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        Micro-Morphology of the Snow Surface at the Quelccaya Ice Cap, Peru
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        Micro-Morphology of the Snow Surface at the Quelccaya Ice Cap, Peru
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Abstract

During the June-July 1979 expedition a large variety of micro-forms was observed at the surface of the Quelccaya ice cap, their altitudinal distribution being primarily controlled by the heat budget. At 5200–5300 m penitentes are best developed, with azimuth orientation and inclination of features conforming to the insolation geometry around local noon. At a westward-facing slope in 5360–5380 m a set of penitentes striking parallel to the contours is superimposed on the pattern dominating at the lower elevations. The ablation forms of penitentes give way to various deposition features above a transition zone around 5400 m in broad agreement with the larger net all-wave radiation and greater importance of melting at lower elevations. The succession of forms with an upward change from surface-parallel plates to elaborate dendritic forms appears to be controlled by the temperature conditions. The conspicuous development of forms encountered during the 1979 expedition appears characteristic of prolonged absence of fresh snow-fall subsequent to a season with abundant precipitation.

1. Introduction

A multi-annual field project is being conducted on the Quelccaya ice cap in the eastern Andes of Peru, geared at the retrieval of ice cores for climate reconstruction. The study of the recent climate and heat and mass budget is an important component of this field effort, in terms of providing a modern background for paleoclimatic interpretations. The Quelccaya ice cap is located at around lat. 14° S., has an area of about 54 km2 and a summit elevation of 5650 m (Fig. 1). Details of environmental setting and of earlier project results have been described in various publications (Hastenrath, 1978; Thompson and others, 1979). The present paper discusses some field observations during the June–July 1979 expedition conducted by the Institute of Polar Studies of Ohio State University with participation by the Department of Meteorology of the University of Wisconsin, the Polar Ice Coring Office at the University of Nebraska, and the Instituto de Geología Minería of Peru.

Fig. 1. Orientation map. Ice rim is indicated by heavy solid, and travel route by dotted line. B and S denote base camp summit, respectively. Elevations in meters.

2. Observations

The various project tasks in the peak region required daily trips between the camp established near the ice rim at 5150 m and the summit at 5650 m. These traverses provided ample opportunity to observe the change of snow surface characteristics with elevation. Altitudinal variations in surface morphology were found to be rather more pronounced than during the earlier expeditions. Characteristic features are described in the following.

At the lowest elevations, between the ice rim near 5200 m and about 5300 m, penitente forms were found in best development (Fig. 2). Penitentes consisted of sheets or boards of snow arranged with a regular west–east striking and a dip of about 50° towards the north. This compares well with the noon zenith angle of the sun for the winter solstice at 14° S., namely about 38°, as discussed in the literature (Troll, 1942, p. 33-36; Hofmann, 1964; Kraus, 1966).

Fig. 2. Penitente field at 5200 m. Compass and string indicate north direction to left. Plastic ruler as scale.

Above 5300 m the penitents are smaller and the pattern becomes irregular. Between 5360 and 5380 m on a wide westward-facing slope, another penitents pattern with a broadly contour-parallel strike, larger zenith angle, and sheets pointing towards the west, appears superimposed on the pattern described above for the lower elevations (Figs 34). Proceeding upward the pattern parallel to the contours becomes the more conspicuous one.

Fig. 3. Cross-pattern of penitentes at 5370 m. Compass and string indicate north direction to left, and plastic ruler is placed approximately parallel to terrain contours.

Fig. 4. Field of cross-patterned penitentes at 5370 m. Compass, string, and plastic ruler serve same purpose as in Figure 3.

At elevations around 5420 m the ablation forms of penitentes vanish, and give way to the appearance of large essentially surface-parallel plate-shaped ice crystals, with typical diameters of 5–10 mm (Fig. 5). Proceeding towards higher elevations, the crystal plates occupy an increasing fraction of the total surface; large plates accounting for about half of the area at 5600 m.

Fig. 5. Plate-shaped ice crystals at 5470 m. Plastic ruler as scale.

Above 5600 m, plates are replaced by column-shaped crystals (Fig. 6), over a comparatively small elevation interval. Needle-shaped crystals seem to be less common. The highest part of the summit plateau upward of 5630 m is dominated by elaborate dendritic crystal forms (Fig. 7). Elements tend to be oriented towards west of north, in accordance with the seasonally-prevailing wind direction.

Fig. 6. Column shaped ice crystals at 5640 m. Plastic ruler as scale

Fig. 7. Dendritic ice crystals at 5650 m. Plastic ruler and compass as scale.

Observations during this prolonged period without snow-fall thus show a pronounced altitudinal variation of surface morphology, ranging from various ablation forms in the lower, to deposition phenomena in the upper part of the ice cap. As a background for the understanding of the observed altitudinal zonation of surface features, some aspects of the heat budget will be reviewed in the following section.

3. Heat Budget

The heat budget equation for the surface can in approximate form be written

(1)

Here the left-hand terms denote downward and upward directed short-wave and net long-wave radiation. The first three right-hand terms signify latent heat flux, heat used for melting, and sensible heat flux, respectively. The last right-hand term combines storage and vertical heat fluxes within the ice.

Based on measurements during the 1976 and 1977 expeditions, methods have been developed to calculate surface net all-wave radiation, that is the left side of Equation (1), as a function of cloudiness and albedo; and representative albedo values have been tabulated for elevation bands (Hastenrath, 1978). These data will be used here although somewhat smaller albedo values were measured after a prolonged period without snow-fall in early July 1979. A qualitative discussion appears appropriate here.

The first and third terms on the left-hand side of Equation (1) are rather uniform all over the ice cap, while the second left-hand term is a function of albedo and hence elevation. Accordingly, the net all-wave radiation decreases from appreciable positive values near the ice rim to figures near zero on the summit plateau. The net all-wave radiation in turn must approximately equal the first two right-hand terms of Equation (1), inasmuch as the last two terms on the right are small. The energy available for ablation thus decreases strongly with elevation.

The dependence of the ablation of ice mass on elevation is further accentuated by the temperature conditions, in that the latent heats of evaporation and melting differ by almost an order of magnitude. The thermal regime at the Quelccaya summit in southern winter is characterized by daily maximum, mean, and minimum air temperatures around —3, —8, and —13° C, respectively. Accordingly, melting at the surface, and hence more sizeable ablation, can be expected at elevations from around 5400 m downward, in particular. By contrast, on the vast summit plateau, where net all-wave radiation is anyhow near zero, ablation would be confined to the energetically expensive evaporation. This state of affairs is confirmed by concurrent radiation, lysimeter, and profile measurements during the 1976 and 1977 expeditions (Hastenrath, 1978).

In relation to the penitente phenomenon, the radiation geometry around the time of day with largest insolation is of interest. For an approximately horizontal surface the corresponding solar azimuth is north and the zenith angle equal to declination plus latitude. Conditions are more complicated for slopes.

4. Conclusions

The prominent characteristics in the altitudinal distribution of surface features will be examined in terms of the heat budget. This seems appropriate because the surface has remained unaffected by fresh snow-fall for a prolonged period. The following aspects are of interest in particular:

  • (i) The transition from the ablation form of penitentes to the dominance of variously shaped ice crystals, which represent deposition features, takes place around 5400 m, in broad agreement with the larger net all-wave radiation and greater importance of melting at lower elevations.

  • (ii) Penitentes are best developed in the lowest elevation band, from 5200 m to 5300 m, where surface net all-wave radiation and temperature are largest, thus providing the energetic prerequisites for this phenomenon (Hofmann, 1964).

  • (iii) In the lower portion of the ice cap at 5200–5 300 m, where penitentes are best developed, their orientation in terms of azimuth and elevation angle conforms to the insolation geometry around local noon, as discussed in the literature (Troll, 1942, p. 33-36; Hofmann,1964; Kraus, 1966). The existence of a thick snow layer over the lower part of the ice cap this year is conducive to the maintenance of the penitentes. Where the ice below is reached, these features tend to collapse.

  • (iv) The aspect of large-scale topography may play a role for the cross-pattern of penitentes observed on the westward-facing slope at 5360 to 5380 m.

  • (v) Ice crystals at the surface in this prolonged period without fresh snow-fall indicate that deposition prevails over ablation. An approximate balance between night-time deposition and day-time evaporation related to the delicate surface radiation budget has already been identified as a feature characteristic of the upper plateau of the Quelccaya (Hastenrath,1978). During 1979 conditions seemed to have been particularly favorable for deposition.

  • (vi) Preferred shapes of ice crystals show a marked dependence on elevation: proceeding upward there is a change from surface-parallel plates to elaborate dendritic forms. Columnsand needles approximately perpendicular to the surface are also encountered. In the study ofcloud physics, a similar progression in crystal shape has been found as a function of tempera-ture. For supersaturations beyond 15–20% with respect to ice, Mason (1975, p. 78-89) reports from his laboratory experiments the following characteristic forms: hexagonal plates for 0 to —3° C; needles for —3 to —5° C; prisms for —5 to —8° C; plates for —8 to — 12° C; dendrites for —12 to — 16° C; and again plates below — 16° C. A more complex dependenceof forms on both temperature and vapor-pressure conditions is indicated for smaller super-saturations. At night when crystal formation with preference takes place, temperatures between —8 and — 14° C may occur at various elevation bands of Quelccaya. From the afore-mentioned daily temperature variation, night-time supersaturations of 20% near the surface of the Quelccaya plateau are expected to be common. The sporadic occurrence of columns and needle-shaped crystals may be related to more complex vapor-pressure conditions. The spatial sequence of typical shapes described in Section 3 thus appears consistent with the upward decrease of temperature. Wind seems to play a role in the orientation of dendrites at the summit.

In conclusion, the large variety in the micro-morphology of the Quelccaya snow surface and the systematic altitude dependence of forms appear to be primarily controlled by the heat budget, with upward decrease of temperature and orientation of slope being important features in the origin of some features. The marked development of micro-forms encountered during the 1979 expedition was seemingly favored by the prolonged absence of fresh snow-fall, following a season of extremely abundant precipitation. Abundant snow-fall during most of the year, however, leads to a much different appearance of the surface at Quelccaya.

References

Hastenrath, S., 1978. Heat-budget measurements on the Quelccaya ice cap, Peruvian Andes. Journal of Glaciology, Vol. 20, No. 82, p. 8597.
Hofmann, G. 1964. Zur Rolle des Wärmehaushaltes bei der selektiven Ablation. Carinthia II (Klagenfurt), Sonderht. 24, p. 25966.
Kraus, H. 1966. Freie und bedeckte Ablation. Ergebnisse des Forschungsunternehmens Nepal-Himalaya, Lief. 3, p. 20336.
Mason, B. J. 1975. Clouds, rain, and rainmaking. Second edition. Cambridge, Cambridge University Press.
Thompson, L. G., and others. 1979. Climatic ice core records from the tropical Quelccaya ice cap, by Thompson, L. G., Hastenrath, S., and Morales Arnao, B.. Science, Vol. 203, No. 4386, p. 124043.
Troll, C. 1942. Büsserschnee in den Hochgebirgen der Erde. Petermanns Geographische Mitteilungen. Ergänzungsht. 240.