Description and implications of valley moraines in upper Eskdale,Lake District
Peter Wilson
WILSON, P. 2004. Description and implications of valley moraines in upper Eskdale, LakeDistrict. Proceedings of the Geologists' Association, 115, 55-61. Moraine ridges and mounds atseveral locations in upper Eskdale, in the English Lake District, are mapped and described.Although moraine age has not been constrained by absolute dates, moraine construction musthave occurred in either a late stage of the Dimlington Stade (DS) or in the Loch Lomond Stade(LLS). The patterns displayed by the moraine ridges indicate that ice removal from the valleyinvolved active retreat/stillstands and/or readvances, rather than decay in situ. Implicationsarising from identification and consideration of these moraines are not restricted to Eskdale butextend to other Lake District valleys and testify to a more complex Late Pleistocene glacialhistory than some recent studies suggest.
Key words: moraine construction, Eskdale, Lake District, England, Late Pleistocene,Dimlington Stade, Loch Lomond Stade
School of Environmental Sciences, University of Ulster at Coleraine, Cromore Road, Coleraine,Co. Londonderry BT52 I SA, Northern Ireland
1. INTRODUCTION
Moraine ridges and mounds occur in most of thevalleys that penetrate the high fells of the English LakeDistrict. Moraines at various places have been noted,described and/or discussed on numerous occasions(Ward, 1873, 1875; Upham, 1898; Marr, 1916;Raistrick, 1925; Mitchell, 1931; Hay, 1934, 1944;Hollingworth, 1951; Gresswell, 1952; Manley,1959; Walker, 1966; Wilson, 1977; Pennington, 1978;Sissons, 1980; Clark, 1990, 1992; Clark & Wilson,1994, 2001, 2002; Evans, 1994, 1997; Oxford, 1994;Evans & Cox, 1995; McDougall, 2001; Wilson &Clark, 1998, 1999; Wilson, 2002). Several of themoraine complexes have been ascribed to glaciationduring the Loch Lomond Stade (LLS; c. 12.9-11.5 cal.ka BP) on the basis of biostratigraphical evidencefrom sites inside and outside of the moraine limits(Pennington, 1964, 1978; Walker, 1965). Because oftheir locational and morphological similarities,moraines in other valleys have been correlated withthose at the biostratigraphically constrained sites.Thus, from aerial photographic interpretation and fieldmapping of moraines and drift limits, Sissons (1980)identified the margins of 64 LLS glaciers in the LakeDistrict. Subsequent work has argued for a moreextensive LLS glaciation than portrayed by Sissons:some glacier limits have been extended and someadditional glacier sites recognized (Clark, 1992;Evans, 1994, 1997; Oxford, 1994; Evans & Cox, 1995;Wilson & Clark 1998, 1999; Clark & Wilson, 2001;McDougall, 200 I; Wilson, 2002).
Proceedings of the Geologists' Association, 115, 55-61.
Notwithstanding this large amount of fieldwork,there remain several other valleys in which prominentmoraine ridges and mounds exist. These moraines areeither unrecorded or have been regarded as older thanthe LLS and, therefore, of limited interest. Pennington(1970, 1978) expressed the view that valley-floormoraines related to stillstands of glaciers pre-datingthe LLS were virtually absent and believed that thiswas evidence for the 'rapid decay in situ' of thoseglaciers. Valley moraines beyond presently proposedLLS limits are in fact not as uncommon as Penningtonclaimed.
In the context of Lake District landscape history it isimportant that valley moraine locations and morphology are documented as these can provide insightsinto patterns of and processes associated with LatePleistocene valley glaciation. Those moraines thatlie beyond proposed LLS limits pose interestingquestions of age, origin and significance. In upperEskdale, for example, substantial areas of thevalley floor and sides carry moraine ridges andmounds. Manley (1959) noted these, but subsequentworkers (Pennington, 1978; Sissons, 1980) did notinclude them in their schemes of LLS glaciation.Furthermore, Lamb & Ballantyne (1998) in theirassessment of a high-level weathering limit on theScafell Pike massif state 'in the upper Esk valley... thereis no evidence for renewed glaciation during the LochLomond Stade'.
Whatever their age, the upper Eskdale morainesdeserve attention and require commentary because
they represent, in part, the margins of former valleyglaciers and can, therefore, inform about fluctuationsin ice mass extent. To this end, the moraines aredescribed and their possible age(s) and associatedimplications discussed, In the absence of any absolutedates for these moraines, some discussion is necessarilyspeculative,
2. STUDY AREA AND METHODS
Eskdale is a glaciated trough that served as one ofseveral major ice discharge routes during the Dimlington Stade (DS; c. 30-16 cal. ka BP), In its upperreaches, the dale is flanked on the west by the highestand wettest ground in the Lake District and intowhich several cirques have been eroded (Evans & Cox,1995). At Grid Ref. NY 227 037 the River Esk isjoined by its main tributary Lingcove Beck, withhead streams from the Esk Pike-Bowfell-CrinkleCrags ridge. Moraine ridges and mounds occur inboth valleys and also below their confluence in thevicinity of the Scale Gill tributary and Brotherilkeld(Fig. I).
Moraines were mapped in the field onto 1:10 000scale base maps with a 10m contour interval, using ahand-held global positioning satellite system (GPS)receiver with a resolution of < 10m. Details of morainecharacteristics and their surroundings were recorded ateach location.
3. MORAINE DESCRIPTION
Areas of moraine are designated A-L on Figure 1.Areas A and B are almost entirely within enclosed landimmediately up-valley of Brotherilkeld farm and bothare overlooked by debris-strewn and cliffed slopes. Themost extensive area of moraine (A) occupies theground between c. 200 m aD and the riverside flats(120-130 m Ofr) and contains several distinct ridgesthat trend down-valley oblique to the valley axis. Themost prominent of these is at the southern margin ofthe area where it forms a broad and rounded terminalslope (Fig. 2a). For the most part the moraineslack surface boulders but there are some clusters ofangular and sub-angular large boulders: maximumboulder length is 6 m. Two distinct oblique ridgesdominate area B, in the wedge of ground between ScaleGill and the River Esk. Several low mounds are alsoapparent.
Moraine mounds (area C), rising 20-30 m abovetheEsk, occur on both banks adjacent to the markedsouthward turn of the channel [NY 225 047]. Thewest-side mound is a more prominent feature than thatto the east, with sharper basal breaks of slope. Bothareas of moraine rest against rising ground on theirsouthern margin. A north-south depression c. 3 mdeep cuts across the east-side moraine close to itswestern margin.
The western margin of moraine area D is poorlydefined as a result of peat encroachment from GreatMoss. The southern and eastern margins are also illdefined because the drift thins gradually againstrising ground. Only along its northern edge does themoraine possess a sharp boundary and here it ischaracterized by three low ridges projecting fromthe hillfoot. Flanking depressions contain peat ofunknown thickness.
The southeast ridge of Scafell Pike terminates at c.600 m Of) at Dow Crag, below which is a complexof moraine ridges and mounds (area E, Fig. 2b).Most of the ridges trend obliquely down-valley.Those in the south are short and emerge from abank of hillside drift at c. 400 m Ol). The northernarea is dominated by a ridge 330 m in length thatfalls from c. 470 m to 385 m Of) at an averagegradient of 360
• Alongside this ridge to the north areshorter parallel ridges and the downslope marginof the area is delimited by a river-cut bluff. Theupslope limit of the drift merges with coarse talusaccumulations and some of the large boulders on andbetween ridges probably also result from rockfallactivity.
Moraine area F, on the east bank of the Esk, extendsnorth-south for over I km. In the north, the drift massextends from the riverside flats to a very clear limit atc. 500 m Of) and comprises a suite of nested lateralmoraines marking successive positions of a downwasting valley glacier (Fig. 2c). Stream-cut gulliesindicate drift thicknesses of 4-5 m. To the south; theupper limit of the drift descends west and passes belowslopes with numerous low cliffs. At the hillfoot, anarrow bench of drift with a river-cut outer slopeextends towards area D.
Two tongue-shaped masses of thick drift occupysteep slopes near the head of the Esk (area G). Bothareas have steepened riverside flanks, The western drifttongue has a pronounced central crestline; the easternarea has a rather subdued appearance,
Area H, in the valley of Lingcove Beck, comprises asmall drift mound and a ridge with oblique downvalleytrend. These occur across valley from the western endof area I which is a substantial area of thick driftwith a surface morphology of subdued mounds. A lobeof this drift mass extends a short distance down thehead slopes of Mosedale and there are clusters ofsurface boulders on the slope rising east from thewatershed.
Very prominent moraine ridges and mounds occurin the northern part of area J. Several ridges and chainsof mounds with scattered surface boulders, overlookedby cliffed slopes, are aligned down-valley oblique to thevalley axis (Fig. 2d). Elsewhere, although drift isextensive there are several bedrock exposures thatindicate localized variation in drift thickness. On theopposite side of Lingcove Beck there is a large extentof subdued drift (K) at c. 370--480 m 00. On its lowerslopes, this drift has broad low-amplitude ridges withoblique down-valley orientations.
Fig. 2. (a) Terminal slopes of southernmost moraine ridge in area A. Debris-strewn and c1iffed slopes overlook the moraine area. (b) Moraine ridges and mounds on thehillside below Dow Crag (area E). (c) Hillside drift (area F) showing a clear upper limit and a suite of nested lateral moraines marking the successive positions of adown-wasting valley glacier. Drift thickness is shown by the depth of the gully to right of centre. (d) Prominent moraine ridges and mounds and steep backing slope,northern part of area J, alongside Lingcove Beck.
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VALLEY MORAINES IN THE LAKE DISTRICT 59
On the lower reaches of slopes rising towards theThree Tarns col thick drift occurs in the height range c.430-550 m Ol) (area L). Tributaries of Lingcove Beckare incised in the drift and have created alluvial fansaround points of confluence.
4. DISCUSSION
The majority of the ridges and mounds describedabove are regarded as moraines constructed at themargins of former valley glaciers. Gullies and associated alluvial fans in areas F, G and L indicate somereshaping of the drift has taken place, but fluvialincision cannot account for the chevron-like pattern ofridges evident in most of the mapped areas. Theoblique down-valley trend of the ridges is also inconsistent with an origin by rock-slope failure(s), eventhough cliffed slopes overlook the most prominentridges and mounds. However, the cliffed slopes probably acted as sources of increased debris input to theice margins, thus allowing construction of larger andmore prominent ridges in those places. This interpretation is supported by the presence of less prominentridges and mounds in locations that are not overlooked by rock walls (cf. Benn, 1989). Maximum icethicknesses as indicated by drift limits on the hillsidesare 100 mat F, 80m at I and 100-110 mat K.
The only previous recognition of valley moraines inupper Eskdale appears to have been by Manley (1959).His small-scale map indicates two substantial LLS icemasses in the dale: the larger being in the Great Mossvalley beneath the Scafell-Scafell Pike-Great Endridge, the smaller in the Lingcove Beck valley. He alsoregarded Eskdale as having had the second largest areaof LLS glacier ice in the Lake District. The averagealtitude of the associated moraines was given as 350 mOf) and the climatic snowline for the glaciers as580-610 m Of). By giving an 'average' value of moraine altitude it would seem that Manley had includedin his calculation the moraines in areas A and B nearBrotherilkeld. However, his diagram of glacier extentdoes not show ice in that vicinity, and 350 m Of)corresponds to the approximate lower limit ofmoraines in both the Great Moss and Lingcove Beckvalleys.
Pennington (1978) and Sissons (1980) did notinclude Eskdale as a site of LLS glacier development,although Sissons noted that the eastern slopes ofScafell and Scafell Pike might have been expected tohave nourished glacier ice. The steep and rocky groundform was considered as unsuitable for the preservationof glacial debris. The mounds with scattered largeboulders reported by Sissons at NY 216 053, on thewest side of the Esk opposite Great Moss, andattributed to deposition of rock fall debris at the footof a snowbed, actually show exposures of bedrockand, therefore, cannot be due in their entirety tosnowbed-related processes.
Thus, subsequent to Manley (1959) researchers haveeither failed to recognize or have disregarded theEskdale moraines and have, thus, excluded the valleyfrom considerations of the extent of LLS glaciation.Although not stated explicitly, the reason for thisperceived absence of LLS glaciers is likely to be thesoutherly aspect of the axes of the two valley heads.With respect to direct insolation, this would have beenan unfavourable aspect for snow survival and itsconversion to glacier ice. Although Manley (1959)depicted LLS glaciers in other south-facing majorvalleys in addition to Eskdale (e.g. Rydal andKentmere), Sissons (1980) did not and it is his viewthat has tended to prevail. Therefore, the Eskdalemoraines present a challenge to understanding theLate Pleistocene glacial history of the Lake Districtand the following sections consider some implicationsarising from the different ages that might be assignedto the moraines.
Implications of a Loch Lomond Stade age
If a LLS age could be demonstrated for all the Eskdalemoraines it would indicate a glacier of c. 6.7 km length(Esk Hause to near Brotherilkeld) at its maximumextent. Such a glacier is likely to have received aconsiderable input of ice from the eastern side ofScafell and Scafell Pike. Five cirques have been recognized on the eastern slopes of Scafell and Scafell Pike,including two of the highest in the Lake District(Evans & Cox, 1995) and it is extremely unlikely thatthese remained empty during the LLS given theirfavourable aspects and proximity to the highest andwettest ground in the region. The absence of morainesassociated with these glaciers may be because the steepground form has permitted erosion of such features(cf. Sissons, 1980) or that moraines were produceddown-valley, outside of the cirques. This situation isanalogous to that of the eastern slopes of Bowfell andCrinkle Crags that contributed ice to the GreatLangdale valley glacier (cf. Sissons, 1980; McDougall,2001).
The Eskdale glacier may have connected with thosein Borrowdale (Grains Gill and Langstrath) throughEsk Hause and are Gap, and Great Langdale throughThree Tarns, and via cols between Scafell and GreatEnd with glaciers sourced on the west and northwest ofthat ridge. In addition, the south ridge of Esk Pikewould probably have been covered by ice as a result ofthe thickening and lateral spread of the Great Mossand Lingcove Beck glaciers. Under these circumstances, the Eskdale glacier would have been linked tothe plateau icefield system identified by McDougall(200 I). Furthermore, the upper limit of LLS glacier icein Eskdale is likely to have been very close to theweathering limit associated with the maximum altitudeof DS ice (Lamb & Ballantyne, 1998). Accordingly, theEskdale glacier would have been longer than any of theLLS glaciers mapped by Sissons (1980) but would have
60 P. WILSON
been exceeded in length by the LLS glaciers inLangstrath and Great Langdale as mapped byMcDougall (2001). In Manley's (1959) scheme of LLSglaciers, the Eskdale glacier was second largest.
The moraine patterns indicate that decay of theEskdale glacier was marked by active retreat and/orslight readvances and that downwastage and backwastage resulted in the separation of the Great Mossand Lingcove Beck glaciers along the line of thesouth ridge of Esk Pike. The moraine ridges at E and Frelate to a stage that post-dates the separation of icenourished on the steep slopes of Scafell from that inthe valley upstream of Great Moss.
A LLS age for the Eskdale moraines also hasimplications for the age(s) of moraines recorded byManley (1959) and Pennington (1978) in other southfacing valleys of the Lake District such as Rydal andKentmere.
Implications of a Dimlington Stade age
At its maximum extent active DS ice in the LakeDistrict attained an altitude of 830-870 m Ol) in theScafell Pike-Bowfell area and, from the orientations ofhigh-level striae and ice-moulded outcrops, the cols inthe area were over-run by ice moving westwards orsouthwestwards (Lamb & Ballantyne, 1998).Therefore,if all the Eskdale moraines relate to DS glaciation theymust have been created during a late stage in thatglaciation and represent stillstands or slight readvancesof decaying valley glaciers. The timing of these phasesremains unknown but McCabe et at. (1998) have arguedfor a readvance of the DS ice sheet in the northern IrishSea region at c. 17.6-16.8 cal. ka BP in response toNorth Atlantic Heinrich event I. Lithostratigraphicalevidence from west Cumbria was presented by Merritt& Auton (2000) in support of the Scottish Readvanceonto the coast of Cumbria at approximately the sametime as Heinrich 1. However, although the locations ofvalley glacier margins in the Lake District coeval withthis readvance remain conjectural, the possibility ofa dynamic response from those glaciers cannot bediscounted (cf. Merritt & Auton, 2000).
Whether or not the Eskdale moraines share a temporal link with a readvance of the Irish Sea ice sheet,they do indicate that the valley glacier underwentmulti-stage withdrawal. This style of DS ice loss isradically different to that envisaged by Pennington(1978) (see above). Therefore, it would be appropriateto seek evidence for DS ice margins and re-evaluate thenature of ice loss in other Lake District valleys.
Implications if some moraines are of Loch LomondStade and some of Dimlington Stade age
Separating the moraines into DS and LLS componentsis an entirely subjective exercise. One possible separ-
ation could assign the moraines at A and B (Fig. 1) tothe DS and the rest to the LLS. Such a subdivisionmight be based on moraine surface characteristics:moraines at A and B have fewer surface boulders thanthe other moraines and, therefore, look somewhatdifferent. However, this might be a function of theirlocation within areas of enclosed and improved landand the partial clearance of boulders (cf. Clark &Wilson, 1994). Nevertheless, if the moraines at A andB were of DS age considerations similar to thosediscussed above for such an age would apply. Ifmoraines C-L were of LLS age two caveats to theimplications outlined above might be appropriate.Firstly, the LLS 'glacier' could have comprised eithertwo non-confluent ice masses, or two ice masses thatwere confluent in the triangle of steep ground betweenthe Esk and Lingcove Beck (cf. Manley, 1959) and thelarger glacier is likely to have been that sourced aboveGreat Moss in upper Eskdale. Second, the smallerglacier in Lingcove Beck valley may not have extendedthrough the cols to connect with the Langstrath glacierat are Gap or with the Great Langdale glacier atThree Tarns. Nevertheless, these modifications to thepattern of LLS glaciers in Eskdale do not invalidatestatements made above regarding the nature of glacierwithdrawal.
5. CONCLUSIONS
The presence of moraine ridges and mounds at variouslocations in upper Eskdale is testimony to activeretreat/stillstands and/or readvances of the valley glacier system. Moraine ages have not been constrainedby absolute dating but moraine construction musthave occurred in either a late stage of the DS or duringthe LLS. Depending on what age may eventually bedemonstrated for the Eskdale moraines, several implications arise concerning the nature of ice loss in the DSand/or ice extent in the LLS. These implicationsextend to other valleys in the Lake District fromwhich moraines have been reported (Manley, 1959;Pennington, 1978), thus, demonstrating a significancefor these landforms that extends beyond Eskdale.Moraines in these valleys need to be re-evaluated inorder to further understanding of the Late Pleistocenelandscape history.
ACKNOWLEDGEMENTS
Lisa Rodgers and Nigel McDowell at the University ofUlster prepared the illustrations for publication andRichard Clark, David Evans and Ian Evans arethanked for their comments on the originalmanuscript.
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Manuscript received 20 March 2003; revised typescript accepted 22 August 2003
