Introduction

Reconstructions of the geometry of former ice sheets and their evolution through time can be made by piecing together the fragmentary geomorphological and geological evidence that they leave behind. Changes of ice-sheet extent can be reconstructed utilizing stacked glacial—nonglacial deposits to define the position of the ice-sheet perimeter in space and time. Internal components of ice-sheet geometry, the flow patterns and ice divides, can be reconstructed from ice-flow indicators such as erratic dispersal, glacial striae and subglacial bedforms. Of these, subglacial bedforms provide the most frequent and spatially extensive evidence of ice flow which is often used to build or support ice-sheet reconstructions (e.g. Reference Dyke and PrestDyke and Prest, 1987; Reference Boulton and ClarkBoulton and Clark, 1990a, Reference Boulton and Clarkb; Reference Kleman, Hättestrand, Borgström and StroevenKleman and others, 1997).

Subglacial bedforms include flutes, megaflutes, drum- lins, and megalineations (Reference ClarkClark, 1993), all of which are drift landforms produced parallel to ice flow, hereafter termed as subglacial drift lineations. Ribbed (Rogen) moraine are also bedforms, but are not dealt with in this paper. Together, they probably cover over 80% of former ice-sheet beds and have important palaeoglaciological information encoded within them. If we had complete knowledge of their pattern, distribution and genesis, we would be able to make unequivocal reconstructions of aspects of the geometry of the ice sheets that produced them. Such knowledge has remained elusive, leading to a range of competing theories of formation which, when applied to a sample of the bedform population, has inevitably led to widely varying reconstructions of former ice sheets. This is illustrated by the radical changes of view regarding Laurentide ice sheet geometry over the last 40 years (cf. Reference PrestPrest, 1990). Because of different assumptions made about the glaciodynamic context of bedform generation, some reconstructions produced a large single-domed model and others a smaller multiple-domed ice sheet. These are large differences in terms of overall ice volume, height and surface profile and have major implications for palaeoclimate, sea level and isostasy.

At the simplest level, subglacial lineations can be used to deduce the orientation and direction of ice flow. As they are formed by the action of ice moving over the substrate, it is also widely presumed that this indicates a warm-based thermal regime at the time of generation (e.g. Reference Kleman and BorgströmKleman and Borgström, 1996). In order to derive from them a greater level of palaeoglaciological information, we need to know:

1. (1) What were the processes of generation?

   There are numerous qualitative hypotheses, inferences and associations that attempt to relate landform and process, and a number of theories. Conclusive proof has not been forthcoming. According to different theories of formation, a drumlin field, for example, could be taken to infer widespread subglacial sediment deformation (Reference Boulton, Menzies and RoseBoulton, 1987) or a subglacial flood event (Reference ShawShaw, 1994). Ribbed moraines could be used to infer zones of compressive ice flow (Reference BouchardBouchard, 1989) or extending flow at a transition in basal thermal regime (Reference HättestrandHättestrand, 1997).

2. (2) What was the glaciodynamic context of generation?

   If we knew the answer to (1), it would be possible to deduce logically their glaciodynamic context; where, beneath the ice sheet were they generated? We are left wondering whether they formed close to the margins or over large areas within internal portions of ice sheets, or were they restricted to certain glaciodynamic phenomena, such as in ice streams or surges?

This paper focuses on the second and more infrequently posed question, as it is critical in terms of how we use land- form patterns to build reconstructions of ice sheets. The key questions are:

1. (1) Under which portions of ice sheets were bedforms generated?

2. (2) When, during the glacial cycle, were they generated?

3. (3) How can they be preserved beneath subsequent ice flow?

4. (4) What are the implications for palaeoglaciology?

Glaciodynamic Context of Bedform Generation

As former ice sheets produced bedforms in abundance, it is likely contemporary ice masses are doing the same. If geophysical methods could remotely sense the bed of contemporary ice sheets in enough detail, we could build up a picture of the glaciodynamic context of particular bedform types. Megalineations, for example, might only be found under active ice streams. Such associations between glaciology and landforms could then be used in inverse mode to convert maps of glacial geomorphology of exposed ice-sheet beds into the palaeoglaciology that produced them. Until such time when this approach is practical, we are forced to either make gross assumptions or to examine the now-exposed beds of ice sheets and try and relate the bedform patterns to our knowledge of ice-sheet geometry and history.

This approach, however, has led to some confusion, as subglacial bedforms have often been used to bolster or fill gaps in a reconstruction, without due regard to the uncertainties of their location and timing of generation. Critical assumptions have often been made without explicit comment, and the questions explored in this paper have often been circumvented by simplifying flow patterns into “generalized flow- lines”. In this section, we review the range of possible assumptions and modes of interpretation, provide examples from the literature and critically examine these alternatives.

Subglacial lineations tend to exist as collections of land- forms rather than as isolated individuals, a field of drumlins being the classic example. Once the landforms are mapped, it is relatively straightforward to group similar landforms into spatially coherent and distinctive patterns which Reference ClarkClark (1994, Reference Clark1997) has called flow-sets. This grouping is usually performed by subjective visual pattern recognition, based on some combination of the following criteria:

1. (1) Parallel concordance: each landform should have a similar orientation to its neighbours.

2. (2) Close proximity: each landform should be closely packed with its neighbours. The spacing will typically be of the order of up to two to three times the dimensions of the landform.

3. (3) Similar morphometry: neighbouring landforms usually display similar morphometry.

To be able to use these flow-sets to derive information about the ice sheet, we need to ascertain, or make assumptions, about their glaciodynamic context; do they record submarginal, or interior flow patterns or the activity of individual ice streams of lobes? Were the flow-sets generated under buildup, maximum or retreat stages of the ice sheet?

Following from Reference ClarkClark (1994) and Reference Kleman and BorgströmKleman and Borgström (1996), we can build a logical argument as follows. All land-forms within a flow-set may have been created either synchronously or incrementally at successive time-steps. This is demonstrated in Figure 1, where individual lineations forming a flow-set (Fig. 1a) may either have all formed at a single point in time or successively through time. For the former, we can use the flow-set to infer actual palaeo-flowlines and draw form lines perpendicular to these, representing the surface form of the ice sheet (Fig. 1b). For the latter case, the most likely explanation is that the bedforms were generated in a zone behind a retreating ice margin (t ₁-t ₃ in Fig. 1a and b), thus laying down a time-transgressive pattern, that becomes younger in an inward direction. The synchroneity of bedform production within a flow-set is therefore the key to answering the questions posed earlier: under what portions of the ice sheet were they generated, and when during the glacial cycle? Our main question therefore reduces to: was the flow-set produced isochronously or time-trans- gressively?

Fig. 1. (a) Flow-set of subglacial drift lineations that may have formed isochronously at time t_n or time-transgressively from t₁— t₃ or t_a — t_c. (b) Alternative modes of interpretation of such a pattern. (c) Consequent presumptions about glaciodynamic context, as either along extensive palaeo-flow- lines or restricted to submarginal positions.

A hypothetical range of glaciodynamic contexts, under which subglacial lineations could form, are illustrated in Figure 2. It is assumed that the generation of subglacial lineations is restricted to warm-based ice and appropriate “envelopes””of basal shear-stress, sediment supply, sediment rheology and hydrology. These conditions are likely to vary considerably over local and regional-scale distances and over time (cf. Reference Piotrowski and KrausPiotrowski and Kraus, 1997). At the ice-sheet scale, lineations cannot form beneath ice divides because of very low basal shear-stresses in these areas, i.e. little or no horizontal velocity component, and cold-based ice will similarly inhibit bedform production. The schematic ice sheet (Fig. 2) is subdivided into a bedform record restricted to submarginal generation (left-hand side) and hence time-trans- gressive formation, and a record that is created by isochronous formation (right-hand side). Each glaciody- namic context is discussed below.

Fig. 2. Schematic ice sheet illustrating range ofglaciodynamic contexts under which subglacial lineations may be generated; time-transgressive (left) and isochronous generation (right).

Criteria to Distinguish Time-Transgressive and Isochronously Generated Drift Lineations

In this section we argue that lineations within a flow-set, generated time-transgressively or isochronously, will display different and perhaps distinctive, spatial and morphometric characteristics. Table 1 summarizes how the three main factors of ice thickness, flow topology and stability permit predictions to be made of the consequent lineation characteristics. Time-transgressive generation is conducted close behind a retreating ice margin, where we would typically expect thin ice cover, lobate margins and rapidly varying flow patterns with occasional margin stillstands during recession. This contrasts with isochronous generation, which predominantly forms some distance from the margins where we would expect thicker ice with internal rather than marginal flow patterns and, consequently, much greater stability. It is argued that these contrasting conditions should produce distinctive lineation patterns.

Table 1. Distinguishing criteria for time-transgressive and isochronously generated drift lineations.

The planform shape of terrestrial ice-sheet margins are usually crenulate, consisting of a series of lobes produced by strongly diverging flow patterns. This characteristic splaying flow pattern is markedly distinct from the types of flow topology experienced within the interior portions ofthe ice sheet. This provides a useful criterion for identifying lineation flow-sets produced submarginally. Added to this is the nature of lineation patterns that should accrue as these splayed flow patterns retreat (Reference ClarkClark, 1994). As lobes are typically of low profile with thin ice cover, the trajectory of lobe retreat is highly influenced by topography and subglacial geology. This is likely to lead to individual lobes changing shape and position as they retre producing a complex flow-pattern record. Under these conditions, it is likely the lineation record will display cross-cutting and superimpositions. In inverse mode, we can thus interpret a broadly splayed set of lineations with cross-cuts as representing a time-transgres-sive flow-set, recording margin retreat. A good example of this is demonstrated by Reference MooersMooers (1989) for part of the southern margin of the Laurentide ice sheet.

When the bedform-generating episode is short, in relation to how quickly flow directions may vary (i.e. isochronous generation), the lineations should display high- parallel conformity with their neighbours and aspects of their morphometry, such as elongation ratio, should vary in a systematic and gradual manner over space. This is because the whole flow-set formed in-an-instant and its characteristics should reflect this. The converse situation, whereby flow patterns actually vary during the bedform- generating episode, will produce a less well-ordered linea- tion pattern. This is what we expect of time-transgressive flow-sets. Such lineations may have slightly different orientations than their neighbours (low-parallel conformity) and spatial variations in morphometry are likely to contain abrupt discontinuities, reflecting changes in subglacial conditions arising from phases of more rapid margin retreat, separated by stillstands. Indeed, quantitative investigations of drumlin fields have often reported a transverse banding in their morphometry (e.g. Reference HillHill, 1973; Reference Patterson and HookePatterson and Hooke, 1995) which we take as a key indicator of a time-transgres- sively produced flow-set. Figure 3 illustrates these differences in morphometry and spatial pattern.

Fig. 3. Predicted characteristics of lineation pattern arising from isochronous (a) and time-transgressive (b) generation. An isochronously produced flow-set should contain lineations of high parallel conformity, no cross-cuts and with gradual variations in morphometry (see inset graph of A—B). Conversely, for the time-transgressive case, we expect low parallel conformity, possible occurrence of cross-cuts and abrupt discontinuities in morphometry (transverse banding of inset graph). Associated and appropriately aligned eskers and end moraines provide further evidence.

Landform associations can also be used as a guide. If a flow-set is accompanied by a series of marginally produced retreat moraines that are orthogonal to the lineation orientation, then it is safe to presume the whole land-system assemblage was laid down time-transgressively. A similar argument has been made for eskers that are found to lie in an approximately parallel arrangement with lineations (Reference KlemanKleman, 1990). Although there is still some debate (cf. Reference Menzies, Shilts and MenziesMenzies and Shilts, 1996), sub- or englacial conduits and their sedimentary product, eskers, are usually regarded to be time-transgressive features, with formation occurring close to the ice margin as it steadily retreats (Reference Hebrand and ÅmarkHebrand and Årmark, 1989; Reference Kleman and BorgströmKleman and Borgström, 1996; Reference Menzies, Shilts and MenziesMenzies and Shilts, 1996). If this interpretation is true for all eskers, then, when they are found in subparallel arrangement with lineations, they must record time-transgressive retreat patterns. This association of eskers and lineations is an extremely common occurrence for the Laurentide and Fennoscandian ice sheets, and is usefully described as a “wet-bed deglaciation fan” by Reference Kleman and BorgströmKleman and Borgström (1996).

The means of distinguishing between time-transgressive and isochronous lineament generation is thus by careful observation of flow topology, cross-cutting, the degree of parallel conformity and the nature of the spatial variation in morphometry. If a whole lineation field was generated in a single phase, we would expect the pattern to be well-organized, coherent and with no obvious discontinuities. But for formation arising from time-transgressive retreat, the pattern should be more variable with lineations displaying less-parallel conformity, and with cross-cutting patterns and abrupt changes in morphometry. Additionally, landform association with retreat moraines and eskers helps to confirm a time- transgressive mode of formation.

Bedform Preservation

The preservation of land surfaces beneath ice sheets is an important issue in palaeoglaciology, as it is critical for determining ice-sheet extent (e.g. Reference SugdenSugden and Watts, 1977), for apportioning subglacial land-systems to specific glacials and times within them (e.g. Reference KlemanKleman and others, 1994; Reference Boulton and ClarkBoulton and Clark, 1990a, Reference Boulton and Clarkb) and for determining the thermal evolution of ice sheets (e.g. Reference Sollid and SørbelSollid and Sørbel, 1994; Reference Kleman, Hättestrand, Borgström and StroevenKleman and others, 1997).

Preservation of old landforms, surfaces and deposits beneath ice cover has long been reported (e.g. Reference IvesIves, 1966; Reference SugdenSugden, 1968; Reference Rose and LetzerRose and Letzer, 1977; Reference SugdenSugden and Watts, 1977). More recently, it has been shown that preservation can easily occur and is, in fact, quite widespread (e.g. Reference KlemanKleman, 1994). There are numerous examples of surfaces, deposits and landforms that lie out of accord with known deglacial patterns and are therefore inferred to be preserved remnants from earlier in the glacial cycle or from previous glacials.

It is important at this stage to be clear as to what we mean by the term preservation. The purist form of preservation is where the actual land-surface is left virtually unmodified, which we can call surface preservation (Fig. 4a). Subglacial survival of periglacially produced stone circles is an example of this type (e.g. Reference GoldthwaitGoldthwait, 1960). Deposit preservation is a situation whereby older deposits have survived erasure but the current surface is in fact an erosional unconformity, such that we do not know how much of the original deposit is missing (Fig. 4b). A similar situation may also arise concerning the shape that defines a landform. A large drumlin, for example, may suffer considerable erosion by over-riding ice and, yet, the subdued form may still retain the characteristic shape of a drumlin leading us to identify it as such. This can be termed landform preservation (Fig. 4c). Larger landforms, such as mega-scale lineations, will have a stronger potential for preservation than smaller forms such as flutes. It is important not to confuse these different degrees of preservation, as we have a range of modification from none to perhaps up to tens of metres of erosion or modification. Unless the original land surface can be identified, deposit- and landform-preservation cannot be taken to indicate a complete lack of modification by subsequent ice flow.The implication of the different degrees of preservation is that it should not be universally treated as a binary switch, which is either on or off. For the deposit- and landform-types of preservation, where modification is gradually occurring, the duration of flow will clearly be important.

Fig. 4. Preservation beneath ice sheets can be split into three categories, depending upon the degree and depth of modification. Surface preservation requires no modification, whereby delicate features such as periglacial stone circles are protected. Yet for deposit and landform preservation, many metres of erosion/ modification may have taken place without this being apparent.

A plausible and logically complete ice-sheet reconstruction requires a mechanism or explanation that accounts for the preservation of landscape patches. Simply put, we get preservation when basal shear-stress is lower than bed strength. Three possible explanations for subglacial preservation are explored below.

Preservation by shallowing of deformation layer or basal uncoupling

The response of a bed of soft sediment to the normal and shear stresses applied by over-riding ice flow is highly dependent on meltwater production and drainage. This is because high pore-water pressures reduce bed strength which encourages deformation and hence modification of the geology and landforms of the bed. Figure 5 illustrates four possible hydrologically controlled states which a soft- sediment bed may experience. Different pore-water pressures exert a control on the strengths of the sediment and ice—bed interface. For very low water pressures, a stable rigid bed should exist, but with the surface experiencing some sliding, ploughing and limited brittle shear (Fig. 5c; Reference Benn and EvansBenn and Evans, 1998). Higher pore-water pressures will lower the sediment strength and promote ductile deformation which may be shallow (b) or deep (a) corresponding to a low or higher ice flux (Reference BoultonBoulton, 1996).Very high pressures of pore water may weaken the ice—bed interface more than the sediment body and thus promote basal sliding ((d); Reference Iverson, Hanson, Hooke and JanssonIverson and others, 1995; Piotroski and Kraus, 1997). To understand the potential for preservation, we must consider which states do not lead to actual surface lowering (i.e. erosion sensu stricto) or modification (reorganization of material). Deep deformation (a) is clearly going to reorganize the bed, and according to the deforming-bed model (Reference Boulton, Menzies and RoseBoulton, 1987; Reference HartHart, 1995), may actually generate new lineations. If we move from this state, arising from decreased ice flux or lower pwp, we have a shallower (b) or no deforming layer (c). Whilst both of these conditions are likely to modify the surface, preservation of large landforms and deposits should occur. Alternatively, a rise in pwp may lead to uncoupling of ice from the bed and basal sliding. This will also serve to preserve or, at least, minimally erode the underlying surface.

If all the preservation mechanisms discussed above were operable, then we must be cautious of simply ascribing occurrences of preservation to just one mechanism. It is tempting, for example, to ascribe all cases of preservation to cold-based ice as this is easiest to conceptualize in a reconstruction, whereas preservation that relies on low rates of modification requires extra considerations of the length of time for which it operates. In order to better reconstruct ice sheets, it would be ideal if we could distinguish between the types of preservation. This, however, is likely to be hard. A further complication is that the mechanisms may be inextricably linked. If we consider a situation of decreasing ice flux, the ice—bed interface will experience progressively less shear stress which will promote preservation, but there may also be a reduction in strain heating which may be enough to change the thermal regime from warm to cold-based.

Fig. 5. Four hydrologically controlled states experienced by a soft-sediment bed, split into relative categories concerning their potential for generation and preservation. Deep deformation (a) will reorganize the bed and may generate new lineations. Moving from this state, arising from decreased ice flux or lower pwp, we have a shallower (b) or no deforming layer (c), both of which are likely to modify the surface, but may preserve deposits or large landforms. A rise in pwp (d) may lead to uncoupling of ice from the bed and basal sliding, minimally eroding the underlying surface.

Bedform Generation and Preservation under the Labrador Sector of the Laurentide Ice Sheet

The Quebec—Labrador sector of the Laurentide ice sheet, Canada, is used to demonstrate how the preceding arguments can be used to help decipher glacial history from the bedform record. This sector formed one of three major components of the ice sheet during the Wisconsinan glaciation, covering an area > 3 000 000 km² and probably reaching the order of 2 km in thickness. The bedform record was originally mapped from aerial photographs to produce the Glacial Map of Canada (Reference Prest, Grant and RamptonPrest and others, 1968) and has been more recently mapped from satellite images (Reference Boulton and ClarkBoulton and Clark, 1990a, Reference Boulton and Clarkb; Clark and others, submitted). Using a variety of assumptions about the glaciodynamic contexts of lineation generation, there have been a number of radically different interpretations: that all bedforms were sheet-flow submarginally restricted, producing a deglacial reconstruction (Reference Bryson, Wendland, Ives and AndrewsBryson and others, 1969; Reference Boulton, Smith, Jones and NewsomeBoulton and others, 1985); sheet-flow pervasive, producing a maximal configuration (Reference ShiltsShilts, 1980; Reference PrestPrest, 1984); or sheet-flow patch, recording a migrating ice divide (Reference Boulton and ClarkBoulton and Clark, 1990a, Reference Boulton and Clarkb). Whilst the former two models do not incorporate preservation of land systems in a significant way, Reference Boulton and ClarkBoulton and Clark (1990a, Reference Boulton and Clarkb) invoke protection beneath ice divides to explain aspects of their bedform record, which Reference KlemanKleman (1994) reinterprets using the distribution and character of meltwater channels to indicate cold-based ice as the preserving mechanism.

New mapping, along with the considerations of glaciodynamic context discussed in this paper, have permitted Clark and others (submitted) to produce a revized model of glacial history for the region. Lineations were grouped into flow-sets (Fig. 6a) and judged to be isochronously or time-transgressively produced according to the rules outlined earlier. In conjunction with associations with esker and moraine patterns, this allowed the glaciodynamic context of each flow-set to be ascertained, or assumed (Fig. 6b). When viewing the lineation characteristics, there is a striking contrast between those that comprise flow-set (a) which fulfil the time-transgressive criteria and have associated moraines and a dense and parallel network of eskers, and those that drain northwards (b) and (d)—(g), which display the criteria of isochronous formation.

Fig. 6. (a) Subglacial drift lineations of Quebec—Labrador, summarized into flow-sets (after Clark and others, submitted). (b)Flow-sets arbitrarily referenced from (a) to (g). Using the criteria described in this paper, flow-set (a) was produced time-transgressively and the rest generated isochronously. The inferred glaciodynamic contexts of flow-sets are as follows: (c) and (d) as sheet-flow patch; (b) as sheet-flow patch or surge; (e), (f) and (g) as ice streams; and the large set (a) as sheet-flow submarginally restricted. Transect marked X—Y forms the basis of Figure 7.

To make sense of the overlapping flow-sets of Figure 6 requires a reconstruction with changing flow geometry and zones of lineation generation—preservation through time. Figure 7 illustrates a schematic version of part of the reconstructed flow history, which attempts to explain the context of lineation generation and preservation as the ice sheet retreated. Focusing on the main lineation sets, this reconstruction manages to explain why most of the lineations of flow-sets (a) and (b) are extremely clear and well-formed, whilst those in the overlap region of (a)-on-(b) (see point Z, Fig. 6) are subtle and subdued. This is because they narrowly escaped erasure due to the brief period of lineament generation during deglaciation that overprinted flowset (a). North of this area the lineations of flow-set (b) appear well-defined and fresh due to cold-based preservation.

Fig. 7. Time-distance plot of a schematic reconstruction of ice-sheet history along transect X—Y (see Fig. 6) from glacial maximum until disappearance. This illustrates the context of linealineament generation and preservation beneath an evolving ice sheet. The southern margin and ice divide retreated northwards, along with zones of cold-based based ice (stippled), low velocity promoting preservation (blank), and lineation generation (crosses). Horizontal lines schematically illustrate the inferred glaciodynamic contexts of flow-sets, (a), (b) and (f). “Viewing” the glacial history along time-line 1 for a fixed point on the transect, we can see that at the glacial maximum the area experienced low velocity promoting preservation of possibly earlier-produced bedforms, but which were completely erased during passage of the lineation-generation zone producing flow-set (a). The north— south extent of (a) was built up time-transgressively behind the retreating margin. Time-line 2 illustrates the presumed warm-based surge event that isochronously produced flow-set (b). These landforms were preserved under cold-based ice and then, for a brief period during deglaciation, they experienced a new phase of lineament generation, subduing their form and overprinting a new pattern. This contrasts with time-line 3, where an ice stream (f) and surge (b) event produced bedforms that have been perfectly preserved beneath the retreating cold- base ice sheet. Note this is a theoretical reconstruction, as flow- set activity, margin and divide migration etc. are not dated.

Summary and Conclusions

Subglacially produced drift lineations have long been used to build or bolster ice-sheet reconstructions, even though we are unsure of their genesis and glaciodynamic context. Reconstructions of glacial history are highly sensitive to key assumptions we make, like when during the glacial cycle and where within the ice sheet they were generated. A hypothetical range of glaciodynamic contexts for lineament generation has been explored which include: sheet-flow submarginally restricted; sheet-flow pervasive; sheet-flow patch; ice stream; and surge or re-advance. Examples of each are provided. Sheet-flow pervasive is no longer regarded as a valid context for interpreting the lineament record. It is argued that the crux of deciphering the appropriate context is whether lineations within a group, or flowset, were laid down time-transgressively or isochronously. The following characteristics are proposed for distinguishing between these styles of generation:

1. (1) predominantly splayed vs parallel-flow topologies;

2. (2) presence of within-flow-set cross-cutting of lineations;

3. (3) degree of parallel conformity;

4. (4) spatial variation in morphometry, as gradual or with abrupt discontinuities; and

5. (5) land-system associations with eskers or end moraines.

Application of these criteria to lineation patterns should help resolve uncertainty in interpreting the bedform record for palaeoglaciological reconstruction.

Increased discovery of complex bedform patterns, along with relict surfaces, landforms and deposits, has led us to realize that the erasure capability of ice sheets is much less than previously presumed. It is argued that preservation can be idealized as comprising three types: surface, deposit-and-landform preservation. Each requires a different degree of preservation, from high whereby delicate surfaces are protected, to low whereby an original landform can still be recognized in spite of metres of surface lowering or modification. The implication of this is that deposit- and landform- types of preservation should not be treated as a binary switch which is either on or off, as modification is gradually occurring as a function of ice velocity and time (Fig. 8).

Fig. 8. Degrees of preservation idealized as being controlled by a thermal switch and a time function.

Possible explanations to account for the preservation of land-system patches are explored: cold-based ice; lowvelocity basal sliding under warm-based ice; shallowing of deformation layer; or basal uncoupling.

It is concluded that preservation by cold-based ice is unlikely to account for the full range of relict land-system patches that are found, as protection is also likely to occur under warm-based ice. In these latter cases, ice velocity and hydrologic-control on sediment strength control the rate of modification, and the time elapsed determines the final amount of modification/preservation (Fig. 8).

The application of aspects of the ideas reported in this paper is made by reference to the bedform record of the Quebec—Labrador sector of the Laurentide ice sheet. A complex pattern of overlapping flow-sets can be interpreted in terms of generation and subsequent preservation by considering the thermal and basal shear-stress history of the ice sheet.

In conclusion, it is emphasized that patterns of subglacial drift lineations have a great deal of glacial history encoded in them, but we mustcareful about making specific glaciodynamic assumptions as it greatly influences the nature of our final ice-sheet reconstruction. At the very least, the range of diversity of glaciodynamic contexts of generation and preservation should be considered, and where possible spatial analysis of lineation patterns should be made to narrow the uncertainties.