Introduction

An attempt to study the surface structure of ice was made using a mass-transfer measurement. The method most extensively adopted to measure surface mass transfer is the observation of the relaxation of surface grooves. According to Reference MullinsMullins (1959), a surface which initially has a sinusoidal profile in the z−x plane of z = z ₀ sin ωx will decay with time t as

where ω = 27π/λ is the frequency of the grooves and B, C, A′, A and F are constants depending on the mass-transfer mechanisms. The values of these constants at a particular wavelength and temperature indicate the relative contribution of each mechanism to the total relaxation.

If β, the mean free path of the molecules from the solid in the non-reactive atmosphere, is much greater than the wavelength, the evaporation–condensation mechanism contributes to the surface relaxation as Aω ² where

here p ₀ is the equilibrium vapor pressure over a flat surface, γ _s is the surface free energy of the solid, Ω is the molecular volume, M is the mass of the molecule and kT is Boltzmann’s constant times the absolute temperature.

For the case of high atmospheric pressure and β ⪡ λ, the mechanism of “evaporation–condensation” becomes “evaporation-diffusion through the atmosphere–condensation” which contributes A′ω ³ where:

in which ρ ₀ is the equilibrium vapor density over a flat surface, and D _G is the diffusion coefficient of vapor molecules in the atmosphere.

The self-diffusion in the bulk crystal also depends on an up ω ³ term as Cω ³ where

in which D _v is the volume self-diffusion coefficient.

The surface diffusion term is expressed as Bω ⁴ where

Here, v is the number of molecules per unit area, and D _s the surface self-diffusion coefficient. Viscous flow contributes as Fω, where

Here, η is the coefficient of viscosity.

A study of the power of ω dependence of

would reveal the dominant mechanism of mass transfer at a fixed temperature. A series of measurements were made at (−10±0.5)° C, in which the groove frequency was varied and the decay constant K was calculated.

Experiment

The relaxation of grooves was observed by a Zeiss interference microscope enclosed in a constant-temperature box. The original thallium lamp was removed, and instead, a heliumneon CW gas laser (6328 Å, 0.3 mW) was used as a light source outside the constant temperature box. This replacement was necessary for the following reasons: (1) To avoid temperature fluctuations in the constant-temperature box due to the heat generated by the thallium lamp. (2) To increase the light intensity and decrease the exposure time. The exposure time was reduced from 15 min to 30 s without a condenser lens and to 2 s with a condenser lens. (3) To increase the coherence of the illumination so that interference fringes will appear irrespective of the reference mirror adjustment. A mechanically actuated oscillating ground glass was used as a diffuser to eliminate the granular image which commonly appears in photography using a laser light source. The gap between the inset sample stage of the interference microscope and the objective lens was sealed by a thin flexible rubber film to enable the required adjustments to be made while the surface of the ice sample was kept in an ice-saturated atmosphere. Because the alignment of the laser was critical, it was mounted on an adjustable platform. All other components were attached to a plywood base with heat glue to insure stability.

Mass transfer measurements were made on the (0001) plane of naturally grown Mendenhall Glacier ice single crystals in the <1010> direction. The impurity concentration of a good quality glacier ice single crystal is very small (Reference ItagakiItagaki, 1967[b]) and the dislocation density is very low (10⁴ to 10⁵/cm²) (Reference Muguruma and HigashiMuguruma and Higashi, 1963; Reference Fukuda and HigashiFukuda and Higashi, 1969). A large single crystal was cut down to a rectangular slab (5 cm × 3 cm × 1 cm) in the desired orientation and freeze-mounted on a glass slide (5 cm × 7.5 cm). The top surface was smoothed without strain by the “freeze-tap method” (Reference Tobin and ItagakiTobin and Itagaki, 1970). A series of periodic grooves (parallel to <1020>, spacing 19 to 80 μm) were engraved on the ice surface by a “hotwire grooving engine” (Reference Tobin and ItagakiTobin and Itagaki, 1971). The strain-free condition was satisfied during this procedure as verified by a low thermal etch-pit density. The strain-free condition must be fulfilled, otherwise a mass transfer mechanism activated by straining may overlap the other mechanisms and alter the results. The higher harmonics of the grooves rapidly decayed and smooth sinusoidal profiles appeared within a few hours.

The modification of surface profiles was recorded by interference photomicrographs as a function of time. The time period of observation for flattening ranged from 2 h for a 19 μm groove spacing to 24 h for 80 μm groove spacings. The depth of the grooves was measured by interpolating the interference fringes.

Results

Figure 1 is typical of the interference photomicrographs depicting the decay of grooves over an 18 h period. A few thermal etch pits appear in the field but do not interfere with amplitude measurements made in the center of the observation field.

Fig. 1.Series of interferograms indicating the decay of grooves. Wavelength 76.2 μm. Temperature −10±0.5° C. Fringe separation = 0.316 μm. Groove direction <0001> on <1010> plane.

The slope of the line obtained by the least-square fit of the plot of logarithm of depth versus time, as shown in Figure 2, is the decay constant, K.

Fig. 2.Groove depth versus time. Wavelength 76.2 μm. Temperature −10±0.5° C. Slope equals the decay constant for this wavelength.

The plot of log K versus log A is linear as shown in Figure 3. The slope of the least-square fit was −1.28.

Fig. 3.Wavelength λ versus decay constant K at −10±0.5° C.

If any single mechanism dominates the process of groove decay, Equation (7) can be approximated as

where n should be 1, 2, 3 or 4 and k correspondingly F, A, A′ or C, or B. Consequently, a plot of log K versus log λ would have a slope of −1, −2, −3 or −4. Since this plot of experimental data (Fig. 3) has a non-integral slope, the decay proceeds by at least a combination of two mechanisms or a new mechanism not considered in Mullins’ theory.

Discussion

For the wavelengths used, the contributions from bulk diffusion and surface diffusion were calculated from Equations (4) and (5). These contributions are listed in columns 3 and 5 of Table I. As shown in columns 4 and 6 of Table I, the percentage contribution to the K value obtained in this experiment from these terms is very small. The surface self-diffusion coefficient in Equation (5) was obtained by a radioactive tracer method using microtomed ice surface (Itagaki, unpublished). This number may be larger than that for ice surfaces in this experiment because microtoming introduces strains into the ice surface. Even if the previously determined value is an order of magnitude in error, the percentage contribution to surface modification in the present study will still be negligible.

Table 1Contribution of Individual Mechanisms to The Decay Constant K as a Function of Wavelength

The direct evaporation–condensation mechanism cannot be responsible for groove decay since the mean free path of the water molecules under atmospheric pressure is three orders of magnitude smaller than the wavelength range used. The term containing A is therefore omitted.

Only two mechanisms, “evaporation–diffusion through the atmosphere–condensation” and “viscous flow”, remain responsible for the groove decay and will contribute as an ω ³ and ω dependence respectively.

The values A′ and F were fitted to the measured decay constants for each value of ω as the coefficient of ω ³ and ω terms by a least-squares method.

The results are A′ = 1.9 × 10⁻²¹ m³ s⁻¹ and F = 4.29 × 10⁻¹⁰ m s⁻¹. As can be seen in the columns 8 and 10 of Table 1 the major mechanisms of groove decay are predominantly “viscous-flow type” with a smaller contribution from the “evaporation–diffusion through the atmosphere–condensation” mechanisms which contributed a maximum of c. 30% for the shortest wavelength measured. This result is based on the assumptions that (1) only two mechanisms are operative and (2) the contributions of the mechanisms to groove decay are proportional to ω ³ and ω respectively and are additive.

Both F and A′ can be theoretically calculated, from Equations (6) and (3) respectively. However, the F values calculated from Equation (6) using known values of viscosity are 21 m s⁻¹ for supercooled water and 6.8 × 10⁻¹⁵ m s⁻¹ for river ice. Neither of these is correct. The former is unrealistic, because the viscosity assumed is that of a supercooled water and notice. The latter viscosity is obtained from the macroscopic deformation of river ice and may not be applicable to the present case since the actual viscous deformation of bulk single crystal must be through dislocation motion. The lack of etch pits in the area measured, however, does not support dislocation motion as the mechanism for the surface flattening seen here.

Any of the anomalous surface features postulated by many researchers (for example, Reference FaradayFaraday, 1860; Reference WeylWeyl, 1951; Reference Nakaya and MatsumotoNakaya and Matsumoto, 1953; Fletcher, 1962, 1968; Reference JellinekJellinek, 1967) including a liquid layer, two-dimensional liquid layer, a high point-defect density layer (Reference Itagaki and ŌuraItagaki, 1967[a],Reference Itagaki[c]) etc., could account for the groove decay observed in this experiment.

If the viscous flow is not in the bulk crystal viscosity as considered in Mullins’ theory but limited to the surface layer, the Mullins equation for the viscous-flow contribution may have to be modified to a certain extent. A study on this problem is in progress.

The theoretical value of A′ = ρ ₀ D _GγsΩ²/kT is 4.37 × 10⁻²⁰ molecules m³/s at −10° C. This value is more than twenty times larger than the measured value. Reference Hobbs and MasonHobbs and Mason (1964) suggested that a correction must be made for materials with high latent heat of sublimation and low thermal conductivity such as ice. This correction replaces the ρ ₀ΩD _G term in A′ with where ρ is the density of ice, m is the molecular mass of water, and K _t is the thermal conductivity of air. The correction reduces the calculated A′ to 3.35 × 10⁻²⁰, but it is still 17 times larger than the measured value.

There are some possible sources of this discrepancy both in the theoretical calculation and experimental results. The surface free energy has been measured by an indirect method giving values ranging from 0.085 to 0.122 J m⁻². The most direct measurement made by Reference Ketcham and HobbsKetcham and Hobbs (1969) resulted in the value of 0.109 J m⁻² which was used for the present calculation. Though the variation of the value could not be the sole source of the discrepancy it would contribute to a certain degree.

Another possible source of error is the vapor density ρ ₀ used to calculate the evaporation–condensation term. This term is based on the assumption that the process can be described by macroscopic thermodynamics. This notion, however, may not be correct. Evaporation–condensation on a crystal surface must be treated as growth and sublimation of a crystal, which would follow spiral growth, (Reference FrankFrank, 1949; Reference BurtonBurton and others, 1951), and evaporation (Reference Cabrera and LevineCabrera and Levine, 1956), due to dislocations. The recent measurement by Reference Lester and SomorjaiLester and Somorjai (1968) indicated that the evaporation rate of a NaCl crystal with a dislocation density 10¹⁰/m² is 2.5 times slower than that of a crystal with a dislocation density of 10¹¹/m².

The present crystal has a much lower dislocation density (10⁸−10⁹/m²). In addition the measurements were made in a selected area with no dislocation etch pits as shown in Figure 1. The evaporation–condensation process under such low dislocation density would be much slower than predicted by a theory based on simple thermodynamic considerations. However, the extent of this effect on the present study is not known. Some other effect such as the impurity cover on the ice or undersaturation of water vapor in the atmosphere may also reduce the rate of evaporation–condensation though the contribution is not known yet.

The present result indicates that mass transfer on an ice surface may take place by mechanisms not accounted for in the Mullins’ theory. Possible models for this behavior could include enhanced surface layer diffusion and viscous flow of a two-dimensional liquid.