Introduction

Reference BoultonBoulton (1978) has suggested that when large boulders with a smoothed and striated, often bullet-nosed up-glacier termination, and an abruptly truncated down-glacier termination (henceforth termed a stoss-and-lee form), and a single well-defined set of striae which diverge slightly in a down-glacier direction are found in a till unit, then that unit is probably a lodgement till. The long-axis orientation of such boulders has been used as an indicator of ice-flow direction by Reference KrügerKrüger (1979).

A boulder which ploughs deeply into the subglacial till bed during lodgement may cease to move relative to over-riding debris-rich glacier ice and offer a steady unrotating resistance to ice flow. A steady-flow pattern is set up around the boulder, and its up-glacier face is abraded and streamlined by debris-rich basal ice. If the ice digs into the till on the boulder’s up-glacier side, a bullet-nosed end may develop. The lee-side surface of the boulder may be a remanié surface, which has not suffered erosion, or may be shaped by fracture at a point of contact with large over-riding particles, if cavitation has occurred around the boulder, leaving its lee side unsupported (Reference BoultonBoulton. 1978) (Fig. I).

Fig. 1. Streamlined, deeply embedded boulder with stoss-and-lee form. Large angular fragments derived from the lee side of the boulder lie on the till surface at the foot of the lee-side slope.

The aim of the present study was to investigate the extent to which such erosional modification of large clasts occurs in lodgement tills at Skálafellsjökull, south-east Iceland (lat. 65° 16’ N., long. I6°05’W.). In particular, the influence of size and lithology of clasts was examined.

Methods

To determine whether the morphology of deeply embedded boulders was significantly different from that of lightly embedded boulders which had not ploughed into the lodgement till surface, a random sample of 50 lightly and 50 deeply embedded boulders greater than 0.3 m in diameter was selected. The study site was on the stoss slope of a roche moutonnée and had been deglaciated within the last 20 years. Boulders were classified as either coarse- or fine-grained igneous rocks. The former were either gabbro or granophyre. and the latter basalts or andesites. The roundness of each boulder was assessed using the visual classification of Reference PowersPowers (1953). If the boulder had a stoss-and-lee form, this was recorded and the long-axis orientation of the boulder was measured. If the boulder was striated, this was recorded and the orientation of the dominant striation set, if one existed, was measured. If the boulder was not striated or did not have a stoss-and-lee form, this was also recorded (Table I).

Table I. Shapes and surface characteristics of lightly and deeply embedded boulders, SkÁlafellsjokull. south-east Iceland

To determine the proportion of boulders in the till which had a stoss-and-lee form, and the influence of boulder size and lithology on this. 20 quadrats I m by I m were established on the till surface. In each quadrat, every clast with a B-axis diameter of more than 32 mm was examined, a total of 1105. The lithology, B-axis diameter, and presence or absence of a stoss-and-lee form was recorded for each clast (Table II).

Table II. Proportion of clasts in Skalariilsiökijll lodgement tills having stoss and lee Form. In relation to size and litholooy of clasts

Results

There are no significant differences between lightly and deeply embedded boulders in terms of lithology, roundness, degree of striation, or degree of development of a consistently orientated striation set. Deeply embedded boulders are, however, more likely to have a stoss-and-lee form than lightly embedded boulders (x ² = 24.0, df = 3, p < 0.005). Overall, 82 (7.78%) of the 1105 clasts sampled had a stoss-and-lee form.

Lithology appears to influence boulder morphology. Lightly embedded fine-grained boulders are more likely to be striated than lightly embedded coarse-grained boulders (x ² = 12.45, df = 3, p < 0.01). Deeply embedded fine-grained boulders are more striated (x ² = 30.75, df = 3, p < 0.005) and more likely to have a stoss-and-lee form (x ² = 11 .39, df = 3, p < 0 .01) than deeply embedded coarse-grained boulders. Lithology does not, however, affect the roundness of lightly or deeply embedded boulders, nor the proportions of lightly embedded boulders with stoss-and-lee form.

Deeply embedded fine-grained boulders are more striated (x ² = 13.02, df = 3, p < 0.005) and more likely to have a stoss-and-lee form than lightly embedded boulders of similar lithology (x ² = 17.95, df = 3, p < 0.005). They are not, however, more rounded, or more likely to have a consistently orientated dominant set of striae. There are no differences in the roundness, degree of development of stoss-and-lee form, or striation of lightly and deeply embedded coarse-grained boulders.

65/903 fine-grained clasts had a stoss-and-lee form (7.19%), compared with 17/199 coarsegrained clasts (8.41%). Within each lithological class, the proportion of clasts with stoss-and-lee form increased with the B-axis diameter (Table II), so that larger clasts were more likely to have a stoss-and-lee form.

Sixty-five of the 100 boulders in the random sample were striated and their shapes were dominantly rounded to sub-angular. Only 8/100 were angular or very angular, suggesting that virtually all had passed through the zone of traction at the glacier bed (Reference BoultonBoulton, 1978). Observations on the distribution of debris in the adjacent glacier ice confirmed that large clasts are only present in the basal layers.

Excavation of five deeply embedded boulders showed that their lower surfaces had not been smoothed and streamlined in the same way as their upper surfaces. In several instances, fractured blocks were found at the foot of the lee surface of a boulder (e.g. Fig. 1), and in all 40 cases where boulders had a stoss-and -lee form, the lee surface was judged to be a clean fracture rather than a remanié surface.

To determine whether the long-axis orientation of boulders with stoss-and-lee form, and the orientation of their dominant striation set can in fact be used as indicators of ice-flow direction, these were analysed using 2-D vector analysis (Reference KrumbeinKrumbein, 1939) and compared with ice-flow directions deduced from the orientation of bedrock striae. Vector magnitudes for the long-axis orientation of deeply embedded stoss-and-lee boulders and the direction of striations on them were significant at the 0.05 level. The directions of the resultant vectors were within 5° of the direction of ice flow. Vector magnitudes for the long-axis orientation of lightly embedded stoss-and-lee boulders, and the direction of the dominant striation set on them, were not significant (Fig. 2).

Fig. 2. a. Long-axis orientations of deeply embedded boulders with stoss-and-lee form. Vector magnitude = 632%, N = 32. b. Long-axis orientations of lightly embedded boulders with stoss-and-lee form. Vector magnitude = 7.5%, N = 8. c. Orientation of dominant striation set on deeply embedded boulders. Vector magnitude = 71.8%, N = 30. d. Orientation of dominant striation set on lightly embedded boulders. Vector magnitude = 18.8%, N = 23. Symbols:→ Ice-flow direction indicated by bedrock striae. --→ Resultant vector.

Discussion

The stoss-and-lee form does seem to be a feature characteristic of deeply embedded boulders, though the frequency with which it occurs probably varies with boulder size and lithology. Large boulders are more likely to have a stoss-and-lee form than smaller ones, though they are less common in the till. The analysis of 50 lightly and deeply embedded boulders suggests that finegrained rocks are more likely to have a stoss-and-lee form than coarse-grained rocks, but this is not confirmed by the less detailed analysis of a further 1105 clasts. This discrepancy could be explained by a difference in the size distribution of clasts of the two lithologies.

The higher frequency of stoss-and-lee shapes among deeply embedded boulders, the increased rounding of deeply embedded fine-grained boulders, the fractured nature of boulder lee-side surfaces, the lack of modification of the lower surfaces of stoss-and-lee boulders, and the close alignment of the long axes of stoss-and-lee boulders with ice-flow direction all suggest that such boulder shapes develop in the way suggested by Reference BoultonBoulton (1978). Modification of boulders by abrasion will occur if the debris particles in transport in the basal ice are as hard as or harder than the lodged boulder. The amount of modification which occurs will depend upon the concentration and rate of transport of debris particles in the glacier sole, and the length of time for which the boulder is exposed. Similar factors will control the likelihood of fracture occurring on the lee-side. Although lodgement tends to be concentrated around protruding obstacles at the glacier bed, it should still take longer to bury a large boulder than a small one, if only because rates of lodgement will decrease over time as the proportion of the boulder protruding decreases. Large boulders will therefore be exposed for longer and are more likely to be modified by erosion. This is confirmed by the results of this study (Table II).

The proportion of clasts in a till which develop a stoss-and-lee form will presumably thus depend upon the mix of lithologies in the till and the size distribution of clasts of each lithology, as well as the factors mentioned above. Reference HalletHallet (1981) has shown that, as a result of drag between debris in traction and the glacier bed, the rate of basal sliding of a glacier may decrease as the concentration of debris in the glacier sole increases above 10%. Rates of lodgement may also increase at such high debris concentrations as sliding rates drop to values equivalent to the rate at which basal ice melts due to geothermal heating. It is possible, therefore, that there is a critical value of debris concentration in the basal ice above which the chances of a deeply embedded boulder being modified subsequent to lodgement are much reduced.

Eight of the 50 lightly embedded boulders had a stoss-and-lee form, but their long axis orientations were highly variable and divergent from mean ice-flow direction at the site. They had probably once been deeply embedded but had since been incorporated and re-deposited by minor advances of the ice front responsible for constructing small push moraines (cf. Reference Boulton and PaulBoulton and Paul, 1976, p. 168).

Two possible explanations are suggested for the observation that deeply embedded boulders are not more likely to have a single dominant striation set than lightly embedded boulders. Many of the fine-grained clasts have been derived very locally from polished and striated bedrock surfaces and may inherit a consistent striation set from them. Furthermore, Reference DrakeDrake (1977) has shown that rod- and blade-shaped clasts may develop consistently orientated striae parallel to their long axes during transport at the glacier bed, because they experience very little clast rotation during transport.

The orientation of the long axis of clasts with stoss-and-lee form is closely related to the direction of ice flow, and the position of the lee-side surface makes it possible to determine the direction from which the ice was flowing. The orientation of striae on such deeply embedded clasts is also a good indicator of former ice-flow directions.