Introduction

We report here on a subglacial landform, horned crag-and- tail (Figs 1 and 2), characterized by two parallel ridges at the lateral flanks of a bedrock crag. This landform type is morphologically distinct and unique in that it only appears in one specific lineation swarm, in contrast to other subglacial lineations with ubiquitous occurrence, such as flutings, drumlins and conventional crag-and-tails. Horned crag- and-tails appear to occur exclusively in the Ungava Bay landform swarm, and cover an area of approximately 30 000 km . They coexist with all classical lineation types in this area. They have not been reported from the other main flow-trace systems in Quebec—Labrador, Canada. During overview mapping from aerial photographs (several million square kilometres evenly distributed over the entire shield areas), we found no similar landforms in any other part of the Laurentide ice sheet area, nor in Fennoscandia. The horned crag-and-tails are important because their more complex morphology, when compared to conventional crag-and-tails, may give important clues to landform-shaping subglacial processes. If their genesis can be understood, they may also provide additional information about the history of the lineation swarm to which their occurrence seems to be restricted, the Ungava Bay landform swarm. The interpretations of the Ungava Bay swarm range from it being young and reflecting late Wisconsinan deglaciation (Reference PrestPrest, 1970; Reference Dyke and PrestDyke and Prest, 1987; Reference Boulton and ClarkBoulton and Clark, 1990), to it being a relict feature probably preserved in a frozen-bed zone during the late Wisconsinan (Reference Kleman and BorgstromKleman and others, 1994).

Fig. 1.

Geographical distribution of horned crag-and-tails in relation to three of the main ice-flow systems in central Quebec- Labrador. Grey-coloured areas show where ice-flow indicators from Reference Prest, Grant and RamptonPrest and others (1968) and Reference Kleman and BorgstromKleman and others (1994) were used for delimiting the ice-flow systems.

Fig. 2.

(a) Stereogram showing horned crag-and-tail ridge varieties (A) and small-scale glacial lineations and drumlins (B) 75 km west of the northern part of Menihek Lakes. Scale bar is 2 km. (b) A schematic outline of the horned crag-and- tails that exhibit a range of morphological variation, from extremely immature features with poorly developed horns of low relief to well-developed horned crag-and-tails with tails several kilometres long at the lateral flanks. A depression in the direct lee-side position of the crag is the common morphological feature.

Here we address two crucial questions: (1) under which glaciological conditions did the horned crag-and-tails form? and; (2) why do they only exist in the Ungava Bay landform swarm? The detailed morphology of this particular landform type is described and analyzed, and a genetic model proposed.

Physiography

The study area can be subdivided into five physiographical subdivisions (Fig. 3), the Larch Plateau, Lake Plateau, Caniapiscau Plateau, Labrador Hills and Whale Lowland. Horned crag-and-tails occur on the Caniapiscau, Larch and Lake Plateaus. Larch Plateau is dominated by an undulating surface around 600ma.s.l. in the areas between Caniapiscau, Sérigny, and Pons River (Fig. 1), and down to 400 ma.s.l. in the northern part of the study area. The Archean bedrock is widely exposed and drift is thin over most of its surface (Bo- Reference Bostockstock, 1970). Lake Plateau has been described as a rolling plain with numerous lakes (Reference HareHare, 1959), with elevations of 400 to 700 m a.s.l. The bedrock is composed mainly of Archean granites and granitic gneisses. Today, Larch Plateau is dominated by the Caniapiscau Reservoir at about 535 ma.s.l. Caniapiscau Plateau (Reference BostockBostock, 1970) or Caniapiscau Upland is characterized by massive, rounded rocky hills (Reference GreeneGreene, 1974) where fracture systems are conspicuously etched (Reference BostockBostock, 1970). The main fracture systems trend southeast—northwest and southwest—northeast. Summits around the Caniapiscau River reach 680 ma.s.l. and the floor levels of the lowest valleys in the north are around 300 ma.s.l.

Fig. 3.

The five physiographical subdivisions of the study area (redrawn from Reference BostockBostock, 1970).

Methods and Data

The glacial geomorphology was mapped by interpretation of aerial photographs at a scale of 1: 60 000. The ice-flow systems in Figure 1 are defined by coherent landform sys tems, mainly composed of till lineations. The outline of ice- flow systems outside the mapped area is based on data from Reference Prest, Grant and RamptonPrest and others (1968) and Reference Kleman and BorgstromKleman and others (1994).

The height of individual horned crag-and-tails was measured by a stereomicrometer. Topographical profiles were constructed over the area with the highest density of horned crag-and-tails (Fig. 1). The profiles were constructed from topographical maps at a scale of 1:250 000 and include crag-and-tails and horned crag-and-tails in 7.5 km wide bands on each side of the profiles. Air reconnaissance of some horned crag-and-tails was carried out about 200 km northwest of Wabush, Labrador in conjunction with detailed glacial-geological field mapping in 1997.

Results

Mode of Formation

The horned crag-and-tails are always oriented parallel to surrounding conventional till lineations (drumlins, fluting, crag-and-tails) belonging to the Ungava Bay landform swarm (Fig. 1), and show a distinctly different vertical distribution when compared to conventional crag-and-tails. A subglacial formation of the horned crag-and-tails appears clear and the directional agreement to intervening drumlins and conventional crag-and-tails suggests they formed at the same time as the other lineation features in the Ungava Bay landform swarm. This is in conflict with an earlier interpretation of these features as postglacial nivation hollows (Reference HendersonHenderson, 1956).

Processes such as subglacial lodgement (Reference FairchildFairchild, 1907; Reference Boulton, Davidson-Arnott, Nickling and FaheyBoulton, 1982), deformation of a deforming till layer (Reference Smalley and UnwinSmalley and Unwin, 1968; Menzies, 1979; Reference Boulton, Menzies, Rose, Rotterdam and BalkemaBoulton, 1987; Reference HartHart, 1997) and meltout of basal debris-rich ice (Reference ShawShaw, 1980) have been suggested for drumlin formation. These theories address the mode of deposition and shaping of drumlins, and by inference also the tails of conventional crag-and-tails (the crags assumed to be inherited irregularities of the bedrock surface). It is also conceivable that drumlins may in some cases form predominantly by erosion of an originally smooth, pre-existing drift sheet (Reference Whittecar and MickelsonWhittecar and Mickelson, 1977). Regardless of the precise mode of formation, it can safely be stated that most composite rock/drift lineations in formerly glaciated areas are of the conventional crag-and-tail type, i.e. the drift is only present in a direct lee-side position in relation to the tail.

Differences in morphology and topographical distribution between horned crag-and-tails and conventional crag- and-tails and the concentration to one specific lineation system seems to indicate that a traditional crag-and-tail formation hypothesis is not sufficient. In our opinion, any formation hypothesis should be able to explain the following characteristics: (1) that the tails begin appreciably lower than the summit of the crag; (2) the lack of deposits directly in the lee of the crag; (3) the difference in topographical distribution between horned crag-and-tails and conventional crag-and-tails; and (4) their restriction to north-central Quebec—Labrador and the Ungava Bay landform swarm.

Reference Boulton, Menzies, Rose, Rotterdam and BalkemaBoulton (1987) suggested accumulation by deforming sediment around a more-resistant mass for the barchan-like drumlins in Northern Ireland (cf. Reference Dardis, McCabe and MitchellDardis and others, 1984) and that those landforms reflect a sediment starvation, where relatively little deforming sediment moves over the summit and around the flanks of the core. However, the very specific distribution pattern, both on the local and regional scale, suggests that it is unlikely that a general characteristic such as ice velocity or a relative lack of basal debris can credibly explain the horned crag-and-tails.

We search instead for conditions, or chains of events, that could induce abrupt erosion—transport—deposition boundaries at hill-sized obstacles. A secondary requisite is that the appropriate conditions would have to favour horned crag- and-tail development at higher elevations, but the formation of conventional crag-and-tails at lower elevations.

The lack of sediment immediately behind the crag, which is the hallmark of the landform type, can result from either: (a) much more efficient removal (entrainment) of debris from this position; or (b) inhibited transport of material into the direct lee position.

Therefore, we look for mechanisms or chains of events that would allow (a) or (b) to happen. An additional requisite is that they should not be commonplace, or else these land- forms would not be restricted to one particular lineation swarm. Basal melting on the upstream side of the crag, and entrainment and removal of debris by refreezing in the lee of the crag could potentially explain the lack of lee-side deposit. But being a local mechanism related to each individual crag, it fails to explain the selective topographical distribution of horned crag-and-tails. We therefore favor an explanation of type (b), inhibited transport of material into the direct lee-side position.

The affinity of the horned crag-and-tails to topographical highs and conventional crag-and-tails to low points, and the lack of deposits behind crags which is inferred to be a result of inhibited till transport across the summits, suggests that a frozen bed at the summit may be involved. The fact that they are apparently restricted to only one lineation swarm, but lacking in all others, may indicate they did not form under steady-state conditions, but rather are the result of one particular chain of subglacial events. We suggest the following sequence of events (Fig. 5), where the first stage in formation is the existence of a non-erosive ice sheet (Fig. 5a) with fully frozen-bed conditions. This is suggested because an ice sheet with a fully thawed bed will probably form conventional crag-and-tails, instead of horned crag-and-tails. We envisage a transformation to wet-bed conditions at subglacial low points and frozen patches at higher elevations (Fig. 5b). These basal conditions obstruct till transport across the cold-based bedrock crag and thereby prevent accumulation at a direct lee-side position of the crag. Such a small-scale basal zonation allows till transport during wet- based conditions along the lower shoulders of the crag and accumulation in two tails at the lateral flanks.

Fig. 5.

Model of horned crag-and-tail ridge formation, showing the successive transformation of subglacial conditions during which these features were formed. (a) The existence of non-erosive cold-based ice is crucial to avoiding formation of conventional crag-and-tails during this stage of ice-sheet coverage. (b) The basal temperature distribution underwent a transformation from fully frozen-bed conditions to frozen only on summits. These basal conditions with thawed bed at low points and frozen patches at higher elevation prevents till transport across the cold-based bedrock crag Such a small- scale basal zonation allows till transport during wet-based conditions along the lower shoulders of the crag and accumulation in two tails at the lateral flanks. (c) The end result after a fully frozen deglaciation. These basal conditions preserve the entire horned crag-and-tail ridge system. (d) A transition from warm-based with cold patches on summits to a thawed-bed deglaciation This prevents the preservation of the horned crag-and-tail system and instead leads to infilling of the depression between the two tails.

The last phase of the formation of a horned crag-and-tail ridge is by basal freezing of the horned crag-and-tail ridge system and preservation throughout a fully frozen-bed deglaciation (Fig. 5c). This suggested scenario requires that the ice sheet undergoes a transition from frozen-bed conditions to basal melting with frozen patches and back to frozen-bed conditions. If this is not the case, formation of conventional crag-and-tails will occur (Fig. 5d).

The difference in vertical distribution may indicate that horned crag-and-tails are immature crag-and-tails, i.e. that after some time of fully thawed-bed conditions, all horned crag-and-tails would evolve into conventional crag-and-tails.

Horned crag-and-tails may develop during a chain of changes in basal conditions, with a period of patchy frozen— thawed-bed conditions being an important ingredient. Figure 6 visualizes the occurrences of horned crag-and-tails in their topographical context. It shows how a smoothed undulating surface, approximately delimiting the lower limit of horned crag-and-tails, intersects the terrain. The topography in an area north of Lac Rousson (Fig. 1) was digitized from 1:250 000 scale maps, with a contour interval of ~30.5 m (100 ft). The area includes profile A—A' and parts of profile B—B' (Fig. 1) and has a relative relief of about 150 m. The digitized data were used to construct a surface map with a grid- line spacing of 0.3 km. Kriging was used as the gridding method. The next step was to assign x, y and z values to mapped horned crag-and-tails. To account for the fact that horns adjacent to the larger crags, which typically reach higher absolute elevations, occur well below the crag summits, the z values of individual crags — 610 m a.s.l. were lowered by 40 m, z values < 610–579 m a.s.l. were lowered by 20 m, and z values < 579 m were not corrected. The smoothed surface describing the elevations of the horned crag-and-tails was subtracted from the topographical surface map. The result is a contour map where the negative values are coloured grey and the positive white, which was superimposed on the gridded surface map and indicates land above and below the smoothed surface. Areas above this smoothed surface are shown in white and terrain below it in grey. Based on the inference that the horned crag-and-tails form because frozen- bed conditions inhibit debris transport across topographical highs, we suggest that the white areas in Figure 6 approximate the frozen-bed areas during formation of the horned crag-and-tails. Similar frozen—thawed-bed patchworks in low-relief terrain have been described from northern Sweden by Reference Kleman and BorgstromKleman and Borgström (1990, Reference Kleman and Borgstrom1994) and Reference Clarhall and KlemanClarhäll and Kleman (1999).

Fig. 6.

Visualization of horned crag-and-tails in their topographical context. It shows a smoothed surface approximately delimiting the lower limit of horned crag-and-tails. We infer that the white areas approximate the frozen-bed areas during formation of the horned crag-and-tails.

Implications for Ice-Sheet Dynamics during and after formation of the Horned Crag-and-Tails and the Ungava Bay Landform Swarm

The horned crag-and-tails appear to be unique to one particular flow-trace swarm and, according to the formation hypothesis discussed, did not form under steady-state conditions, but instead required a specific chain of subglacial events for their formation.

The landform swarm in which the horned crag-and-tails occur is strongly convergent. In view of the above formation hypothesis, we suggest that it was fully wet-based in the central and distal (northern) parts, whereas the southern part, where the horned crag-and-tails occur only briefly, experienced some wet-bed conditions before refreezing. The dispersal centre during formation was to the south of the occurrence area of horned crag-and-tails and, in view of recent work suggesting frozen-bed core areas to be a normal features of mid-latitude ice sheets (Reference Sollid and SrbelSollid and Sørbel, 1988; Reference Huybrechts and siobbelHuybrechts and T’siobbell, 1995; Reference Kleman, Hattestrand, Borgstrom and StroevenKleman and others, 1997), it appears likely they formed in a transition zone between frozen and thawed bed. This is unlikely to have been a stable position of a subglacial boundary, because there are indications that the Ungava Bay swarm represents one or more rapid-flow events (Reference ClarkClark, 1999).

The horned crag-and-tails suggest that at least the southern part of the Ungava Bay swarm formed as the result of a brief period of partial basal thawing and rapid flow, followed by refreezing of the bed. This is in line with the scenario suggested by Reference ClarkClark (1999) for the glacial dynamics of the Labrador sector of the Laurentide ice sheet.

The existence of horned crag-and-tails in the Ungava Bay landform swarm may indicate unique conditions during formation, but more probably a unique chain of changes in basal conditions during a long period of glacerization in north-central Quebec—Labrador. The terrain in the area is not unusual, but the moderate relief with solitary hills may have been an important factor in favouring a small-scale frozen-thawed-bed patchwork.

The lack of eskers, the well-ordered suites of marginal meltwater channels (Reference Kleman and BorgstromKleman and others, 1994) and the lack of subglacial lineations matching the retreat pattern indicated by the meltwater landforms, suggest that final deglaciation of the study area occurred under frozen-bed conditions, conducive to the preservation of the Ungava Bay landform swarm. However, the intervening glacial history (between formation of the Ungava Bay swarm and final deglaciation) is debatable and poorly constrained, and a better understanding of the glaciodynamic context of these peculiar landforms must probably await a better understanding of the complex flow-pattern evolution in the area.

Conclusions

Horned crag-and-tails are a morphologically distinct member of the glacial lineation family. They are characterized by two flow-aligned till ridges emanating from the lateral extremities of a bedrock crag.

Horned crag-and-tails are only known from one glacial lineation swarm, the Ungava Bay landform swarm, where they occur in abundance in the proximal part of the swarm.

The present geographical distribution of horned crag-and- tails is thought to be partly a function of younger glacial erosion.

We suggest that the horned crag-and-tails formed as the result of a sequence of subglacial events involving partial thawing of the bed and preservation resulting from refreezing.