Recrystallization processes, microstructure and crystallographic preferred orientation evolution in polycrystalline ice during high-temperature simple shear
- 1Department of Earth and Space Sciences, University of Washington, NASA Astrobiology Institute, Seattle, USA
- 2Université Grenoble Alpes, CNRS, IRD, G-INP, IGE, 38000 Grenoble, France
- 3PGP, Department of Geoscience, University of Oslo, Oslo, Norway
- 4Géosciences Montpellier, Université de Montpellier/CNRS, 34095 Montpellier, France
Correspondence: Baptiste Journaux (email@example.com) and Maurine Montagnat (firstname.lastname@example.org)
Torsion experiments were performed in polycrystalline ice at high temperature (0.97 Tm) to reproduce the simple shear kinematics that are believed to dominate in ice streams and at the base of fast-flowing glaciers. As clearly documented more than 30 years ago, under simple shear ice develops a two-maxima c axis crystallographic preferred orientation (CPO), which evolves rapidly into a single cluster CPO with a c axis perpendicular to the shear plane. Dynamic recrystallization mechanisms that occur in both laboratory conditions and naturally deformed ice are likely candidates to explain the observed CPO evolution. In this study, we use electron backscatter diffraction (EBSD) and automatic ice texture analyzer (AITA) to characterize the mechanisms accommodating deformation, the stress and strain heterogeneities that form under torsion of an initially isotropic polycrystalline ice sample at high temperature, and the role of dynamic recrystallization in accommodating these heterogeneities. These analyses highlight an interlocking microstructure, which results from heterogeneity-driven serrated grain boundary migration, and sub-grain boundaries composed of dislocations with a [c]-component Burgers vector, indicating that strong local stress heterogeneity develops, in particular, close to grain boundaries, even at high temperature and high finite shear strain. Based on these observations, we propose that nucleation by bulging, assisted by sub-grain boundary formation and followed by grain growth, is a very likely candidate to explain the progressive disappearance of the c axis CPO cluster at low angle to the shear plane and the stability of the one normal to it. We therefore strongly support the development of new polycrystal plasticity models limiting dislocation slip on non-basal slip systems and allowing for efficient accommodation of strain incompatibilities by an association of bulging and formation of sub-grain boundaries with a significant [c] component.
Ice deforms by shear in many natural conditions such as glaciers and ice sheets, and in particular along ice streams. In most of the deep ice cores studied, compression and extension are the dominant deformation geometries owing to the core location close to geographical domes or along ridges. Simple shear occurs in the deeper portions of these cores. However, the strongest simple shear occurs in fast-flowing glaciers and ice streams (see review by Hudleston, 2015). During large-scale ice flow, deformation induces development of strong crystallographic preferred orientation (CPO) or texture. Since the late 1970s a growing number of studies have provided measurements of increasing accuracy of the CPO evolution along ice cores (refer to Gow and Williamson, 1976; Alley, 1988; Lipenkov et al., 1989, for pioneer work, and Faria et al., 2014b, for a review). Pioneer work of Hudleston (1977) analyzed the CPO evolution in a narrow shear zone of the Barnes Ice Cap (Canada), providing well-documented observations of CPO development owing to shear in natural conditions.
CPO development in ice is related to the strong viscoplastic anisotropy of this material (Alley, 1992). Ice Ih is hexagonal with Space group P63∕mmc, no. 194 and Laue class 6/mmm. Plastic strain in ice Ih is mainly accommodated at high temperature by dislocation glide on the basal plane through three equivalent slip systems (Duval et al., 1983; Hondoh, 2000). The viscoplastic anisotropy of the ice crystal results in strong strain heterogeneities at the inter- and intragranular scale when polycrystalline ice is submitted to a macroscopic stress (Duval et al., 1983; Grennerat et al., 2012, and references therein) and hence in activation of dynamic recrystallization processes, even at very low strains (Duval, 1979; Duval et al., 1983; De La Chapelle et al., 1998; Chauve et al., 2017a).
In return, the CPO-induced anisotropy at the macroscale leads to a bulk anisotropic viscosity of ice that impacts ice rheology. This macroscale mechanical anisotropy is responsible for modifications in ice stratigraphy and age–depth relationship (see, e.g., Martín et al., 2009; Buiron et al., 2011). It may also produce large-scale flow heterogeneities, such as basal folding (see, e.g., Dahl-Jensen et al., 1997; Thorsteinsson and Waddington, 2002; Gillet-Chaulet et al., 2006; Ma et al., 2010; Bons et al., 2016). In simple shear the evolution of CPO (as well as other factors like the grain size) is associated with an increase in shear strain rate by a factor of 10 at constant stress (Cuffey and Paterson, 2010; Hudleston, 2015).
This phenomenon is well-studied in the Earth mantle, where olivine CPOs produced by similar deformation and recrystallization mechanisms (see reviews by Ismaïl and Mainprice, 1998; Tommasi and Vauchez, 2015) result in elastic and viscoplastic anisotropy. The elastic anisotropy in the mantle may be directly observed in seismic data (see Tommasi and Vauchez, 2015). The viscoplastic anisotropy is only observed indirectly, via the changes it produces in the deformation patterns. It nevertheless plays a major role in the development of plate tectonics (Tommasi et al., 2009).
In addition to the obvious implications of ice rheology studies for ice caps and glacier dynamics, ice is also often used as a reference material to study anisotropic mechanical behaviors in rocks and alloys. Since ductile deformation experiments in rocks are challenging, ice is a good analogue to polycrystalline geo-materials since “high-temperature” deformation in ice at T∕Tm close to 1 can be achieved in a cold room and at ambient pressure. Mantle rocks deformed close to the melting point in the asthenosphere beneath mid-ocean ridges, sampled in ophiolites, display strong olivine CPO due to deformation and dynamic recrystallization with fast grain boundary migration (e.g., Cassard et al., 1981; Boudier and Coleman, 1981; Higgie and Tommasi, 2012). The mechanical anisotropy due to these CPOs may significantly change the flow patterns beneath the ridge (Blackman et al., 2017).
Pioneering experimental studies have shown that at low shear strains (γ<0.6), an initially random CPO polycrystalline ice sample develops a bimodal distribution of the grain's c axes (Kamb, 1972; Duval, 1981; Bouchez and Duval, 1982). These are noted as the M1 sub-maximum, which remains normal to the macroscopic shear plane, and the M2 sub-maximum, which rotates from near parallel to the shear plane towards the M1 maximum with increasing finite shear strain (Bouchez and Duval, 1982). For important shear strains (γ≥2), only the M1 maximum persists. This orientation corresponds to crystals with their basal planes well-oriented for dislocation glide parallel to the shear plane. A similar evolution was observed in more recent shear experiments on artificial ice polycrystals by Li et al. (2000) and Budd et al. (2013), as well as by Wilson and Peternell (2012), who analyzed the influence of the initial CPO and the importance of recrystallization processes on the CPO evolution. The vanishing of the M2 maximum has been hypothesized by Bouchez and Duval (1982) to result from rigid body rotation and recrystallization of grains unfavorably oriented for slip.
A large part of the knowledge on the microscopic processes occurring in polycrystalline ice under simple shear deformation is still derived from data published over 30 years ago (Kamb, 1959, 1972; Duval, 1981; Bouchez and Duval, 1982; Burg et al., 1986). The tools and methods used in these studies to analyze the CPO were often manual and highly dependent on the operator experience. Electron backscatter diffraction (EBSD) and automatic ice CPO analyzer (AITA) can now provide high-spatial- and high-angular-resolution quantitative data, enabling a global and statistical study of the processes accommodating strain at the micro-scale. Recent experiments (Qi et al., 2017, 2019) using these new characterization techniques have shed new light on some aspects of the question. They have, for instance, disproved the hypothesis by Kamb (1972) that CPO evolution in ice mainly depends on the finite shear strain and is not sensitive to temperature, strain rate or stress. Indeed, Qi et al. (2017) showed that during axial compression the final CPO is sensitive to stress or strain rate and Qi et al. (2019) that the rate of evolution of the CPO in simple shear is sensitive to temperature.
A modern and comprehensive update of the observations of ice deformation in simple shear seems more and more necessary as the increase in calculation power allows us to run mean-field or full-field polycrystal plasticity models routinely (see Montagnat et al., 2014, for a review and Llorens et al., 2017, for a recent application). These new numerical approaches require accurate experimental constraints on the microstructure evolution. It is worth noting that these models are still unable to accurately reproduce the double sub-maximum of the c axis preferred orientation evolution of polycrystalline ice observed in simple shear experiments (Bouchez and Duval, 1982; Burg et al., 1986; Wilson and Peternell, 2012) and natural shear zone (Hudleston, 1977).
The complex interplay of dislocation slip system activities, their interactions, and the role of the various mechanisms accommodating the local strain and stress heterogeneities, such as cross-slip, kink-banding and dynamic recrystallization, is still either not or poorly represented in most of the existing modeling approaches, very likely because of the complexity of the interactions between these mechanisms. Concerning the olivine CPO development in the mantle, Signorelli and Tommasi (2015) succeeded in reproducing the evolution of olivine CPO in simple shear with a mean-field modeling approach, by making use of a two-level mechanical interaction scheme that integrates the formation of low-angle grain boundaries as expected during dynamic recrystallization.
The present work aims at providing new constraints on the processes controlling CPO evolution in simple shear in polycrystalline ice by presenting a comprehensive description of the evolution of CPO and grain shape fabric in polycrystalline ice during hot torsion experiments. We use state of the art analytical techniques: EBSD equipped with a cryostage and an automatic ice texture analyzer (AITA), to retrieve quantitative data of unprecedented spatial and angular resolution on crystallographic orientations, grain size and grain shape fabrics as a function of shear strain. These data then are used to estimate the active dislocation systems and to investigate the role of sub-grain-scale processes on the recrystallization regime that allows the formation of a CPO and microstructure more favorable to shear strain.
2.1 Polycrystalline ice preparation
Unstrained equiaxial polycrystalline ice was prepared by evenly packing 200 µm sieved ice particles in a mold. The container was sealed and the air contained in the porosity was removed using a primary vacuum rotary vane oil pump. Outgassed water at 0 ∘C was quickly introduced afterwards to fill the porosity. The resulting mush was frozen bottom up at −5 ∘C for 48 h. To enable a more homogenous grain size and recovery of any small strain accumulated during grain growth, the granular ice cylinders were annealed for at least 120 h at −7 ∘C. This method produces untextured homogenous samples with negligible porosity and ∼1.5 mm mean grain size. Ultra pure Milli-Q™ water (18 MΩcm) was used for all sample preparations. Cylinders around 35 mm in diameter and 60 mm in height were carved from the granular ice using a lathe located in a −10 ∘C cold room. Specific sample sizes are indicated in Table 1.
2.2 Torsion experiments
Deformation experiments were performed using a torsion apparatus placed inside a cold room at a temperature of ∘C (0.97Tm, with Tm the melting temperature at 0 ∘C). Samples were carefully fixed in the apparatus ensuring no axial load. The design of the torsion apparatus does not allow for displacements parallel to the rotation axis; the imposed deformation is therefore perfect simple shear. During the experiments, the evolution of the CPO under these fixed-end boundary conditions might produce axial stresses (Swift, 1947; Li et al., 2000). The latter cannot be measured in the present apparatus, but polycrystal plasticity models indicate that these axial stresses may attain values similar to those of the shear stresses when the CPO is oblique to the imposed shear (Castelnau et al., 1996). A more precise description of the apparatus is provided in the Supplement. Straight lines parallel to the rotation axis were traced on the surface of the sample to allow for observation of any strain heterogeneity along the cylinder (Fig. 1). The surface of the sample was coated with silicon grease and wrapped gently with a cellophane foil to ensure negligible loss by sublimation.
We imposed a constant torque M on one site of the sample corresponding to a maximum stress τmax between 0.4 and 0.6 MPa (Table 1). The τmax was calculated from the torque M using a stress–strain power law as described in Paterson and Olgaard (2000). Since most of the present experiments recorded secondary creep conditions (Fig. 1), a stress exponent of n=3 was chosen based on results from Duval et al. (1983) and more recent work from Treverrow et al. (2012) that observed stress exponents between 2.9 and 3.1 during the secondary creep regime, and of 3.5 for tertiary creep in compression and shear tests. The actual torque applied to each sample is indicated in Table 1. These values of maximum tangential stress have been chosen because they allow high enough strain rates while preventing the formation of cracks.
Macroscopic strain (Fig. 1) was followed using a linear variable differential transformer (LVDT) during the primary creep regime (i.e., small strains) and a homemade optical rotary encoder device (5000 counts per revolution) for larger strains. Maximum macroscopic shear strain γ, the maximum natural extensional strain ε, and the strain rate , calculated through
2.3 Analytical methods
CPO, microstructure and sub-grain strain heterogeneity analyses were performed using both AITA and EBSD, as the combination of the two techniques allows the acquisition of a comprehensive dataset. AITA enables the analyses of large samples (up to cm2), but only recovers the c axis (optical axis) crystallographic orientations. Conversely, the cryo-EBSD setup used in the present study (CamScan X500FE CrystalProbe at Géosciences Montpellier) is only capable of mapping smaller ice samples of cm2, but is able to recover the full orientation of the crystal (all crystallographic axes) with an expected angular resolution better than 0.7∘ (Randle, 1992) and with a practical spatial resolution for ice down to 5 µm. Sections tangential to the experimental cylinders were cut out for both AITA and EBSD analyses. The general geometry of these sections is illustrated in Fig. 2. To provide flat surfaces for AITA thin sections and EBSD samples, the sample sections were microtomed by less than 1 mm, which gives an error on γmax of less than 5 %.
AITA has been performed on thin sections typically 300 µm thick, as is routinely carried out on ice (Russell-Head and Wilson, 1999; Montagnat et al., 2011; Peternell et al., 2011; Chauve et al., 2015; Wilson et al., 2015). We worked at a spatial resolution of 25 µm and were able to obtain an angular resolution of about ∼3∘. All optical CPO measurements were conducted at −7 ∘C. Grain boundaries (GBs) were extracted using the segmentation technique described in Montagnat et al. (2015), which automatically defines grain boundaries using color change detection in AITA maps, followed by manual corrections based on coherent microstructure shapes and discernible misorientations. All manual corrections are operator dependent, so all analyses have been performed by the first author for consistency. This allowed us to differentiate, with a good level of confidence, sub-grain boundaries (SGBs) from grain boundaries, even if optical measurements do not give access to the full crystallographic orientation, as EBSD measurements do. From the extracted skeleton images we derived grain size and shape statistics using the PolyLX MATLAB® toolbox developed by Lexa (2003). Grain size frequency plots are reported for every finite shear strain in the Supplement. From the grain shapes, we calculated the PARIS grain shape factor to quantify grain boundary interlocking as PARIS %, with P the perimeter and PE the convex hull perimeter (Heilbronner and Barrett, 2014). This parameter increases with increasing grain boundary sinuosity.
Electron backscatter diffraction (EBSD) patterns were obtained with a CamScan X500FE CrystalProbe equipped with a liquid nitrogen cryogenic stage (GATAN®) at Géosciences Montpellier (France). Sample surfaces were prepared by carefully flattening the surface with a microtome blade at −60 ∘C inside a freezer placed near the EBSD just before loading it quickly on the cold stage. This method provides a very good surface finish with no significant frost during measurements and limits to a minimum the heat transfer to the sample, ensuring limited microstructure evolution due to annealing. The CrystalProbe–EBSD working conditions were 15 kV, 3.5 nA, and a low vacuum with 1 Pa of gaseous nitrogen and 25 mm working distance. More details on the EBSD geometry can be found in Demouchy et al. (2011). To avoid ice sample sublimation in the vacuum chamber, which happens at approximately −60 ∘C at 1 Pa for ice Ih (Fernicola et al., 2011), the temperature of the cold stage was kept at ∘C during the analyses. EBSD Kikuchi patterns were automatically indexed using the HKL Channel5™ software suite (Oxford Instruments®). Maps were acquired with a spatial resolution of 25 µm identified as a good compromise between resolution and time constrains, with an indexation rate higher than 85 %. Analyses of the EBSD maps were made using the MTEX MATLAB® toolbox (Hielscher and Schaeben, 2008; Bachmann et al., 2010, 2011; Mainprice et al., 2014).
To observe the geometry of sub-grain boundaries and extract statistical quantities, local misorientation analyses, such as kernel average misorientation (KAM) or the local misorientation relative to the mean orientation (Mis2Mean), were performed on the EBSD data (see review by Wright et al., 2011). Both analyses enable visualization of the spatial distribution of intragranular stored strain structures, generally in the form of sub-grain boundaries (Wright et al., 2011), but do not provide any information about the type of dislocations accommodating the observed misorientation. Conversely, the weighted Burgers vector (WBV) analysis allows us to extract a minimum value for the dislocation density in sub-grain boundaries and provides an estimate of the slip systems necessary to explain the observed misorientations (Wheeler et al., 2009). As conventional EBSD maps are 2-D, only five components of the Nye tensor α can be extracted (α12, α21, α13, α23, α33). This allows us to obtain a projection of the Nye tensor on the EBSD map plane which partially constrains the Burgers vector. It provides a lower bound for the dislocation density and constrains the Burgers vector of geometrically necessary dislocations (GNDs) accommodating the observed misorientations. Even if WBV analysis does not recover the full Burger vectors coordinates, it does not provide “false” components. This means that if a [c] component is deduced from WBV analysis of a 2-D EBSD map, the true Burgers vector does actually contain at least this amount of [c] component. For the WBV analysis we used the MATLAB® toolbox developed by Wheeler et al. (2009) and previously used on ice in Chauve et al. (2017b). To provide the relative number of [c]-component dislocations, the calculated WBV for each pixel is projected on the non-independent four hexagonal lattice directions (, , , ), respectively called WBVa1, WBVa2, WBVa3 and WBVc. The ratio of [c] component (WBVc) is then given by the relation rWBV), with the Euclidian norm of the WBV. A high-pass value of 0.4∘ ( µm−1) was imposed for the misorientation analysis to filter the noise resulting from the angular resolution of the EBSD data. We suggest referring to Appendix A of Chauve et al. (2017b) for more details about this analysis. Nevertheless, it should be recalled that the WBV analysis does not directly provide information about mobile dislocations, responsible for the majority of the plastic deformation. It only measures the GND, as it is based upon the Nye tensor.
Five torsion experiments were performed up to different finite shear strains γmax, from 0.012 to 1.94. Data for all experiments are presented in Table 1. One sample (TGI0.71), with a γmax of 0.71, was annealed for 72 h at −7∘ after the deformation experiment to study the effect of annealing on both CPO and microstructure. The microstructure of one of these samples has been partially described in Chauve et al. (2017b) to compare the statistical representation of WBV (or Burgers vector) with [c] component in GNDs in samples submitted to uniaxial unconfined compression and torsion.
3.1 Macroscopic strain
Retrieved samples presented homogeneous strain with no apparent localization or cracks, as illustrated in Fig. 1. TGI0.012 and TGI0.2 shear strain data were very noisy due to signal transmission issues on the acquisition setup, which were fixed for the TGI0.42 and TGI1.96 runs. Typical primary creep regime (i.e., hardening) is observed for TGI0.42 and TGI1.96 in Fig. 1 until approximately 20 000 s (≈6 h). The noise in TGI0.012 and TGI0.2 data was too strong to distinguish any primary creep hardening. After this phase of hardening, a minimum in strain rate is reached (secondary creep regime). This minimum is clearly visible in experiments TGI0.2, TGI0.42, TGI0.71 and TGI1.96 at 200 000 s (≈56 h). For the longer TGI1.96 experiment, after the secondary creep phase, strain rate continuously increased until achieving an almost steady-state strain rate of s−1, suggesting that tertiary creep regime was reached for this run (Fig. 1). TGI0.012 stayed mostly in the primary creep regime with a γmax=0.012. Samples TGI0.2 and TGI0.42 experienced a maximum shear strain of 0.2 and 0.42, respectively. The final strain rate for these two experiments is illustrated by the tangent dashed line in Fig. 1, which shows that softening was still occurring when the samples were unloaded (only the last data points lie on the tangent). We therefore consider that those experiments were still in a transient regime when stopped. A strain step is visible for TGI0.42 between 550 000 s (≈153 h) and 650 000 s (≈180 h); it corresponds to a period where the weight used to apply constant torque was in contact with the metallic frame of the torsion apparatus, consequently decreasing the applied stress. After 650 000 s (≈180 h), the weight was put back in a good configuration and the strain curve recovered its pre-step slope. The significant variations observed in strain rate evolution with time between the different runs cannot be attributed to a variation in initial grain size, CPOs or in the applied torque alone (Table 1), but rather to coarse-grained microstructure of the samples, which resulted in fewer than 25 grains per radii and, hence, in a not perfectly isotropic macroscopic behavior. The strain–time curves presented in Fig. 1 are therefore useful to characterize each run creep regime independently, but should be used with care in comparison between different samples or with other experiments.
3.2 Microstructure evolution
AITA maps of tangential sections for each sample and associated analyses are presented in Fig. 2 and Table 2. The evolution of CPO and microstructure (grain size and shape) as a function of finite shear strain is clearly visible. The color wheel gives the orientation of the c axis. The annealed sample TGI0.71 is discussed separately at the end of this section. As the shear strain increases, the distribution of colors changes from random color toward a predominance of red and blue grains, until the map becomes dominated by red grains for TGI1.96 (γmax=1.96).
This evolution records the progressive change in orientation of the c axis with increasing shear strain, displayed as pole figures in Fig. 2b. For the undeformed ice sample (γmax=0) we observe approximately random orientations of c axes with a texture (CPO) index Ji=1.07. The c axis texture (CPO) J index is derived by calculating the second moment of the Euler angles' orientation distribution function (ODF) of discrete crystal orientation data (Bunge, 1982). It is commonly used to quantify CPO strength in geology and in material science. The strain reached by TGI0.012 sample is not high enough to produce any significant change in the CPO. As the strain increases we observe the formation of two sub-maxima, as reported in previous studies (Kamb, 1959, 1972; Duval, 1981; Bouchez and Duval, 1982; Burg et al., 1986), one almost perpendicular to the shear plane (M1) and the other one at a low angle (initially 11–17∘) from the shear plane (M2) as indicated in Fig. 2. With increasing shear, M2 rotates into higher angles to the shear plane (up to 47∘) while M1 remains stable at 90∘ from the macroscopic shear plane. More importantly, the maxima M1 and M2 increase and decrease in intensity, respectively. This evolution towards a single maximum CPO results in an increase in the J index (Fig. 3). The plane containing the finite extension direction (ED) and normal to the compression direction (CD) has a very low [c] axis CPO density for γ≥0.2. One should note that for , the bimodal pattern formed by the two M1 and M2 sub-maxima is almost symmetric relative to the maximum finite extension axis (ED).
Nevertheless the symmetry between M1 and M2 around the finite extension direction is not perfect. The angle between M2 and ED is generally larger than the angle between M1 and ED by 1 to 3∘. The exception is the annealed sample TGI0.71, where the difference between the two is 17.4∘, with M2 closer to ED than it should have been for a perfect symmetry. This change may be due to a post-deformation CPO evolution, due to grain growth during annealing. A small lag in the reorientation of the M2 sub-maximum relative to the M1 sub-maximum is also observed in other simple shear experiments (Bouchez and Duval, 1982; Qi et al., 2019). The limited number of experiments performed in the present study precludes a statistical analysis of this behavior. The evolution of the angle between M1 and M2 (φ) with increasing shear strain is discussed in more detail in Qi et al. (2019), who compared observations from ice shear experiments carried out at different temperatures and numerical modeling.
AITA-extracted grain statistics are presented in Table 2. With increasing γ the median grain size (with associated interquartile range) diminishes from 0.7(4) to 0.12(16) mm. The median is preferred relative to the mean because of the non-normal distribution of grain sizes. The coarser grain size in the TGI0.42 sample compared to TGI0.2 and TGI0.012 is probably due to a difference in the initial grain size, but the grain sizes remain comparable if interquartile ranges are considered. Grain shape fabrics calculated using moment-based ellipse fitting technics (Lexa, 2003) are illustrated as rose diagrams in Fig. 2c. As the shear strain increases, we observe the development of a grain shape fabric following the maximum finite elongation direction indicated with the corresponding overlying strain ellipse in Fig. 2c. The grain shape fabric clearly evolves until γ=0.42 and then does not vary significantly up to γ=1.96
Grain boundary interlocking estimated through the PARIS factor (reported in Table 2) increases during the transient strain regime (from 2.2 % at γ=0 to 11.5 % at γ=0.42) and then decreases. At the highest shear strain of γ=1.96, the PARIS (5.9 %) is half of the one at a shear strain of 0.42.
The annealed sample TGI0.71 shows a median grain size of 1.7 mm, above the initial unstrained value of 0.7 (Table 2). The CPO does not seem to be modified by the annealing with the M1 and M2 maxima maintained and a J index =2.96, which lies in between the values for γmax 0.42 and 1.96, as would be expected from a non-annealed sample with the same finite shear strain (Fig. 2b). The grain shape fabric in the annealed sample is nevertheless more marked than in the strained but non-annealed samples. The PARIS factor decreases significantly, as much of the interlocking of grains is smoothed by annealing.
In summary, the crystallographic orientation evolution during simple shear strain of polycrystalline ice can be described as follows. M1 orientations rapidly develop (by γ=0.2). They remain stable in orientation and increase in intensity until they become predominant at high strains (γ>1.96). The M2 maximum also rapidly develops; it is roughly symmetric to M1 with respect to the maximum finite shortening direction. However the M2 maximum continuously decreases in intensity during the transient regime. The nearly complete disappearance of M2 correlates with achievement of steady state (tertiary creep). All other crystallographic orientations start to disappear as early as γ=0.2 and this tendency is accentuated with increasing shear strain. Finally, if annealing occurs after the strain stops, the CPO is maintained even if the grain shape fabric and grain size are modified.
3.3.1 Maps and textures
Multiple EBSD maps were acquired for every final shear strain. Representative examples of EBSD maps for each sample are shown in Fig. 4a, with the number of maps nm acquired for each γmax indicated at the bottom. The access to the full crystallographic orientations enables more complete grain segmentation based on misorientation data. Grain boundaries are characterized by misorientations ≥5∘ and sub-grain boundaries between 1 and 5∘ (Chauve et al., 2017b).
The orientations of and axes relative to the shear plane and direction are shown in Fig. 4b. All maps acquired for each γmax were combined for better statistical analysis. An excellent level of agreement with CPOs from AITA is observed for CPOs, which rapidly develop M1 and M2 sub-maxima, with disappearance of the M2 maximum and reinforcement of the M1 one at high shear strain. The increase in c axis CPO J index confirms this evolution, with very consistent values with those based on the AITA measurements for a same γmax (Fig. 3). For the high shear strain sample at γmax=1.96, the and axes ( and axis) form a girdle, which tends to align in the shear plane. Within this girdle, there is a preferred orientation of both and directions toward the shear direction. The present CPO is similar to those formed in direct shear experiments (Qi et al., 2019). It is consistent with equivalent contribution of the three axes in accommodating shear on the (0001) plane.
Some elongation of the distribution of the M1 and M2 sub-maxima towards the z direction (Fig. 4b), which is the normal to the shear direction in the shear plane, is visible in our results. This elongation is best expressed for the M1 maximum in the highest-strain sample TG1.96, for which pole figures for and lattice vectors are now represented in two perpendicular reference frames in Fig. 4b for better readability. Similar elongated distributions of axes have been reported in direct shear experiments by Qi et al. (2019). Some elongation of the M1 maximum is also observed in the highest shear strain sample (γ=2) of Bouchez and Duval (1982) as well as in other shear experiments in Li et al. (2000), Wilson and Peternell (2012), and Budd et al. (2013). However, most naturally sheared ice samples do not have elongated maxima (Hudleston, 1977).
3.3.2 Weighted Burgers vector analysis and intragranular strain
During plastic strain, some of the stress on the ice lattice is relieved by the formation and glide of dislocations. Some of those dislocations are trapped in the crystal lattice, forming stable arrays of geometrically necessary dislocations (GNDs), which may define sub-grain boundaries. Such intragranular strain heterogeneities are observed in numerous experimental studies on polycrystalline ice and in natural environments, (Wilson et al., 1986; Mansuy et al., 2000; Piazolo et al., 2008; Montagnat et al., 2011; Weikusat et al., 2011; Faria et al., 2014a; Chauve et al., 2017b). As described in the methods section, WBV analysis allows the calculation of a minimum density of GNDs and definition of the relative proportion of dislocations with and [c]-component Burgers vector within this GND population. Figure 5 provides representative maps at every finite shear strain investigated.
In these WBV maps (Fig. 5) we observe a large number of linear sub-grain boundaries already developed at γmax=0.2. Evolution of the GNDs density with increasing strain is hard to assess by visually comparing the maps for different finite shear strains, but it can be assessed by the analysis of the quantitative statistical distribution of and [c] GNDs (Fig. 6). The sub-grain boundaries are mostly organized in walls and the direction of the trace of these planes on the thin section typically corresponds to the parent grain [c]-axis direction. This kind of sub-grain boundary, very common in both natural and experimentally deformed ice, has been identified as a basal tilt boundary composed of basal edge dislocations (b=a, with b the Burgers vector) through EBSD and X-ray Laue diffraction (Piazolo et al., 2008; Weikusat et al., 2011; Chauve et al., 2017b). These sub-grain boundaries are visible in Fig. 5b as purple and blue lines. Other types of low-angle boundaries were also identified in both natural and experimentally deformed ice; these are basal twist boundaries with basal screw dislocation and non-basal tilt boundaries with variable numbers of dislocations with a [c] axis Burgers vector component (i.e., and [c]) (Piazolo et al., 2008, 2015; Weikusat et al., 2011; Chauve et al., 2017b). Such sub-boundaries are also identified in the present study (green to yellow lines in Fig. 5b). It is interesting to note that even in the most deformed sample, which has a strong CPO with one single sub-maxima at γmax=1.96 (at steady-state tertiary creep), GNDs are very common. Both the undeformed sample (TGI0.012) and the annealed sample (TGI0.71) have much lower low-angle boundary densities than the other samples. The undeformed sample map shows low-angle boundaries located very close to high-angle boundaries and as unconnected pixels and small segments within grains. These are best explained as low-angle indexing errors. Most grains in the annealed sample contain very few angle boundaries. In this annealed sample, only about four grains contain low-angle boundaries similar to the one extensively observed in the deformed but not annealed samples (Fig. 5a).
As demonstrated by Chauve et al. (2017b), the total density of GNDs (with above threshold) increases with strain (Fig. 6f). However, the ratio of [c] component (rWBV) of GNDs remains constant at ca. 35 % (rWBV, or ). For the lowest shear strain (TGI0.012) the [c]-component ratio is larger, but this could be due to the smaller sample size, as the density of GNDs (i.e., number of pixels with a µm−1) is much lower. By classifying grains by orientation, it is possible to look at the individual statistics for the grains composing the M1 and the M2 maxima and in other orientations (Fig. 6a to e). Analysis of the pixel orientation statistic shows that the proportion pixels with M2 orientation rapidly increases compared to the one with M1 orientation at γmax=0.2 and then gradually decreases at γmax=0.42, eventually disappearing at γmax=1.96. When performing the WBV analysis for each grain orientation family, the presence of GNDs with a [c]-component Burgers vector does not seem to be correlated with the orientation of the grain. The only exception is the annealed case at γmax=0.71, where recovery processes and noise due to the small sample size limit the use of such analysis. The present observations are consistent with previously published data on [c]-component GNDs for both shear and compression experiments from Chauve et al. (2017b).
We computed the probability density function of rWBVc as a function of the distance to the grain boundary and represented it for rWBV, and rWBV in Fig. 7. We are able to observe that the rWBV density clearly decreases around 100 µm close to the grain boundary, when both and rWBV densities increase (rWBV almost doubles). This statistical analysis clearly shows the increase in [c]-component dislocations proportion in the substructures at a distance lower than 100 µm from the grain boundary. It is important to note that we do not observe any significant differences between different finite shear strains.
As indicated by the evolution of the macroscopic strain rates in Fig. 1, we were able to analyze the CPO and microstructure at different creep regimes. The near-constant strain rate ( s−1) achieved for the TGI1.96 run can be interpreted as the evidence that this sample was close to steady state in terms of mechanical behavior, typical of tertiary creep regime. The appearance and evolution of c axis orientation sub-maxima M1 and M2 in the CPO are consistent with previous data from Hudleston (1977) and Bouchez and Duval (1982) and from the recent direct shear experiments from Qi et al. (2019). The M1 maximum always remains normal to the shear plane and the M2 sub-maximum, initially as strong as M1, progressively rotates with shear during transient creep and decreases in intensity until it disappears, possibly as tertiary creep regime is reached.
The slow evolution of the grain shape preferred orientations and their saturation at shear strains higher than 0.2, visible from the grain shape orientation rose diagram (Fig. 2c), could be the effect of recrystallization processes and fast grain boundary migration that counter the formation of a strong grain shape fabric. These processes may also explain why we observe a decrease in the grain boundary interlocking at high strains and even more in the annealed sample through the PARIS factor (Table 2). Both dynamic and static recrystallization should enable the appearance and growth of new grains with small PARIS factors at the expenses of older grains with serrated grain boundaries (higher PARIS). This observation underlines the fact that the estimation of strain magnitude from grain elongation or shape is not reliable at high temperature, as noted by Burg et al. (1986). The efficiency of grain boundary migration and recovery of shape fabric is expected to significantly decrease with decreasing temperatures.
The case of the annealed sample TGI0.71 is interesting to understand how metadynamic annealing processes like grain boundary migration driven by dislocation density variation may change the microstructure and CPO. The CPO is maintained, the grain shape fabric is reinforced and the final grain size is larger than the initial one. The preservation of the CPO suggests that most new “dislocation free” nuclei were already close to M1 or M2 orientations before annealing. This suggests bulging as the dominant mechanism for nucleation at the conditions of our experiments (prior to annealing), as it tends to create grains with a closer orientation to the parent grains. Furthermore we report an offset angle between the M1 and M2 sub-maxima 17.4∘ greater than what would be expected for a perfect symmetry to the finite extension direction. Other experiments, which did not undergo annealing, show a difference in angle of only 1–3∘ with the perfect symmetry. In the TGI0.71 annealed sample, M2 is much closer to M1, as would be expected for a higher finite shear strain. This could be interpreted as a sign of preferential growth of bulging nuclei with orientation closer to M1 than the bulk CPO of the sample before annealing. Conservation of the CPO with annealing also means that if stress is somehow lowered in a natural context, and annealing takes place, the CPO could still be interpreted, even if information about grain shape fabric is lost. The conservation of the CPO during annealing has also been observed in experimental and natural samples of quartzite (Heilbronner and Tullis, 2002; Augenstein and Burg, 2011), and rock analog materials such as chloropropane or norcamphor (Park et al., 2001). The reinforcement of the grain shape fabric with elongation toward the finite extension direction (Fig. 2c) also suggests some oriented grain growth. It is possible that during strain, the formation of a large number of isometric nuclei weakens the shape fabric, but that this evolution is counteracted by grain growth during static annealing.
The full lattice preferred orientations derived from EBSD data reveal that both and axes display preferential orientation within the shear plane toward the finite extension direction, as observed in Qi et al. (2019). From theory the slip system is supposed to be dominant in the basal plane (Hondoh, 2000); this assumption is consistent with the present data since such a CPO may result from similar activation of all three directions, but could also mean an equivalent activation of glide in either or directions.
From the WBV analysis of the EBSD maps, we were able to map GNDs and obtain information about their Burgers vector components. If the density of GNDs increases with shear strain, the proportion of GNDs with Burgers vector with a [c] component seems to be independent of the amount of deformation. However there is a clear increase in the number of GNDs with a [c]-component Burgers vector in the vicinity of the grain boundaries, as illustrated in Fig. 7. The observation of an increase in proportion close to GBs of the [c]-component GNDs, predicted to be unfavorable compared to basal plane dislocations, is consistent with stress concentrations particularly important close to GBs. As pointed out by Chauve et al. (2017a), there is a clear connection between the nucleation by the bulging mechanism and GNDs located near serrated grain boundaries. The closing of bulges by the formation of a sub-grain boundary was suggested early as an important nucleation process in Urai et al. (2013). For instance Chauve et al. (2017b) have shown observations of GND loops in ice that require [c]-component dislocation walls to be closed. This would support the hypothesis that the increase in [c]-component GNDs near the grain boundary helps to form GND loops that give birth to new grains. These observations, combined with our present WBV statistical analysis, point towards a possible way to estimate the maximum size of a bulging nucleus, which would be lower than 100 µm in the present case. It would be important in future studies to test if this critical dimension would vary with temperature or stress, as well as to obtain misorientation data at higher spatial resolution to better constrain the evolution of these higher zones with strong [c]-component concentration. The fact that the estimated maximum size of a bulging nucleus is constant at all finite shear strains suggests that bulging is very active at all creep regimes, further stressing its importance for understanding the rheology of ice and other materials at high temperatures.
The pioneering work on 2-D modeling of polycrystalline aggregates under simple shear performed by Etchecopar (1977) was able to reproduce CPO with sub-maxima M1 and M2. This was simply performed by considering a single slip system (basal slip system for ice) and adding an accommodation process which allows cells to subdivide (Etchecopar defines this as grain breaking but grain polygonization would have the same kinematic effect) and undergo rigid body rotation. The very good agreement of this simplistic model with evolution of CPOs observed experimentally for ice under shear was emphasized by Bouchez and Duval (1982), who hypothesized that the polygonization processes in ice would be formation of GNDs and kink bands. In our results few kink bands were observed, but the prevalence of GNDs at most finite shear strains suggests that Bouchez and Duval (1982) supposition is reasonable. Although Etchecopar (1977) modeling is too simplistic to pretend reproduction of every shear-induced CPO in ice, it was useful to raise the likely role of polygonization as an efficient accommodation mechanism for solving strain incompatibility problems.
Modeling of shear in ice has been carried out by mean-field approaches as in Castelnau et al. (1996) or more recently by full-field modeling as in Llorens et al. (2016). Both works reproduced the formation of a strong single maximum CPO from shear strain of about 0.4 and above. Nevertheless, neither the orientation of this single maximum normal to the shear plane nor the existence of two sub-maxima as observed at lower strains in the field or experimentally is correctly reproduced. The fact that the single sub-maximum prescribed is inclined from the tangent to the shear plane is significant, and arises from the fact that these homogenization techniques require the activation of non-basal slip systems. The activation of secondary slip systems, whose contribution to strain has never been proven experimentally, induces a geometrical rotation of the crystal that is responsible for the modeled inclination of the clustered CPO compared to the vertical. The activity of these secondary slip systems relative to the basal ones is controlled by a parameter that is arbitrarily defined (it has been defined in comparison to experimental observations in Castelnau et al., 1997, using the mean-field Visco-Plastic Self-Consistent (VPSC) code approach, and values different than the one chosen in the previously cited studies were obtained). The higher the non-basal activity, the softer the mechanical response of the crystal to accommodate the imposed conditions. The geometrical constraint of crystal rotation under shear, owing to the activity of non-basal slip systems, can be artificially relaxed, such as in Wenk and Tomé (1999), by forcing the growth of selected grains, or as in Signorelli and Tommasi (2015), by an association of polygonization and local (within a grain) relaxation of the strain compatibility constraints.
By comparing these various modeling approaches, and their inclusion of recrystallization mechanisms, it appears that accommodation mechanisms, other than non-basal slip systems, must come into play to explain recrystallization-induced shear CPOs in ice. Although we consider the fact that fast grain boundary migration might be an efficient strain accommodation mechanism, we suggest here that an efficient additional contribution to the CPO reorientation, at the high homologous temperatures of our experimental studies (and the ones of Bouchez and Duval, 1982, or Qi et al., 2017, 2019), might well be nucleation assisted by polygonization (or sub-grain boundary rotation).
The analysis of the CPO evolution in the experiments suggests that plastic strain through dislocation creep is probably as commonly claimed largely dominated by basal slip. Nevertheless, stored GNDs (including non-basal GNDs with [c]-component Burgers vector) allow recrystallization accommodation mechanisms such as nucleation by bulging. The fact that the PARIS factor initially increases then decreases above γmax=0.42 enables us to make further assumptions about active recrystallization mechanisms and their evolution (or sequence) with increasing strain. Until a strain close to γmax=0.42, heterogeneities in dislocation storage close to grain boundaries favor spatially irregular grain boundary migration to dominate, creating numerous serrated grain boundaries, as indicated by the increasing PARIS factor. With increasing finite strain, the influence of nucleation gradually increases, forming more isodiametric grains, lowering the PARIS factor, and eventually erasing the M2 maximum. Indeed, SGBs required to close bulges may necessitate strong local stress levels (in order to activate [c]-component dislocations, for instance) that are obtained after a given amount of accumulated strain, while grain boundary migration may occur since the very beginning of the deformation.
Our results also underline the efforts remaining to match experimental observations and mean-field and full-field numerical modeling. The present data indicate an important role of dynamic recrystallization processes, namely bulging nucleation and grain boundary migration, in the CPO evolution in simple shear. They also establish the importance of non-basal dislocation slip participating in SGB-related polygonization.
By using state-of-the-art analytical techniques (i.e., AITA, EBSD and weighted Burgers vector analysis), we were able to characterize the CPO, microstructure and geometrically necessary dislocation structures in ice deformed under torsion in the laboratory at an unprecedented resolution. The experiments, performed at high temperature, up to shear strains of 2, favored dynamic recrystallization observed in natural conditions with slower strain rates such as cold glaciers, ice streams and some deep ice core areas. The present experiments corroborate previous observations: under simple shear, ice develops a two-maxima c axis crystallographic preferred orientation (CPO), which evolves rapidly into a single-cluster CPO with c axis perpendicular to the shear plane.
From new high-resolution observations and analyses, we were able to determine that
abundant sub-grain boundary formation, boundary migration and bulging nucleation are the dominant detected recrystallization mechanisms at these conditions.
sub-grain boundary density and GND components are characterized as abundant at all observed finite shear strain, even at this high temperature (0.97Tm).
at large finite strain (γmax≤1.96) a significant preferred orientation of both and directions toward the shear direction is observed.
annealing of shear strained polycrystalline ice preserves the CPO and creates a strong grain shape fabric elongated toward the finite extension direction.
around 30 % of geometrically necessary dislocations exhibit a significant [c] component, due to strong local stresses arising from the strong strain heterogeneities, even at these high-temperature conditions.
the density of the [c] component of GNDs increases close to grain boundaries; this effect may help the closure of bulging grain boundary and allow efficient bulging nucleation.
So far, full-field modeling approaches that simulate plastic deformation by activating non-basal slip systems in ice were unable to fully reproduce the strongly clustered simple shear CPO observed experimentally and in nature. As was already suggested by Etchecopar (1977), polygonization may play a crucial role in accommodating dislocation glide dominated by basal slip. Our observations suggest that bulging, associated with sub-grain boundary mechanisms, could be responsible for this and explain the observed strongly clustered CPO at relatively high strain and high temperature. We conclude that non-basal dislocation slip should not be involved in modeling to obtain realistic CPOs in polycrystalline ice and other anisotropic material, but that GNDs with [c] component should play a major role in strain accommodation and nucleation processes. We hope that these new results will help the modeling community to provide realistic modeling CPO evolution of simple shear in ice, which is capital for a better predictive ability of ice landmass evolution in the coming decades and centuries.
MTEX is a free MATLAB® toolbox for analyzing and modeling crystallographic CPOs by means of EBSD or pole figure data (Hielscher and Schaeben, 2008; Bachmann et al., 2010, 2011; Mainprice et al., 2014). It is available on http://mtex-toolbox.github.io/.
PolyLX is a free MATLAB® toolbox for quantitative analysis of microstructures, developed by Lexa (2003), and available on https://petrol.natur.cuni.cz/~ondro/oldweb/polylx:home.
The supplement related to this article is available online at: https://doi.org/10.5194/tc-13-1495-2019-supplement.
BJ was the leading author of this paper. Sample preparation and torsion experiments were performed in Grenoble by BJ and LG. EBSD measurements were carried out in Montpellier by BJ, TC, MM, FB and LG. Data analysis was conducted by BJ and TC. Interpretation was performed by BJ, TC, MM, AT and DM. BJ and MM wrote the paper with input from all authors.
The authors declare that they have no conflict of interest.
The authors acknowledge the financial support provided by the French “Agence Nationale de la Recherche”, project DREAM, ANR-13-BS09-0001-01, awarded to Maurine Montagnat. This work benefited from support from the INSIS and INSU institutes of CNRS. Some of the present work was supported by a grant from Labex OSUG@2020 (ANR10LABEX56) and from INP-Grenoble and UJF in the frame of the proposal called “Grenoble Innovation Recherche AGIR” (AGI13SMI15). Support for Baptiste Journaux also came from the NASA postdoctoral program fellowship awarded to Baptiste Journaux, by the NASA Solar System Workings grant 80NSSC17K0775 and by the Icy Worlds node of NASA's Astrobiology Institute (08-NAI5-0021).
The authors thank Paul Duval for insightful scientific discussions and useful advice on the experimental and theoretical aspects and John Wheeler for sharing the weighted Burgers vector code and providing precious advice on it.
This paper was edited by Martin Schneebeli and reviewed by David Prior and Jacob Tielke.
Augenstein, C. and Burg, J.-P.: Natural annealing of dynamically recrystallised quartzite fabrics: Example from the Cévennes, SE French Massif Central, J. Struct. Geol., 33, 244–254, https://doi.org/10.1016/j.jsg.2010.10.008, 2011. a
Bachmann, F., Hielscher, R., and Schaeben, H.: Texture Analysis with MTEX – Free and Open Source Software Toolbox, Sol. St. Phen., 160, 63–68, https://doi.org/10.4028/www.scientific.net/SSP.160.63, 2010. a, b
Bachmann, F., Hielscher, R., and Schaeben, H.: Grain detection from 2d and 3d EBSD data – Specification of the MTEX algorithm, Ultramicroscopy, 111, 1720–1733, https://doi.org/10.1016/j.ultramic.2011.08.002, 2011. a, b
Blackman, D. K., Boyce, D. E., Castelnau, O., Dawson, P. R., and Laske, G.: Effects of crystal preferred orientation on upper-mantle flow near plate boundaries: rheologic feedbacks and seismic anisotropy, Geophys. J. Int., 210, 1481–1493, https://doi.org/10.1093/gji/ggx251, 2017. a
Bons, P. D., Jansen, D., Mundel, F., Bauer, C. C., Binder, T., Eisen, O., Jessell, M. W., Llorens, M.-G., Steinbach, F., Steinhage, D., and Weikusat, I.: Converging flow and anisotropy cause large-scale folding in Greenland's ice sheet, Nat. Commun., 7, 11427, https://doi.org/10.1038/ncomms11427, 2016. a
Bouchez, J. l. and Duval, P.: The Fabric of Polycrystalline Ice Deformed in Simple Shear: Experiments in Torsion, Natural Deformation and Geometrical Interpretation, Texture. Microstruct., 5, 171–190, https://doi.org/10.1155/TSM.5.171, 1982. a, b, c, d, e, f, g, h, i, j, k, l
Boudier, F. and Coleman, R. G.: Cross section through the peridotite in the Samail Ophiolite, southeastern Oman Mountains, J. Geophys. Res., 86, 2573–2592, https://doi.org/10.1029/JB086iB04p02573, 1981. a
Budd, W. F., Warner, R. C., Jacka, T. H., Li, J., and Treverrow, A.: Ice flow relations for stress and strain-rate components from combined shear and compression laboratory experiments, J. Glaciol., 59, 374–392, https://doi.org/10.3189/2013JoG12J106, 2013. a, b
Buiron, D., Chappellaz, J., Stenni, B., Frezzotti, M., Baumgartner, M., Capron, E., Landais, A., Lemieux-Dudon, B., Masson-Delmotte, V., Montagnat, M., Parrenin, F., and Schilt, A.: TALDICE-1 age scale of the Talos Dome deep ice core, East Antarctica, Clim. Past, 7, 1–16, https://doi.org/10.5194/cp-7-1-2011, 2011. a
Burg, J. P., Wilson, C. J. L., and Mitchell, J. C.: Dynamic recrystallization and fabric development during the simple shear deformation of ice, J. Struct. Geol., 8, 857–870, https://doi.org/10.1016/0191-8141(86)90031-3, 1986. a, b, c, d
Cassard, D., Nicolas, A., Rabinovitch, M., Moutte, J., Leblanc, M., and Prinzhofer, A.: Structural classification of chromite pods in southern New Caledonia, Econ. Geol., 76, 805–831, https://doi.org/10.2113/gsecongeo.76.4.805, 1981. a
Castelnau, O., Duval, P., Lebensohn, R. A., and Canova, G. R.: Viscoplastic modeling of texture development in polycrystalline ice with a self-consistent approach: Comparison with bound estimates, J. Geophys. Res., 101, 13851–13868, https://doi.org/10.1029/96JB00412, 1996. a, b
Castelnau, O., Canova, G. R., Lebensohn, R. A., and Duval, P.: Modelling viscoplastic behavior of anisotropic polycrystalline ice with a self-consistent approach, Acta Mater., 45, 4823–4834, https://doi.org/10.1016/S1359-6454(97)00098-0, 1997. a
Chauve, T., Montagnat, M., and Vacher, P.: Strain field evolution during dynamic recrystallization nucleation; A case study on ice, Acta Mater., 101, 116–124, https://doi.org/10.1016/j.actamat.2015.08.033, 2015. a
Chauve, T., Montagnat, M., Barou, F., Hidas, K., Tommasi, A., and Mainprice, D.: Investigation of nucleation processes during dynamic recrystallization of ice using cryo-EBSD, Philos. T. R. Soc. A, 375, 20150345, https://doi.org/10.1098/rsta.2015.0345, 2017a. a, b
Chauve, T., Montagnat, M., Piazolo, S., Journaux, B., Wheeler, J., Barou, F., Mainprice, D., and Tommasi, A.: Non-basal dislocations should be accounted for in simulating ice mass flow, Earth Planet. Sc. Lett., 473, 247–255, https://doi.org/10.1016/j.epsl.2017.06.020, 2017b. a, b, c, d, e, f, g, h, i, j, k
Cuffey, K. and Paterson, W. S. B.: The Physics of Glaciers, 4th edn., Academic Press, Cambridge, MA, USA, 2010. a
Dahl-Jensen, D., Thorsteinsson, T., Alley, R., and Shoji, H.: Flow properties of the ice from the Greenland Ice Core Project ice core: The reason for folds?, J. Geophys. Res., 102, 26831–26840, https://doi.org/10.1029/97JC01266, 1997. a
De La Chapelle, S., Castelnau, O., Lipenkov, V., and Duval, P.: Dynamic recrystallization and texture development in ice as revealed by the study of deep ice cores in Antarctica and Greenland, J. Geophys. Res., 103, 5091–5105, https://doi.org/10.1029/97JB02621, 1998. a
Demouchy, S., Mainprice, D., Tommasi, A., Couvy, H., Barou, F., Frost, D. J., and Cordier, P.: Forsterite to wadsleyite phase transformation under shear stress and consequences for the Earth's mantle transition zone, Phys. Earth Planet. In., 184, 91–104, https://doi.org/10.1016/j.pepi.2010.11.001, 2011. a
Duval, P.: Creep and recrystallization of polycrystalline ice, B. Mineral., 102, 80–85, 1979. a
Fernicola, V., Rosso, L., and Giovannini, M.: Investigation of the Ice–Water Vapor Equilibrium Along the Sublimation Line, Int. J. Thermophysics, 33, 1363–1373, https://doi.org/10.1007/s10765-011-1128-2, 2011. a
Gillet-Chaulet, F., Gagliardini, O., Meyssonnier, J., Zwinger, T., and Ruokolainen, J.: Flow-induced anisotropy in polar ice and related ice-sheet flow modelling, J. Non-Newtonian Fluid, 134, 33–43, https://doi.org/10.1016/j.jnnfm.2005.11.005, 2006. a
Gow, A. J. and Williamson, T.: Rheological implications of the internal structure and crystal fabrics of the West Antarctic ice sheet as revealed by deep core drilling at Byrd Station, GSA Bulletin, 87, 1665–1677, https://doi.org/10.1130/0016-7606(1976)87<1665:RIOTIS>2.0.CO;2, 1976. a
Grennerat, F., Montagnat, M., Castelnau, O., Vacher, P., Moulinec, H., Suquet, P., and Duval, P.: Experimental characterization of the intragranular strain field in columnar ice during transient creep, Acta Mater., 60, 3655–3666, https://doi.org/10.1016/j.actamat.2012.03.025, 2012. a
Heilbronner, R. and Barrett, S.: Image Analysis in Earth Sciences, in: Microstructures and Textures of Earth Materials, Springer-Verlag Berlin Heidelberg, https://doi.org/10.1007/978-3-642-10343-8, 2014. a
Heilbronner, R. and Tullis, J.: The effect of static annealing on microstructures and crystallographic preferred orientations of quartzites experimentally deformed in axial compression and shear, Geological Society, London, Special Publications, 200, 191–218, https://doi.org/10.1144/GSL.SP.2001.200.01.12, 2002. a
Higgie, K. and Tommasi, A.: Feedbacks between deformation and melt distribution in the crust–mantle transition zone of the Oman ophiolite, Earth Planet. Sc. Lett., 359-360, 61–72, https://doi.org/10.1016/j.epsl.2012.10.003, 2012. a
Hudleston, P. J.: Progressive Deformation and Development of Fabric Across Zones of Shear in Glacial Ice, in: Energetics of Geological Processes, edited by: Saxena, S. K., Bhattacharji, S., Annersten, H., and Stephansson, O., Springer Berlin Heidelberg, 121–150, https://doi.org/10.1007/978-3-642-86574-9_7, 1977. a, b, c, d
Ismaïl, W. B. and Mainprice, D.: An olivine fabric database: an overview of upper mantle fabrics and seismic anisotropy, Tectonophysics, 296, 145–157, https://doi.org/10.1016/S0040-1951(98)00141-3, 1998. a
Journaux, B., Chauve, T., Montagnat, M., Tommasi, A., Barou, F., Mainprice, D., and Gest, L.: Recrystallization processes, microstructure and texture evolution in polycrystalline ice during high temperature simple shear, PANGAEA, https://doi.org/10.1594/PANGAEA.901009, 2019. a
Li, J., Jacka, T. H., and Budd, W. F.: Strong single-maximum crystal fabrics developed in ice undergoing shear with unconstrained normal deformation, Ann. Glaciol., 30, 88–92, https://doi.org/10.3189/172756400781820615, 2000. a, b, c
Lipenkov, V. Y., Barkov, N. I., Duval, P., and Pimienta, P.: Crystalline Texture of the 2083 m Ice Core at Vostok Station, Antarctica, J. Glaciol., 35, 392–398, https://doi.org/10.3189/S0022143000009321, 1989. a
Llorens, M.-G., Griera, A., Bons, P. D., Lebensohn, R. A., Evans, L. A., Jansen, D., and Weikusat, I.: Full-field predictions of ice dynamic recrystallisation under simple shear conditions, Earth Planet. Sc. Lett., 450, 233–242, https://doi.org/10.1016/j.epsl.2016.06.045, 2016. a
Llorens, M.-G., Griera, A., Steinbach, F., Bons, P. D., Gomez-Rivas, E., Jansen, D., Roessiger, J., Lebensohn, R. A., and Weikusat, I.: Dynamic recrystallization during deformation of polycrystalline ice: insights from numerical simulations, Philos. T. R. Soc. A, 375, 20150346, https://doi.org/10.1098/rsta.2015.0346, 2017. a
Ma, Y., Gagliardini, O., Ritz, C., Gillet-Chaulet, F., Durand, G., and Montagnat, M.: Enhancement factors for grounded ice and ice shelves inferred from an anisotropic ice-flow model, J. Glaciol., 56, 805–812, https://doi.org/10.3189/002214310794457209, 2010. a
Mainprice, D., Bachmann, F., Hielscher, R., and Schaeben, H.: Descriptive tools for the analysis of texture projects with large datasets using MTEX: strength, symmetry and components, Geological Society, London, Special Publications, 409, SP409–8, 2014. a, b
Mansuy, P., Philip, A., and Meyssonnier, J.: Identification of strain heterogeneities arising during deformation of ice, Ann. Glaciol., 30, 121–126, https://doi.org/10.3189/172756400781820651, 2000. a
Martín, C., Gudmundsson, G. H., Pritchard, H. D., and Gagliardini, O.: On the effects of anisotropic rheology on ice flow, internal structure, and the age-depth relationship at ice divides, J. Geophys. Res., 114, F04001, https://doi.org/10.1029/2008JF001204, 2009. a
Montagnat, M., Blackford, J. R., Piazolo, S., Arnaud, L., and Lebensohn, R. A.: Measurements and full-field predictions of deformation heterogeneities in ice, Earth Planet. Sc. Lett., 305, 153–160, https://doi.org/10.1016/j.epsl.2011.02.050, 2011. a, b
Montagnat, M., Castelnau, O., Bons, P. D., Faria, S. H., Gagliardini, O., Gillet-Chaulet, F., Grennerat, F., Griera, A., Lebensohn, R. A., Moulinec, H., Roessiger, J., and Suquet, P.: Multiscale modeling of ice deformation behavior, J. Struct. Geol., 61, 78–108, https://doi.org/10.1016/j.jsg.2013.05.002, 2014. a
Montagnat, M., Chauve, T., Barou, F., Tommasi, A., Beausir, B., and Fressengeas, C.: Analysis of Dynamic Recrystallization of Ice from EBSD Orientation Mapping, Front. Earth Sci., 3, 81, https://doi.org/10.3389/feart.2015.00081, 2015. a
Park, Y., Ree, J.-H., and Kim, S.: Lattice preferred orientation in deformed-then-annealed material: observations from experimental and natural polycrystalline aggregates, Int. J. Earth Sci., 90, 127–135, https://doi.org/10.1007/s005310000163, 2001. a
Peternell, M., Russell-Head, D., and Wilson, C.: A technique for recording polycrystalline structure and orientation during in situ deformation cycles of rock analogues using an automated fabric analyser, J. Microsc., 242, 181–188, https://doi.org/10.1111/j.1365-2818.2010.03456.x, 2011. a
Piazolo, S., Montagnat, M., and Blackford, J. R.: Sub-structure characterization of experimentally and naturally deformed ice using cryo-EBSD, J. Microsc., 230, 509–519, https://doi.org/10.1111/j.1365-2818.2008.02014.x, 2008. a, b, c
Piazolo, S., Montagnat, M., Grennerat, F., Moulinec, H., and Wheeler, J.: Effect of local stress heterogeneities on dislocation fields: Examples from transient creep in polycrystalline ice, Acta Mater., 90, 303–309, https://doi.org/10.1016/j.actamat.2015.02.046, 2015. a
Qi, C., Goldsby, D. L., and Prior, D. J.: The down-stress transition from cluster to cone fabrics in experimentally deformed ice, Earth Planet. Sc. Lett., 471, 136–147, https://doi.org/10.1016/j.epsl.2017.05.008, 2017. a, b, c
Qi, C., Prior, D. J., Craw, L., Fan, S., Llorens, M.-G., Griera, A., Negrini, M., Bons, P. D., and Goldsby, D. L.: Crystallographic preferred orientations of ice deformed in direct-shear experiments at low temperatures, The Cryosphere, 13, 351–371, https://doi.org/10.5194/tc-13-351-2019, 2019. a, b, c, d, e, f, g, h, i
Randle, V.: Microtexture determination and its applications, The Institute of Materials, London, UK, 1992. a
Russell-Head, D. S. and Wilson, C. J. L.: Automated fabric analyser system for quartz and ice, Geological Society of Australia Abstracts, 64, 159–159, 1999. a
Signorelli, J. and Tommasi, A.: Modeling the effect of subgrain rotation recrystallization on the evolution of olivine crystal preferred orientations in simple shear, Earth Planet. Sc. Lett., 430, 356–366, https://doi.org/10.1016/j.epsl.2015.08.018, 2015. a, b
Swift, W.: Length Changes in Metals Under Torsional Overstrain, Engineering, 163, 253 pp., 1947. a
Tommasi, A., Knoll, M., Vauchez, A., Signorelli, J. W., Thoraval, C., and Logé, R.: Structural reactivation in plate tectonics controlled by olivine crystal anisotropy, Nat. Geosci., 2, 423–427, https://doi.org/10.1038/ngeo528, 2009. a
Treverrow, A., Budd, W. F., Jacka, T. H., and Warner, R. C.: The tertiary creep of polycrystalline ice: experimental evidence for stress-dependent levels of strain-rate enhancement, J. Glaciol., 58, 301–314, https://doi.org/10.3189/2012JoG11J149, 2012. a
Urai, J. L., Means, W. D., and Lister, G. S.: Dynamic recrystallization of minerals. Mineral and rock deformation, American Geophysical Union Geophysical Monograph Series 36, 166–199, 1986. a
Weikusat, I., Miyamoto, A., Faria, S. H., Kipfstuhl, S., Azuma, N., and Hondoh, T.: Subgrain boundaries in Antarctic ice quantified by X-ray Laue diffraction, J. Glaciol., 57, 111–120, https://doi.org/10.3189/002214311795306628, 2011. a, b, c
Wheeler, J., Mariani, E., Piazolo, S., Prior, D., Trimby, P., and Drury, M.: The weighted Burgers vector: a new quantity for constraining dislocation densities and types using electron backscatter diffraction on 2D sections through crystalline materials, J. Microsc., 233, 482–494, https://doi.org/10.1111/j.1365-2818.2009.03136.x, 2009. a, b, c
Wilson, C. J. L. and Peternell, M.: Ice deformed in compression and simple shear: control of temperature and initial fabric, J. Glaciol., 58, 11–22, https://doi.org/10.3189/2012JoG11J065, 2012. a, b, c
Wilson, C. J. L., Luzin, V., Piazolo, S., Peternell, M., and Hammes, D.: Experimental deformation of deuterated ice in 3D and 2D: identification of grain-scale processes, Proceedings of the Royal Society of Victoria, 127, 99–104, http://www.publish.csiro.au/paper/RS15011, 2015. a
Wright, S. I., Nowell, M. M., and Field, D. P.: A review of strain analysis using electron backscatter diffraction, Microsc. Microanal., 17, 316–329, https://doi.org/10.1017/S1431927611000055, 2011. a, b