Introduction

Glacial geomorphologists living in presently unglaciated areas of the world must normally travel some distance to study freshly deglaciated terrain. Occasionally, however, unweathered glaciated bedrock is revealed in areas that have not been glaciated for many thousands of years. The most common example is where till is stripped off bedrock during construction work, but a less frequent opportunity arises where a lake bed is exposed during construction or operation of a hydro-electric power scheme or other engineering project.

During construction of the Dinorwic hydro-electric pumped storage scheme near Llanberis, Snowdonia, north-west Wales (Fig. 1), the largest such scheme in Europe, the water was pumped from the two lakes that were to form the upper and lower reservoirs for the scheme. Some smalt-scale glacial features exposed on unweathered bedrock from the floor of the upper reservoir, Marchlyn Mawr, have been described in a previous paper (Reference Gray and LoweGray and Lowe, 1982). This paper describes glacial features from the bed of the lower reservoir (Llyn Peris), and aims to draw the attention of glacial geomorphologists to the opportunities for research at such sites.

Fig. 1. Location map of the Llyn Peris area, north-west Wales.

Study area

Llyn Peris, together with Llyn Padarn to the north-west, occupy an overdeepened basin towards the lower end of the Pass of Llanberis glacial trough (Fig. 1). The two lakes were formerly continuous but have been divided by the growth of a fan at Pont-y-Bala deposited from the south-west by the Afon Arddu. Before construction work began, the lake surfaces lay at about 100 m o.d. but bore holes sunk at the south-east end of Llyn Peris and on the Pont-y-Bala fan indicate rockhead at 45 m o.d. at both sites. The bore holes revealed considerable thicknesses of glacial lake rhythmites, sands and gravels, organic lake mud and wood-debris peats overlying bedrock (Reference Tinsley and DerbyshireTinsley and Derbyshire, 1976). The bedrock in the area is largely Cambrian slate with cleavage and joints mainly trending transverse to the long axis of the lake, although Cambrian grits crop out along the south-west shore of the lake as far north as site 12 (Fig. 2).

Fig. 2. Study sites and striae orientations at Llyn Peris.

Prior to construction, Llyn Peris was about 1.1 km long and about 300 m wide at the widest point about half-way along the lake where there is a bay on the south-west shore (Fig. 2). Most of the north-east side has been disturbed by the now disused Dinorwic slate workings and prior to construction much of this shore consisted of slate waste. The presence of this disturbance accounts for the fact that most of the bedrock sites studied in this paper lie along the south-west side of the lake bed (Fig. 2). The deep central strip of the lake is underlain by soft lake sediments which were covered with slate waste during construction so that it was possible to walk about on the former lake floor and examine many of the steep rock faces forming the sides of the trough. From these slopes muds and other sediments were largely removed by mechanical diggers to expose the bedrock and at site A (Fig. 2) a thick area of silty till was removed which contained several massive boulders, the largest of which measured about 8 m by 8 m by 5 m. Even so, many of the bedrock surfaces described here had to be dug out or brushed clean of sediment.

The trough was last glaciated in the Late Devensian, probably becoming ice-free at least 13000 years ago (Reference Coope and BrophyCoope and Brophy, 1972; Reference InceInce, unpublished). The basin was not glaciated during the Loch Lomond (Younger Dryas) stadial (Reference GrayGray, 1982).

Abrasion

Abraded bedrock is the most striking feature or the bed or Llyn Peris. One of the main reasons is that the homogeneous fine-grained slate bedrock is particularly susceptible to scratching and polishing. Heavily abraded, steeply sloping slabs of slate up to 10 m high are found at sites 5, 6, 13, and 14 (Figs 2 and 3). It is noticeable that the striae on most of these faces indicate upward movement of the ice at 5–10° in the direction of movement, though, where the ice moved against bedrock obstructions on the slopes, the striae can be seen to sweep upwards over the obstacles, sometimes reaching angles of inclination of over 20° (e.g. at sites 13 and 14).

Fig. 3. Steep abraded face at site 6. Ice moved from right to left. Irregular blocks have been plucked from the face.

Striae orientations on flat surfaces have been measured at a number of sites and the means of 3–25 orientations taken at each site are plotted on Figure 2. The mean orientations at sites 9, 10, 11, and 12 are 299°, 299°, 306°, and 299°, respectively, whereas those at sites 2, 7, and 4 are 318°, 319°, and 325°, respectively, and indicate a slight change in direction of ice movement as it moved north-westward along the trough. Once past the confining steep slopes of the Pass of Llanberis at site 8, the ice apparently swung into the bay on the south-west shore as it became less confined towards the wider valley stretch around Llanberis (see Fig. 2).

There are also many examples of small-scale topographic features influencing striae trends. For example, at site 7, a dyke c. 1 m wide is responsible for a trench 1–1.5 m deep running transverse to the main trend of the striae, but the walls of the trench bear striae parallel to its trend. Leading down-ice from this transverse trench are several linear grooves about 0.5 m wide, all of which are joint-controlled. Striae can be seen to curve from the walls of the trench into the grooves, indicating streaming of the basal ice into them.

The best examples of striated glacial grooves occur in an embayment at site 9. They are 10–30 cm wide and deep, rise steeply (40–60°) down-ice out of the embayment (see Fig. 4), and all follow joints. It is possible that these grooves owe their origin to “streaming” of debris-rich ice in this low point in the glacier bed in a way similar to that suggested by Reference BoultonBoulton (1979). Although such steeply rising deep grooves are confined to one part of site 9, at several other localities there are shallow sinuous grooves into and out of which striae can be seen to converge and diverge. Horizontal grooves cut into steep faces also occur, the most impressive one at site 9 (Fig. 5). The floor of this groove exhibits the most highly polished slate in the study area.

Fig. 4. Glacial grooves up which the let moved at site 9.

Fig. 5. Horizontal glacial groove at site 9. Ice moved towards the camera. The floor of the groove is very highly polished.

Lithological differences have also had an effect on glacial abrasion. The strike of the original bedding in the metamorphosed mudstones and shales trends south-west to north-east and thus transverse to ice movement. At site 7, the smoothing towards the top of the curved stoss slope of an unjointed slate slab several metres square (Fig. 6) shows a marked change in angle and this is related to a change in lithology. The long lee slope at this site (7) is conspicuously stepped as a result of lithologica] changes and joints, but where homogeneous slate occurs on treads it is often remarkably well striated (see Fig. 6).

Fig. 6. Abraded pavement at site 7. The ice moved away from the camera. The stoss slope steepens at a change in lithology. Slate waste being used to cover the lake-floor sediments can be seen in the upper left corner.

At site 13, two small more resistant patches occur within the slate, possibly as reduction spots or as offshoots from a dyke. Differential glacial abrasion has resulted in small-scale crag-and-tail forms on the steep face (Fig. 7). Even smaller crag-and-tails are also present at this locality, emanating from numerous iron pyrites crystals a few millimetres square. These have often been weathered out, leaving square pits with slate tails extending down-ice for a few centimetres (Fig. 7).

Fig. 7. Small-scale crag-and-tails developed at two resistant patches in the slate at site 13. Ice moved left lo right. On the left, iron pyrites crystals have formed miniature crag-and-tails though the crystals themselves have mostly been weathered out leaving slate tails in the lee of rusty square pits. In the right centre, a joint has been preferentially widened up-ice.

Bedrock fracture and plucking

Although erosional processes have often been divided into abrasion and plucking, recently it has been recognized that fracture must occur before rock fragments can be plucked by ice. Thus, recent authors have discussed “bedrock fracture” or “crushing” separately from abrasion and plucking (e.g. Reference Boulton and CoatesBoulton, [^C1974]: Reference Sugden and JohnSugden and John. 1976). Reference Boulton and CoatesBoulton ([^c1974]) described three-processes of bedrock fracture associated with glaciers, viz. freeze-thaw shattering, pressure-release jointing, and lee-slope stress fracturing. To these processes can be added the production of friction cracks by casts moving over bedrock (see e.g. Reference Embleton and KingEmbleton and King, 1975). though some authors have classified this as abrasional (e.g. Reference JohnsonJohnson, unpublished).

Few examples of friction cracks have been found on the abraded bedrock in the Peris basin. Much more common are irregularly shaped transverse marks, where several chips of rock have been removed and which often extend several centimetres laterally beyond the confines of the striae and grooves to which they are related. Thus many surfaces have been given a roughened appearance perpendicular to ice movement (Fig. 8b) largely due to the exploitation of the transverse cleavage planes. In some cases (e.g. at site 14), regularity of form and spacing can be detected (see Figs 8a and 9) with curved chips concave up-ice having been removed from both sides of a groove, or, in some cases (e.g. upper one in Fig. 9), from one side only. The spacing of the chips varies from a few millimetres to less than 1 mm. It remains to be seen whether they are unique to this area or to slate outcrops but, if not, the name “swallow-wing fractures” is proposed.

Fig. 8. Transverse friction marks associated with striae and abrasion grooves. a. New type from Llyn Peris; b. irregular transverse chipping common at Llyn Peris; c. Crescentic gouges related to a groove (“jagged groove” of Reference HarrisHarris (1943)); d. Chattermarks in a groove (from Reference HarrisHarris, 1943).

Fig. 9. Transverse friction cracks at site 14. Ice moved from left to right.

There are many localities where fracturing and plucking have been facilitated by the presence of jointing or cleavage in the slate. In some places, jointing is poorly developed leading to remarkably unbroken abraded areas of slate. In other places, however, abraded areas are broken by angular depressions of various size aligned along joints. Examples of removal of large plucked blocks occur at site 13, where a number of vertical joints break a steep face over 10 m high and 100 m long (Fig. 10). At site 7, the stepped appearance along the lee slope already described is partly due to transverse joints which led to the plucking of slate blocks, while at sites 9 and 12 the jointing trends north-south, somewhat oblique to the direction of ice movement, and a pronounced series of oblique trenches and ribs has resulted.

Fig. 10. Plucking associated with vertical joints at site 13. Ice moved from left to right and striae are rising at 5−10°

The role of cleavage in fracture and plucking is displayed at many of the same sites. As illustrated in Figure 11, the plucking of large blocks frequently results in flat abraded surfaces terminated abruptly by near-vertical, joint-controlled faces. On these faces, thin cleavage controlled sheets of slate have often been broken off to give an irregular appearance. This process results in a gradual retreat of the down-ice side of the abraded sections. It is probable that the same applies to joints on abraded faces. Initially, freezing of melt water may enlarge the joint but once widened other processes such as stress fracturing can act to further enlarge the basin by breaking off small fragments along cleavage planes. Support for this sequence comes from the observation that at Peris the joints are commonly enlarged in an up-ice direction. An example is shown in Figure 7.

Fig. 11. Plucking associated with slate cleavage on the lee side of the abraded pavement shown in Figure 6.

The role of melt water

Although plucking has resulted in many lee slopes that conform to the classic angular form, it was noticeable that at Peris many sharp edges had been rounded off. Indeed, smoothed lee-faces with small shallow bowls are very common in the study area (e.g. at sites 2, 3, 4, 5, 9, and 13) and an example is shown in Figure 12. Since the features resemble melt-water-produced forms observed by Reference Vivian and BocquetVivian and Bocquet (1973) in cavities below the glacier d’Argentiere in the French Alps, it is suggested that this is the most likely explanation for the widespread smoothing of Ice slopes at Peris.

Fig. 12. Smoothed and rounded slope in the lee of an abraded outcrop. Ice moved left to right.

Another example is shown in Figure 13. On the left and right of the photograph the steep faces are heavily abraded but they are separated by a patch or bedrock which in general is smooth, unstriated. and scalloped in places. Although the area concerned is 3–4 m high and up to 2 m wide, it is only a few centimetres deep relative to the abraded surfaces on either side. The implication is that a very shallow subglacial cavity existed at this point, and its failure to close must indicate rapidly moving ice. There is clear evidence that abrasion and melt water were occurring contemporaneously, for on the bedrock area on the right of Figure 13 there are places where melt-water erosion has failed to erode the deeper sections of an abraded race, yet the smooth melt-water-eroded face is itself abraded.

Fig. 13. Smoothed bedrock separating abraded sections at site 13. Ice moved lift to right.

There are a few other features for which melt-water erosion is a possible origin. At site 8 a number of curves and facets, sometimes with sharp edges and with striated grooves extending down-ice. occur on a vertical rock face (Fig. 14). They resemble some sichelwannen in a similar situation illustrated by Reference Sugden and JohnSugden and John (1976, fig. 15.1).

Fig. 14. Possible sichelwannen at site 8. Ice moved from left to right. Note the striae and also how the features largely disregarded the joints.

Figure 15 illustrates another example of a feature whose origin is in some doubt. It is a sinuous channel about 1 m wide with sharp edges in part, a striated floor, and overdeepened sections. It is one of a group of similar forms occurring at site 7. down-ice from the crest of a rock obstruction. In many ways it resembles several of the p-forms recently studied by the present author on the Isle of Mull, Scotland, though unlike the vast majority of the Mull features (and those in Figure 14), it is developed along a joint. The Mull p-forms were explained by melt-water corrasion and/or cavitation, with active ice subsequently moving through the channels to striate them (Reference GrayGray, 1981). This origin is favoured for the Llyn Peris features shown in Figures 14 and 15. Alternative processes are till squeezing (Reference GjessingGjessing, 1965) or glacial abrasion (Reference Boulton and CoatesBoulton, [^C1974]). The latter has been invoked in this paper to explain large grooves but the features in Figures 14 and 15 differ in having flat beds and only superficial striations. It is likely, therefore, that “grooves” or “channels” can be created in various ways and that some have complex origins.

Fig. 15. Striated channel at site 7 with overdeepened floor, longitudinal joint, and sharp edge on the left. Ice moved away from the camera.

Discussions and conclusions