The effect of grain size on strain rate of ice in the upper 2207 m in the North Greenland Eemian Ice Drilling (NEEM) deep ice core was investigated using a rheological model based on the composite flow law of Goldsby and Kohlstedt (1997, 2001). The grain size was described by both a mean grain size and a grain size distribution, which allowed the strain rate to be calculated using two different model end-members: (i) the microscale constant stress model where each grain deforms by the same stress and (ii) the microscale constant strain rate model where each grain deforms by the same strain rate. The model results predict that grain-size-sensitive flow produces almost all of the deformation in the upper 2207 m of the NEEM ice core, while dislocation creep hardly contributes to deformation. The difference in calculated strain rate between the two model end-members is relatively small. The predicted strain rate in the fine-grained Glacial ice (that is, ice deposited during the last Glacial maximum at depths of 1419 to 2207 m) varies strongly within this depth range and, furthermore, is about 4–5 times higher than in the coarser-grained Holocene ice (0–1419 m). Two peaks in strain rate are predicted at about 1980 and 2100 m depth. The prediction that grain-size-sensitive creep is the fastest process is inconsistent with the microstructures in the Holocene age ice, indicating that the rate of dislocation creep is underestimated in the model. The occurrence of recrystallization processes in the polar ice that did not occur in the experiments may account for this discrepancy. The prediction of the composite flow law model is consistent with microstructures in the Glacial ice, suggesting that fine-grained layers in the Glacial ice may act as internal preferential sliding zones in the Greenland ice sheet.
Ice sheets regulate global mean sea level (GMSL) by storing large amounts of fresh water in the form of ice on land. As a consequence of increased anthropogenic global warming, the contribution of the Greenland and the Antarctic ice sheets to GMSL rise is likely to increase in the next few centuries (IPCC, 2014). It is therefore important to improve the implementation of ice flow in ice sheet models that calculate the discharge of ice into the ocean, since the amount of water stored in ice sheets is enough to raise GMSL by about 70 m (Alley et al., 2005; Church et al., 2013). The mass balance of an ice sheet depends on the accumulation of snow on the surface, release of meltwater by runoff, and the solid discharge via floating ice shelves and calving of icebergs into the ocean (e.g., Petrenko and Withworth, 1999; Marshall, 2006). In the coldest parts of Antarctica, sublimation and wind erosion can be important ablation mechanisms as well (Bintanja, 2009). The amount of ice available for calving and melting depends on the flow of ice from the interior towards the margins of the ice sheet. This flow of ice is controlled by two processes: sliding of the ice over the bedrock, which includes various subglacial processes (Zwally et al., 2002; Vaughan and Arthern, 2007; Thoma et al., 2010; Wolovick and Creyts, 2016), and the internal deformation of the polycrystalline ice, which is governed by various processes like dislocation creep, grain boundary migration (strain-induced grain boundary migration, SIBM, using the terminology of Faria et al., 2014b) and grain boundary sliding (GBS) (e.g., Duval et al., 1983; Alley, 1992; Goldsby and Kohlstedt, 1997, 2001; Montagnat and Duval, 2000, 2004; Schulson and Duval, 2009; Faria et al., 2014a).
For large-scale flow models, the deformation of the ice polycrystal is
approximated in a homogenized way by continuum mechanics principles.
Together with balance equations for mass, momentum and energy, continuum
mechanics uses the relation between stress and strain rate given by a
constitutive relation, also called the “flow law”. The most commonly used
flow law in ice sheet models is Glen's flow law (Glen, 1952, 1955; Paterson,
1994), which describes the flow of polycrystalline ice during deformation by
a power law relating equivalent strain rate (
Pimienta and Duval (1987) proposed that in the low-stress regime with
During experiments with very fine-grained ice (with a grain diameter between
3 and 90
The hypothesis of Goldsby and Kohlstedt (1997, 2001) concerning the role of GBS in ice has been seriously questioned by Duval and Montagnat (2002), who noted that deformation by dominant GBS is inconsistent with the strong crystallographic preferred orientations (CPOs) found in polar ice, which can be explained by deformation involving basal slip accommodated by grain boundary migration (Pimenta and Duval, 1987; Montagnat and Duval, 2000). In response, Goldsby and Kohlstedt (2002) noted that a CPO could develop in the case of GBS accommodated by easy basal slip. While the detailed deformation mechanisms are controversial, there is actually a consensus that the low stress deformation of ice involves slip on the easy basal slip system accommodated by grain boundary processes (Goldsby and Kohlstedt, 2002; Duval and Montagnant, 2002) and that deformation in the low-stress regime is likely to be grain size sensitive (Montagnant et al., 2003; Duval and Montagnat, 2006).
The recent study by Saruya et al. (2019) confirms the occurrence of GSS creep in fine-grained ice and proposes a different mechanism, where grain boundaries enhance creep by acting as sinks for dislocations. We emphasize that even though the exact mechanisms involved in GSS flow are not understood in detail, there is good experimental evidence for GSS creep in ice and the available flow laws provide a reasonable basis to investigate the role of these mechanisms in polar ice sheets.
Goldsby and Kohlstedt (2001), Goldsby (2006), and Durham et al. (2010)
suggested that Glen's flow law actually represents a combination of
deformation mechanisms at the stress range 0.1–1.0 MPa (Glen, 1952, 1955)
rather than just dislocation creep. This forms a possible explanation for a
lack of accuracy in calculating ice strain rates when using Glen's flow law
with fixed
The different GSS and GSI creep regimes recognized by Goldsby and Kohlstedt (1997, 2001) have been combined by these authors in the form of one composite flow law. The major advantage of such a composite flow law is that it explicitly denotes the components of the different creep mechanisms, rather than just describing bulk behavior. This provides the opportunity to calculate the relative importance of the GSS and GSI deformation mechanisms over the range of temperatures, differential stresses and grain sizes found in ice sheets and compare their contribution to the total strain rate. This is not possible with the flow law developed by Baker (1981), for example, which adds a factor to the preexisting Glen's flow law to account for the effect of grain size.
It is well known that grain size varies throughout both the Greenland and Antarctic ice sheets (e.g., Gow et al., 1997; Faria et al., 2014b; Binder, 2014; Fitzpatrick et al., 2014). However, the effect of grain size on strain rate is usually not considered in ice sheet models that apply flow laws of the type of Glen's flow law. Furthermore, the grain size is often expressed as a single mean grain size, which is generally not a good representation for a grain size distribution (Kipfstuhl et al., 2009). For instance, small grains in a distribution might contribute differently to the overall behavior than large grains, with a given set of GSS and GSI mechanisms. Ter Heege et al. (2004) showed that using a mean grain size instead of a full grain size distribution in composite flow laws can lead to an overestimate or underestimate of the strain rates of natural rocks.
In the NEEM ice core in northwestern Greenland (77.45
In this paper, the composite flow law is used to investigate the effect of grain size, grain size distribution and different microscale models on the dominant deformation mechanism and the predicted strain rate down to 2207 m depth in the NEEM deep ice core, and the results are compared to results obtained with Glen's flow law. The grain size data are described using both a mean grain size and a grain size distribution to evaluate the natural variability in grain size and the effect of grain size variation on predicted strain rate in polar ice. The deformation mechanisms predicted from the composite flow law are compared with the mechanisms inferred from microstructural and CPO studies of the ice cores. The actual variation in strain rate with depth is currently being investigated by continuing borehole logging studies (Dahl-Jansen et al., 2016; Dorthe Dahl-Jansen, personal communication, 2019) in the NEEM bore hole. Preliminary results (Greve et al., 2017) indicate that enhanced strain rates occur in the NEEM Glacial age layers. This study is in progress and will provide important information on the effect of grain size, CPO and impurity content on ice deformation by providing strain rate measurements with depth to compare with those predicted by the model presented here.
The NEEM deep ice core was chosen because a comprehensive light microscope
dataset was available (Kipfstuhl, 2010) enabled by a fast line scan
technique with microscopic resolution (LASM, Large Area Scanning
Macroscope; Krischke et al., 2015). From these LM images the grain size
distribution is available (Binder et al., 2013). The NEEM ice core was
drilled between 2008 and 2012 and is located close to an ice ridge (NEEM
community members, 2013). The flow at the NEEM ice core is mainly parallel
to the ridge, with a small divergent component perpendicular to the line of
the ridge (Montagnat et al., 2014). The top 1419 m of the NEEM deep ice core
consists of ice deposited during the Holocene (Holocene ice), which shows a
steadily increasing crystallographic preferred orientation (CPO) towards a
vertical
Compilation of microstructure and borehole data of the NEEM ice
core:
The difference in microstructure between the Holocene ice and the Glacial
ice of the NEEM ice core is shown in Fig. 2. The Holocene ice core section
(Fig. 2a) was taken from a depth of 921 m and contains coarse grains with
an aspect ratio of about
Reflected LM images of ice core sections at
In this study, 615 LM images of the Holocene and Glacial ice were used to
determine the evolution of the grain size with depth in the NEEM ice core.
These LM images were made of sections that were cut parallel to the long
(vertical) axis of the ice core (Kipfstuhl et al., 2006). Each LM image is
about 90 mm long and about 55 mm wide and was digitally analyzed using the
Ice-image software (
Reflected LM image
The composite flow law as proposed by Goldsby and Kohlstedt (2001) is
formulated as follows:
As explained by Durham and Stern (2001) and Durham et al. (2001, 2010), GBS
and dislocation slip are sequential processes where one cannot proceed
without the other and the slowest mechanism determines the overall strain
rate, i.e., is rate-limiting, so that if
Figure 4 shows the effect of grain size and stress on strain rate for
GBS-limited creep (
The effect of grain size and stress on calculated strain rate plotted for Glen's flow law and the dislocation creep mechanism and GBS-limited creep of the composite flow law at a constant temperature of 243 K using the flow law parameters in Table 1.
Parameters for the simplified composite flow law and for Glen's
flow law given by Eq. (3) that relates grain size, temperature and stress
to strain rate. Values taken from Goldsby and Kohlstedt (2001, G&K) and Paterson
(1994). The
The smaller grains in a polycrystal can potentially deform by a different mechanism than the larger grains, since the smaller grains are more susceptible to GSS deformation mechanisms. In order to study the effect of the variation in grain size, a grain size distribution was used as well as a mean grain size in the flow law (Freeman and Ferguson, 1986; Heilbronner and Bruhn, 1998; Ter Heege et al., 2004). As shown by Freeman and Ferguson (1986) and Ter Heege et al. (2004), applying a grain size distribution into a composite flow law leads to application of two theoretical end-members to describe the deformation of ice: the homogeneous stress, or microscale constant stress model, and the homogeneous strain rate, or microscale constant strain rate model.
The microscale constant stress model assumes that each grain experiences
the same stress, which is equal to the bulk stress of the material. However,
the strain rate produced by each grain is different. The driving stress and
the bulk strain rate produced by this model can be expressed as follows:
The microscale constant strain rate model assumes that each grain deforms
by the same strain rate, which is equal to the strain rate of the bulk
material. The stress required to produce this strain rate is different for
each grain size class. This end-member assumes that the larger grains in the
polycrystalline material support more stress than the smaller grains and can
be described as follows:
The temperature in the NEEM borehole reaches 269.8 K at the bedrock
interface, which is only 0.9 K below the estimated pressure-melting point
(Sheldon et al., 2014). At this temperature it is expected that the
deformation of ice is affected by pre-melting (e.g., Mellor and Testa, 1969b;
Barnes et al., 1971; Morgan, 1991; Goldsby and Kohlstedt, 2001). To omit the
effect of the different temperature thresholds given in Table 1 for Glen's
flow law (263 K), the GBS-limited mechanism (255 K) and the dislocation creep
mechanism (258 K) of the composite flow law (Goldsby and Kohlstedt, 2001;
Goldsby, 2006), the high-temperature flow law parameters, and therefore the
effect of pre-melting on strain rate, were not included in this study. Since
the effect of pre-melting is expected to start close to the Glacial–Eemian
interface at about
The method of Heilbronner and Bruhn (1998) was used to convert 2D sectional areas to 3D volume fractions. This method uses an equivalent grain diameter that was determined for each grain and a 3D volume fraction was calculated with the assumption of a spherical grain. This method corrects for the overrepresentation of small grains in an LM image compared to the bulk volume. The grain size distribution contains 80 grain size classes defined by steps of the equivalent diameter of 0.3 mm each, covering the full breath of the observed grain size distribution in the Holocene and Glacial ice. The equivalent diameter of each grain in each ice core section was calculated and included in the corresponding grain size class. Figure 5 shows an example of the volume contribution of sectional circles and the corresponding volume contribution of spheres for an ice core section at 921 m depth (details of the microstructure are shown in Fig. 2a).
Relative contribution of each grain size class to the bulk volume of an ice core section containing 965 grains at 921 m depth calculated for sectional circles (blue) and spherical grains (red) using the method of Heilbronner and Bruhn (1988).
The mean grain size was determined by dividing the total area, as classified by the “grain” category in the Ice-image software, by the number of grains for each LM image. This way, the areas affected by bubbles, fracturing or frost are excluded from the mean grain size calculation. A mean equivalent diameter for each ice core section was calculated by assuming a circular grain. Since the composite flow law of Goldsby and Kohlstedt (1997, 2001) requires a grain diameter instead of grain area as an input variable, the conversion of grain area to equivalent grain diameter is required. This conversion might induce a small but systematic error, since recrystallized materials tend to have a lognormal grain size distribution, which leads the calculated equivalent grain diameter to be larger than the mean grain diameter. When using a mean grain size, there are no series of volume fractions (Eqs. 8 and 10) so no application of the microscale constant stress model and the microscale constant strain rate model is required.
To calculate the strain rate using Glen's flow law and the composite flow law at the location of the NEEM ice core, information about the variation in stress with depth in the ice sheet is required. As stress itself cannot be measured, the stress has to be estimated based on theoretical considerations and constraints on strain rates in the NEEM ice core.
The shear stress in an ice sheet is driven by gravity and is determined by
the surface slope of the ice sheet and the depth from the surface
The equivalent shear stress (
The upper part of the NEEM ice core is dominated by longitudinal stress,
perpendicular to the plane of the divide, leading to thinning of the annual
layers (Dansgaard and Johnsen, 1969; Montagnat et al., 2014). Longitudinal
stresses can be calculated from the increase in the ice slope away from the
divide if the rheology of ice is assumed (Raymond, 1983; Dahl-Jensen,
1989a). In this study, the simple approach of assuming an imposed
stress–depth relationship will be taken to investigate how ice rheology is
influenced by grain size, temperature and imposed stress. The layer thinning
in the upper part of an ice core, caused by the increased overburden
pressure resulting from the deposition of a new snow layer each year,
provides a constraint on the vertical strain rate. In case of the NEEM ice
core this gives a value of about
Modified dislocation creep parameters for the composite flow law as derived from Fig. 7. The transition temperature is taken to be 262 K (see Sects. 2.3 and 3).
The assumption of constant equivalent stress with depth is not realistic for ice sheets in general (e.g., Dahl-Jensen, 1989b). However, this assumption is a useful first approximation for the NEEM ice core where the equivalent stress, related to the shear stress in the lower part of the ice core, is by coincidence similar to the magnitude of equivalent stress related to the vertical stress in the upper part of the ice core. While this approach is simple, it is a useful first step. We have also investigated the effect of changing the constant equivalent stress in the range of 0.01 to 0.50 MPa. When calculating strain rates, no distinction is made between simple shear and vertical flattening deformation.
The most recently updated flow law parameters for the simplified composite
flow law (Goldsby, 2006) and the most often used form of Glen's flow law
with
A comparison of the calculated strain rate for dislocation creep with the
experimental data points from Fig. 7 of Goldsby and Kohlstedt (2001) was
made. The calculated strain rates were based on the flow law parameters in
Table 1 and using Eq. (3). This comparison is shown in Fig. 7a. The
solid blue line shows the calculated strain rate for dislocation creep when
the flow law parameters of Table 1 were used and forced with a stress of 6.3 MPa, which is the same stress as used in Fig. 6 of Goldsby and Kohlstedt (2001). The calculated strain rate does not coincide with the three
experimental data points for a temperature of
Arrhenius plot showing
We have modified the flow law parameters for dislocation creep (dashed blue
line, Fig. 7a). A transition temperature of 262 K was taken for both
dislocation creep and GBS-limited creep, as this is the expected temperature
threshold at which pre-melting starts to dominate ice rheology (see Kuiper et al., 2020). The modified flow law parameters for dislocation creep
that are proposed here are shown in Table 2; the flow law parameters for
GBS-limited creep are the same as given in Table 1 except for the
temperature threshold. For dislocation creep, the material parameter
For both the composite flow law and Glen's flow law, the influence of CPO on strain rate is not taken into account during this study, for example, by a pre-exponential enhancement factor. It is well known that dislocation creep in ice is strongly influenced by CPO development (Azuma, 1994), and it is likely that flow involving basal slip rate-limited by GBS is also strongly influenced by CPO. The effect of CPO development on the grain-size-sensitive mechanisms cannot be included yet as experimental data are lacking.
As noted in the introduction, we did not include any grain size evolution in the model, so the model simply applies to the current grain sizes found in the NEEM ice core. It is well known that grain size and grain size distributions are not fixed parameters in ice depending on the recrystallization mechanisms and on parameters such as stress, strain and temperature (Wilson et al., 2014; Faria et al., 2014b; Peternell et al., 2019). The grain size produced by dynamic recrystallization will scale with the stress (Jacka and Li, 1994). As larger grain sizes are produced at lower stress, dynamic recrystallization can limit the importance of GSS creep (de Bresser et al., 2001). The grain sizes in the GRIP ice core from Greenland and the Byrd ice core from the Antarctic are smaller than the stress–grain size relationship and the GSI-GSS transitions (Goldsby and Kohlstedt, 2002, Fig. 2; Goldsby, 2006, Fig. 60.5) indicating that GSS creep is potentially favored in the upper sections of polar ice sheets compared to the coarser-grained deeper ice.
Figure 8a and b show the strain rate per grain size class and the contribution of the two deformation mechanisms (Eq. 6) for an ice core section at 921 m depth (see detail in Fig. 2a). This ice core section is located in the middle of the Holocene ice and has a relatively high variation in grain size. Since dislocation creep is a GSI mechanism, the strain rate produced by this deformation mechanism is the same for each grain size class in the microscale constant stress model (Fig. 8a). GBS-limited creep shows faster strain rates than dislocation creep for all grain size classes and strongly decreases in strain rate with increasing grain size, which is consistent with the inverse relationship to grain size given in Eq. (3). The volume contribution of each grain size class (black bars in Fig. 8a and b) is used in Eq. (8) to calculate the bulk strain rate for this ice core section and in Eq. (10) to iteratively calculate the stress supported by each grain size class.
Grain size class versus log strain rate for an ice core section at
921 m depth for
The total strain rate produced by each grain size class is set to be the same for the microscale constant strain rate model (Fig. 8b). The relative contribution of each deformation mechanism differs between grain size classes. GBS-limited creep is the dominant deformation mechanism for the smallest grains, whereas dislocation creep becomes increasingly more important for classes with larger grain sizes. However, even for the largest grains in this ice core section the strain rate produced by GBS-limited creep is still slightly larger than the strain rate produced by dislocation creep.
The stress supported per grain size class for the microscale constant stress and microscale constant strain rate model for the composite flow law is shown in Fig. 8c. The stress supported per grain size class using the microscale constant strain rate model is used in Eq. (10) to iteratively calculate the stress in the bulk material of the ice core section. The smallest grain size classes support only a small amount of stress, since they are more sensitive to GBS-limited creep. As a consequence, the larger grains support more stress and activate a significant amount of dislocation creep.
Figure 9 shows plots of the equivalent strain rate as a function of depth for Glen's flow law and the composite flow law with its two different deformation mechanisms and the three different model end-members calculated using the modified flow law parameters for dislocation creep (Table 2) and the original parameters for GBS-limited creep (Table 1). The contribution of GBS-limited creep to bulk strain rate is also shown. The temperature input for all the models is shown in Fig. 1c. The results using the full grain size distribution with the microscale constant stress model (Fig. 9a) and the microscale constant strain rate model with the grain size distribution (Fig. 9b) are shown, as well as the results using the mean grain size model (Fig. 9c). All models show similarities, such as (i) a relatively constant strain rate between 400 and 1400 m depth, (ii) a strain rate increase below 1400 m depth and (iii) a higher strain rate for Glen's flow law compared to the composite flow law along the entire depth range down to 2207 m of the NEEM ice core. In all of the three model end-members, dislocation creep hardly contributes to the overall strain. The calculated strain rate for GBS-limited creep and the composite flow law both show a more variable strain rate below 1400 m. This depth coincides with the transition from the coarse-grained Holocene ice to the finer-grained Glacial ice and with an increase in temperature (Fig. 1c). Two strain rate peaks occur at about 1980 and 2100 m depth and show a two- to three-fold increase in strain rate compared to the mean strain rate in the Glacial ice predicted by the composite flow law.
The difference between the strain rates of GBS-limited creep and dislocation creep in the Holocene ice is smaller for the microscale constant strain rate model than for the microscale constant stress model and the mean grain size model. Compared to the microscale constant stress model, the microscale constant strain rate model predicts slightly lower absolute strain rates from GBS-limited creep along the entire upper 2207 m depth of the NEEM ice core (Fig. 9a, b) and especially below 1419 m depth, where the strain rate is more variable. Using a mean grain size produces a weaker variability in strain rate with depth than the two model end-members using a grain size distribution (Fig. 9c). The average strain rate in the Holocene ice is about 60 % higher using the microscale constant stress model compared to the microscale constant strain rate model. For the Glacial ice, this difference between the two model end-members is about 40 %.
To study the dominant deformation mechanism of the composite flow law at different stress levels and its comparison in strain rate to Glen's flow law, both flow laws were forced at different stress values, which roughly cover the range of equivalent stresses in the Greenland and Antarctic ice sheets (Sergienko et al., 2014). Figure 10a shows the calculated strain rate for dislocation creep and GBS-limited creep using the grain size distribution with the microscale constant stress model and the temperature profile of NEEM, forced with different constant stress values. At the lowest stress of 0.01 MPa, the strain rate produced by dislocation creep is about 3 orders of magnitude lower than the strain rate produced by GBS-limited creep. With increasing stress, the contribution of dislocation creep to the overall strain rate becomes bigger, and at a stress of 0.25 MPa dislocation creep and GBS-limited creep have roughly the same contribution. The strain rate produced by the dislocation creep mechanism at 0.50 MPa is roughly 5 times higher than for GBS-limited creep. A similar graph showing the calculated strain rate for the composite flow law and Glen's flow law is shown in Fig. 10b. At the lowest stress of 0.01 MPa the composite flow law predicts a slightly higher strain rate compared to Glen's flow law. However, with increasing stress, Glen's flow law predicts progressively higher strain rates than the composite flow law. At the highest stress of 0.50 MPa, the strain rate predicted by Glen's flow law is almost an order of magnitude higher than the strain rate predicted by the composite flow law.
Stress sensitivity of the deformation mechanisms in the Holocene
and Glacial ice.
We will first discuss the results from the different microscale end-member models for distributed grain sizes in Sect. 5.1, then compare the results of models with a distributed grain size against a mean grain size in Sect. 5.2. The effect of stress levels on predicted strain rates will be discussed in Sect. 5.3 followed by a consideration of the variation in predicted strain rates with depth in Sect. 5.4. In the last section, the predictions of the composite flow law are compared with the deformation mechanisms indicated by the microstructures and CPOs from the NEEM ice core.
The main difference between the microscale constant stress model and the microscale constant strain rate model is that the microscale constant stress model allows the smallest grains to deform more than an order of magnitude faster than the larger grains (Fig. 8a), while this is not possible in the microscale constant strain rate model (Fig. 8b). For the microscale constant strain rate model, the strain rate is set to be the same for each grain size class. GBS-limited creep and dislocation creep are therefore codependent, since the sum of the two deformation mechanisms has to add up to a certain strain rate (Eq. 6). Consequently, since the strain rate produced by GBS-limited creep decreases with increasing grain size, the contribution of dislocation creep to bulk strain rate increases with grain size. This effect is shown in Fig. 8b, where the bulk strain rate is similar for each grain size class but the contribution of dislocation creep to the bulk strain rate increases with increasing grain size. Due to this codependence of dislocation creep and GBS-limited creep in the microscale constant strain rate model, the strain rate produced by dislocation creep varies slightly with depth, as is shown in Fig. 9b.
For most ice core samples, the finest grain size classes contribute only
slightly to the bulk volume of the material, as is also the case for the ice
core section at 921 m depth shown in Fig. 8. For this particular ice
core section, the smallest grain size classes (
By assuming that each grain deforms by the same amount in the microscale constant strain rate model, the strain heterogeneities that have often been observed in ice core microstructures (e.g., Obbard et al., 2006; Weikusat et al., 2009a; Faria et al., 2014a; Piazolo et al., 2015; Jansen et al., 2016) are ignored. Contrary to the microscale constant stress model, where the contribution of the finest grains is relatively large compared to their volume contribution, the microscale constant strain rate model probably overestimates the role of the larger grains on the bulk strain rate in the ice core section. Therefore, the two models represent the lower and upper limit of deformation behavior of a polycrystal with a distributed grain size (Ter Heege et al., 2004). Natural deformation in ice sheets is likely to involve microscale variations in stress and strain rate (e.g., Faria et al., 2014a; Piazolo et al., 2015).
The difference in calculated strain rate between using a grain size distribution with the microscale constant strain rate model and the mean grain size model is relatively small (Fig. 9b and c). A single mean grain size eliminates the effect that smaller grains have on the bulk strain rate. However, the effect of the smaller grains on strain rate in the microscale constant strain rate model is also limited since all grain size classes deform by the same amount, and thus the difference in bulk strain rate between the microscale constant strain rate model and mean grain size model is small. The much larger computational expense of the microscale constant strain rate model and the small difference in calculated strain with the mean grain size model argues for using a mean grain size model over a microscale constant strain rate model when modeling GSS behavior in polar ice sheets.
The difference in calculated strain rate between the microscale constant stress model and using a mean grain size model is larger than the difference between the microscale constant strain rate model and the mean grain size model. The strain rate peaks predicted in the layers at about 1980 m and 2100 m depth are 2 to 3 times larger for the microscale constant stress model compared to the mean grain size model (Fig. 9a, c). This difference is mainly caused by the effect that the finest grains have on the bulk strain rate in the microscale constant stress model (Fig. 8a).
Figure 10a shows that, at equivalent stresses below 0.25 MPa, the strain
rate produced by GBS-limited creep is higher than the strain rate produced
by dislocation creep, while at an equivalent stress of 0.50 MPa the strain
rate produced by dislocation creep is higher than GBS-limited creep. The
stress sensitivity of dislocation creep is controlled by a stress exponent
of
Interestingly, the stress of 0.10–0.50 MPa is within the range of stresses
(0.1–1.0 MPa) that was used during the deformation experiments of Glen (1952, 1955). The grain size 1–2 mm reported by Glen (1952) is similar to
the grain size in the Glacial ice of the NEEM ice core. The results in
Fig. 10a for 0.25 MPa show that the contribution of dislocation creep and
GBS-limited creep to the total strain rate in the Glacial ice is roughly
equal. This result supports the hypothesis of Durham et al. (2001, 2010),
Goldsby and Kohlstedt (2001, 2002), Goldsby (2006), and Bons et al. (2018)
that the stress exponent of
Comparison of the results using the composite flow law with Glen's flow law
at different equivalent stresses (Fig. 10b) shows that at a stress of 0.01 MPa the composite flow law predicts a higher strain rate than Glen's flow
law in most of the upper 2207 m depth in the NEEM ice core. In the finest-grained parts of the Glacial ice, the composite flow law predicts a strain
rate that is about 5 times faster than predicted by Glen's flow law at
the low equivalent stress of 0.01 MPa. As the equivalent stress increases,
Glen's flow law becomes progressively faster relative to the composite flow
law. Since the dominant deformation mechanism of the composite flow law at
low equivalent stress is GBS-limited creep (Fig. 10a), the effective
stress exponent will also be close to the stress exponent for GBS-limited
creep (
Levels of high borehole closure and borehole tilting have been observed in many polar ice cores and often coincide with high-impurity content and small grain sizes (e.g., Fisher and Koerner, 1986; Paterson, 1994). These depth levels can be seen as layers with a different microstructure than the surrounding ice and therefore deform at a higher strain rate. The reason that small grain size and high-impurity content coincide is still not well understood (Eichler et al., 2017). The results using the composite flow law suggest that prominent soft layers, i.e., layers with a high strain rate, could be present at two depths of about 1980 and 2100 m in the NEEM ice core. The predictions from the composite flow law are consistent with preliminary results from ongoing borehole tilt measurements at NEEM (Dahl-Jansen et al., 2016; Greve et al., 2017; Dorthe Dahl-Jensen, personal communication, 2019). These soft layers are located in the lower part of the NEEM ice core, which is dominated by simple shear (Dansgaard and Johnson, 1969; Montagnat et al., 2014). The soft layers can therefore be seen as depths where a high rate of simple shear occurs, instead of layers with enhanced extrusion (Waddington, 2010). It is likely that not all soft layers that are caused by finer grains have been identified in the model, since the available sampling rate of 615 LM images along 2207 m depth of the NEEM ice core leaves many depth intervals not studied. Glen's flow law is unable to predict soft layers related to grain size variations since the flow law is forced by stress and temperature only. The effects of anisotropy, grain size and/or impurity content on strain rate are often incorporated in the form of an enhancement factor (Azuma, 1994; Thorsteinsson et al., 1999). However, information about the softening effects, like grain size, are needed in order to incorporate the enhancement factor with the right value and at the right depth. This can only be achieved by a flow law that explicitly describes GSS deformation, such as the flow laws of Goldsby and Kohlstedt (2001) or Saruya et al. (2019). GSS deformation is also expected for flow involving basal slip accommodated by grain boundary migration (Montagnant et al., 2003), although there is no calibrated quantitative flow law for this mechanism.
Another reason why soft layers might have been missed during this study is
that by taking the grain size distribution of the
The microstructures and CPOs in the NEEM core provide constraints on the active deformation mechanisms. The microstructures in the Holocene ice (Fig. 2a) with irregular grain boundaries indicate strain-induced grain boundary migration (SIBM, using the terminology of Faria et al., 2014b), and subgrain development in the grains indicates that dislocation creep and dynamic recrystallization are important (Montagnat et al., 2014; Weikusat et al., 2017; Steinbach et al., 2017). The microstructures in the Holocene ice are clearly different from the microstructure developed in experimental samples by GSS creep (Goldsby and Kohlstedt, 1997; Saruya et al., 2019). So the results from the composite flow model (Fig. 9) are inconsistent with the microstructures in the Holocene ice.
In the Glacial ice, different microstructures occur and the grain size is smaller than in the Holocene ice. In the Glacial ice, grain boundaries are straight to smooth and the grain aspect ratio found in subhorizontal fine-grained bands (Fig. 2b) is similar to that reported by Goldsby and Kohlstedt (1997, Fig. 6 therein) in the GBS-limited creep experiments. Also, similar to Goldsby and Kohlstedt (1997), aligned grain boundaries and numerous quadruple junctions were found (Fig. 2b). These flattened grains, aligned grain boundaries and quadruple junctions were only found in the finest-grained parts of the Glacial ice, which could well indicate that these layers have deformed by GBS, possibly enforced by micro-shear (Faria et al., 2014b).
The
For both the composite flow law and Glen's flow law, the influence of CPO on strain rate is not taken into account during this study, for example, by a pre-exponential enhancement factor. In bed-parallel simple shear, a strong vertical single maximum CPO produces fewer strain incompatibilities at grain boundaries by aligning the basal planes of the ice crystals in the direction of the flow. This means that less accommodation of basal slip is required by either non-basal slip or GBS per unit of strain, which causes the strain rate to increase compared to an isotropic ice sample. The strain rate enhancement caused by a well-developed CPO is about 2.3 times stronger in simple shear than in pure shear (Budd and Jacka, 1989; Treverrow et al., 2012). Therefore, the difference in equivalent strain rate between the Holocene and the Glacial ice is probably larger than shown in Fig. 9, since the Holocene ice is predominantly deforming by pure shear, while the Glacial ice is predominantly deforming by simple shear (Montagnat et al., 2014). Both deformation mechanisms of the composite flow law assume basal slip to be the dominant strain-producing mechanism and being rate-limited by either grain boundary sliding or non-basal slip. We suggest that both dislocation creep and GSS creep are both enhanced by a strong single maximum CPO as a strong alignment of the dominant slip system produces fewer strain incompatibilities at grain boundaries and triple junctions.
We will now consider the discrepancy between the model predictions and the deformation mechanisms indicated by the NEEM Holocene microstructures. The results from the composite flow law model shown in Fig. 9 suggest that ice deformation in the upper 2207 m depth of the NEEM ice core is almost entirely produced by GSS creep. However, there is evidence that significant non-basal slip is activated in the polar ice sheets (e.g., Weikusat et al., 2009b, 2011, 2017). Goldsby (2006) compared the results of the composite flow law using the original flow law parameters (Table 1) to the grain size and strain rate variability with depth in the basal layer of the Meserve glacier, Antarctica (Cuffey et al., 2000b). It was found that the composite flow law overestimates the contribution of GBS-limited creep in the basal part of the Meserve glacier. The in situ temperature (256 K) and the estimated shear stress (0.05 MPa) in the basal layer of the Meserve glacier are fairly similar to the temperature and stress estimated for the Glacial ice in the NEEM ice core (Fig. 1c). With the modified flow law parameters for dislocation creep (Table 2), the calculated contribution of GBS-limited creep to total strain rate would be close to 100 %, which is similar to the results with the NEEM ice core (Fig. 9). Therefore, it is proposed that the composite flow law severely underestimates the strain rate produced by dislocation creep, as high stresses of about 0.25 MPa are required for dislocation creep to become roughly as fast as GBS-limited creep in the NEEM ice core (Fig. 10a). This while the large and interlocking grains in the Holocene ice of the NEEM ice core (Fig. 2a) argue against GBS as the dominant rate limiting mechanism for basal slip. It is interesting to note that the constant strain rate model predicts a larger role for dislocation creep so this model may be more appropriate for the shallow ice that is deforming mainly by pure shear, with all layers deforming at the same strain rate.
The deformation experiments in the GSI and GSS regime of Goldsby and Kohlstedt (1997, 2001) were performed at low temperature in order to prevent grain growth during the deformation experiments. Significant grain growth during the deformation experiments would have complicated the derivation of the flow law parameters in the GSS creep regime. Goldsby and Kohlstedt (1997) stated that “grains in deformed samples were equiaxed with straight grain boundaries; irregular grain boundaries typical of dynamical recrystallization by grain boundary migration were not observed”. However, suppressing SIBM during the deformation experiments also meant that SIBM could not remove strain incompatibilities at grain boundaries and/or triple junctions. Recrystallization by SIBM is considered an important softening mechanism in polar ice (e.g., Duval et al., 2000; Montagnat and Duval, 2000; 2004; Wilson et al., 2014). It is well established that SIBM is active at all depths in polar ice cores (e.g., Weikusat et al., 2009a), although the amount of SIBM varies strongly with depth (e.g., Duval and Castelnau, 1995; Kipfstuhl et al., 2009; Faria et al., 2014a). In the NEEM ice core, SIBM is probably less extensive in the finer-grained Glacial ice than in the coarser-grained Holocene ice, which is supported by the lower grain boundary curvature in the Glacial ice (Binder, 2014). It is therefore proposed that SIBM is an important softening mechanism in the Holocene ice of the NEEM ice core, while it was suppressed during the deformation experiments of Goldsby and Kohlstedt (1997, 2001). Therefore, the ice during the GSI deformation experiments of Goldsby and Kohlstedt (2001) was probably relatively hard, compared to natural polar ice, as the synthetic ice in experiments was not softened by SIBM. This would have affected the flow law parameters that were derived from the results of these deformation experiments, potentially underestimating dislocation creep strain rates when using the composite flow law.
In order to study the effect of grain size and grain size variation with depth in polar ice sheets, the composite flow law of Goldsby and Kohlstedt (2001) was used with temperature and grain size data from the upper 2207 m depth in the NEEM ice core. A constant equivalent stress with depth was assumed, with a magnitude of 0.07 MPa constrained from the surface slope and layer thinning data from NEEM. GSS deformation was described using a mean grain size and a grain size distribution in combination with two model end-members: the microscale constant stress model and the microscale constant strain rate model. A modification of the flow law parameters for dislocation creep (GSI) in the composite flow law showed a better fit with the experimental data obtained during the deformation experiments of Goldsby and Kohlstedt (1997, 2001).
The difference between the model end-members is relatively small, with the microscale constant stress model predicting higher strain rates than the microscale constant strain rate model and using a mean grain size. The results using the modified flow law parameters and a constant equivalent stress of 0.07 MPa, predict that GSS creep produces almost all deformation in the upper 2207 m depth in the NEEM ice core. A strain rate increase, mainly resulting from a reduction in grain size, is predicted below 1400 m depth for all model end-members. Two depths in the Glacial ice with a higher strain rate, caused by enhanced GSS creep, are predicted at about 1980 and 2100 m depth.
At the grain size and temperature conditions of the NEEM ice core, GSS creep is predicted to be the dominant deformation mechanism over dislocation creep for equivalent stresses up to about 0.25 MPa. At higher stresses, which occur at the edges of polar ice sheets, dislocation creep is dominant over GSS creep. At low stresses of about 0.01 MPa, the composite flow law predicts a faster strain rate than Glen's flow law. However, the stress exponent of Glen's flow law is higher than the effective stress exponent for the composite flow law and therefore the strain rate increase with increasing stress is higher for Glen's flow law than for the composite flow law. At NEEM grain size and temperature conditions, Glen's flow law predicts a higher strain rate than the composite flow law at equivalent stresses higher than 0.05 MPa.
The prediction from the composite flow model that GSS creep is the dominant process at all depths is inconsistent with microstructures in the Holocene ice, indicating that the rate of dislocation creep is underestimated in the model. One possible explanation for this is that recrystallization by SIBM was not active during the experiments of Goldsby and Kohlstedt (1997, 2001), while recrystallization by SIBM is an important softening mechanism in the Holocene ice. In the Glacial ice the microstructures and CPO indicate that large strains are accommodated by basal slip, while the occurrence of straight grain boundaries and quadruple points indicate that GBS may be significant. These features are consistent with GSS creep mechanisms involving large activity of the easy slip system, such as basal slip rate-limited by GBS as proposed by Goldsby and Kohlstedt (2001) or grain-size-enhanced dislocation creep as recently proposed by Saruya et al. (2019). The composite flow law model and the microstructures in the Glacial ice both indicate that the fine-grained layers in the Glacial ice may potentially act as internal preferential sliding zones in the Greenland ice sheet.
The models were calculated using C
EJNK prepared the code, data, and setup of simulations and conducted model runs. JHPdB developed the algorithm for the code and provided the initial idea. MRD and GMP supervised and initiated the simulation setups and interpretations. DJ and IW provided ice core samples and data, glaciological background, and data preparation. All authors jointly interpreted results and wrote the manuscript.
The authors declare that they have no conflict of interest.
This work has been carried out as part of the Helmholtz Junior Research
group “The effect of deformation mechanisms for ice sheet dynamics”
(VH-NG-802). The NEEM light microscope data used in this study has been made
available by
This research has been supported by the Hermann von Helmholtz-Gemeinschaft Deutscher Forschungszentren e.V. and the Helmholtz Foundation (grant no. VH-NG-802).
This paper was edited by Robert Arthern and reviewed by David Prior, Chris Wilson and one anonymous referee.