Morphology of the Ultevis plateau

The Ultevis plateau is a gently undulating mountain plateau at 800–1100 m a.s.l (Fig. 1). It is tilted slightly towards the south-southeast and has a local relief of 100–150 m. The bedrock is mostly composed of Precambrian porphyrites. Quartzites occur in the southwestern part of the mapped area (Reference KullingKulling, 1977). None of the mapped glacial-geological boundaries conform to any known bedrock structures or boundaries. The hills on the plateau surface are generally elongated in a north-northwest—south-southeast direction. The dip of the plateau surface and the topographic grain is transverse to the latest recorded ice-flow direction towards the northeast. This relationship has, as will be described later in this section, some implications for the distribution of the relict surfaces. The area bears many characteristics of a preglacial landscape such as described by Reference GjessingGjessing (1967) from southern Norway: convex-concave profiles, round summits, wide shallow valleys and open passes. Steep slopes, glacially incised valleys and lake basins are not generally present. The glacial reshaping is minor and restricted mainly to the lower parts of the plateau surface. Most of the hills are featureless and covered with sorted polygons, sorted stone stripes or boulder fields (Reference Hoppe and MelanderHoppe and Melander, 1977). Where inspected in the field, these periglacial surfaces were composed of locally derived, stony, monolithological material. No permafrost was encountered in a 1.5 m deep pit. Where glacial reshaping has taken place on the plateau surface, the ground is covered by a thin fluted or moulded till blanket. There are no eskers or other evidence of substantial subglacial drainage. Some of the preglacial surfaces have a slight glacial imprint. Older landforms, glacial or non-glacial, are preserved in that they are still discernible morphologically, but have been slightly reshaped, in most cases by faint fluting. These areas are represented in Figure 1by a light grey tone. They typically form extensions of the true relict surfaces.

Fig. 1.

Glacial geomorphology of the Ultevis plateau.

Virtually no periglacial sorting phenomena were observed to have developed in the fluted or drumlinized areas (of late Weichselian age) during postglacial time. The only ones noted were stones circles at lake shores, where the water table was close to the ground surface. Hence, the impact of Holocene periglacial processes in the area appears to have been extremely limited.

Characteristics of the relict surfaces

The relict surfaces at Ultevis are characterized by residual soils, patterned ground and ventifacted boulders. Landforms diagnostic of glacial erosion, such as lineations, lake basins, marginal moraines and glacial facets, are not present. The surface is smooth and bedrock outcrops are rare on the hill summits. The well-developed patterned ground, in the form of sorted polygons and boulder stripes, is an important diagnostic criterion for the relict surfaces. The patterned ground and fluting spatially are mutually exclusive, which would not be the case if the development of the patterned ground postdated the fluting.

Sparse, but well-established vegetation of grasses, mosses and dwarf birch grows in the finer material between boulder stripes. The individual boulder circles and stripes are hardly visible in the aerial photographs, but the regular pattern of boulders and the sparse grass cover on the fine material creates an easily discernible spotty, velvety texture in the aerial photographs. This texture is an important marker when mapping the relict surfaces in aerial photographs.

Landforms within the relict landscape and relative ages

On Tjate Hill (Fig. 2a and b), the regular pattern of boulder stripes is disrupted by a mound of glacially derived debris. The mound is about 2.5 m high and 20 m in diameter and is situated on the southwestern slope, about 100 m from the crest of the elongated hill, at an elevation of approximately 950 m a.s.l. No permafrost was encountered in a 1.5 m deep pit which was dug close to the edge of the mound. Stratigraphical investigations of the site show that the mound sits on top of the patterned ground and consists of material different from the underlying residuum. The material of the mound is a coarse sediment with a greyish matrix of coarse sand. Rounded cobbles, up to 150 mm in size, are frequent. The lithological composition of these stones is very diverse. A simple stone count of 100 stones gave 25 different lithologies. Not a single cobble consisted of the porphyry that constitutes the local bedrock. The mound material does not show any surficial signs of cryoturbation processes. Beneath the mound, the material is similar to the ground surface surrounding the mound; a reddish residuum with angular boulders. The boulders have a monolithological composition of porphyry with the sorted stripes still well preserved. In the excavation pit, we found two buried boulder stripes and intervening coarse sand. The transition between the two units is sharp and the voids between the boulders are still open and not filled in with the superimposed glacial debris (Fig. 2c). We regard the glacial mound on Tjate Hill as very strong support for a pre-late Weichselian age of the mapped relict surfaces. As formation of patterned ground implies ice-free conditions, and as the mound is a clear sign of later glacial transport into the area, the patterned ground must be inherited from an earlier interstadial or interglacial. These features are fragile and would easily be destroyed if basal sliding occurred even during a very brief period. We suggest that the material was transported englacially into the area, which under frozen-bed conditions could occur without destruction of the basal interface.

Fig. 2.

Mound of glacial material superimposed on fossil patterned ground, (a) Oblique aerial photograph, (b) Ground view, (c) Stratigraphical section. Lower part is a buried stone stripe. Voids between stones are not filled in with fine material. Topmost part is glacial material of the overlying mound. (d) Cross-section of glacial mound with underlying stone stripes.

The only other major glacially related mechanism that can be traced on the relict surfaces is the action of marginal meltwater run-off. The imprint of glacial meltwater exists in the form of well-shaped lateral meltwater channels, which are in agreement with the concept of cold-based ice (Reference Sugden and JohnSugden and john, 1976; Reference Sollid and SørbelSollid and Sørbel, 1988; Reference DykeDyke, 1993; Reference Kleman and BorgströmKleman and Borgström, 1996). As meltwater cannot penetrate cold ice, the water runs alongside a glacier tongue cutting a channel into the hillside. This mechanism only occurs when the ice is so thin that the hills protrude above the glacier surface. Between the channels, the ground bears no sign of glacial modification. The lateral channels are incised in residuum in several localities, similar to relationships described by Reference KaitanenKaitanen (1969) and Reference DykeDyke (1993) and thus demonstrate that those deposits are not postglacial.

Lateral channel systems occur in two different generations on the Ultevis plateau. The most extensive system was created by a southeast-flowing ice sheet with a margin generally retreating towards the northwest. Because of the funnelling effect of the valleys, the meltwater was steered along the flanks of the northwest—southeast trending hills. These channels are in many places cross-cut by a younger system indicating drainage towards the northeast. The older southeast-trending channels fit well to the reconstruction by Reference Kleman, Hättestrand, Borgström and StroevenKleman and others (1997) of the early Weichselian ice sheet. The subdued appearance of these features also suggests they are of considerable antiquity. One of these localities, in the southeastern part of the investigation area, was described by Reference RodheRodhe (1988). Other evidence for a major southeasterly ice flow is a group of very large lateral moraines on the northeastern slope of the Ultevis plateau (Fig. 1). These moraines can, with the exception of minor gaps due to stream erosion, be followed over 15 km and are, in part, at least 30 m thick. They were created by lateral deposition by an outlet glacier draining an older mountain-centred ice sheet. Erosion during the last deglaciation reshaped the top of the moraines slightly and left a faint fluting at right angles to the lateral moraines. Based on this direction, the fluting must be linked to the deglacial phase as it can be traced further down-ice, where it also conforms to the deglacial esker pattern (Reference KlemanKleman, 1992; Reference HättestrandHättestrand, 1998).

Landforms bordering the relict surfaces

Reference Kleman and BorgströmKleman and Borgström (1994) described transverse lee-side till scarps as a landform frequently occurring at the transition between an up-ice frozen-bed patch and a distal thawed zone. Such transverse lee-side till scarps are frequent in the Ultevis area. Since there is reason to believe that plucking on the lee side of hills can occur, and has occurred, in any type of loose deposit, we henceforth use the broader term“transverse lee-side scarp”.

A lateral sliding boundary separates a zone of subglacial lineations from adjacent areas with morphology (till lineations) indicating a completely different ice-flow direction, or displaying relict non-glacial morphology. The very narrow transition (10-50 m) found at many locations (Reference Kleman and BorgströmKleman and Borgström, 1994) is easily detected in aerial photographs, but may be difficult to discern in the field. Two lateral sliding boundaries have been identified in the investigation area. The first one is at Mount Tjuolma, where it separates a relict area with patterned ground and old meltwater channels from the late Weichselian drumlinized landscape (Reference KlemanKleman, 1992). The drumlinoids cut across the old meltwater channels and have partly destroyed them, but the channels are still discernible between the drumlin ridges. The other lateral sliding boundary is situated in the southeasternmost part of the investigation area. Like the Tjuolma boundary, this one is sharp and separates two landscapes with different textures; a relict smooth surface and a late Weichselian eroded surface (Fig. 3). Like the lateral boundaries described by Reference Dyke and MorrisDyke and Morris (1988), those on Ultevis do not coincide with any abrupt change in slope.

Fig. 3.

Transverse lee-side scarp, (a) Vertical aerial photograph showing relict surface (lower left) and eroded surface (upper right). (b) Ground view of transverse lee-side scarp.On distal side (right) is a blanket of boulders tranported in the ice-flow direction.

Transverse lee-side scarps are numerous on the Ultevis plateau. Most hills show a sharp break in texture on the northeastern slope, which constitutes the proximal end of the relict surface. This break is the actual scarp, often made up of a step in the ground surface down to the weathered bedrock. Distally, the material from the scarp has been drawn out as boulder blankets or flutes, in the direction of ice movement. The boulder frequency diminishes in the inferred direction of flow.

Formation of lee-side scarps

Transverse lee-side scarps are very conspicuous landforms of an ice-sheet bed with mixed temperature characteristics. They constitute most of the distal boundaries of the relict patches in the area and offer an opportunity to study the very sharp break in texture between relict and eroded surfaces. The formation mechanism for these scarps is far from clear. When they formed, a frozen patch existed immediately up-ice and there must have been minimal basal water present at the location of the scarp. We suggest that the area immediately down-ice of the transverse scarps did not experience true wet-bed conditions. Rather, the coupling between soil and bedrock became weak when the phase-change surface (PCS) rose to the soil—bedrock interface. The decreased effective pressure on the lee side of topographical highs facilitated brittle fracture and plucking of the still-frozen till sheet. Direct evidence for wet-bed conditions, such as true moulding of the till sheet, is only found slightly lower in the terrain and at some distance from the scarps.

Importance of convergence—divergence patterns for basal temperature

Reference GlasserGlasser (1995) modelled the temperature distribution for a transect of the Scottish ice sheet. He stressed that the bed topography was critical in determining the location of areas of basal melting. Increased strain heating from convergent flow in lower areas caused the temperature to rise to the melting point. At Ultevis, an area of more gentle relief, convergence of flow does not seem to be as important. If strain- heating led to streaming, the relict patches should be elongated in the direction of flow, but no such pattern is apparent in Figure 1. Instead, the elongation of individual patches is governed by the topography. Furthermore, the flow traces should be divergent on the up-ice side of the relict patches and convergent on the down-ice side. No such pattern is to be found in the area.

Sequence of events (Table 1)

The first early Weichselian ice sheet left a significant glacial landform record. Previous glacial deposits were largely eroded and redistributed (Reference LagerbäckLagerbäck, 1988b; Reference Kleman, Hättestrand, Borgström and StroevenKleman and others, 1997; Reference HättestrandHättestrand, 1998). Landforms on Ultevis that can be ascribed to that stage are the large lateral moraines and the southeast trending lateral drainage channels. The early Weichselian ice sheet did not necessarily erode the higher parts of the landscape. The non-glaciogenic properties of the hilltop soils, and the direct evidence of later ice- sheet overriding, implies they could be pre-Weichselian in age. However, the patterned ground in these soils developed its present appearance during one or more Weichselian interstadials. During the middle Weichselian and the major part of the late Weichselian, the area was covered by cold-based ice and no reshaping took place. During the Last Glacial Maximum (LGM), the ice divide was situated far out in the Gulf of Bothnia and, as the deglaciation proceeded, it migrated westward towards its last position in the Scandinavian mountain chain (Reference LjungnerLjungner, 1949; Reference KlemanKleman, 1992). There is no imprint of this ice flow expected from the east during the LGM, but from the latest stage, when the ice divide had moved over the area to a westerly position. The ice flow was then from the southwest. The glacial imprint at this last stage is strongly associated with a partly melting bed. As the ascending PCS met the bed at the lower parts of the terrain, valleys were the areas that first experienced basal melting and glacial erosion, in line with glaciological theory (Reference Hughes, Denton and HughesHughes, 1981). A continuously rising PCS would eventually lead to a completely thawed bed, but hilltops would remain cold-based the longest. At Ultevis, the rising of the PCS probably continued until the ice-marginal retreat exposed the area. No more signs of glacial erosion can be seen in the up-ice direction (Reference HättestrandHättestrand, 1998), which is interpreted to reflect fully frozen-bed conditions on the eastern side of the last ice-sheet remnant. The distance to the last ice divide was less than 70 km.

Table 1.

Tablet Sequence of events at the Ultevis plateau.

The short duration of active erosion can also explain the only slightly eroded surfaces, where older landforms are mainly preserved despite some fluting overprint.

Glaciological implications

The area we have studied appears to have been located in a transition zone between two basal thermal regimes. Further northeastward (down-ice), the landscape has experienced fully wet-based conditions and is characterized by a conventional wet-bed glacial-landform assemblage with large drumlins and eskers. Southwestward, on the up-ice side, the landscape lacks any subglacial landform record at all from the late Weichselian. For individual landform types, the transition along the northeast—southwest gradient is gradual. Eskers go from large and continuous to small and fragmented and are finally absent. Instead, lateral drainage channels are more frequent in the inner zone, suggesting that the meltwater drainage became more and more supra- glacial. Drumlins undergo a similar transition from large and frequent to less significant, finally giving way to fluting and boulder blankets or boulder streaks. Despite differences in topography, this is a general pattern remarkably similar to the one reported by Reference Dyke, Morris, Green and EnglandDyke and others (1992) from Prince of Wales Island, Northwest Territories, Canada, where drumlins diminish in size and frequency, but relict patches of older landforms gradually become more abundant towards the head of a palaeo ice stream. Observations from other areas, such as Southampton and Baffin Islands, Arctic Canada, and Varanger Peninsula, Norway (Clarhäll and Kleman, unpublished maps) suggest that the observed “archipelago-type”” boundary between frozen and thawed- bed zones is a normal ice-sheet feature.

The individual relict patches on the Ultevis plateau are on the order of 1–10 km. They are usually elongated in the northwest—southeast direction, which is in accordance with the general elongation of the hilly topography. Hence, there is no significant tendency for elongation in the ice-flow direction, although two sliding boundaries are strictly parallel to the ice-flow direction. Such lateral boundaries appear to be more abundant in terrain where the topographical grain parallels the ice-flow direction (Reference Kleman and BorgströmKleman and Borgström, 1994). We suggest that the development of positionally stable, lateral, sliding boundaries is favoured by a suitable flow-parallel topography, with the most extreme manifestation being the self-enhancing system of selective linear erosion (Reference Sugden and JohnSugden and John, 1976).