formation zones on Law Dome. I Ablation zone; II Infiltration-congelation zone; III Infiltration zone; IV Warm infiltration zone; V Cold infiltration zone; VI Regelation-recrystallization zone; VII Recrystallization zone.

The distribution of these zones on Law Dome was asymmetric: zonal boundaries occurred at higher elevation on the west side than on the east (Figure 2), reflecting the asymmetry in accumulation and thermal conditions.

Fig. 3. Curves showing change of crystal size (S), bubble elongation ratio (E), borehole inclination for 1 year (I), and oxygen isotope ratio (δ¹⁸) with depth (Z) for BHC 2.

The pits near Cape Folger (shown in Figure 1 as C.F.) located on the boundary between the infiltration-congelation zone and infiltration zone are very sensitive to climatic changes. Thus these pits can indicate a possible climatic change. The change from fine-grained infiltration ice at 10 m depth to coarse infiltration-congelation ice, and to congelation ice at 0.5 m depth suggested an increase of air temperature and a decrease of accumulation over the last ten years, which was supported by climatic records of Wilkes Station (1958-69) and Casey Station (1970-82).

Fig. 4. Fabric diagram of thin sections of ice cores from BHC2 (1-3-5-10-15-20- 25% per 1% area).

ICE CRYSTALLIGRAPHIC STUDIES

The main ice crystallographic analyses were made on ice cores taken from top to bottom of two boreholes about 300 m apart, with depths of 344 m (BHC 2) and 300 m (BHC 1) near Cape Folger, approximately 15 km from the coast where the elevation of ice cap surface is about 250 m. Surface velocity is 9.4 - 9.6 ma^-1, mean accumulation rate is 250-300 mm water aquivalance, and mean annual temperature is estimated at -12°C-- -13°C.

Samples were taken approximately every 20 m in BHC 2 and every 10 m in BHC 1. Ice crystallographic studies for every sample included texture and air bubble observations, ice crystal size and ice fabric measurements. Because of the similarity of the results of crystallographic borehole and ice core studies for BHC 2 and BHC1, only the results of BHC 2 are shown in Figures 3 and 4.

The ice crystallographic characteristics of BHC 1 and BHC 2 were quite similar. The change of microtexture, crystal size an

SPECIAL CRYSTALLOGRAPHIC FEATURES OF ICE FROM THE LAST GLACIAL MAXIMUM

Ice originating from the last glacial maximum obtained from many different sites, has common crystallographic features. These become clear in particular when one compares the crystal properties of ice from the Holocene with those of ice from the Wisconsin period.

A marked decrease in crystal size at the boundary between the Holocene and Wisconsin ice has also been reported for Camp Century, Greenland (Herrón and Langway 1980), Devon Island ice cap, Canada (Koerner and Fisher 1979) and for the following Antarctic sites: Byrd Station (Gow and Williamson 1976), Vostok (Korotkevith and others 1978), Dome C (Duval and Lorius 1980). Where orientation fabrics have been measured, the finer grained ice of the Wisconsin period is found to have a single-pole fabric. This evidence suggests that climate may modify or otherwise influence the crystallographic processes involved with grain growth and fabric development, as noted by Koerner and Fisher (1979), Herron and Langway (1982) and Paterson (1981).

Possible factors affecting the crystallographic properties of ice may result from large variations of trace chemical content and microparticle concentration. At all sites studied, ice from the late Wisconsin period typically contains several-fold higher concentrations of chemicals and microparticles than ice from the Holocene or earlier periods. This increase in impurities has been explained by increased vigour of the atmospheric circulation, increased atmospheric activity and the presence of large areas of exposed continental shelf. The concentrations were further enhanced by lower precipitation levels during the cold glacial maximum. Difference in the crystal size could also be due to different crystal growth at different temperature, according to Duval and Lorius (1980).

These conditions are comparable to those found in the East Tian Shan and the Qilian Shan, where glaciers are of continental type with monsoonal nourishment (Xie 19S0). There winters are arid and summers moist. A strong dust layer is found on the glaciers corresponding to the winter period, when accumulation is small, winds are stronger and there is increased dust transport from surrounding deserts.

It is not known which of the components of the impurities contained in the Wisconsin ice could affect crystallographic properties, or whether some other process occurred at the time of the formation of the snow. More work, both in the field and in the laboratory, is required to explain these differences and resolve the questions posed here,