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Propagating compaction bands in confined compression of snow

Abstract

Some materials are strong in response to a slowly applied deformation, yet weak when subject to rapid deformations—a materials property known as strain-rate softening1. Snow exhibits such behaviour: it is comparatively strong at low deformation rates, where it is quasi-plastic, but weak at high rates, where it deforms in a quasi-brittle manner2. During deformation, strain-rate-softening materials ranging from metals3,4 to micellar systems5 exhibit complex spatio-temporal deformation patterns, including regular or chaotic deformation-rate oscillations and travelling deformation waves6. Here we report a systematic investigation of such phenomena in snow and show that snow can deform with the formation and propagation of localized deformation bands accompanied by oscillations of the driving force. We propose a model that accounts for these observations. Our findings demonstrate that in snow, strain localization can occur even in initially homogeneous samples deforming under homogeneous loads.

Main

Irreversible deformation of snow plays an important role in a number of problems, ranging from the interaction of snow with winter sports equipment7, vehicle traction8, to snowpack stability and avalanche release9. Snow strength depends strongly on cohesive bonds between ice granules in the snow microstructure. Shear deformation reduces snow strength as bonds are broken or sheared10, whereas formation of new cohesive bonds between ice granules—a thermodynamically driven sintering process11,12,13—leads to strengthening of snow over time (ageing)14. Rapid deformation leaves insufficient time for sintering to restore broken bonds; therefore, snow is at high rates of deformation weaker than at low rates. This goes along with a transition from quasi-plastic (low rates) to quasi-brittle deformation behaviour (high rates), which has been observed in shear14 as well as in compressive deformation15.

Here we report the results of confined compression experiments performed at strain rates intermediate between the quasi-plastic and quasi-brittle regimes. Specimens of both natural and artificially produced dry snow with densities ρ between 275 kg m−3 and 370 kg m−3 and mean grain size ξ ≈ 0.2 mm were contained within a rectangular transparent container with aluminium alloy side walls and a glass front and back. After different waiting (ageing) times at a temperature of −10 °C, the specimens were compacted by a piston moving at fixed rates ranging from 0.01 mm s−1 to 5 mm s−1, providing nominal strain rates from to 2.5 × 10−2 s−1. The axial driving force acting on the specimens was recorded by load cells located both above the piston and between the specimens and the apparatus ground plate. A 18-megapixel camera recorded images of the specimens, which were illuminated from behind, at 0.25 s intervals. To quantitatively characterize the deformation patterns, digital image correlation (DIC) was used to obtain spatio-temporal displacement records from which local strain and strain-rate tensors were calculated. For details of the experimental set-up, specimen preparation, and data analysis, see Supplementary Methods 1.

Figure 1 shows an image taken from the record of a typical compression test of an artificial snow sample, together with the corresponding εxx(x, z) and strain rate fields. The full record is shown in Supplementary Movie 1. Compaction proceeds in a strongly heterogeneous manner: a compacted region, visible as a darker area, is separated from an uncompacted region by a moving front where the strain rate concentrates. This front is perpendicular to the compression axis (in the figure, x axis). We visualize band motion by spacetime plots where we average over the perpendicular z coordinate and plot the averaged strain rate in colourscale as a function of x and t (Figs 2 and 3). In these plots we use Lagrangian coordinates where x denotes the position along the compression axis in the initial, undeformed configuration. The colour contrast demonstrates strong deformation localization. The moving deformation bands appear on the spacetime plots as inclined zones of high strain rate. The slope of inclination defines the band velocity vB in the Lagrangian frame. The first band nucleates at the top of the sample and moves at constant (Lagrangian) speed downwards until it reaches the bottom of the sample, leaving the sample in an almost homogeneously deformed state with strain eB ≈ 0.2 (‘band strain’). The band is then reflected and moves upwards across the sample until it reaches the top. Repetition of this process leads to a bouncing motion of the locus of deformation (see Supplementary Movie 1). Oscillatory features are also manifest on the force versus time curves, as band nucleation is associated with an up–down oscillation of the driving force. Occasionally the bouncing pattern is interrupted, as seen in Fig. 2c and Supplementary Movie 2, where the first band gets stuck and deformation is accommodated by a second band nucleating at the bottom and moving upwards until it merges with the first, whence a new band nucleates at the top and the bouncing pattern is resumed.

Figure 1: Strain and strain-rate patterns in a laboratory-made snow specimen.
figure1

Deformation rate , snapshot at 9.94% compressive strain. (Left) Photographic image showing the compaction front, the arrow indicates the front propagation direction; (centre) corresponding strain pattern as obtained by DIC; (right) corresponding strain-rate pattern. Note that the outermost edges of the sample are not covered by the DIC analysis.

Figure 2: Spacetime plots of deformation activity in laboratory-made snow.
figure2

Snow density ρ = 370 kg m−3, specimen age ta = 3 × 102 s. a. b, . c, . The top plots show the deformation activity as deduced experimentally from DIC, while the bottom plots show simulation data. The centre graphs are the corresponding force versus time/strain curves. Note that all three graphs in a column have the same x axis.

Figure 3: Spacetime plots of deformation activity in natural snow.
figure3

Snow density ρ = 275 kg m−3, deformation rate . a,b, As-harvested samples. c, sieved sample. The top plots show the deformation activity as deduced experimentally from DIC, while the bottom plots show simulation data. The centre graphs are the corresponding force versus time/strain curves. The deformation of samples a and c is also shown in Supplementary Movies 3 and 4.

Systematic investigation of a series of artificial snow samples of different age ta ranging from 3 × 102 s to 3 × 105 s reveals that the stress required for initiation and propagation of the first deformation band and also the band strain increase with specimen age (Supplementary Fig. 6). Increasing the strain rate from to increases the band velocity proportionally, but leaves the overall deformation pattern unchanged. A decrease in strain rate to values of or less makes the deformation bands disappear: at low strain rates, band formation gives way to homogeneous plastic flow (Fig. 2a).

Whereas artificial snow samples have the advantage of known specimen history and reproducible microstructure, it is essential to ascertain that natural snow shows similar behaviour. To this end we deformed natural snow samples harvested in the Cairngorm Mountains. The corresponding spacetime plots in Fig. 3 demonstrate the ubiquity of propagating compaction bands. Samples that were saw-cut from a block of natural snow (Fig. 3a, b) show irregular band propagation patterns where bands often nucleate in the centre of the sample, and propagation is jerky with multiple band arrests and jumps of activity between different locations (Supplementary Movie 3). Nevertheless, the band strains ɛB ≈ 0.2 and band velocities vB deduced from the spacetime plots compare well with those of artificial snow samples. Samples that were homogenized by sieving the snow into the sample container before the experiment deform differently (see Fig. 3c and Supplementary Movie 4); in such samples the band sequence is extremely regular, with bands bouncing repeatedly between the sample top and bottom, and the overall behaviour is similar to artificial snow.

The interplay between softening and ageing processes which makes snow a strain-rate-softening material has been modelled by a number of authors, for example, Louchet16 and Reiweger and colleagues17. However, these models cannot describe spatio-temporal strain localization because they do not account for the spatial structure of the deformation field. To model the observed phenomena we use a phenomenological plasticity model, which we present here in a simplified, scalar version. The reader is referred to Supplementary Methods 2 for a derivation of the scalar equations from a fully tensorial constitutive model. Deformation is described in terms of the spatially homogeneous stress s, the plastic strain e(x), which is a function of the axial position, and an internal variable S which characterizes the structural strength contribution of intergranular bonds. This variable accounts, in a phenomenological manner, for the competing processes of bond breaking and bond recovery (sintering/ageing).

The stress is calculated from the plastic strain e(x) and the strain eext that is imposed by the downward motion of the piston according to

where 〈〉 denotes the spatial average and E is the Young’s modulus of the sample. Equation (1) states a quasi-static relation between stress and strain: it neglects dynamic effects associated with elastic wave propagation. This is motivated by the observation that, with typical sound velocities in dense snow above 500 m s−1 (ref. 18), sound propagation times in our samples are below 5 × 10−4 s—over four orders of magnitudes less than all other characteristic times in our experiments. By contrast, Guillard et al. 19 relate propagating compaction bands in brittle porous materials such as cereals, which exhibit some remarkable similarities with the present observations, to viscoelastic waves. A detailed discussion of this issue is provided in Supplementary Methods 3.

The plastic strain rate is given by

where m is the strain-rate exponent, a prefactor with the dimension of a strain rate, and H is Heaviside’s function (H(φ) = 1 for Φ > 0 and H = 0 otherwise). The yield stress σy and yield function Φ depend on stress, strain, and on the internal variable S according to

The yield stress σy is a measure of the compressive strength of the material. It increases with increasing density (increasing compressive strain e) and diverges at a critical compressive strain ec. This divergence is characterized by the exponent b, which for a cohesionless granulate corresponds to the jamming exponent. The factor σ0 characterizes the strength of the unbonded (S = 0) and uncompacted (e = 0) granulate. The yield function Φ is evaluated as the difference between the compressive stress s and the yield stress σy, corrected by a spatial coupling term with length scale ξ. This term increases the rate of plastic flow in locations where e has a minimum (exx > 0) and decreases it in locations where e has a maximum; it is thus of a diffusive nature.

Finally, the evolution of the internal variable S is given by

This equation describes the competition between deformation-induced structural softening (first term on the right-hand side of equation (4), where ɛS is the characteristic softening strain) and strength recovery by rapid sintering/ageing (second term on the right-hand side, with ageing time constant τ).

Equations (1)–(4) define a set of integro-differential equations which we solve under the boundary condition that the plastic strain gradient xe must vanish at the specimen ends x = 0 and x = h. A detailed discussion of model parameters and initial conditions is found in Supplementary Methods 2. We use a common set of parameters for both natural and artificial snow samples, while accounting for differences in density by re-scaling the elastic constants and initial strength parameters by density-dependent factors (see Supplementary Table 2). The remaining differences in deformation behaviour between the different samples can be related to differences in specimen age, and in the degree of disorder of the snow microstructure. All simulations shown in Fig. 2 refer to specimens with age ta = 300 s. For specimens of different age, we adjust the initial strength by an age-dependent factor such that σy(t = 0) ta0.2 (ref. 20). For saw-cut natural snow a high initial strength corresponding to an estimated age ta = 106 s was used, whereas for the sieved samples we set ta = 300 s, corresponding to the time between sieving and testing. Disorder of the snow microstructure is modelled by assigning statistically distributed initial strength values to the sites of our discretization grid of lattice constant ξ. For the strength distribution we use a Weibull distribution where, for artificial snow samples as well as for sieved natural snow, we assume a high Weibull exponent β = 10 corresponding to fairly uniform local strength, whereas for saw-cut natural snow we use a low exponent β = 1, which is in line with experimental investigations of the strength statistics of saw-cut natural snow samples reported by Kirchner and colleagues21. The simulations reproduce all essential features of the observed band propagation patterns and stress–strain curves. Nucleation of new bands is associated with stress oscillations. In homogeneous samples we consistently observe bouncing bands (see Figs 2b and 3c). Local strength fluctuations (low Weibull exponent) may induce band arrest and/or intermittent band propagation, as in Fig. 3a, b. Increasing the initial strength to reflect increased sample age leads to larger band strains and higher band propagation stresses, consistent with the experimental data (Supplementary Fig. 6).

Further experimental work will be needed to directly characterize the microstructural processes occurring in the compaction bands. To this end, in situ X-ray microtomography (XRMT) would be the method of choice. This method has been used to study microstructure evolution during compaction of solid foams (see, for example, ref. 22), where local structural softening (cell wall fracture or buckling) and compaction band formation are intrinsic features of the early stage of deformation23,24. XRMT has also been successfully used to study microstructure evolution during low-velocity deformation of snow25,26. However, currently accessible image acquisition rates do not allow for in situ monitoring of the propagating bands observed in our experiments, as band propagation times are typically of the order of a few minutes only. Advances in high-throughput XRMT may enable this in the foreseeable future. Even in the absence of in situ imaging possibilities, ex situ XRTM images taken before and after deformation may help, in conjunction with micro-scale mechanical modelling27, to parametrize macroscopic constitutive models and to further validate their predictions.

Data availability.

The data that support the plots within this paper and other findings of this study are available from the corresponding author upon request.

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Acknowledgements

T.W.B. acknowledges financial support by EPSRC - DTP. S.L., S.S., G.W. and M.Z. acknowledge computational support by ZISC.

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T.W.B., T.J.S. and J.R.B. designed the apparatus and DIC imaging system, T.W.B. carried out the experiments, S.S. and S.L. analysed the DIC data, G.W., S.S. and S.L. wrote the simulation code and performed simulations, M.Z. formulated and parametrized the model, performed simulations and wrote the manuscript. All authors were involved in editing the manuscript.

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Correspondence to Michael Zaiser.

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Barraclough, T., Blackford, J., Liebenstein, S. et al. Propagating compaction bands in confined compression of snow. Nature Phys 13, 272–275 (2017). https://doi.org/10.1038/nphys3966

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