1. Introduction

Microstructural evolution strongly affects the deformation process in ice: both grain size and orientation affect the deformation rates and rate-controlling mechanisms. Decreasing the grain size can change the creep mechanism from dislocation glide to diffusion-based grain boundary sliding (Reference Goldsby and KohlstedtGoldsby and Kohlstedt, 1997). Previous studies (Reference BakerBaker, 1981, Reference Baker1982) indicated that crystal fabric has important effects on the flow of polycrystalline ice. Reference Jacka and MaccagnanJacka and Maccagnan (1984) found a three-fold increase in creep rate as the crystal fabric changed from random to small circle. Reference Cuffey, Conway, Gades, Hallet, Raymond and WhitlowCuffey and others (2000a, b) found an enhanced shear strain rate of ice-age ice in South Greenland and suggested that this arose from the development of c-axis fabric with a strong shear single-maximum pattern and decrease in grain size, with these two phenomena accounting for roughly 70% and 30% of the average enhancement, respectively.

The effect of particles on the creep of polycrystalline ice has been investigated by a number of workers (e.g. Reference Holdsworth and BullHoldsworth and Bull, 1970; Reference Baker and GerberichBaker and Gerberich, 1979; Reference Shoji and LangwayShoji and Langway, 1985; Reference Durham, Kirby and SternDurham and others, 1992). However, the effect of particles on the microstructural evolution in freshwater ice has not been systematically studied. Under high stress, recrystallization may occur through the nucleation and growth of many small grains along the grain boundaries as a consequence of the high strain energy that builds up along grain boundaries. This process will inevitably increase the number of grains. Furthermore, because strain energy can build up around hard inclusions during deformation, soil particles can also stimulate the nucleation of new grains. Under low stress, on the other hand, recrystallization may occur through grain boundary migration since the strain energy along the grain boundaries may not be high enough to nucleate new grains.

The present work was part of a larger research effort to understand how dispersed fine particles affect flow rates in granular freshwater ice, and illustrates how the presence of soil particles influences dynamic recrystallization during compressive creep straining.

2. Experimental

Deionized, distilled and degassed water was used to grow thin plates of large-grained ice. These ice plates were then broken up, and a 3–5 mm sieve fraction was obtained. These grains were used to seed granular freshwater ice specimens prepared by the method of Reference ColeCole (1979). The final cylindrical specimen dimensions were 127 mm in length and 50.4 mm in diameter.

For particle-containing ice, water with silt-sized soil particles (obtained from Hanover, NH, and sieved to 50 ± 10 mm) was frozen to a thickness of about 5 mm from bottom to top using a cooling plate. Another layer of ice with particles was then grown on the top of the first layer. This procedure was repeated several times until the thickness of the ice plate was about 30 mm. Growing a multilayer ice plate was necessary to distribute the particles throughout the ice grains. The ice plate was subsequently broken up, and a 3–5 mm sieve fraction was obtained. These grains were then used to seed granular ice specimens as described above. Both particle-free and particle-containing ice had an average initial grain size of approximately 5 mm. The grain size was determined by measuring the diameter of all the grains in one thin section and taking the average. The maximum error in the average grain size is <2 mm. Figure 1 shows a thin section and an enlarged view of ice with 1 wt.% (∼0.43 vol.%) particles. It can be seen that the particles are uniformly distributed (Fig. 1b).

Fig. 1.

(a) Photograph of a thin section of an ice specimen with 1 wt.% particles. (b) Enlarged view of the thin section under polarized light showing the distribution of particles.

Constant-load compressive creep tests with an initial stress level of 1.45 MPa at −10°C or 0.4 MPa at −5°C were used to study the effect of particles on the creep behavior. The creep tests were performed using a creep jig, which has been described in detail by Reference Song, Cole and BakerSong and others (2005). The creep jig was located in a cold room at a temperature 2°C lower than the test temperature. Two insulated boxes were used to isolate the jig from the cold room, and a temperature-regulating system was located between the boxes. This method controlled the temperature in the inner box to 10.1°C. To minimize ice sublimation during the long-term creep testing, a rubber cover was put on the surface of the specimens. Eight specimens (four particle-free specimens and four particle-containing specimens) were used to determine the variability in the creep rate (two specimens for each creep test condition). The maximum variation from the average creep rate was found to be less than 20%. After the creep strain reached ∼10%, the stress had decreased to ∼1.3 or ∼0.36 MPa, respectively, about 10% lower than the initial stress, due to the increase in the specimen’s cross-sectional area. A load cell mounted in line with the specimens monitored the axial load, and two displacement transducers mounted on circumferential rings (located at one-third and two-thirds along the length of the specimens) provided the deformation measurements.

The specimens were thin-sectioned after creep straining to ∼10% and compared with thin sections of unstrained material in order to study the effects of particles on the microstructures during creep. Microstructural analysis was performed using optical microscopy with polarized light.

3. Results

3.1. Creep

Figure 2 shows the relationship between strain rate and strain for both the particle-free and the particle-containing ice under creep with initial stress levels of 1.45 MPa at −10°C and 0.4 MPa at −5°C. Note that for both circumstances (high creep stress and low creep stress), the creep rate of the particle-containing ice was always higher than that of the particle-free specimens, even at strains that are too low for appreciable recrystallization to occur. This agrees well with a previous study (Reference Song, Cole and BakerSong and others, 2004), in which particles are distributed only along the grain boundaries and also show increased creep rates, compared to those of particle-free ice. That analysis indicated that the higher creep rates of ice with particles was due to an increased dislocation density caused by the particles. Since under these conditions (1.45 MPa at −10°C and 0.4 MPa at −5°C) the main creep mechanism is dislocation glide on the basal plane (Reference Duval, Ashby and AndermanDuval and others, 1983), an increase in dislocation density will inevitably increase the creep rate. The curves in Figure 2 show typical creep behavior: the creep rate initially decreases (primary creep) to a minimum value and then increases (tertiary creep). It can be seen that the strain at the minimum creep rate is about 1% for both particle-free ice and particle-containing ice, in accordance with previous studies (Reference Mellor and ColeMellor and Cole, 1983; Reference JackaJacka, 1984). Reference Jones and ChewJones and Chew (1981) examined the effect of the ratio of cross-sectional diameter of the specimen to the grain size for slow strain-rate compression tests on ice. They found that the strength was clearly independent of this ratio for values greater than 11–12 and was clearly dependent on the ratio for values of ∼8. More generally, a ratio of specimen diameter to grain size of 10 : 1 is considered sufficient for the specimen to act as a true polycrystal. In the present work, the ratio of specimen diameter to grain size was 10 : 1.

Fig. 2.

Relationship between strain rate and strain of particle-free ice and particle-containing ice (1 wt.%). (a) Initial stress of 1.45 MPa at −10°C. (b) Initial stress of 0.4 MPa at −5°C. Note that each condition includes two curves from two specimens.

3.2. Microstructures

Figure 3 shows thin sections of the particle-free and particle-containing ice between crossed polarizers before and after creep to ∼10% strain. Figure 4 shows higher-magnification images, where it is evident that dynamic recrystallization has occurred throughout the specimen after creep to 10% strain at 1.45 MPa and −10°C. New grains replace the initial microstructure, resulting in a decrease in the average grain size after 10% strain. It should be noted that particle-containing ice has a much higher recrystallization ratio (>80%) and smaller grain size after creep, compared to particle-free ice (<50%). After creep to ∼10% strain at 0.4 MPa and −5°C, the whole microstructure of particle-containing ice was largely recrystallized, and almost all the old grains were replaced by the new, small recrystallized grains. However, no small grains appeared in the particle-free ice since the recrystallization is through grain boundary migration. Table 1 shows the relationship between average grain size and strain level for particle-free and particle-containing ice before and after creep to ∼10% strain (two values for each test condition). It can be seen that the ice with particles shows a much larger grain-size reduction compared to the particle-free ice.

Fig. 3.

Thin sections of both particle-free ice (a–c) and particle-containing ice (1 wt.%) (d–f) between crossed polarizers before and after strain to ∼10%. (a, d) No strain; (b, e) initial stress of 1.45 MPa at −10°C; and (c, f) initial stress of 0.4 MPa at −5°C.

Fig. 4.

Enlarged microstructural views of the respective thin sections shown in Figure 3.

Table 1.

The relationship between average grain size and strain for both particle-free ice and particle-containing ice (1 wt.%). Two tests were performed for each condition

4. Discussion

The laboratory results clearly show that the creep rate of particle-containing ice is higher than that of particle-free ice under either high or low creep stress. It is well known that dislocation glide along the basal plane is the main deformation mechanism at stresses higher than 0.2 MPa and temperatures from −0.05°C to −50°C (Reference Budd and JackaBudd and Jacka, 1989). Although fabric development and an increase in grain boundary sliding (due to grain refinement) may help increase the creep rate in tertiary creep, they are not the main reasons for the higher creep rates in the ice with particles. This is especially evident in the early stages of creep, when dynamic recrystallization has only just begun, but creep rates are nonetheless higher when particles are present. Generally, the creep rate is affected by both the dislocation density and the dislocation glide velocity. Under the same temperature and stress conditions, dislocation glide should have the same (or similar) average velocity for a randomly oriented polycrystal, even if coarsely spaced particles are present. Thus, the creep rate is controlled by the dislocation density. It is evident that the particles cause an increase in the dislocation density relative to particle-free ice, and that this difference persists as straining proceeds, and produces higher creep rates through all stages of creep deformation. Since the particles are distributed uniformly throughout the microstructure, three possible mechanisms might help generate a higher dislocation density, compared with particle-free ice. First, the particles inside the grain interiors can develop stress concentrations during deformation, and thus increase the dislocation nucleation rates sufficiently to enhance creep rates. Second, the particles along the grain boundaries can inhibit grain boundary sliding, leading to intergranular stress concentrations, and thus increasing the dislocation density. Third, differences in the thermal expansion coefficients of ice and soil particles can lead to stress concentrations and produce dislocations.

Under the higher creep stress of 1.45 MPa, dynamic recrystallization is through nucleation and growth of new grains for both particle-free ice and particle-containing ice. When particles are present along the grain boundaries (Reference Song, Cole and BakerSong and others, 2004), they inhibit grain boundary sliding so that even at the 0.4 MPa stress level, the resulting build-up of strain energy makes the grain boundaries favorable sites for the nucleation of new grains. This has the effect of increasing the nucleation rate for new grains and leads to a greater reduction in grain size with increasing strain compared to the particle-free ice. This phenomenon is in accordance with a previous study (Reference Song, Cole and BakerSong and others, 2004), which focused on the effect of particles that are located only along the grain boundaries. It should be noted that the particles inside the grains can also act as nucleation sites for new grains due to the strain energy built up around them (Reference Ahmad, Shearwood, Whitworth, Maeno and HondohAhmad and others, 1992).

In contrast, for particle-free ice deformed at the 0.4 MPa stress level, dynamic recrystallization involved grain boundary migration instead of the nucleation of new grains. In this case, the build-up of strain energy is sufficient to drive grain boundary migration, but is insufficient to drive the nucleation of new grains. The microstructural consequence of recrystallization by grain boundary migration is that the grain size is not reduced.

According to the above discussion, the particles increase both dislocation multiplication and dynamic recrystallization (nucleation of new grains). Both processes increase the creep rate. Dislocation multiplication increases the creep rate by increasing the dislocation density, while dynamic recrystallization increases the creep rate by decreasing the grain size and changing the grain orientations of the specimens. However, dynamic recrystallization generally decreases the dislocation density. From Figures 2 and 4 we know that the ice with particles has both a higher creep rate and a higher grain nucleation rate throughout the whole deformation process than the particle-free ice. Therefore, it is evident that the decrease in dislocation density due to dynamic recrystallization is low compared to the increase in dislocation density associated with the presence of the particles. An earlier study (Reference Hooke, Dahlin and KauperHooke and others, 1972) suggested that for ice containing particles the creep stress exponent, n, may be less than 2. However, our previous study (Reference Song, Cole and BakerSong and others, 2006) showed that from 0.4 MPa to 1.4 MPa and from −20°C to −2°C, n = 3 for both particle-free ice and ice containing particles, with higher creep rates for particle-containing ice.

5. Conclusion

The effect of particles on the creep rate and microstructures in granular freshwater ice has been investigated and the following conclusions are drawn:

1. 1. Particle-containing ice (1 wt.%) shows a higher creep rate compared to particle-free ice.

2. 2. Under an initial creep stress of 1.45 MPa at −10°C, dynamic recrystallization occurs through the nucleation of new grains along grain boundaries for both particle-free and particle-containing ice.

3. 3. Under an initial creep stress of 0.4 MPa at −5°C, dynamic recrystallization occurs through the nucleation of new grains along grain boundaries for particle-containing ice but through grain boundary migration for particle-free ice.

4. 4. Particles inhibit grain boundary sliding and enhance dynamic recrystallization through the nucleation of new grains, thus dramatically increasing the nucleation rate and decreasing the average grain size.