Methods of snow-structure analysis

Stratigraphic investigations were undertaken at the primary snow-study site on Red Mountain Pass (3400 m) as well as on surrounding test slopes or potential avalanche-release zones with elevations and orientations comparable to active avalanche-release zones. Such studies were acquired as a series at fixed sites to determine changes in snow structure with time. A third type of snow-pit study was undertaken at actual avalanche fracture lines.

In addition to conventional methods, stratigraphic data were obtained through the application of a profiling snow gauge which provides in situ density values at 1.0 cm intervals by means of gamma-ray attenuation. This instrument allows continuous non-destructive density measurements within the same stratigraphic sample, providing a progressive record from new-snow deposition through the respective stages of metamorphism.

Three winter seasons of field investigations led to a comprehensive definition of the local snow climate (Reference LaChapelleLaChapelle, 1974, p. 140). Slopes with a northerly aspect and steeper than 30° receive little solar radiation during winter and experience persistent strong radiation cooling. Total snow depths are not great (1.0–3.0 m), nor are storm increments, which rarely exceed 30 cm. Optimum conditions thus exist for extreme temperature differences between the ground, consistently at or near 0.0°C, and the low temperatures at the snow surface above. Vapor transfer occurring along the temperature gradient results in the formation of large, loosely packed crystals or depth hoar. Temperature-gradient metamorphism dominates snow structure genesis on southerly slopes as well, with vapor-pressure gradients often exceeding those measured on north-facing slopes due to higher mean snow-cover temperatures, combined with comparable temperature gradients. Little stabilization, often associated with substantial solar energy, occurs even on south-facing slopes. While the mean internal temperature gradients of north- and south-facing slopes do not differ to a significant extent, such values being a function of long-term mean daily air temperatures, it is within the near-surface layers that the radical contrast exists. At the altitude (3400–3900 m) and latitude (37°N.) of the study area, southerly slopes experience extreme diurnal fluctuations in the radiation-determined temperature of the near-surface layers. This condition continues throughout the winter and a highly complex stratigraphy develops, characterized by large variations in structure and strength. Layers of relatively homogeneous, stronger snow, comprising the individual precipitation increments, are separated by thin layers of temperature-gradient snow and freeze–thaw crusts that have developed during clear-weather periods between storms. Poor layer bonding is prevalent in these situations and the snow cover can be described as conditionally unstable. By this it is meant that at any given time while the snow cover IS at sub-freezing temperatures, it is only marginally unstable with respect to spontaneous slab release due to internal causes, but remains throughout each winter highly susceptible to load-induced avalanche release.

Relationship between avalanche release and snow structure

Initial investigation indicated that over 90% of the mid-winter avalanches within the study area occurred during storm periods. Delayed-action events were rare. Good statistical relationships between avalanche events and meteorological conditions, primarily precipitation factors, could be established (Reference BovisBovis, 1977). However, inconsistencies appeared when the magnitude and type of avalanche were related to precipitation factors alone. Periods of significant precipitation and wind transport might in one case produce large slab releases, while the same meteorological conditions at another time might produce little or no avalanche activity. Conversely, relatively small amounts of precipitation sometimes resulted in widespread and deep slab releases.

The basic pattern of avalanche release mechanics has been consistent during the study period. Of the fracture-line studies, over 85 % exhibited a climax avalanche structure (slab failure occurred in older snow layers deposited and metamorphosed prior to the triggering event). In 75% of the cases investigated, the lubricating layer beneath the slab was identified as recrystallized snow resulting from temperature-gradient processes.

If snow structure actually controlled the type and depth of avalanche release, a pattern should emerge if snow structure conditions were monitored throughout the avalanche season. An example of this type of analysis is found in Figures 1 and 2. Figure 1 shows the typically poor relationship between avalanche events and the total precipitation (millimeters of water equivalent) comprising each discrete storm period. The linear regression r-value for Figure 1 is only 0.08. However, when the season is divided into four time periods, the precipitation and avalanche event data tend to conform to a systematic pattern (Fig. 2). The periods are subdivided by date based on the best four chronological regression groupings. Mean snow-cover temperature-gradient values for each period, as measured at the Red Mountain Pass study site, are provided as an additional index of snow-cover conditions. These mean temperature gradients appear below the appropriate dates in Figure 2. Linear regression r-values appear for each of the four time periods and the relative instability of the snow structure associated with each period is depicted by the slope value for the appropriate avalanche- precipitation relationship (inset in Fig. 2d). The period I November to 16 December indicates the steepest temperature gradient and while the general snow structure is weakening in response to this condition, it is not until the period 17 December to 12 January that the weakness attains a maximum, creating a pattern where large numbers of avalanches result from relatively small amounts of precipitation. The period 13 January to 5 March represents a period of transition with the snow cover gaining strength as the temperature gradient decreases. The final period represents the snow cover as it approaches an isothermal condition.

Fig 1.

Relationship between individual storm precipitation totals (mm water equivalent) and number of observed slab avalanches larger than size one during the 1974–75 winter.

Fig 2.

Relationship between individual storm precipitation totals and number of observed slab avalanches larger than size one subdivided into four periods according to progressive changes in snow structure for the 1974–75 winter

The deviation of data points A in Figure 2a, B in Figure 2C and C in Figure 2d were not included in the regression analysis and can be dealt with as individual cases based on the following supplemental data: Point A represents an early precipitation episode when new snow was accumulating on bare ground or shallow old snow. In case B, 23 February 1975, although little direct precipitation was recorded, additional loading did occur as the result of a wind-transport episode with a duration of 18 h and a mean wind speed of 13 m/so Case c, 13 April 1975, occurred when numerous, small, soft slab events occurred within the new snow. During the last 12 d preceeding this cycle, 95 mm of precipitation had been recorded at the Red Mountain Pass study site without significant avalanche activity. The structural regime represented by Figure 2d is that of new snow collecting on an exceedingly stable, near-isothermal snow cover. Failure within the older snow structure was therefore precluded and a shear failure plane developed in conjunction with a freez e- thaw crust that was established during a brief clear-weather episode within the longer period of heavy precipitation. This cycle is an isola ted example of slab release within new snow, an avalanche pattern which frequently occurs in climates where stable old-snow structure prevails, but is the exception within the San Juan snow climate.

Having established that snow structure may exhibit significant control over the nature of avala nche release, what then are the physical conditions which create such a stratigraphy? There appear to be three distinct situations: a substantially thick layer of temperature-gradient snow or depth hoar at the base of the snow cover, alternating layers of melt-freeze crusts and temperature-gradient snow, and instability resulting from restricted consolidation of near-surface snow layers. Once a substantial basal layer of mechanically weak depth hoar has formed within a release zone, only a significant avalanche cycle can eliminate this condition. Minimal intergranular bonding prevails and even as the depth and thus load of the overlying snow cover increases as the winter progresses, and the initial steep temperature gradient is diminished, either due to increasing snow depth or increasing air temperatures of late winter and early spring or both, only minimal improvement in intergranular cohesion occurs. Figure 3 shows the increase in rammsonde resistance with d epth within the mid-pack layers followed by the sharp break in this relationship as the lower depth-hoar layers are reached. Figure 4 shows the limited densification with time of the depth-hoar layer (from 0–60 cm) compared to the layers above, which were exposed to less steep temperature gra dients. Figure 5 demonstrates the resistance to settlement exhibited by well-advanced temperature-gradient snow (settlement curve I). Curves 2 through 4 represent the settlement rate of snow layers deposited during mid-winter and exposed to a lesser temperature gradient (0.08 to 0.15 deg/cm). Curves 5 through 7 represent the settlement of snow layers at or very near an isothermal condition (0.02 to 0.07 deg/cm).

Fig 3.

Integrated rammsonde resistance curves for seven selected dates at the Red Mountain Pass study site during the 1974–75 winter

Fig 4.

A time-stratigraphic diagram of density variations (Mg/m³) at the Red Mountain Pass study site for the period 15 October 1974 through 30 April 1975.

Fig 5.

Initial settlement rates at seven points within the snow cover at the Red Mountain Pass study site, 1974–75. Number 1 is representative of the early winter snow cover, numbers 2 through 4 are mid-winter and 5 through 7 are early spring conditions.

If in a given release zone the basal depth-hoar layer is not removed by mid-winter avalanching, it may provide a structure which increases the probability of wet-slab avalanches in the spring. As percolating melt water comes in contact with a snow cover which has been developing over several months, optimum shear boundary conditions are created for slab-type releases. In contrast to this situation, a winter with frequent, deep avalanching results in the removal of a major portion of the snow cover metamorphosed under early to mid-winter conditions. Subsequent snowfalls in late winter and early spring are exposed to less significant temperature-gradient metamorphism and thus comprise a more homogeneous and stable structure.

The second type of weak layer results from alternating melt–freeze crusts and recrystallized snow. All slopes excepting those with a northerly exposure have been observed to experience subsurface warming due to the penetration and absorption of solar radiation. At any time during the winter season this warming can be sufficient to cause the snow temperature to reach the melting point with the eventual formation of a melt- freeze crust. This phenomenon has been observed by Reference YosidaYosida (1960). Even at the warmest point in the diurnal temperature cycle, when melt is occurring 1.0–3.0 cm beneath the surface, the temperature of the snowair interface, due to radiation cooling, may remain several degrees below freezing, creating an extremely steep temperature gradient across the uppermost several millimeters of the snow cover. This combination provides optimum conditions for temperature-gradient recrystallization; mean snow temperatures at or near freezing providing maximum vapor supply, a snow layer of low density allowing maximum vapor diffusion, and a temperature gradient as high as several degrees per centimeter. Vapor-pressure gradients within these surface layers may commonly be as high as 0.60 to 0.80 mbar/cm, values which are as much as ten times greater than those considered adequate to initiate temperature-gradient metamorphism (Reference LaChapelle and ArmstrongLaChapelle and Armstrong, in press). Consequently, advanced temperature-gradient recrystallization may occur within 24 h. This process has been called “radiation recrystallization” by Reference LaChapelleLaChapelle (1970) and has been frequently observed in the San Juan Mountains. Initially created near the surface of the snow cover, the recrystallized layer is buried by subsequent snowfalls and provides an ideal lubricating layer. Beneath the recrystallized layer, the refrozen thaw layer provides a sliding surface. In this situation, poor adhesion between the slab and the sliding surface appears to contribute towards the failure, rather than a separate and distinct weak layer of substantial thickness. Figure 6 contains an example of this type of stratigraphy as it has developed through mid-winter. Figure 7 shows the relationship between calculated shear stress of the slab and measured density of the lubricating layer below. Density samples were limited to average values across 50 mm layers, whereas the actual shear failure zone may often have been less than 10 mm in thickness.

Fig 6.

Stratigraphic snow-cover data typical of a south-facing slope during mid-winter in the San Juan Mountains showing alternating layers of melt-freeze crusts and recrystallized temperature-gradient snow.

Fig 7.

Relationship between calculated slab shear stress at the point of failure (fracture line) and the measured density of the lubricating layer at the base of the slab.

The third condition creating a weak layer is caused by retarded settlement of near-surface snow layers due to low temperatures (–15.0 to –25.0°C) as well as minimal overburden pressure. Low-density shallow snowfalls are common to this a rea with the average storm depth being 17 cm and an average mid-winter d ensity of 0.065 Mg/m³. This situation differ from climates where snowfall amounts are greater and snow and air temperatures are consistently closer to freezing. Relationships between overburden pressure, temperature and layer densification have been analyzed elsewhere (de Reference QuervainQuervain, 1958; Reference KofimaKofima, [1975]) with the unconsolidated and shallow temperature-gradient layers showing minimal or no increase in density or strength with time. Only substantial loading caused strength increases but in terms of avalanching, shear failure may well occur beforehand.

The first two conditions which result in the formation of weak layers are directly controlled by temperature-gradient metamorphism and while the third is initially related to meteorological conditions during precipitation periods, it is the subsequent clear-sky radiational cooling which establishes steep temperature gradients and preserves the unconsolidated structure of the layers. Under compressive bulk stress, snow commonly densities, creates new bonds and increases in mechanical strength with time. However, temperature-gradient snow does not behave in this fashion. Studies conducted by de Reference QuervainQuervain (1958) and Reference AkitayaAkitaya (1974) have indicated that while temperature-gradient snow is quite weak in shear, it retains a relatively high compressive viscosity, and once the initial changes associated with surface-free energy adjustments in the new snow are accomplished, temperature-gradient metamorphism tends severely to inhibit the densification process and thus any associated gain in shear strength. The cumulative loading of new snow above these temperature-gradient layers causes them to density only slightly compared to layers which experienced initial metamorphism under less steep temperature gradients. Even as temperature gradients become minimal (0.05 dcg/cm) across a layer of well-developed, coarse-grained temperature-gradient crystals, only minor increases in shear strength occur, partially because shear strength in a coarse granular material is inversely proportional to grain size and also because the larger grains have fewer physical opportunities for bond growth once a lesser gradient allowing the growth prevails.