Skip to main content Accessibility help
×
Home

Information:

  • Access
  • Cited by 3

Figures:

Actions:

      • Send article to Kindle

        To send this article to your Kindle, first ensure no-reply@cambridge.org is added to your Approved Personal Document E-mail List under your Personal Document Settings on the Manage Your Content and Devices page of your Amazon account. Then enter the ‘name’ part of your Kindle email address below. Find out more about sending to your Kindle. Find out more about sending to your Kindle.

        Note you can select to send to either the @free.kindle.com or @kindle.com variations. ‘@free.kindle.com’ emails are free but can only be sent to your device when it is connected to wi-fi. ‘@kindle.com’ emails can be delivered even when you are not connected to wi-fi, but note that service fees apply.

        Find out more about the Kindle Personal Document Service.

        Crystal-growth rates in firn and shallow ice at high-accumulation sites
        Available formats
        ×

        Send article to Dropbox

        To send this article to your Dropbox account, please select one or more formats and confirm that you agree to abide by our usage policies. If this is the first time you use this feature, you will be asked to authorise Cambridge Core to connect with your <service> account. Find out more about sending content to Dropbox.

        Crystal-growth rates in firn and shallow ice at high-accumulation sites
        Available formats
        ×

        Send article to Google Drive

        To send this article to your Google Drive account, please select one or more formats and confirm that you agree to abide by our usage policies. If this is the first time you use this feature, you will be asked to authorise Cambridge Core to connect with your <service> account. Find out more about sending content to Google Drive.

        Crystal-growth rates in firn and shallow ice at high-accumulation sites
        Available formats
        ×
Export citation

Abstract

Crystal growth in firn and shallow ice is studied by examining crystal size and ,c-axis orientation fabrics in two ice cores drilled at sites Dome Summit South and DE08, near the summit of Law Dome, East Antarctica. The snow-accumulation rates at the core sites are particularly high (640 and 1160 kg m−2 a−1, respectively) compared to other Antarctic sites. Crystal-growth rates above the firn/ice transition depth (at 70-80 m) are found to be in agreement with the generally used growth-rate-temperature relation (Stephenson, 1967; Gow, 1969), sometimes referred to as "normal grain growth". In the shallow ice layers below this depth and down to about 300 m, the observed crystal-growth rates are enhanced compared to normal grain growth. Also in this shallow ice, crystal ,c-axis orientation measurements show development of anisotropic fabrics indicative of ice flow at strains well above 1%.

In earlier work, Jacka and Li (1994) described the development in clean ice of steady-state ice-crystal size (inversely proportional to the stress and largely independent of temperature) during the onset of flow-related crystal anisotropy, i.e. dynamic recrystallisation. It is concluded here that as a consequence of the high accumulation rates, relatively high deformation rates are generated in the shallow ice. The deformation rates are sufficiently high that "dynamic recrystallisation" takes over from "normal crystal growth" as the dominant crystal-growth mechanism. This leads to a rapid increase in crystal size from the slow-growing small firn crystals towards the larger size appropriate to the stress.

Introduction

It is important to record and to understand the patterns of crystal-size and -structure change in polar ice sheets because they influence and are influenced by many of the other physical properties, including the ice flow itself. Detailed examinations have therefore been carried out of crystal size and structure from deep and intermediate cores drilled by Australian National Antarctic Research Expeditions (ANARE) on Law Dome, East Antarctica (e.g. Wakahama, 1974; Russell-Head and Budd, 1979; Jacka and Gao, 1989; Li, 1995; Morgan and others, 1997; Li and others, 1998).

In the upper snow layer the original crystalline form and density change soon after new snow is deposited on the surface, as indicated by gradual crystal growth and compaction with increasing depth and time. The rate of densification and crystal growth depends on surface meteorological conditions, especially surface mean temperature and accumulation rate which affects the amount of time for which the firn is influenced by the high summer temperatures. The annual climatic cycle produces detectable annual sequences of stratification, i.e. fluctuations of physical properties of snow such as density, crystal size and surface melting features. These phenomena vary from place to place, reflecting the corresponding changes in surface conditions. The study of the physical properties of the upper snow layer of polar ice sheets helps in the understanding of the formation and the nature of the ice sheet in relation to the surface climatic conditions of the region. Field studies of the physical properties of the snow layer on Law Dome have been carried out by Xie (1985), Han and Young (1989), Li and others (1991) and Li (1995).

It is important to understand the development of crystal size and structure in the near-surface firn and ice, down to a depth of ∼ 300 m. This upper ice is the start material for the subsequent crystallographic and flow developments. A detailed study has been carried out of the near-surface crystal structure from cores collected at 16 sites on Law Dome, and results from that study are in preparation for publication. Here, two particular firn/ice cores are examined, both from relatively high-snow-accumulation sites. In these two cores, apparently high crystal-growth rates were discovered below the firn/ice transition. A mechanism for the higher growth rates is proposed.

Crystal-size and c-axis orientation data are presented for samples collected from the firn and near-surface ice layers of the DE08 and Dome Summit South (DSS) ice cores. The DE08 site (66°43′S, 113°12′E; 1250ma.s.l.) is 16 km east of Law Dome summit. The accumulation rate is −1160 kg m-2a-1 1 and the annual mean temperature is −18.8°G (Etheridge and Wookey, 1989). DSS (66°46’ S, 112°48′E; 1370 ma.s.l.) is 4.7 km south-southwest of the Law Dome summit. The accumulation rate is ∼ 6 4 0 kg m-2 a−1 and the annual mean temperature is −21.8° C. Further details of these sites, of the ice-core properties and of the drilling techniques can be found in Etheridge and Wookey (1989) and Morgan and others (1997). Snow-pit stratigraphy studies at both sites indicate they are in dry-snow zones (Li, 1995).

For ice under insignificant stress in the upper firn layers of polar ice sheets, crystal growth is a process based primarily on crystal-boundary migration due to surface curvature driven by a reduction of free energy in total crystal-boundary area. Crystal-growth rate is dependent on temperature, and mean crystal size is determined by the relation between temperature, growth time and initial mean crystal size (Stephenson, 1967; Gow, 1969; Alley and others, 1986a, b). This process has been well studied in polar firn and in the upper ice layers (typically to several hundred meters depth at low-accumulation-rate sites) where deformation is small.

For deforming ice, laboratory studies on clean, initially isotropic ice (Budd and Jacka, 1989) have shown that crystal anisotropy begins to develop after a minimum strain rate is reached at about 1% strain. A steady-state crystal-orientation fabric pattern can develop after about 10% strain, provided the stress configuration remains unchanged. A steady-state ice-crystal size also develops during the transition from minimum isotropic flow to steady-state anisotropic flow. The steady-state crystal size seems to depend primarily on the magnitude of the stress and is largely independent of temperature (Jacka and Li, 1994), because of the compensating nature of the effects of temperature and strain rate.

Firn and Ice-Crystal Measurement Techniques

Crystal-size measurements were carried out on thin sections cut perpendicular to the long axis of the firn/ice cores. All ice thin sections were prepared by freezing a thick section to a glass slide then cutting it to −0.3 mm using a microtome; these were photographed at the drill site within 2 h of core extraction. Firn thin sections from the DE08 core (i.e. samples above 80 m depth) were prepared in the laboratory at Casey station (-100 km from the drill site). No firn samples are available for the DSS core. To prepare a firn thin section, firstly a thick (-1 mm) section is cut. This is soaked in Dodecane (C12H26) and placed on a glass slide at a temperature below −15°C to allow the Dodecane to freeze. The thickness of the firn section is then reduced to 0.3-0.4 mm using a microtome. The temperature is then increased above −10°C to allow the Dodecane to melt. Photographs of the firn thin sections showing crystal textures were taken between crossed polarisers. A detailed description of this technique and of the properties of Dodecane is given by Alley (1980).

Crystal size in this study is represented by mean crystal area averaged over at least 100 crystals. Because of the large number of pores and gaps between crystals in the firn thin sections, crystals were randomly selected from enlarged photographs and measured individually for each thin section from the DE08 core. The area of each crystal was calculated assuming that the crystal area can be approximated by that of an ellipse whose long and short axes are the diameters of the measured largest inscribed circle and smallest circumscribed circle, respectively, for that crystal. The mean area for a thin section is then the arithmetic mean of the areas for the measured crystals. Mean crystal size for the DSS ice core was obtained by counting the number of crystals in given areas of thin section of ice. A detailed comparison of crystal-size measurement techniques (using three different crystal-selecting methods) is given by Li and others (1990). They found that provided enough crystals (>100 to 200) are selected, the variability of measured mean crystal size appears to be small (of the order of ±10%)

Crystal ,-axis orientation fabrics were measured at the drill site using a universal stage (Langway, 1958). Eight thin sections at depth intervals of ∼ 2 0 m were measured between 55 and 204 m depth from the DE08 core. Crystal-size measurements from firn thin sections from the DE08 core were made at −10 m depth intervals. Crystal size and ,-axis orientation fabrics from the DSS ice core were measured between 78 m and the bottom of the core (-1200 m) with an average depth interval of ∼ 6 m (Li, 1995). In this study, measurements only from the top 300 m of this core are examined.

Results from the Firn/Ice Cores

Crystal-size profiles

Changes in crystal size with increasing depth from near the surface to 300 m for the DE08 core and from 78 to 300 m for the DSS core are illustrated in Figure 1. Crystal size at DE08 is generally smaller than at DSS at the same depth. Note that the 10 m firn temperature at DE08 (-18.8°C) is higher than at DSS (-21.8°C). The crystal-size difference is greatest at ∼ 9 5 m depth, slightly below the firn/ice transition depth (i.e. the depth of bubble close-off which occurs at a density of 830 kg m−3) which at DE08 is 80 m. Below ∼ 9 5 m the increase of crystal size with depth at DE08 is significantly enhanced. The DSS crystal size increases approximately linearly with depth from ∼ 7 8 m Gust below the firn/ice transition at 70 m) to ∼ 300 m. For DSS, it is clear that at some depth above 78 m (i.e. within the firn or just below the firn/ ice transition) there is an enhancement of crystal-growth rate in comparison with the growth rate higher in the firn.

Fig 1. Plot of crystal size as a function of depth at DE08 (triangles)and DSS (filled circles).

Figure 2 shows crystal size as a function of age for the two cores. Ages for the DSS (Morgan and others, 1997) and DE08 cores were obtained by counting seasonal cycles detected by measurement of electric conductivity and oxygen-isotope ratio. For the DSS core, where crystal size was not measured in the firn, crystal size has been estimated (Gow,1969) and is indicated by a dashed line down to the firn/ice transition, below which measurements are included. A sharp increase in crystal-growth rate at ∼55 a BP at DE08 is clear. Based on the estimated crystal size above the firn/ice transition, there is a crystal-growth enhancement at DSS at ∼78 a BP. Since we have measured crystal-size data below this depth, this estimation (i.e. from the calculation based on Gow (1969)) would seem to be the maximum age for the crystal-growth enhancement.

Fig. 2. Plot of crystal size as a function of age at DE08 and DSS. The dashed line in firn for DSS is estimated using Gow (1969).

Crystal-growth rates

In firn and unstrained ice, crystal size can be expressed as a function of time and temperature by the relation

where D2 is the mean crystal area at time t, is the initial mean crystal area and K is the crystal-growth rate which depends on temperature according to the Arrhenius equation,

where K0 is a constant, R is the gas constant, T is the temperature in Kelvin and E is the activation energy of the growth process (Stephenson, 1967; Gow 1969,1975).

Fig. 3. Plot of crystal-growth rate against reciprocal of the absolute temperature. The dashed line is the best fit to the data shown by closed circles (from Paterson, 1994). The values for the firn and ice from DE08 and for the ice from DSS are indicated.

From the regression lines shown in Figure 2, the crystal-growth rate at DE08 is 1.79 x 10−2 mm2 a−1 in firn (0-94 m) and 7.67 X10−2 mm2 a−1 in ice (94-233 m). The crystal-growth rate at DSS is 3.84 x lO−2 mm2 a−1 in ice. A plot of these growth rates as a function of temperature is shown in Figure 3, together with data from several other polar sites (from Paterson, 1994). Crystal-growth rate in the DE08 firn closely agrees with the generally found growth-rate-temperature relation indicated by the dashed line in Figure 3. However, the growth rates in the ice at DE08 and DSS are significantly greater than the general trend.

Borehole measurements show that the temperature at DE08 decreases from −18.8°C at 10 m depth to ∼-20°C at 100 m depth, and below this is almost constant to 230 m depth near the bottom of the hole (Etheridge and Wookey, 1989). At ∼ 5 0 to 350 m depth, temperatures at DSS remain approximately isothermal at ∼-22°C (Van Ommen and others, 1999). Detailed analysis of oxygen isotope ratio in the DE08 and DSS ice cores shows that no large or rapid temperature changes have occurred in the ice above −300 m (Etheridge and others, 1996; Morgan and others, 1997). Thus, enhanced crystal growth in shallow ice layers at these two sites cannot be attributed to temperature effects.

c-axis orientation fabrics

Fabric diagrams (plotted on Schmidt equal-area projections) of c-axis orientation data together with corresponding histograms of the frequency of crystals within each 5° inclination interval are shown in Figure 4 for the DE08 and DSS cores. The data used to compile these fabric diagrams are composites of orientation data measured from several thin sections over 50 m depth intervals. Note therefore that the fabric diagrams for the DSS core contain more data points than those for the DE08 core because thin sections were cut and measured at more closely spaced intervals of the DSS core. The sine curve plotted along with each histogram is the expected distribution for the case of uniformly distributed c axes. Thus for differences from an isotropic crystal pattern, variations from the sine curve should be considered. Figure 4 shows the development with increasing depth in both the DE08 and DSS cores, of some central tendency of the c axes. Each histogram shows that the frequency of, axes with inclination greater than −50° is less than expected for a random distribution, while the frequency of inclinations less than −45° is greater than expected for a random distribution. A report of the DSS crystal fabrics is in preparation for publication elsewhere, showing greater detail of the anisotropy development through the core. Even for the shallow depth interval, 50-100 m in the firn/ice transition region, a non-random pattern is evident. This development of a central tendency of the c axes is indicative of ice flow due to internal deformation.

Comparison with Other Polar Ice Cores

Figure 5 shows crystal size as a function of depth for firn and shallow ice from cores drilled at Dome C (Alley, 1980), Byrd Station (Gow,1970), Little America V (Crary, 1961; Gow, 1970), Maudheim (Gow,1969; Paterson, 1994) and Camp Century (Gow,1971; Paterson, 1994). A plot of crystal size as a function of age is not shown, because an age scale is not available for all cores. In the firn, crystal-growth rate increases monotonically with temperature from the coldest location included, Dome C (-54.3°C), to the warmest, DE08 (-18.8°C). In addition, the firn crystal-size profiles for DE08 and for all the cores represented in Figure 5 are approximately as expected (Fig. 3) for the temperature-dependent growth rate (Gow, 1969).

Fig. 4. Crystal c-axis orientation fabrics in shallow ice for the DE08 and DSS cores. Note each fabric diagram is a composite of data over 50 m depth intervals.

The crystal-size relations with age for the Byrd Station and Camp Century cores indicate no sharp change of crystal-growth rate across the fim/ice transition. For the Maudheim and (although there are no firn data available) Little America V cores, however, there does appear to be a sharp enhancement of crystal-growth rate, similar in character to that discovered in the DE08 and DSS cores.

Above, it was noted for the DE08 and DSS cores that a crystal-orientation fabric indicative of ice flow through internal deformation had begun to develop. No such fabric development is evident in the ice near the firn/ice transition in the Byrd Station core, leading Gow (1968) to write that "Despite the progressive increase in the size of crystals with depth at Byrd Station, this growth was not accompanied by any increase in the degree of preferred orientation of crystallographic c-axes." The crystal fabrics immediately below the firn/ice transition from Camp Century indicate a random pattern, but a small-circle .-axes distribution pattern has developed at 190 m depth (Herron and Langway, 1982), 65 m below the transition. At Dome C also, crystal fabrics immediately below the firn/ice transition exhibit a random orientation pattern (Duval and Lorius, 1980). There is thus little evidence from the crystal-orientation fabrics from these three cores of significant ice flow at these shallow depths.

At Little America V, Gow (1970) noted "the appearance of strain shadows in crystals at around 65 m depth, and the formation of oriented fabrics by 100 m". Gow also speculated that "other factors, particularly deformation, have been responsible for the more rapid rate of growth of crystals at Little America V". The accumulation rate at Little America V is not as high as at DE08 or DSS, but high horizontal strain rates have been measured at this site (Crary, 1961). Little America V is near the front of the Ross Ice Shelf. The larger-crystal ice is likely therefore to have originated further inland, and to have been exposed to relatively high longitudinal strains as it moved towards the ice front. For the Maudheim Ice Shelf, although little difference from random was noted in the crystal-orientation fabrics, Schytt (1958) came to a similar conclusion, i.e. that the change in crystal size at ∼ 7 5 m depth derived from the inland ice sheet.

Accumulation rate (indicated in Table 1) has a clear influence on the crystal-size-depth profile. Crystal sizes in the Byrd Station and Camp Century cores are larger (compared to the DSS and DE08 cores) because crystals have undergone a longer growth time (at approximately the same temperature) due to the lower accumulation rate. The smaller crystals at DE08 (i.e. at the same depths) have had the shortest time to grow because the accumulation rate at DE08 is highest.

Fig. 5. Plot of crystal size as a function of depth for firn and shallow ice from cores drilled at Dome C, East Antarctica (Alley, 1980); Byrd Station, West Antarctica (Gow, 1971); Little America V, Ross Ice Shelf, Antarctica (Gow, 1970); Maudheim, Maudheim Ice Shelf, East Antarctica (Mellor, 1964, from data of Schytt, 1958); and Camp Century, Greenland (Gow, 1971; Herron and Langway, 1982).

The cause of the change to more rapid crystal-growth rate below the firn/ice transition at DE08 and DSS will now be examined. Particularly high accumulation rate and some development of crystal-orientation fabrics seem to be properties distinguishing these cores from the others studied at the inland sites.

A Mechanism for Enhanced Crystal-Growth Rate

From deformation experiments on initially isotropic laboratory ice samples it has been found that mean crystal size changes and an anisotropic .-axis orientation pattern develops while strain rate increases from a minimum value at about 1% strain to a steady-state value beyond about 10% strain (Budd and Jacka, 1989). In an unchanging stress and temperature field, the change in average crystal size and c-axis orientation ceases once a constant tertiary flow rate has been attained and an equilibrium crystal size is established pertaining to the applied stress pattern. Jacka (1984) studied ice with a range of initial crystal sizes. He found that for samples deformed under the same temperature and stress conditions the crystal sizes attained approximately the same value at the termination of the experiment in the tertiary creep stage independent of whether the initial mean crystal size was larger or smaller than the final size. Jacka and Li (1994) have shown that at steady-state tertiary strain rate, a steady-state crystal size is established strongly dependent upon stress magnitude. Consideration of these laboratory results along with the development of the non-random crystal-fabric patterns shown in Figure 4 suggests that a strain in excess of 1% may be reached at a very shallow depth (50-100 m) at DE08 and DSS. It is suggested here that although steady-state ice flow may not be attained till much deeper in the ice sheet, deformation processes begin to control crystal growth, even at this shallow depth.

Estimation of localised octahedral strain rate, estimated as times the ratio of ice accumulation to thickness (Budd, 1969), gives 8.49 x 10∼4 a−1 at DE08 and 3.90 x 10∼4 a−1 at DSS. These values are 1-2 orders of magnitude higher than estimated for most locations on inland polar ice sheets (e.g. Duval and Lliboutry, 1985). For these higher-accumulation (leading to higher strain rate) sites, a significant effect of deformation on crystal size in the shallow ice layers is evidenced by Figures 2 and 5. Crystal-growth rates (slope of regression lines) at depths less than about 60 m (i.e. above the firn/ice transition) at Byrd Station, Camp Century, DSS and DE08 are similar since the temperatures at these locations are similar. Below the firn/ice transition, crystal size at these four sites differs markedly and it is suggested that these differences are due to the differences in strain rates associated with different accumulation rates at the sites.

Fig. 6. Plot of crystal-growth rate above the firn/ice transition as a function of temperature (crosses and solid line) for several sites listed in Table 1 and Paterson (1994), along with a plot of crystal-growth rate below the firn/ice transition as a function of strain rate (triangles and dashed line) for the sites listed in Table 1. The (inverse) temperature (linear) and strain rate (log) axes were aligned based upon the values at Byrd and DE08 For the other two locations (DSS and Camp Century) at which crystal-growth rates are plotted as a function of both temperature and strain rate, the fitted alignment" is remarkably good.

In Figure 6 we have plotted crystal-growth rate above the firn/ice transition as a function of temperature for the sites listed in Table 1 and from Paterson (1994). This plot is very similar to Figure 3 (rotated); it is an expanded version for the locations at the warmer temperatures, and includes DE08 and DSS. We have also plotted the crystal-growth rate below the firn/ice transition as a function of strain rate for the stations of Table 1. The (inverse) temperature (linear) and strain-rate (log) axes were aligned based upon the values at Byrd and DE08. For the other two locations (DSS and Camp Century) at which crystal-growth rates are plotted as a function of both temperature and strain rate, the "fitted alignment" is remarkably good (not surprising given the nature of the temperature-strain-rate relation). Thus, for Byrd and for Camp Century where the crystal-growth rate is the same above and below the firn/ice transition, the two points are co-located. We propose that normal crystal-growth rate, which occurs in the upper layers of the ice sheets, is temperature-dependent as described by Stephenson (1967) and Gow (1969). In addition, however, crystal-growth rate is enhanced by strain rate at high-accumulation sites. For higher-accumulation sites, e.g. DE08 where (as indicated by the fabric development) a higher strain is attained, the trend toward a steady-state crystal size is most rapid. At DSS, where accumulation (and thus strain rate) is less, the trend toward a steady-state crystal size (i.e. the crystal-growth rate) is less rapid.

Table 1. Physical properties of ice sheets at selected polar sites

Conclusion

Crystal-size data in the firn (at DE08) and shallow ice to below the firn/ice transition depth (at DE08 and DSS) have been presented for these two cores, drilled near the summit of Law Dome, East Antarctica. It was found for the DE08 core in the firn, that crystal-growth rates were temperature-dependent as expected from the established relationship of Gow (1969). Below the firn/ice transition, crystal-growth rate in these two cores increased markedly. Examination of data from other core sites failed to find a comparable dataset for which a similar phenomenon (large increase of crystal-growth rate below the firn/ice transition) could not be otherwise explained.

Evidence has been presented to suggest that crystal size in the polar ice sheets is controlled by two main processes.

  1. (i) Near the surface of the ice sheet, where deformation (apart from compaction) is close to zero, crystal-growth rate is temperature-controlled, as determined by Stephenson (1967) and Gow (1969).

  2. (ii) For regions with high strain rates, once the ice has undergone significant strain (this can be judged by examination of crystal-orientation fabric pattern), crystal-size change is controlled by deformation processes. In this case, crystal-growth rate is linearly dependent upon strain rate. The target crystal size (which in a non-changing stress field is the steady-state crystal size) is inversely dependent upon the cube of the stress magnitude (Jacka and Li, 1994). At most locations in polar ice sheets, deformation is not sufficient to control crystal growth until about one-third of the depth in the ice sheet, where the flow is controlled by internal shear deformation due to the ice-sheet thickness and surface slope. At sites of very high snow accumulation, however (e.g. DE08 and DSS), the stress due to the overburden pressure is sufficient to control the crystal growth.

Acknowledgement

We thank W. F Budd for valuable discussions.

References

Alley, R. B. 1980. Densification and recrystallization of firn at Dome C, East Antarctica. Ohio State Unto. Inst. Polar Stud. Rep 11.
Alley, R. B., Perepezko, J. H. and Bentley, C. R. 1986a. Grain growth in polar ice: I. Theory. J.Glaciol, 32(112), 415-424.
Alley, R. B., Perepezko, J. H. and Bentley, C. R.. 1986b. Grain growth in polar ice: II. Application. J. Glacial., 32(112), 425-433.
Budd, W. 1969. The dynamics of ice masses. ANARE Sci. Rep, Ser. A (IV). Glaciology 108
Budd, W. F. and Jacka, T.H.. 1989. A review of ice rheology for ice sheet modelling. Cold Reg. Sci. Technol, 16(2), 107-144
Crary, A. P. 1961. Glaciological studies at Little America Station, Antarctica, 1957 and 1958. IGY Glaciol. Rep Ser. 5.
Duval, P. and Lliboutry, L.. 1985. Superplasticity owing to grain growth in polar ices. J.Glaciol., 31(107), 60-62.
Duval, P. and Lorius, C.. 1980. Crystal size and climatic record down to the last ice age from Antarctic ice. Earth Planet. Sci. Lett., 48(1), 59-64.
Etheridge, D. M. and Wookey, C. W.. 1989. Ice core drilling at a high accumulation area of Law Dome, Antarctica. In Rado, C. and Beaudoing, D., eds. Ice core dulling. Proceedings of the Third International Workshop on Ice Drilling Technology, Grenoble-France, 10-14 October 1988. Grenoble, Centre National de la Recherche Scientifique. Laboratoire de Glaciologie et Géophysique de l′Environnement, 86-96.
Etheridge, D. M., Steele, L. P., Langenfelds, R. L., Francey, R.J., Barnola, J.-M. and Morgan, V. I.. 1996. Natural and anthropogenic changes in atmospheric C02 over the last 1000 years from air in Antarctic ice and firn. J.Geophys.Res., 101 (D2), 4115-4128.
Gow, A.J. 1968. Deep core studies of the accumulation and densification of snow at Byrd Station and Little AmericaV, Antarctica. CRRELRes. Rep 197
Gow, A.J. 1969. On the rates of growth of grains and crystals in South Polar firn. J.Glaciol., 8(53), 241-252.
Gow, A.J. 1970. Deep core studies of the crystal structure and fabrics of Antarctic glacier ice. CRREL Res. Rep 282.
Gow, A.J. 1971. Depth-time-temperature relationships of ice crystal growth in polar glaciers. CRREL Res. Rep 300.
Gow, A. J. 1975. Time-temperature dependence of sintering in perennial isothermal snowpacks. International Association of Hydrological Sciences Publication 114 (Symposium at Grindelwald 1 9 7 4 - Snow Mechanics), 25-41.
Han, Jiankang and Young, N.W.. 1989. Structural characteristics of snow firn at the surface part on Law Dome ice cap, Antarctica. In Chinese Committee on Antarctic Research. Proceedings of the International Symposium on Antarctic Research, Hangzhou, China. Beijing, China Ocean Press, 53-63.
Herron, S. L. and Langway, C. C. Jr. 1982. A comparison of ice fabrics and textures at Camp Century, Greenland and Byrd Station, Antarctica. Ann. Glaciol, 3, 118-124.
Jacka, T. H. 1984. Laboratory studies on relationships between ice crystal size and flow rate. Cold Reg. Sci. Technol., 10(1), 31-42.
Jacka, T. H. and Gao, Xiangqun. 1989. Ice crystal orientation fabrics and related glaciological parameters from neighbouring Antarctic core sites. In Kun, Guo, ed. Proceedings of the International Symposium on Antarctic Research. Beijing, China Ocean Press. Chinese Committee on Antarctic Research, 41-52.
Jacka, T. H. and Li, Jun. 1994. The steady-state crystal size of deforming ice. Ann. Glaciol., 20, 13-18.
Langway, C.C. Jr. 1958. Ice fabrics and the universal stage. SIPRE Tech. Rep. 62.
Li, Jun. 1995. Interrelation between flow properties and crystal structure of snow and ice. (Ph.D. thesis, University of Melbourne.)
Li, Jun, Young, N. W. and Malcolm, P.F.. 1990. [Grain growth in firn on Law Dome ice cap, East Antarctica.] Antarct. Res., 2(4), 11-20. [In Chinese with English summary]
Li, Jun, Young, N.W. and Wookey, C.W.. 1991. Stratigraphy, density and crystal structure of firn/ice at DE08 - a very high accumulation site on Law Dome. Antarct. Res., 2(2), 1-14.
Li, Jun, Jacka, T. H. and Morgan, V.. 1998. Crystal-size and microparticle record in the ice core from Dome Summit South, Law Dome, East Antarctica. Ann. Glaciol., 27, 343-348.
Mellor, M. 1964. Snow and ice on the Earth’s surface. CRREL Monogr. II-C1.
Morgan, V.I., Wookey, C.W., Li, Jun, van Ommen, T. D., Skinner, W. and Fitzpatrick, M. E. 1997. Site information and initial results from deep drilling on Law Dome, Antarctica. J.Glaciol., 43(143), 3-10.
Paterson, W. S. B. 1994. The physics of glaciers. Third edition. Oxford, etc., Elsevier.
Russell-Head, D. S. and Budd, W.F.. 1979. Ice-sheet flow properties derived from bore-hole shear measurements combined with ice-core studies. J. Glaciol., 24(90), 117-130.
Schytt, V 1960. Glaciology 11(D). Snow and ice temperature in Dronning Maud Land. Norwegian-British-Swedish Antarctic Expedition, 1949-52. Sci. Results IV, 153-179.
Stephenson, P.J. 1967. Some considerations of snow metamorphism in the Antarctic ice sheet in the light of ice crystal studies. In Oura, H., ed. Physics of snow and ice. Vol. l,Part2. Sapporo, Hokkaido University. Institute of Low Temperature Science, 725-740.
Van Ommen, T.D., Morgan, V. I., Jacka, T. H., Woon, S. and Elc‘heikh, A.. 1999. Near-surface temperatures in the Dome Summit South (Law Dome, East Antarctica) borehole. Ann. Glaciol., 29 (see paper in this volume).
Wakahama, G. 1974. [On the structure and texture of deep ice cores from Amery Ice Shelf, Wilkes Dome and Cape Folger, Antarctica.] In Kuroiwa, D., ed. [Physical and chemical studies on ice from glaciers and ice sheets.] Sapporo, Hokkaido University, 99-108. [In Japanese.]
Xie, Zichu. 1985. Ice formation and ice structure on Law Dome, Antarctica. Ann.Glaciol., 6,150-153.