Interactions between the Greenland Ice Sheet and the Liverpool Land coastal ice cap during the last two glaciation cycles

JOURNAL OF QUATERNARY SCIENCE (2005) 20(3) 269–283Copyright � 2005 John Wiley & Sons, Ltd.Published online in Wiley InterScience (www.interscience.wiley.com). DOI: 10.1002/jqs.900

Interactions between the Greenland Ice Sheet andthe Liverpool Land coastal ice cap during the lasttwo glaciation cyclesLENA ADRIELSSON1 and HELENA ALEXANDERSON2*1 Department of Geology, GeoBiosphere Science Centre, Lund University, Solvegatan 12, SE-223 62 Lund, Sweden2 Department of Physical Geography and Quaternary Geology, Stockholm University, SE-106 91 Stockholm, Sweden

Adrielsson, L. and Alexanderson, H. 2005. Interactions between the Greenland Ice Sheet and the Liverpool Land coastal ice cap during the last two glaciation cycles.J. Quaternary Sci., Vol. 20 pp. 269–283. ISSN 0267-8179.

Received 25 February 2004; Revised 25 October 2004; Accepted 11 November 2004

ABSTRACT: The sedimentary record from the Ugleelv Valley on central Jameson Land, East Green-land, adds new information about terrestrial palaeoenvironments and glaciations to the glacial historyof the Scoresby Sund fjord area. A western extension of a coastal ice cap on Liverpool Land reachedeastern Jameson Land during the early Scoresby Sund glaciation (� the Saalian). During the followingglacial maximum the Greenland Ice Sheet inundated the Jameson Land plateau from the west. TheWeichselian also starts with an early phase of glacial advance from the Liverpool Land ice cap, whilepolar desert and ice-free conditions characterised the subsequent part of the Weichselian on theJameson Land plateau. The two glaciation cycles show a repeated pattern of interaction betweenthe Greenland Ice Sheet in the west and an ice cap on Liverpool Land in the east. Each cycle startswith extensive glacier growth in the coastal mountains followed by a decline of the coastal glaciation,a change to cold and arid climate and a late stage of maximum extent of the Greenland Ice Sheet.Copyright � 2005 John Wiley & Sons, Ltd.

KEYWORDS: glaciation cycle; Weichselian; Saalian; Scoresby Sund; Greenland.

Introduction

Glacial fluctuations along the East Greenland ice-sheet marginare mainly known from coastal settings and from sedimentsdeposited by outlet fjord glaciers draining the Greenland IceSheet. Less is known from the terrestrial margins of the IceSheet and about the growth and decay of local ice caps.

The glacial history of central East Greenland (Fig. 1) is knownfrom work carried out during the last three decades on theJameson Land peninsula, in the areas around the ScoresbySund fjord mouth and to some extent also in the inner fjords(e.g. Funder and Hjort, 1973; Funder, 1978, 1990; Funderet al., 1994, 1998; Hansen et al., 1997, 1999; Hansen,2001). Sedimentary successions in the coastal lowlands arecharacterised by marine and deltaic deposits, combined withtills and glacitectonics mainly related to outlet glaciers directedby the fjord topography (Funder et al., 1998).

The interior of Jameson Land contrasts strongly with theyoung glacial landscape along the coast, and deeply incisedvalleys, deflation surfaces with ventifacts, and weathered bed-

rock with tors characterise the landscape (Moller et al., 1994;Ronnert and Nyborg, 1994). This has been taken as an indica-tion of long periods of subaerial conditions, possibly combinedwith the protective effect of cold-based glaciers. However,patches of old glacial sediments, originally named the JamesonLand Drift by Nordenskjold (1907), are found in the interiorparts of the peninsula, and erratics of western provenance,e.g. Scolithos-quartzite, are scattered on residuum-mantledbedrock surfaces. Investigations of the Jameson Land Drift havesuggested a complex glacial history with glacial advances dat-ing back to the Saalian or earlier (Moller et al., 1994), but thereare no indications that the Greenland Ice Sheet reached interiorJameson Land during the Weichselian.

This paper describes the sedimentology, stratigraphy,geomorphology and chronology of a central part of JamesonLand, the Ugleelv Valley and its surroundings. The study sup-plements the glacial record from the coastal areas along Scor-esby Sund by adding new data from an area well above themarine limits and outside the direct influence of the outletfjord glaciers from the Greenland Ice Sheet. Our purpose isto reconstruct the terrestrial environment, focusing on thedynamic nature of glacial advances and on the palaeoenviron-mental conditions during periods of non-deposition and sub-aerial exposure, and to contribute palaeoclimatic data forthe last glaciation cycles in East Greenland.

* Correspondence to: H. Alexanderson, Department of Physical Geography andQuaternary Geology, Stockholm University, SE-106 91 Stockholm, Sweden.E-mail: [email protected]

The setting: geology, topography and climate

The Scoresby Sund area in central East Greenland (Fig. 1) ischaracterised by large fjords cutting deeply into ice-coveredhigh plateaux (e.g. Renland), by alpine landscapes with localglaciation (e.g. Liverpool Land) and by low-lying ice-free areas(e.g. Jameson Land). The Jameson Land peninsula, which liesless than 200 km from the present edge of the Greenland IceSheet, is dominated by a low-relief plateau landscape around500 m a.s.l.

The bedrock on Jameson Land is composed of soft Mesozoicsandstones, shales and coal cut by a number of dolerite dykes(Henriksen, 1989; and Fig. 1). Liverpool Land in the east andmuch of the area to the west, outside the Ice Sheet, consistsof Caledonide crystalline rocks like granites and gneisses. Ter-tiary basalt covers the Geikie Plateau to the south and south-west. Quaternary sediments are found mainly in two areas onJameson Land: (1) as patches of older drift on the central pla-teau (the Jameson Land Drift; Nordenskjold, 1907), and (2) asa belt of younger drift along the western and southern coast(e.g. Ronnert and Nyborg, 1994). The low-relief plateau sedi-ments (‘older drift’) are largely glacial sediments of at leastSaalian age (Moller et al., 1994), situated well above the mar-ine limits. The coastal belt (‘younger drift’) consists of Eemianand Weichselian marine and fluvial sediments deposited dur-ing ice-free periods and of thick glacigenic sediments (Funder

et al., 1998). Between these areas is a driftless zone, where thefrost-shattered and weathered Mesozoic bedrock is exposed,partly in a channel and tor landscape (Schunke, 1986; Hjortand Salvigsen, 1991). Glacial overriding is here indicated onlyby scattered, mostly western erratics (Moller et al., 1994).

The central plateau landscape is deeply dissected by fluvialerosion. The main water divide, which is pronouncedly east-centred, is topographically diffuse and rivers draining towardsthe east and west interfinger in their upper reaches. TheUgleelv River, the largest river draining east, discharges intonorthernmost Hurry Fjord and flows in a disproportionatelylarge valley with few tributaries. The uppermost part of thevalley, close to the water divide, is broad and bowl-shapedwith steep headwalls cut into thick Quaternary deposits (Molleret al., 1994). The sediments extend only 1 km east of the waterdivide and the rest of the valley is cut into bedrock, with somefluvial sediments on the valley floor (Funder, 1990).

The climate along the east coast of Greenland is stronglyinfluenced by the cold south-flowing East Greenland Polar Cur-rent and by North Atlantic cyclones advecting warmer air withprecipitation from the south. This generates a steep south tonorth climatic gradient, with decreasing temperature and pre-cipitation northwards along the coast. At present the maximumelevation of the equilibrium line altitude (ELA) is found on gla-ciers well inland from the coast in central East Greenland,where precipitation is low and summer temperatures relativelyhigh (Funder et al., 1998).

Location and methods

Quaternary sediments are exposed in the steep slopes of theupper Ugleelv Valley (Fig. 2). The stratigraphy was brieflyinvestigated during an expedition in 1992 (Moller et al.,1994), and our fieldwork in 2000 comprised more detailed stu-dies of the sedimentary successions and a geomorphologic sur-vey of the surroundings. Sedimentary sections were logged atnine sites (Fig. 2), and the sediments were examined withregard to lithology, sedimentary structures, bed boundaries,clast shape and roundness, and palaeoflow patterns. Clastmacrofabric analysis was performed on 2–6 cm long clasts witha/b-axis ratio >1.5. Samples were collected for clast-lithologyanalysis in the laboratory and for optically stimulated lumines-cence (OSL) dating.

Correlations between the sites rely on lithological properties,lithostratigraphic relationships and boundary unconformities.The relative stratigraphic record from the Ugleelv area was alsocompared with the stratigraphy and environmental history ofother sites in interior Jameson Land (Moller et al., 1994). Thesecorrelations were based on lithostratigraphy, morphostratigra-phy and the relative chronology of glacial events.

Absolute ages of the stratigraphic events were obtained byOSL dating. The OSL dating was performed on quartz (180–250mm) according to the SAR protocol (Murray and Wintle,2000) at the Nordic Laboratory for Luminescence Dating atRisø, Denmark.

Stratigraphic units

Eight lithostratigraphic units, named A to H, were recognised inthe Ugleelv area, and a simplified lithostratigraphy of the sitesis shown in Fig. 2. Thick sedimentary successions, mainly of

Figure 1 Map of Greenland, Scoresby Sund and Jameson Land. Thebedrock map is simplified from Henriksen (1989). The lower part showsa topographical cross-section (A–A0) and the general bathymetry of theadjacent Scoresby Sund fjord to the south, indicating the Kap BrewsterMoraine at the fjord mouth. Lo¼ Lollandselv, Fa¼ Falsterselv,Jy¼ Jyllandselv rivers, JPK¼ J.P. Koch Fjeld mountain. The blacksquare on Jameson Land shows the location of Fig. 2A. The bedrocklegend applies only to the upper part of the figure

270 JOURNAL OF QUATERNARY SCIENCE

Copyright � 2005 John Wiley & Sons, Ltd. J. Quaternary Sci., Vol. 20(3) 269–283 (2005)

Figure 2 Map of the upper Ugleelv Valley (A) and overview of investigated sites (B, C) and their stratigraphy (D). The drift limit in A is according toMoller et al. (1994), partly modified around the Ugleelv Valley. The drift cover corresponds mainly to our unit E and the glaciolacustrine sediments tounit A. The hummocks and terraces are likely to have formed during Liverpool Land glaciations 1 and 2 (units B, G). The aerial photo in B is an excerptfrom no. 858J 5323 (#Kort & Matrikelstyrelsen (17-05). Reproduced with permission.). The rectangles in C mark the positions of sections. The sim-plified units in D are explained in the text. The aeolian unit H is found at various altitudes, as a cover on the valley sides and next to a nivation rampartat site 9. Black arrows denote palaeocurrent directions, open arrows ice-movement directions

TWO GLACIATION CYCLES ON CENTRAL EAST GREENLAND 271


units A–C, are exposed in the steep headwalls of the uppervalley. Units D–H provide a spatially fragmented lithostratigra-phy, found at different levels along the valley sides. The sedi-mentology of each unit is described and interpreted, andstratigraphic correlations within the central plateau area aresuggested.

Unit A: glacial lake and delta sediments

Unit A, an extensive depositional sequence of silty and sandysediments, was studied in detail at site 1 (Fig. 3) and site 3(Fig. 4), and surveyed at sites 4, 5 and 7 (Fig. 2D). Rhythmicallylaminated silt and silty clay (cf. Ugleelv unit A1 in Moller et al.,1994) are found in the broad upper valley bottom between 415and 440 m a.s.l. (sites 4 and 6; Fig. 2). Sandy lithofacies (cf.Ugleelv unit A2-B in Moller et al., 1994) are found at higheraltitudes, 440–480 m a.s.l. Ripple-laminated and planar paral-lel-laminated fine sand predominate, occasionally interruptedby beds of massive, often normally graded sand, and thin inter-beds of mud. A consistent palaeocurrent pattern indicates flowdirections from W-SW, and provenance studies show a clastlithology dominated by felsic crystallines (type 2 in Fig. 5), sug-gesting a source area in the western Caledonides.

The coarsening-upward succession of unit A is interpreted asa delta prograding into a glacial lake, probably dammed by gla-ciers in Scoresby Sund and in Hurry Fjord, and with a lake levelof at least 480 m a.s.l. Deposition was mainly from low-densityturbidity currents, hyperpycnal effluents from a glacial river.Turbidites at site 1 are dominated by thick bed-sets of ripple-laminated sand, suggesting sedimentation mainly from sus-tained underflows moving down a low-gradient delta slope(Fig. 3; Smith and Ashley, 1985). Slope instability, causing grav-itational failure and resedimentation, is indicated by occasionalslumps, synsedimentary deformation, density flows and surge-type turbidity currents, especially in the lower part of the succes-sion at site 3 (Fig. 4; Mulder and Alexander, 2001). High sedi-ment supply, shown by the large extent of the delta, suggests awell-developed drainage system of a warm-based glacier.

The unit is correlated with similar glacial lake and delta sedi-ments, situated at the same altitude (440–500 m a.s.l.), 5–15 kmto the west and southwest, e.g. along the upper reaches of theJyllandselv River (Moller et al., 1994). The sediments do notextend east of our study area (Fig. 2A).

Unit B: Liverpool Land till 1

An unconformity separates the delta sediments from unit B, amassive, matrix-supported diamicton up to 2 m thick. Thebed geometry is sheet-like and the diamicton can be tracedalong the southern valley side for several hundred metres.Detailed investigations are from site 3 (Fig. 4). The lowerboundary of the diamicton is erosive and slopes gently towardsthe east. Small boulders are lodged into theunderlying stratified sandy sediments, and in places a zone ofdeformed and homogenised sand approximately 10 cm thick isfound at the base. The diamicton is massive and has a sandymatrix. Clasts are mainly subangular or subrounded, and clastfabric analysis shows a preferred E–W orientation (S1¼ 0.77,0.60; Fig. 4), with almost horizontal clast long-axes. The clastlithology is characterised by black shale and sandstones (type1, Fig. 5), which are of local provenance (cf. the Vardekløft For-mation; Surlyk and Birkelund, 1972). A few Scolithos-quartziteerratics of distant origin were also found in the diamicton.

The diamicton has the characteristics of a subglacial till; forexample preferred orientation of clast long-axes and clasts that

were ploughed and lodged into the underlying sand(Dreimanis, 1989; Benn and Evans, 1996). Subglacial shearingis indicated by pervasive deformation and obliteration of theoriginal bedding in the stratified substratum (Hart and Boulton,1991). Clast-axes orientation and the sediment deformationstructures suggest that the glacier flowed westwards.

The glacier, extending from the ice cap on Liverpool Land inthe east, advanced over the glacilacustrine sediments (unit Aand corresponding sediments) on the plateau, but a till corre-sponding to our unit B was not found in sections further west(Moller et al., 1994). Consequently, the Ugleelv sites may beclose to the maximum western extent of the glacial advance.

Unit C: glacifluvial sediments

Thick successions of glacifluvial sediments are found both ontop of the unit B diamicton (site 3, Fig. 4) and in broad channelseroded into the Unit A glacilacustrine sediments (e.g. sites 4and 7, Fig. 2). More than 30 m of gravel and sand, exposed atsite 3 (Fig. 4, 466–499 m a.s.l.), are found in a northeast trend-ing flat ridge, faintly indicated along the southern edge of thevalley. The lower half of the succession consists of massive,matrix-rich but mainly clast-supported gravel with cobblesand boulders, interbedded by thin (<10 cm) beds of planar par-allel- or cross-laminated gravelly sand (Fig. 6A). Clasts aremainly subrounded and subangular, and the maximum particlesize (MPS) increases upwards to 40–50 cm. In the middle of thesuccession is an abrupt lithofacies change into laminated siltand sand with thick uniform beds of ripple-laminated sand(Fig. 6B) and low-angle cross-laminated sand, followed by stra-tified and massive gravel and sand. Clast fabric analysis in thelower gravel shows a horizontal cluster of long-axes and imbri-cated intermediate axes, suggesting a palaeocurrent directionfrom the northeast. A similar direction is also indicated bycross-lamination in the sandy lithofacies (Fig. 4). The clastlithology, characterised by black shale (up to >70%, type 1;Fig. 5), has the same local provenance as in unit B.

Clast-supported gravel facies were primarily deposited fromtraction load, while imbricate, matrix-rich gravel facies indi-cate rapid deposition from highly concentrated flow (Bren-nand, 1994). The flat ridge-form suggests sedimentation in anice-walled channel or a subglacial conduit. A rapid changein hydraulic regime is indicated by the laminated silt and sand,and the thick beds of ripple-laminated sand implies verticalaggradation under tranquil, almost constant flow conditions,probably in an ice-walled, open channel. The local source ofclast lithologies and the palaeoflow directions suggest a rela-tionship between the glaciofluvial sediments (unit C) and theLiverpool Land till 1 (unit B). Unit C was deposited in theice-marginal zone of a warm-based glacier with a well-devel-oped subglacial and englacial drainage system, as indicated byextensive glaciofluvial sedimentation, sediment architectureand coarse grain sizes (MPS 40–50 cm).

A possible correlation can be made to eskers and kameterraces found on the high, flat plateau (J. P. Koch Fjeld,Fig. 1) 30 km SSE of the upper Ugleelv site (Moller et al.,1994). These sediments have a high amount of locally derivedclasts, like our unit C, and the palaeocurrent analyses also sug-gest glacifluvial drainage towards the south-southwest.

Unit D, terrace sediments anda periglacial palaeosol

Unit D is found in terraces at 470–484 m a.s.l. on both sides ofthe Ugleelv valley (sites 1, T1 and 2; Figs 3, 7, 8). The sediments



consist of planar parallel- and low-angle cross-laminated fineto medium sand, cross-laminated coarse-grained sand and,occasionally, clast-supported massive gravel. Lags associatedwith thin matrix-supported diamict beds were also observed

(Fig. 6C). Cross-bedding and cross-lamination show palaeo-flow directions mainly from the east. In the upper part of theterrace sediments we found a ca. 0.5 m thick horizon withinvolution structures and a sand wedge/fossil ice-wedge

Figure 3 Sedimentological log from site 1, including legend to all logs. The OSL-dates are partly reversed, with the stratigraphically lowestOSL-sample giving the youngest age



(Figs. 2D, 6C, 6D). The composite wedge is >2 m deep and ca.0.4 m wide, with surrounding beds inflected upwards in thelower part and with collapse structures in the upper part.

The position of the terraces suggests formation after icedisintegration from the ice-contact landscape of unit C. The ter-race sediments have a polygenetic, paraglacial character

(Brodzikowski and van Loon, 1991; Benn and Evans, 1998),and are interpreted as fluvial sediments interlayered by aeolianand debris-flow deposits (Fig. 7). The palaeoflow in the shallowchannels was directed towards the west-northwest. The mor-phological position and the sedimentary structures of the aeo-lian sediments, both in site 1 and T1, indicate sand drift by

Figure 4 Sedimentological log from site 3. For legend, see Fig. 3. Note that imbrication in unit C is shown by B-axes in the fabric diagram



southerly winds. The wedge and the involution horizon wereformed under permafrost conditions, and suggest a period ofcold, periglacial climate.

Unit E, Greenland Ice Sheet till

A matrix-supported diamicton (unit E) is the topmost bed innearly all sections of the upper Ugleelv Valley and coversmuch of the adjacent plateau as well. The thickness variesbetween less than 0.5 and up to 3 m, and a boulder lag, includ-ing Scolithos-quartzites, may replace the diamicton, forexample on the high terraces (sites 1, T1). Apart from occa-sional thin sand lenses, the diamicton is massive (Fig. 6E).The matrix is coarse-grained, but changes upwards into silt(Fig. 8). In some places only the silty facies is represented.Boulders and cobbles are frequent, and the clasts are mainlysubangular to angular. Clast fabric, measured at site 2, is mod-erate (S1¼ 0.66; Fig. 8) with a slight dip of long-axes towardsthe west-northwest. Thin beds of stratified sand, clast-supported gravel and sandy diamicton occur beneath the mas-sive diamicton. At site 2 an unconformity separates these sedi-ments from older strata deformed by low-angle, parallel shearplanes thrusted from the west (Fig. 8). Felsic and basic crystal-lines from the Caledonides dominate the clast lithology of theunit (type 3, Fig. 5).

The diamicton is interpreted as a basal till based on the sheetgeometry, the massive structure and the preferred clast orienta-tion. The sand and gravel beneath the till and the depletion offine-grained material in the lower part of the diamicton can beexplained by a combination of stream flow and porewater flowthat washed out the silt either subglacially or proglacially. Thelow-angle shear structures, interpreted as subglacial shear,were formed before the wash-out and fluvial sedimentation,and it is unclear whether the till on top was formed by activelodging or just by melt-out.

Rocks of western provenance were transported into the areaby an east-flowing glacier. The geomorphic impact of the iceadvance was small and debris of distant provenance was notmixed with locally derived rock types. The basal till coverslandforms of the preexisting landscape, like the high terracesin the Ugleelv Valley. Such landform preservation is usuallyrelated to frozen bed conditions, suggesting that the glacierwas predominantly cold-based, at least during the ice advance

(e.g. Dyke, 1993; Kleman and Borgstrom, 1994). A change inthermal conditions is indicated by a subsequent transition tobasal melting and till deposition.

Unit E is correlated to a till with western erratics, depositedby the Greenland Ice Sheet and covering the western part of thecentral plateau (Moller et al., 1994). The eastern extent of unit Ediamicton is related to a distinct (ca. 100 m wide) till limit, theeastern limit of the older drift on the plateau. This limit is easilytraced in the flat landscape, but is not accentuated by anyglacial landforms. The driftless landscape outside, east of theborder, is characterised by a regolith cover with few scatterederratics, exposed Jurassic sedimentary bedrock and deeplyincised fluvial channels.

Unit F, glacifluvial sediments

Unit F represents sand and gravel found in small terraces on thelower valley slopes between approximately 435 and 420 ma.s.l. The sediments are mainly clast-supported gravel andcross-laminated sand (unit F; Fig. 9) containing mixed clastlithologies.

Unit F is interpreted as remnants of terraces formed duringextensive fluvial erosion of the older deposits of the upperUgleelv Valley. Down-cutting continued to approximately400 m a.s.l. The mixed clast lithologies indicate reworking ofolder sediments from higher elevation in and around the valley.Fluvial erosion into more than 80 m of sediments, and down-stream also into sedimentary bedrock, requires high water dis-charges, which cannot be expected from the present water-divide area without a large drainage basin. Extensive meltingof glacier ice is the only likely source of the required water.We therefore suggest that glacial meltwater caused thedown-cutting of the present Ugleelv Valley and also of partof the deeply incised fluvial valleys directed towards HurryFjord further south in the eastern part of the peninsula.

Unit G, Liverpool Land till 2

A thin cover of silty-clayey diamicton (unit G) can be found onthe low terraces (unit F) within the Ugleelv Valley. The diamic-ton is massive and matrix-supported and contains conspicuouslimestone nodules, but very few boulders. At site 6 this diamic-ton overlies glacilacustrine sediments (unit A) deformed into alarge fold cut by subhorizontal thrust planes (Fig. 10). The syn-cline fold axis strikes 320� with deformation from the northeast.A zone of tectonic lamination, a banded glacitectonite, withalternating bands of brecciated clay and massive fine sandseparates the non-penetratively deformed sediments from themassive diamicton on top.

The large-scale fold is interpreted as a proglacial glacitec-tonic structure formed at the southwestern flank of a glacieradvancing up the valley from the east. Subglacial shear dueto continued ice advance is indicated by subhorizontal thrust-ing, and the glacitectonite and the diamicton on top is conse-quently interpreted as deformation till. The glacitectoniteformed under low effective normal stress, and the basal tem-perature during the subglacial deformation and depositionshould have been at the pressure melting point (Hart, 1995).

Several hummocks and small ridges, a few metres high, arefound in the nearby tributaries to the Ugleelv Valley and at thehead of the valley (Fig. 2A). They contain both sorted and dia-mict sediments, and in places angular coarse debris covers thesurface. The hummocks are interpreted as small moraine

Figure 5 Examples of lithological types: (1) unit B till; (2) unit A deltaslope sediment; (3) unit E till. We analysed the clast lithology for thefraction 4–8 mm by using a microscope and classified the clasts intoseven main lithological groups. The results were treated statisticallyusing the WinSTAT software (v. 2001.1)



ridges, the most distal ones marking the maximum limit of theglacier along the edges of the valley. The lower Ugleelv Valleyis U-shaped, and the glacier is interpreted as a warm-based val-ley glacier discharging westwards from a mountain ice-cap onLiverpool Land.

Unit H, young aeolian sediments

Southerly winds (H1)

A deflation surface with ventifacts (Fig. 6F) has formed on topof the unit E till, both on the surrounding plateau and on the

high terraces in the valley. The aeolian abrasion pattern sug-gests strong southerly winds. Aeolian sediments were notfound on the plateau, but large aeolian dunes, containingsheet- and wedge-shaped units of inclined parallel-laminatedfine to medium sand, cover parts of the steep slopes along thesouthern side of the upper Ugleelv Valley (Fig. 6G). Theseimpeded dunes have accumulated on lower parts of theslopes and in depressions on the lee side from southerly orsouthwesterly winds. Excavations in the slope at site 5(450–455 m a.s.l.) show a distinct lamination in the sand,without deformational structures, which indicates that sandaccumulation occurred without substantial mixing with snow(Koster, 1988).

Figure 6 (A) Coarse facies of unit C, site 4. (B) Thick beds with type-A ripples is a characteristic feature of unit C, site 3. (C) Terrace sediments withcryoturbation structures (unit D) in Terrace I. (D) Composite fossil ice-wedge in fluvial unit D sediments at site 1. (E) Unit E till at site 2. (F) Wind-polished Scolithos-quartzite on Terrace I. (G) Aeolian dunes on the lower slope of the southern valley side (below the line), site 5. (The scale-bar is20 cm)



The dune surface is covered by cobbles. Coarse-grainedsediments of units C and E crop out higher up on the slope,and the cobble-strewn surface may thus derive from slope pro-cesses. Colluvium below the steep slopes on the southern sideis otherwise almost absent, and slope processes are at presentnot very active.

Northerly winds (H2)

Recent and sub-recent aeolian sand is found leeward of north-erly winds, beneath the northwestern headwall, which isformed as a row of broad, arcuate scars, more than 200 macross. Curved ridges protrude from the flank of some of thesemicircular hollows (Fig. 2C). The ridges are interpreted asnivation ramparts, or possibly small moraines, and the arcuatescars in the slope may represent small cirques or nivation hol-lows. One of the ridges, a few metres high, marks the lateralposition of a former stationary snow bank or cirque glacier,which was much larger than the present snow-patch in theslope. The position and the geometry of the ridge indicate thatthe direction of snowdrift at that time was the same as today,from the north-northeast. A vegetation-covered sand duneoccurs on the distal side of the ridge (site 9). The aeolian accu-mulation must have occurred parallel to the formation of therampart, and the sedimentation was interrupted when the snowbank shrank.

Absolute ages of the stratigraphy

The stratigraphic record gives the relative chronology of glacialevents from the upper Ugleelv area. Radiometric ages wereestimated using OSL-dating of selected sedimentary facies(Table 1). Thermoluminescence (TL) ages of correlated unitsfrom other parts of the Jameson Land plateau are alsoconsidered.Unit A: The glacilacustrine sediments in the Ugleelv Valley

provided OSL-ages between 142 and 200 ka (Table 1). PreviousTL-dates from the Jyllandselv and Ugleelv river valleys were in

the same range (146–222 ka) and Moller et al. (1994) thereforesuggested a Saalian age for the glacial lake stage.Unit C: Glacifluvial sediments related to deglaciation of the

first Liverpool Land ice advance provided Saalian ages (150–170 ka; Table 1). Using TL-dating Moller et al. (1994) placedthe formation of the eskers and kame terraces on J. P. KochFjeld in the Saalian. Our OSL-dates support this correlation.Unit D: Fluvial and aeolian sand from paraglacial terrace

sediments of unit D have Saalian OSL-ages (160–190 ka;Table 1).Unit E: An OSL-date from glacifluvial sediments at the base

of unit E yielded 170 ka (Table 1). This unit corresponds to theUgleelv unit C of Moller et al. (1994), who assigned it to theScoresby Sund glaciation during the Saalian ice age.Unit F: Sand from a fluvial terrace formed during meltwater

down-cutting of the Ugleelv valley was OSL-dated to 134 ka

Figure 7 Sedimentological log from Terrace I (T1) at site 3. For legend,see Fig. 3

Figure 8 Sedimentological log from site 2. For legend, see Fig. 3



(Table 1). This age suggests that the glaciation of central Jame-son Land did not terminate until late in the Saalian.Unit G: A thin bed (<10 cm) of aeolian sand on top of a sand-

stone boulder lag underlies the diamict unit G at site 4b (Fig. 2).The OSL-age of the sand (109 ka; Table 1) gives a maximumearly Weichselian age for the second Liverpool Land iceadvance into the Ugleelv Valley.Unit H: One OSL-date from the large aeolian dune repre-

senting southerly winds (site 5; Fig. 2) gave an age of 27 ka(Table 1). The OSL-age of aeolian sediments at site 9(10.3 ka; Table 1) also dates the small moraine or nivation ram-part beneath the northwestern headwall of the Ugleelv Valley.

Dating reliability

For aeolian sediments, incomplete bleaching is usually not aproblem (Murray and Olley 2002), but for some fluvial andfor most glacifluvial and glacilacustrine deposits it must betaken into account. The sediments of glacilacustrine unit A

were probably transported far enough to have been bleached,but the glacifluvial unit C was deposited quite close to the iceand runs a larger risk of not having been completely bleached.Nevertheless, incomplete bleaching is rarely more than a fewGy and Hansen et al. (1999) report incomplete bleachingequivalent to ca. 10 ka in samples from Holocene sandy deltasediments deposited after deglaciation in western JamesonLand. Such effects are negligible for the glacifluvial/glacilacus-trine samples here.

Luminescence dating of pre-Eemian samples is sometimeshampered by saturation of the luminescence signal in quartz(Aitken, 1997), but our samples did not suffer from that limita-tion despite high equivalent doses (Fig. 11, Table 1). The stan-dard errors of our Saalian dates are, however, relatively large(about 10%) and the dates cannot be used to discriminate sin-gle events during the Scoresby Sund glaciation, as evidencedby the lithostratigraphy. For the Weichselian and Holocenedates, the uncertainty lies mainly in the limited number ofdated samples, since there is only one date for each aeolianepisode.

Another potential source of error is the estimation of averagewater content since deposition (Aitken, 1998). In this case, awater content close to saturation was assumed for all samplessince they were taken just above the present-day permafrosttable and are likely to have been permafrozen most of the timesince deposition. However, even if these conditions did notpersist since deposition and so the average water contentshould have been reduced somewhat when calculating doserates, the resulting ages are estimated to fall within the errorlimits of the (saturated) ages for all samples.

Glacial history of Jameson Landand surroundings

Several glacial advances are directly and indirectly evi-denced in the stratigraphy from the upper Ugleelv areaand from the interior of Jameson Land (cf. Fig. 12). The gla-cial history from the Scoresby Sund coastal sections (Funderet al., 1998) supplements this record with evidence ofrepeated outlet glaciers along the fjord. The regional impli-cation of the glacial and environmental history can also bediscussed by comparison with ice-rafted debris (IRD)records from the continental margin directly outside thecoast (Stein et al., 1996) and with climatic signals in the�18O ice-core record from the nearby (Fig. 1) Renland icecap (Johnsen et al., 1992). These comparisons are illustratedin Fig. 13.

The Scoresby Sund glaciation—Saalian

The Scoresby Sund glaciation was suggested by Moller et al.(1994) as comprising one single glacial advance and retreatby the Greenland Ice Sheet during the Saalian. However,our investigations indicate that the stratigraphy of the Scor-esby Sund glaciation is more complex, and we suggest thatthe term Scoresby Sund glaciation should cover a glaciationcycle with more than one advance and retreat. We also sug-gest a division of the Scoresby Sund glaciation into twophases: an early phase with coastal glaciation centred onLiverpool Land and outlet fjord glaciers in Scoresby Sund,and a late phase of major advance by the Greenland Ice Sheetfrom the west.

Figure 9 Sedimentological log from Terrace II (T2). For legend, seeFig. 3

Figure 10 Sedimentological log from site 6 showing glacitectonismcaused by the Liverpool Land 2 glaciation. Note the simplified grain-size scale (x-axis). For legend, see Fig. 3



The early glaciation phase

The early phase is characterised by extensive coastal glacia-tion. A lake at high altitude on central Jameson Land is indi-cated by thick glacilacustrine sediments (unit A; Fig. 12). Thislake must have been dammed by ice in the west (Moller et al.,1994), probably by an outlet glacier occupying the ScoresbySund fjord basin and expanding onto the west and south coasts

of Jameson Land. The eastern limit of the glacilacustrine sedi-ments either indicates a more easterly position of the waterdivide at that time, or damming by a second, contemporaneousglacier advancing westwards from Liverpool Land, as indicatedby the unit B till (unit B; Fig. 12). This advance represents amajor glacier expansion in the coastal mountains. Large quan-tities of glacifluvial sediments (unit C; Fig. 12) were depositedat the west-facing terrestrial margin of the Liverpool Land icecap, and the early glacial advances, both from Liverpool Landand in the Scoresby Sund fjord were characterised by warm-based glaciers with well-developed drainage systems.

The IRD-record from cores on the continental slope off thecoast at the mouth of Scoresby Sund shows maximum peaksolder than MIS 6 (Stein et al., 1996), interpreted as due tocoastal glaciation with calving glaciers and an absence of per-manent sea-ice cover (Funder et al., 1998). This correspondswith our picture of a build-up phase of an ice cap much largerthan today in coastal Liverpool Land, parallel with the onset ofoutlet glacier expansion in the Scoresby Sund fjord, suggestinghigh coastal precipitation probably due to open sea conditionsoutside the coast. A climatic change with evidence of decreas-ing temperature and precipitation (cf. unit D; Fig. 12) resultedin the retreat of the Liverpool Land ice in the Ugleelv Valley,and starvation by decreased precipitation was a possible rea-son for the reduction of the coastal ice cap.

A Saalian age for this glacial stage is indicated by the OSL-dates of units A, C and D and by correlation with dates fromearlier investigations in the area (Moller et al., 1994).

The late glaciation phase

The maximum extent of the Greenland Ice Sheet occurredduring the late glaciation phase. Tills containing western

Table 1 Optically stimulated luminescence (OSL) dates from the Ugleelv Valley. The OSL dating was performed according to the SAR protocol(Murray and Wintle, 2000) at the Nordic Laboratory for Luminescence Dating at Risø, Denmark. Within each unit the samples are sorted accordingto age; for stratigraphic position at each site see relevant logs. For lithofacies codes see Fig. 3

Risø no. Site Sediment type Age (ka) Dose (Gy) No. of aliquots Dose rate (Gy/ka) W.c. (%)

Weichselian/Holocene aeolian sediments001321 9 Aeolian, S 10.3� 0.8 20.7� 0.9 31 2.00 23001324 5 Aeolian, S 27� 2 42.9� 1.6 20 1.59 30001318 4 Aeolian, SiSm 109�8 296� 11 25 2.72 43Unit F001314 TII Fluvial, Stc 134� 11 312� 17 20 2.32 23Unit E001309 2 Glacifluvial, Spp/Ssf 170� 20 351� 36 28 2.11 22Unit D001316 2 Fluvial/redeposited, Spp 160� 10 326� 17 21 2.03 22001308 3 Aeolian, Spp/Spc 170� 20 322� 34 25 1.94 26001302 1 Aeolian, Spp 172� 14 315� 22 20 1.82 22001320 8 Aeolian, Spp 180� 20 352� 43 18 1.93 24001301 1 Fluvial/aeolian, Spp 190� 20 329� 33 24 1.78 26001317 2 Aeolian, Slc 190� 20 346� 30 22 1.79 26Unit C001306 3 Glacifluvial, Sr 150� 13 414� 28 20 2.76 14001315 5 Glacifluvial, Slc 150� 20 332� 37 25 2.18 22001323 3 Glacifluvial, Sr 150� 20 296� 33 26 1.97 30001307 3 Glacifluvial, Slc 170� 20 358� 36 27 2.09 22Unit A001304 1 Glacilacustrine, SiSr 142� 11 344� 21 25 2.41 28001305 3 Glacilacustrine, Spp/Stc 169� 18 332� 29 25 1.97 23001319 8 Glacilacustrine, Spc 195� 17 323� 20 20 1.65 26001303 1 Glacilacustrine, Spp 200� 20 383� 35 21 1.96 26Unit ?001322 9 Glacifluvial, S 150� 20 328� 28 20 2.17 30001313 7 Aeolian, S 220� 30 402� 46 21 1.80 23

Figure 11 Regenerated growth curve for a single aliquot of quartz fromsample 001314. The equivalent dose (De) is estimated from the intersec-tion of the corrected natural OSL response and the growth curve (seedashed lines). The exponential curve shows that the luminescence signalis not saturated at the level of the natural luminescence. Solid cir-cles¼OSL signals from regenerative doses, open circle¼OSL signalfrom final regenerative dose (recycling ratio 0.97), open triangle¼response at zero regenerative dose (recuperation, 6% of natural signal)



crystallines were deposited on the central plateau (unit E; Fig.12), and on the south and southwest coasts of Jameson Land(Israelson et al., 1994; Lysa and Landvik, 1994; Tverangeret al., 1994). The geomorphic impact was small and cold-basedconditions probably prevailed during ice advance. Pre-existingfrozen ground is supported by ice-wedge casts and periglacial

involutions in the terraces (unit D). The till cover on the plateausuggests a thermal change into basal melting conditions. Thisthermal change can be interpreted in two ways. (1) Spatial ther-mal zoning is often recognised in polythermal subpolar andpolar ice sheets, where a cold-based marginal zone is foundoutside an upglacier zone of basal melting. It has been

Figure 12 A simplified scenario illustrating the gradual build-up of the stratigraphy in the Ugleelv Valley



suggested that the Greenland Ice Sheet during this phaseexpanded across the Liverpool Land mountains and onto theshelf (Funder et al., 1998), an assumption based mainly onthe distribution of scattered western erratics (Funder, 1972).The till limit on the flat plateau east of our investigation sitemight then be explained as the maximum extent of the upgla-cier zone of basal melting, while areas of weathered bedrockfurther to the east were covered and preserved by cold-basedice. (2) A thermal change is, however, also to be expected dur-ing climatic warming. The till limit then represents the maxi-mum extent of the terrestrial margin of the ice-sheet at thetime of climatic change. In that case, the scattered erraticsfound east of this limit must have been distributed during ear-lier glaciation(s).

A thermal change caused by climatic warming is supportedby the extensive fluvial incision of the Ugleelv Valley (Unit F;Fig. 12). Fluvial channels on eastern Jameson Land originate ina zone related to the distinct till limit, and deep channels in thetor landscape on southern Jameson Land, interpreted as formedby subglacial fluvial erosion (Hjort and Salvigsen, 1991; Molleret al., 1994), could also fit into a drainage pattern of extensivemarginal incision. Deglaciation with glacifluvial landformsdominated by erosion is typical of Arctic-type glaciers whichhave a scarcity of debris, but which may yield large amountsof water from surface melting during ice decay (Dyke, 1993).

A low abundance of IRD outside the coast during MIS 6 sug-gests a long period of permanent sea-ice cover (Funder et al.1998), which corresponds to the advance of the GreenlandIce Sheet over central Jameson Land. The meltwater incision

on eastern Jameson Land, dated by OSL to 134 ka (unit F), sug-gests that the glaciation of central Jameson Land did not termi-nate until late in the Saalian.

The Weichselian glaciation

The last interglacial/glacial cycle in Scoresby Sund is knownfrom investigations along the fjord coast (Funder et al., 1998;Fig. 13). Subdivision into an early phase of warm-based gla-ciers and a late phase of polar glacier regime in the fjord area(Funder et al., 1998) is supported by climatic signals inter-preted from the Ugleelv stratigraphy.

The early glaciation phase

The Weichselian glaciation in the Ugleelv area started by a val-ley glacier extending westwards from the Liverpool Land icecap (unit G; Fig. 12). The glacier was topographically con-trolled and small moraines on the upper edges of the valleyprobably mark its margins. Glacial erosion, deformation anddeposition during the ice advance suggest a warm-based gla-cier. Additional indications of an early Weichselian glaciationof Liverpool Land and the Hurry Fjord area have been foundbefore (Funder, 1990; Mangerud and Funder, 1994; Tverangeret al., 1994; Hansen et al., 1997). Also, the growth of the Ren-land ice cap just west of Jameson Land (Fig. 1) started at the end

Figure 13 Glaciation curve for the Scoresby Sund area, including the Jameson Land succession. The cross-hatched areas represent the Greenland IceSheet (coarse pattern) and its outlet glaciers (fine pattern), in contrast to local ice caps (grey). The vertical, broken lines show the location of the Ugleelvarea. The �18O-record is from the Renland ice core (Johnsen et al., 1992) and the ice-rafted debris (IRD) record from core PS1726 on the continentalslope off Scoresby Sund (Stein et al., 1996; stretched between MIS boundaries to fit a linear timescale). Information also from Funder et al. (1998) andHansen et al. (1999; Scoresby Sund)



of the Eemian interglacial, and the �18O-record shows that atthat time temperatures were warmer than or similar to the pre-sent, but with 20% more precipitation (Johnsen et al., 1992).We suggest that the initial Weichselian growth of the LiverpoolLand ice cap is a contemporaneous climatic signal, and that thevalley glacier reached the upper Ugleelv valley soon afterdeposition of aeolian sand at site 4b (Fig. 2) around 109 ka.

Repeated advances of outlet glaciers through the ScoresbySund fjord during the early Weichselian stadials are shownby thick beds of basal tills, which also indicate warm-basedice conditions (Funder et al., 1998). These glacial advancesare also seen in the IRD record from the continental shelf (Steinet al., 1996; Funder et al., 1998).

The late glaciation phase

Polar desert conditions seem to have prevailed on central Jame-son Land and we have no indications of any local ice caps dur-ing the late glaciation phase. Extensive deflation surfacesformed during this period on the central plateau of JamesonLand (Moller et al., 1994). Large aeolian dunes (unit H1; Fig.12) on lee-side slopes on the southern side of the UgleelvValley are OSL-dated by one date to 27 ka, which is roughlyat the transition between MIS 3 and 2. The presence of aeoliandunes indicates periglacial, arid conditions and absence of per-manent snow banks. Strong winds from the south are alsoshown by ventifacts on the deflation surfaces.

High dust concentrations associated with low �18O-values inthe Renland ice core also suggest that the coldest periods wereusually stormy (Johnsen et al., 1992). The arid conditions dur-ing this phase, suggested by the ice-core data, support our viewthat local ice caps did not exist on Jameson Land.

A long period (>50 ka) of stable ice cover in Scoresby Sundhas been suggested by Hansen et al. (1997) and Funder et al.(1998) and dated to MIS 4–2. Till deposition during this Flak-kerhuk stade was limited, and the glacier regime has been com-pared with the polar glaciers of northernmost Greenland(Funder et al., 1998). IRD records indicate a transition to per-manent sea ice cover during MIS 4 (Funder et al., 1998).

An early Holocene cooling event

A radical change in the wind system, from southerly to north-erly, and the growth of stationary snow banks or possibly cir-que glaciers in the Ugleelv valley are dated by one OSL-dateto 10.3 ka. Wind-drifted snow and sand (unit H2) accumulatedon the northwestern headwalls of the valley by northerlywinds, the prevailing ones in the present climatic system. Theoutlet glaciers in Scoresby Sund had by that time rapidlyretreated to the inner parts of the fjord (Funder et al., 1998;Funder and Hansen, 1999), but moraine systems from a glacialadvance on Milne Land have been dated to Preboreal times(Funder and Hjort, 1973; Funder, 1978). The snow accumula-tion in the Ugleelv valley fits both with the Milne Land stadetemporary climatic change and with cooling events describedfor the early Holocene by for instance, Bond et al. (1997) andBjorck et al. (2001).

Conclusions

� Sedimentology, lithostratigraphy and luminescence (OSL)dates from the Ugleelv area on central Jameson Land reveal

a record spanning the two last glaciation cycles, the ScoresbySund/Saalian and the Weichselian.

� Three types of glacier advances are recognised on JamesonLand: warm-based valley glaciers extending from a coastalice cap on Liverpool Land, outlet glaciers extending fromthe Greenland Ice Sheet and following the fjord troughs,and the advance of a cold-based terrestrial ice-sheet marginacross the central Jameson Land plateau.

� During the early Scoresby Sund/Saalian glaciation sedimentsand landforms of central Jameson Land were formed by gla-cilacustrine, glacial and glacifluvial deposition. A glaciallake was dammed between an outlet glacier in ScoresbySund and a growing ice cap on Liverpool Land in the east.Permafrost and aeolian activity preceded the late glaciationphase and the advance of the Greenland Ice Sheet in thewest. Extensive meltwater erosion characterised the degla-ciation.

� During the early Weichselian a valley glacier extending fromthe Liverpool Land coastal ice cap intruded into the UgleelvValley. The plateau landscape was only slightly affected andthere is no depositional or erosional evidence of any glacia-tion at all during the Late-Middle Weichselian, when a stableoutlet glacier covered the Scoresby Sund fjord (Hansen et al.,1997; Funder et al., 1998). Instead, extensive deflation sur-faces and aeolian dunes suggest a long ice-free period witharid conditions.

� The interaction between climate and the terrestrial glacieradvances on the Jameson Land plateau shows a repeated pat-tern. The onset of a glaciation cycle was by growth of anindependent coastal ice cap on Liverpool Land, indicatinghigh coastal precipitation and thus partly open sea condi-tions. A change into cold and arid climate on Jameson Landresulted in starvation and decline of the coastal ice cap, butstill permitted a continuous growth to maximum extension ofthe Greenland Ice Sheet, which during the Scoresby Sund/Saalian maximum glaciation overrode central Jameson Land.Rapid break-up and deglaciation, caused by climatic warm-ing, terminated the glaciation cycles.

� A temporary cooling event, around 10.3 ka, interrupted thelast deglaciation and wind-drifted snow and sand accumu-lated on the headwalls of Ugleelv Valley.

Acknowledgements This study has been financed by Helge Ax:sonJohnson’s Foundation, the Crafoord Foundation, the Royal Physio-graphic Society in Lund, the Swedish Society for Anthropology andGeography (SSAG), the Royal Swedish Academy of Sciences (KVA)and the Faculty of Sciences at Lund University. The Danish PolarCentre and the Swedish Polar Research Secretariat provided logistichelp and support. Per Bergenrud and Martin Adrielsson gave excellentassistance during fieldwork. Andrew Murray, Louise Hansen, ChristianHjort, Per Moller and Kurt Kjær are gratefully acknowledged for con-structive reviews, comments and discussions.

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Documents

Interactions between the Greenland Ice Sheet and the Liverpool Land coastal ice cap during the last two glaciation cycles