Introduction

The interdependence between ice-crystal-orientation fabrics and flow rates has been recognized for some time (e.g. Reference SteinemannSteinemann, 1958; Reference BuddBudd, 1972; Reference Kamb, Heard Ι.Y., Borg, Carter and RaleighKamb, 1972). Only recently, however, have laboratory experiments been carried out to the high strains (in excess of 10%) required to establish the various crystal anisotropies found within natural ice masses. With these experiments, tertiary flow rates have also been measured in some of the stress configurations found in the ice masses. In addition, recent work (Jacka, unpublished) has further examined the flow rates for isotropic ice at the lower temperatures and stresses typical of polar ice masses.

This paper has three aims: (1) to illustrate the similarity between crystal-orientation fabrics obtained in the laboratory and those found in natural ice masses. This is done by comparison of laboratory-developed fabrics with those from three ice cores extracted from Law Dome, Antarctica; (2) to present an improved flow relation for isotropic ice; and (3) to propose suitable enhancement factors (over isotropic minimum strain-rates) for tertiary anisotropic strain-rates, given particular crystal-orientation-fabric patterns, stress configurations, and total strains.

A Flow Law For Isotropic Ice Minimum Strain-Rate

Laboratory studies of the flow of isotropic polycrystalline ice show a power-law relation between stress and minimum strain-rate (cf. Reference GlenGlen, 1958). This has been shown (Budd and Jacka, in press) to hold for ice under different stress configurations (to ±50%), provided root-mean-square values (i.e. the conversions to octahedral or effective values) of the stress and strain-rate components are used.

Fig. 1. A flow relation for isotropic ice minimum strain-rates from shear and compression tests, and for the temperature and stress range found in natural ice masses (after Budd and Jacka, in press). Enhancement factors for anisotropic ice in shear and in compression are shown (inset) as a function of total strain.

The power-law relation with index n = 3 has been shown to be valid for the main range of stresses and temperatures experienced within natural ice masses. Figure 1 illustrates the relation obtained between minimum octahedral shear strain-rate and octahedral shear stress over a range of temperatures. Table I provides values of strain-rate from Figure 1 in a form that may be useful for computer modelling of ice masses. Both Figure 1 and Table I have been compiled from laboratory experiments in shear, compression, and extension. These experiments, on initially isotropic ice, cover the octahedral stress range 0.25–10 bar and temperature range 0° to −50°C. Tests at temperatures as cold as −32.5°C have extended beyond minimum strain-rate which occurs at an octahedral strain of ∼1%.

The data conform to a relation between octahedral stress, τ_₀, and strain-rate,

of the form

with n = 3 and where at −10°C, k_θ = 5.2×10⁻¹⁰ bar⁻³ s⁻¹ and the values of k_θ at other temperatures are obtained from Table I. For an indication of the uncertainties in these values of n and k, references should be made to Jacka (unpublished), Jacka (1984), or Reference Mellor and ColeMellor and Cole (1982).

The Development of Crystal Anisotropies

Ice within natural ice masses is not isotropic; crystal anisotropies develop due to the total strain experienced by the ice under different anisotropic stress configurations.

Figure 2 shows the cross-section of an oversnow traverse line (which approximates an ice-flow line) on Law Dome, Antarctica, from the summit of this ice cap to Cape Folger on the coast. Particle trajectories (derived from computer modelling of the flow line) are shown together with positions and depths of ice-core drilling sites. Crystal-orientation fabrics from the cores collected at sites 1, 3, and 8 are shown with the profile in Figure 2.

The ice deformation in the upper zones of the ice sheet is dominated by a net vertical compression of ∼10⁻³a⁻¹. In the deeper zones, horizontal shear dominates, ranging from ∼10⁻³ a⁻¹ near the summit to ∼3×⁻² a⁻¹ near the coast (Reference PfitznerPfitzner, 1980). Bore-hole studies (e.g. Reference Russell–Head and BuddRussell-Head and Budd, 1979) show that the basal ice is characterized by high variability including relatively stagnant zones with large crystals.

The crystal-orientation fabrics from the upper layers in each of the three ice cores of Figure 2 exhibit a random pattern. For the core from site 1, which is very near to the summit of Law Dome, a small amount of central tendency is evident in the crystal-orientation fabrics from 205 and 244 m depth. The fabric from 318 m depth exhibits a strong small-circle girdle pattern. This pattern has been found in the laboratory to be associated with compression to strains in excess of -10% (e.g. Reference Wilson and Russell–HeadWilson and Russell-Head, 1982; Reference Jacka and MaccagnanJacka and Maccagnan, 1984; Reference Gao and JackaGao and Jacka, 1987), and is shown in Figure 3a to be similar to a fabric developed in the laboratory by Jacka and Maccagnan. In addition, creep rates for ice from this core have been shown to be particularly close to those for laboratory-prepared ice after comparable total strains and given the same stress configurations (Reference Gao and JackaGao and Jacka, 1987).

Fig. 2. A cross-section of a traverse line from the summit of Law Dome to Cape Folger on the coast. Particle trajectories are shown along with the positions of ice-core drilling sites. Crystal-orientation fabrics are shown for the ice cores from sites 1, 3 (from Reference Li, Zichu and HuangLi and others, 1988), and 8 (from Reference Thwaites, Wilson and McCrayThwaites and others, 1984).

Fig. 3. Comparison of crystal-orientation fabrics from the ice cores with those developed in the laboratory for different stress configurations: (a) compression, (b) simple shear, and (c) compression followed by stress reduction. Laboratory-developed fabrics are from (a) Jacka and Maccagnan (1984); (b and c) Gao (thesis in preparation).

The development of a single near-vertical maximum pattern, as illustrated by the crystal fabrics from site 3 and by the fabrics at 93 and 170 m depth from site 8, is associated (from laboratory tests) with simple shear to high strains (e.g. Reference Russell–Head and BuddRussell-Head and Budd, 1979; Reference Bouchez and DuvalBouchez and Duval, 1982). In Figure 3b, the fabric from site 3 at 301 m depth is compared with a weak near-vertical maximum fabric from Gao (thesis in preparation) developed in a simple shear experiment after a total octahedral strain of 200%.

Alley (in press) and Reference Azuma and HigashiAzuma and Higashi (1984) have suggested that, provided no new grains are formed, a single near-vertical maximum fabric pattern can also develop as a consequence of vertical compression to very high strains. Gao (thesis in preparation) has conducted compression experiments to 60% strain, resulting in a small-circle girdle fabric pattern with the same cone half-angle (∼27°) as had been developed at 32% strain. In addition, Gao (thesis in preparation) has conducted compression tests to 20% strain on ice initially exhibiting a single-maximum pattern, and these tests resulted in the development from the single maximum to a small-circle girdle. Alley (in press) explains results such as those obtained by Gao as a consequence of the formation of new grains.

A multiple-maxima fabric pattern is exhibited in the ice from near the base of site 8, at a depth of 287 m. Fabrics similar to this have been found elsewhere, typically near the base of ice sheets and particularly at locations where the basal ice temperature is warmer than −10°C (e.g. Reference Gow and WilliamsonGow and Williamson, 1976; Reference Matsuda and WakahamaMatsuda and Wakahama, 1978), and within temperate glaciers (Reference Kamb and ShreveKamb and Shreve, 1963). This ice invariably consists of large crystals, consistent with the warmer temperatures in which it is found. Comparable fabri; patterns (Fig. 3c) have also been developed in the laboratory through crystal growth associated with stress relaxation and annealing (Gao, thesis in preparation). Gao first strained the ice in uniaxial compression through 27.6% octahedral to establish a small-circle girdle fabric pattern, and then reduced the stress (initially 3 bar octahedral) to zero over a period of 60 d. The test temperature was −3.3°C. A similar multiple-maxima fabric was obtained by Reference Azuma and HigashiAzuma and Higashi (1984) through vertical unconfined compression of ice with c-axes oriented near 45°, with a temperature increase from −15.8° to −2.8°C.

In therefore appears that the various crystal-orientation fabric patterns found in the ice cores from Law Dome and elsewhere can be produced in the laboratory by deformation with similar total strain and dominant stress configuration.

A Flow Law For Anisotropic Ice And Tertiary Flow

The flow rate for anisotropic polycrystalline ice in “easy glide” (compatible stress configuration and crystal fabric) can be considered as an enhancement of strain-rate over the minimum isotropic value. For compression of ice exhibiting a strong small-circle girdle fabric pattern, this enhancement factor becomes asymptotic to about 3 after about 15% strain (Jacka and Maccagnan, 1984). For simple shear of ice exhibiting a strong single-maximum pattern, the easy glide enhancement factor may be as high as 8 (Reference Russell–HeadRussell-Head, 1985). For compression or shear, then, the flow relation illustrated in Figure 1 can be used for anisotropic ice, provided an enhancement factor is incorporated. The enhancement, as a function of total strain, is given in the inset to Figure 1.

Thus, for the tertiary steady-state octahedral strain-rates,

of anisotropic ice, where the anisotropy has been developed by the deformation in compression or shear, Equation (1) is replaced by

where the values of k_θ are obtained from Table I.

Russell-Head (unpublished) determined relative shear rates for several crystal-fabric patterns including vertical girdles, two maxima at −40°, and multiple maxima. The Stress configuration throughout most of a natural ice mass, however, is a combination of compression and shear. Laboratory tests in this combined stress configuration have not yet been satisfactorily carried out to the high strains required to attain tertiary steady-state creep.

To establish a flow relation for anisotropic ice in the combined stress configuration, the conventional approach has been to consider the octahedral shear stress and strain-rate, and to assume that the same form of relation (Equation (1)) holds for anisotropic ice as for isotropic ice.

For a combined stress situation with normal stress and strain-rates σ and

and shear stress and strain-rates τ and , respectively, the octahedral relations are given (Jacka, unpublished) by

Although Equation (1) with these values may be expected to hold for isotropic ice, the applicability to tertiary flow or anisotropic ice still needs investigation. In fact, the addition of a high normal stress to a well-established tertiary flow under simple shear with a well-developed single-maximum crystal fabric may be expected to cause recrystallization and a decrease of the shear strain-rate rather than the increase implied by Equations (1), (4), and (5). This illustrates the importance of experimental work to study tertiary flow under combined stress situations.

Conclusions

A flow relation for isotropic ice minimum strain-rate has been presented. For anisotropic ice exhibiting the development of a small-circle girdle crystal-orientation fabric and which is subjected to vertical compression, an enhancement over the isotropic minimum flow rate of up to 3 seems appropriate. If the fabric pattern exhibits development of a single near-vertical maximum under horizontal shear, an enhancement of up to 8 seems appropriate.

Further experimental work is required to establish flow rates of ice exhibiting other fabric patterns and subjected to other stress configurations. For shear and compression combined, the octahedral relations imply higher flow rates than in shear or compression alone. Although this may be the case for isotropic ice, it is not expected for anisotropic ice. Until further tests are carried out, it is recommended for this combined stress configuration that tertiary anisotropic flow rates be estimated by applying an enhancement estimated from the inset to Figure 1 according to the ratio of the compressive stress to the shear stress and to the total strain. For strains in excess of ∼15%, this estimated enhancement will fall between 3 and 8.