Temporal evolution of surface and grain boundary area in artificial ice beads and implications for snow chemistry

Surface snow is a chemically active medium (Domine and Shepson, 2002). It exerts a major effect on overall snow chemistry and can alter the composition of the overlying air mass. This in turn can affect air quality and climate (Grannas and others, 2007). Chemically reactive trace gases and impurities are typically located on the surface of ice and in grain boundaries (GBs) (Domine and others, 2008). Field and laboratory measurements have shown that the morphology and surface area (SA) of ice crystals strongly influence trace gas exchange with the atmosphere during snow metamorphism (Domine and others, 2008). The exact role of GBs in snow and ice chemistry, however, is not well understood (Domine and others, 2008;Barret and others, 2011). Earlier work concerning the adsorption of acetone onto packed single-crystalline ice and packed ice beads did not specifically address the role of GBs in surface chemistry (Bartels-Rausch and others, 2004).

We define a GB as an interface between two ice crystals aligned in different crystal orientations. The observation that acidic trace gases accumulate along GBs in natural snow has led to the suggestion that GBs provide an extensive surface area for reactions with trace gases and impurities (Mulvaney and others, 1988;Huthwelker and others, 2006). The total grain boundary area (GBA) is therefore an important chemical parameter of snow.

Artificial ice beads are often used as a substitute for natural snow in laboratory experiments. This correspondence reports the structural evolution of ice beads stored at two constant temperatures (-5°C and -20°C) over a 7 month period. We measured volume density and specific surface area (SSA) with X-ray tomography (mCT). The GBA was characterized using polarized light microscopy and stereology. The artificial snow consisted of ice beads measuring 0.5-0.6mm in diameter, similar to those used in laboratory experiments concerning the partitioning of trace gases between ice and air (Bartels and others, 2002;Bartels-Rausch and others, 2004;Kerbrat and others, 2010). Accurate determinations of the SSA and density of samples are critical in comparing the structure of the artificial material to that of natural snow. Hitherto, the role of GBA in uptake of trace gases and other reactions has been largely a matter of speculation (Kerbrat and others, 2010).

In atmospheric science, the term GB refers exclusively to ice-ice interfaces. The different types of interfaces described here are shown in Figure 1. The GBA is geometrically measured as the diameter of the neck between individual ice beads (Theile and Schneebeli, 2011). The visible neck is often one of several types of GB present in a given sample. We differentiated between GBs evident as visible necks and GBs inside the ice beads that are not geometrically evident. This second type of GB is referred to as an internal GB. The total area covered by internal GBs defines an internal grain boundary area (IGBA). The ice beads used here were mainly polycrystalline. In natural snow, polycrystalline morphology is characteristic of wet or wind-transported snow. Snow composed of small rounded grains is typically monocrystalline.

Fig. 1. Polarized light images of ice beads. The blue ellipse indicates an example of internal grain boundary area (IGBA), the red ellipse indicates grain boundary area (GBA; between two ice beads) and the green ellipse indicates surface area (SA; interface between ice and air). Both monocrystalline and polycrystalline beads are present.

The ice beads were prepared from Milli-Q-water droplets frozen in liquid nitrogen. Following freezing, ice beads were immediately sieved to collect the 0.5-0.6mm diameter fraction. The ice beads were loaded into mCT-specific sample cylinders 20mm in diameter and 5cm high, and into 3 cm x 1 cm containers used for thin-section mounting and microscopic analysis. Samples were then separated into two fractions stored at temperatures of-5°C and -20°C. Both fractions were stored in isothermal boxes that maintained constant temperatures in and around the samples to adjust for small temperature variations within the storage freezer. Sample storage followed the same protocol used by Lowe and others (2011). Each month, samples from the -5°C and -20°C fractions were retrieved for mCT scanning and microscopic analysis.

Samples remained in the initial sample containers throughout the experiment in order to prevent disturbance. For mCT analysis, the sample container was placed in a secondary sample holder (20 mm diameter) and then loaded into the mCT. The three-dimensional image resolution was 10 mm over a 4.16 x 4.16 x 4.16 mm³ sample volume. The SSA and the volume density of the samples were determined according to methods used by Kerbrat and others (2008).

Three thin sections were evaluated per sample. Thin sections were prepared using uniform vertical section sampling and imaged under polarized light. Approximately 20 images were collected per thin section and analysed stereologically. This technique captured structures containing 180-250 ice beads per sample. The specific area per volume of the structure of interest is given by

where I is the number of intersections between the test lines and the structure of interest - SA, GBA or IGBA − l/p is the length of the test line per point, and P _ice is the number of touch points within the ice structure (methods detailed in Tschanz and others, 2011;Riche and Schneebeli, in press). To obtain the specific area per ice volume (cm² g^-1), specific area S _ice (m^-1) is divided by p _ice, where p _ice is the density of ice (gcm^-3).

Temporal Evolution Of Ice Structure

We found that both polycrystalline and monocrystalline morphologies were present in the ice-bead samples throughout the 27 week observation period (Fig. 1). The percentage of polycrystalline ice beads (polycrystalline ice beads/total number of ice beads) remained constant between 60% and 70% for both the -5°C and -20°C sample sets.

SSA decreased by 10-20% at the beginning of the observation period (from 12 mm^-1 to 8-9 mm^-1) and exhibited similar patterns for both storage temperatures (Fig. 2). We estimate SSA measurement error to be ~5%. Snow composed of small rounded grains has been shown to have similar SSA values. Kaempfer and Schneebeli (2007) and Lowe and others (2011) reported SSA values of 9-12 mm^-1 for snow having a volume density of 50%. These earlier studies also found that the SSA of rounded-grain snow decreased over time (Kaempfer and Schneebeli, 2007;Lowe and others, 2011).

Fig. 2. Evolution of SSA for ice beads stored at _5°C and _20°C.

We measured specific grain boundary areas (SGBAs) ranging from 1 to 2 mm^-1. This parameter showed no detectable change during the experiment. The specific internal grain boundary area (SIGBA) was initially ~8.5 mm^-1 and decreased by almost 40% to ~5 mm^-1 after 27 weeks (Fig. 3). We estimated the error in SGBA measurements to be 5-10%. The total SGBA (SGBA + SIGBA) ranged from 7 to 9 mm^-1. We compared GBA measurements from the laboratory ice beads with those of natural snow. Snow composed of small rounded grains had a total specific GBA of 2-3 mm^-1, which is one-third of the corresponding values measured for the ice beads. The ice beads had approximately the same volumetric density as the natural rounded-grain snow.

Fig. 3. Evolution of specific GBA for ice beads stored at –58C and –208C. SGBA: specific grain boundary area; SIGBA: specific internal grain boundary area.

We found that GBs at neck sites remained mostly unchanged throughout the experiment. The IGBA, however, fell by ~-40% during the first 15 weeks, with no measurable change afterwards. The decrease in IGBA for the polycrystalline ice beads is probably due to GB migration. The surface energy of the smaller internal grains is much larger than that of the large grains, and larger grains may encapsulate smaller grains (Berry and others, 1991;Gottstein and others, 1998; Schonfelder and others, 2005).

Hypothetical trace gas diffusion into GBs (Huthwelker and others, 2006) would depend on the extent of GBs and their evolution with time. Analysis of these two factors facilitates the extrapolation of laboratory results to conditions in the natural environment. The polycrystalline structure of the ice beads is likely to produce a greater number of GBs relative to the monocrystalline structure of natural snow (Takahashi and Fujino, 1976). Ice beads apparently have approximately the same GBA as natural snow. Polycrystalline ice, however, is likely to differ from natural snow in terms of its IGBA. The GBA and IGBA exert similar effects on the chemical properties of ice and snow, but IGBA is not geometrically visible. The contrasting IGBA of ice beads and natural rounded-grain snow provides important constraints for experiments concerning snow types with similar SSA but different GBA.

Our experiments also indicate that IGBA evolves primarily during an initial 10-15 week period, with little change observed in the ensuing weeks and months. Different batches of ice beads may vary in their adherence to these findings, and thus require careful monitoring of initial experimental conditions. Large batches of ice beads, however, are expected to show consistent internal structure after 10-15 weeks.