Dow

nloa

ded

By:

[Sw

ets

Con

tent

Dis

tribu

tion]

At:

10:0

0 20

Jun

e 20

07

Younger Dryas cirque glaciers in western Spitsbergen: smaller thanduring the Little Ice Age

JAN MANGERUD AND JON Y. LANDVIK

BOREAS Mangerud, J. & Landvik, J. Y. 2007 (July): Younger Dryas cirque glaciers in western Spitsbergen: smaller thanduring the Little Ice Age. Boreas, Vol. 36, pp. 278�285. Oslo. ISSN 0300-9483.

The outermost moraines in front of the Scottbreen glacier in Spitsbergen date from c. AD 1900. These morainesrest on top of a marine shoreline radiocarbon-dated to about 11 200 14C yr BP and demonstrate that the AD-1900moraines show the maximum glacier extent since late Allerød time. This means that Scottbreen was smaller duringthe Younger Dryas than at AD 1900, in contrast with glaciers on mainland western Europe, which were all muchlarger during the Younger Dryas. The explanation is probably starvation of precipitation on western Spitsbergenduring the Younger Dryas. In contrast, ice sheets and glaciers in Spitsbergen reacted more or less in concert withglaciers in western Europe, during the global Last Glacial Maximum and the Little Ice Age.

Jan Mangerud (e-mail: Jan.Mangerud@geo.uib.no), Department of Earth Science and Bjerknes Centre for ClimateResearch, University of Bergen, Allegt. 41, NO-5007 Bergen, Norway; Jon Y. Landvik (e-mail: jon.landvik@umb.no), Norwegian University of Life Sciences, Department of Plant and Environmental Sciences, P.O. Box 5003,NO-1432 As, Norway; received 11th August 2006, accepted 31st October 2006.

The Younger Dryas (YD) in western Europe, i.e.downwind of the North Atlantic, is characterized byextensive glacier growth, and all glaciers were muchlarger during the YD than at any time during theHolocene (Gray & Coxon 1991; Andersen et al. 1995;Kerschner et al. 2000; Geirsdottir 2004; Denton et al.2005). On the other hand, further north along the sameseaboard the opposite situation has been reported,i.e. that glaciers on western Spitsbergen were smallerduring the YD than during the Little Ice Age(LIA) (Salvigsen 1979; Mangerud & Svendsen 1990;Svendsen & Mangerud 1992). However, this has beendocumented at only a few sites.

During the Last Glacial Maximum (LGM), theBarents (�Svalbard) Ice Sheet reached the shelf edgewest of our study site (Fig. 1) (Landvik et al. 1998). Theice margin retreat started about 15 000 14C yr BP andthe study area became ice-free at about 12 000 14C yrBP (Landvik et al. 1992; Mangerud et al. 1992). Thedeglaciation dates of 12 830 and 12 570 14C yr BP(T-6000 and Ua-280), performed on sediment-feedingmolluscs collected close to Scottbreen, are now con-sidered to be too old (Mangerud et al. 2006).

In this paper we present radiocarbon dates demon-strating that Scottbreen, a cirque glacier on thewest coast of Spitsbergen in the Svalbard archipelago(Figs 1, 2), was smaller during the YD than during itsLIA maximum extent at c. AD 1900.

Study area and observations

Svalbard is located at 77�808N. The archipelago istherefore characterized by an arctic climate, and about

60% of the land area is covered by glaciers (Fig. 1)(Hagen et al. 1993). However, because of advection ofwarm Atlantic water and southwesterly winds, theclimate, in particular the winter climate, is exception-ally warm compared with other areas at this latitude.At Isfjord Radio, located on the coast 55 km north ofScottbreen (Fig. 1), the mean annual temperature(1961�1990) is �/5.18C (Førland et al. 1997). Themeans for the coldest and warmest months are�/12.48C and �/4.88C, respectively. At Sveagruva,situated some 70 km inland, the corresponding tem-peratures are �/7.18C, �/17.08C and �/5.88C, respec-tively. Annual precipitation is 480 mm at Isfjord and260 mm at Sveagruva (Førland et al. 1997).

Scottbreen (‘breen’�/glacier) (77833?N, 14822?E) is a4.4-km long cirque glacier stretching from 700 to 90 ma.s.l. (Hagen et al. 1993). It is located close to the openocean on the west coast of Spitsbergen (Figs 1, 2). Theregional equilibrium line altitude (ELA) for glaciersalong this coast is�/400 m a.s.l. (Hagen et al. 2003a, b)and the present Scottbreen ELA is estimated to be450�500 m a.s.l. (J. O. Hagen, pers. comm. 2006). Infront of the glacier there is a belt of up to 50�60-m highice-cored end moraines (Figs 3, 4) that were clearlyformed during the LIA. Oblique air photographs from1936 (Fig. 2) show that the glacier reached theproximal slope of the outermost moraine at that time(Norsk Polarinstitutt, S36, photographs 1694 and3189). The small glaciers on western Spitsbergengenerally reached their maximum LIA position aroundAD 1900 (Hagen & Liestøl 1990; Lefauconnier &Hagen 1990) and this was probably the case forScottbreen. The present ice margin is some 800 mbehind the LIA moraine, and the lower part of the

DOI 10.1080/03009480601134827 # 2007 Taylor & Francis

Dow

nloa

ded

By:

[Sw

ets

Con

tent

Dis

tribu

tion]

At:

10:0

0 20

Jun

e 20

07

glacier has a significantly lower surface slope thanshown on the air photographs from 1936.

Most important for the present discussion is that thedistal part of the LIA moraine was deposited on top

of a well preserved beach terrace of about 57 m a.s.l.(Figs 4, 5). Thus the LIA moraine shows the maximumextent of Scottbreen after the formation of this terrace,which, as we will demonstrate, is of Allerød age.

Fig. 1. The inset map shows the location of Svalbard. Present-day glaciers are shown in white on the main map. The maximum extent (LastGlacial Maximum�/LGM) of the Barents Ice Sheet is shown beyond the west coast (Landvik et al. 1998; Ottesen et al. 2005). Theapproximate limit of the Younger Dryas ice sheet on Svalbard (modified from Svendsen et al. 2004) is indicated as a line separatingdeglaciation dates of Younger Dryas and early Holocene ages. We assume errors rarely exceeded 30 km along the west coast. In the easternareas the ice margin was beyond the coast and cores with relevant dates were only obtained from far out in the Barents Sea. Therefore the lineis more generalized here and errors may exceed 100 km. Norwegian Polar Institute, digital map.

BOREAS 36 (2007) Younger Dryas cirque glaciers in western Spitsbergen 279

Dow

nloa

ded

By:

[Sw

ets

Con

tent

Dis

tribu

tion]

At:

10:0

0 20

Jun

e 20

07

The beach terraces in front of Scottbreen aredissected by meltwater channels from the glacier(Figs 3, 4) that have exposed sandy gravelly beachdeposits with shell fragments, predominantly of Myatruncata. Four radiocarbon dates from the molluscshells have yielded uncorrected ages in the range of11 6259/50 to 11 7509/80 14C yr BP (Table 1). Assum-ing a marine reservoir age of 440 years, which is thestandard used for Svalbard (Mangerud & Gulliksen1975), the corrected ages are in the range 11 185�11 310 14C yr BP, i.e. a late Allerød age. A new estimateof the present-day reservoir age of 3809/80 (Mangerudet al. 2006) indicates that the ages are slightly older.Precise Allerød�YD reservoir ages have not beendetermined from Svalbard, but three pairs of molluscshell/driftwood dates from eastern Svalbard coveringthe period 7000�9200 14C yr BP gave reservoir ages ofabout 400 years (J. Mangerud, unpublished). Along the

west coast of Norway the reservoir age was also closeto the present day during most of the Allerød, andsome 300 years higher during parts of the YD(Bondevik et al. 2006). We conclude that the datesindicate a late Allerød or possibly an early YD age forthe shells.

In theory, the molluscs may have lived at severalmetres of water depth or they may have been redepos-ited from higher and older terraces. If so, the 57-mterrace could be younger than the shells. However, thesouthern flank of the moraine cross-cuts a distinctbeach terrace at 61 m a.s.l. as well as beach sedimentsat 66 m a.s.l. According to a relative sea level curvefrom the area immediately to the west (Salvigsen et al.1991), the latter altitude represents the marine limitdated to c. 12 000 14C yr BP and the 57-m terracerepresents a late Allerød sea level, and thus supportsour inference that the shells accurately date the terrace.

Fig. 2. Oblique air photo of Scottbreen (Fig. 1) taken on 28th July 1936, approximately towards the southwest. The arrow shows the locationof Fig. 4. Norwegian Polar Institute, photograph no. S36-1694.

280 Jan Mangerud and Jon Y. Landvik BOREAS 36 (2007)

Dow

nloa

ded

By:

[Sw

ets

Con

tent

Dis

tribu

tion]

At:

10:0

0 20

Jun

e 20

07

Fig. 3. Scottbreen with the large Little Ice Age moraines (oblique arrows). As seen from Fig. 2, the glacier front reached the foot of thismoraine as late as 1936. The vertical arrow indicates the dated marine terrace overrun by the glacier (Fig. 4). Younger terraces are seen ashorizontal lines below. Photograph taken 27th August 2002.

Fig. 4. The person is standing on the Allerød-age shoreline, 57 m a.s.l. The dated shells were found by excavating this terrace. The Little IceAge moraine is seen on top of the terrace to the right of the person, and as the large ridge behind and to the left of the person. The glacier islocated to the right of the photograph.

BOREAS 36 (2007) Younger Dryas cirque glaciers in western Spitsbergen 281

Dow

nloa

ded

By:

[Sw

ets

Con

tent

Dis

tribu

tion]

At:

10:0

0 20

Jun

e 20

07

The marine limit was formed during the deglaciation ofthe Barents�Svalbard Ice Sheet (Landvik et al. 1987;Mangerud et al. 1992), meaning that Scottbreenremained inside the position of the LIA morainesfrom the deglaciation at about 12 000 14C yr BP untilabout AD 1900, i.e. also during the YD.

Discussion

One question arising is whether Scottbreen couldhave been cold-based during the YD and overrun theterrace without depositing any till. Today, a noticeablepart of the bouldery material deposited by the glacieris debris originating from rock falls from the steepmountain slopes onto the glacier surface, a supply thatmust have existed even if the glacier was cold-based.However, we could not find any such debris on topof the terraces and we consider it unlikely that theglacier overran the terrace without depositing at leastsome blocks from englacial or supraglacial transport.

During the YD, a remnant of the Barents�SvalbardIce Sheet still covered much of Svalbard further to theeast (Fig. 1) (Landvik et al. 1998; Svendsen et al. 2004).In that sense the glacial history of Svalbard is similar tothe development in Scandinavia, Scotland and the

Alps, where ice sheets or ice caps also existed duringthe YD. However, there are two major differences inthe glacial behaviour.

First, prominent YD moraines have not been foundon Svalbard, even if a slow-down in glacio-isostaticrebound indicates that the retreat of the ice sheet halted(Landvik et al. 1987, 1998). The YD ice sheet extent inFig. 1 is mainly mapped as the up-fjord limit of YDshorelines and from the distribution of deglaciationages in stratigraphical successions (Mangerud et al.1992). A probable reason for the lack of YD morainesis simply that the ice sheet over Svalbard did not re-advance towards the west, in contrast with theScandinavian, Scottish and Alp ice sheets/ice caps.The last ice sheet over Svalbard comprised fast-flowingice along the fjords and less dynamic, possibly cold-based, ice between these ice streams (Landvik et al.2005). Thus any moraines formed during the YD maybe confined to the floors of fjords or even to valleyspresently occupied by fjord-head glaciers. Some mor-aines of postulated YD age, and interpreted as theresult of a glacial re-advance, have indeed beendescribed recently from the floors of Isfjorden and itstributaries (Forwick & Vorren 2005).

Second is the difference demonstrated in this paperand earlier by Salvigsen (1979), Mangerud & Svendsen

Table 1. Radiocarbon dates from the marine terrace in front of the Scottbreen Little Ice Age moraine. All dates were performed on fragmentsof marine shells, probably Mya truncata. d13C was not measured but a value of 1.0� rel. PDB was assumed and used for correction. Thereservoir age is according to Mangerud & Gulliksen (1975).

Field sample no. Lab. no. 14C ageAssumedreservoir age

Reservoirage-corrected 14C age

JM1995-12a Tua-4270 11 7509/80 440 11 3109/80JM1995-12b Tua-4271 11 7609/70 440 11 3209/70JM1995-12c Tua-4272 11 6509/50 440 11 2109/50JM1995-12d Tua-4273 11 6259/50 440 11 1859/50

±±±±

A B

Fig. 5. A. Longitudinal profile of Scottbreen drawn from the 1:100 000 map sheet Van Keulenfjorden, which was constructed from airphotographs taken in 1936 and has contour intervals of 50 m. Issued by Norsk Polarinstitutt 1985. B. Stratigraphical relationship between thedated shoreline and the Little Ice Age moraine. The radiocarbon dates are corrected for a marine reservoir age of 440 years.

282 Jan Mangerud and Jon Y. Landvik BOREAS 36 (2007)

Dow

nloa

ded

By:

[Sw

ets

Con

tent

Dis

tribu

tion]

At:

10:0

0 20

Jun

e 20

07

(1990) and Svendsen & Mangerud (1992), that gla-ciers located west of the ice sheet on Svalbard(Fig. 1) were smaller during the YD than the LIA.In contrast, all glaciers in western Europe were, asalready mentioned, much larger during the YD thanLIA (Fig. 6). The surprisingly small YD glaciers onSvalbard could be the result of warm summers and/orlimited precipitation (snowfall). The YD summerinsolation at this latitude was about 10% higher thantoday (Berger & Loutre 1991), but this was also thecase for northern Scandinavia and therefore it cannotexplain the difference in glacial response between thetwo areas. Unfortunately, there are no observations onSvalbard that can be used to construct the YD summertemperatures but, according to a compilation by Birkset al. (2005), the summer sea surface temperaturessouth of Svalbard were 2�108C colder than today. It istherefore reasonable to assume that summers werecolder on Svalbard too, and we conclude that theglaciers on western Svalbard remained small be-cause of limited snow accumulation. Regional glacierre-advances in northern Norway during the YD(Andersen et al. 1995; Vorren & Plassen 2002) showthat the latitudinal boundary between the dry climatefavouring glacier starvation and the climate withenough precipitation for glacial advances was locatedbetween Svalbard and the northern tip of Norway(Fig. 6). The explanation for the dry climate may be thehypothesis proposed by Birgel & Hass (2004): prevail-ing easterly winds over Svalbard during the YD.Western Svalbard would then be in the precipitationshadow, whereas there would be more precipitation ineastern Svalbard and the Barents Sea. This pattern isconsistent with the snow accumulation postulated fromthe slow-down of isostatic rebound, as mentionedabove. This is also consistent with modelling experi-ments that produce a YD air pressure pattern givingwesterly winds over all of Scandinavia and east-erly winds over Svalbard, particularly during winter(Renssen et al. 2001).

The YD glaciers in northwest Europe were mainlyfed by precipitation brought in with westerly or south-erly winds from the Atlantic Ocean and the Nordic seas

(Sissons 1980; Larsen et al. 1984). However, it is clearthat the glacial re-advances that took place across sucha large and climatically diverse region as westernEurope and Iceland were mainly caused by coldsummers. Precipitation differences would regionallymodify the large-scale pattern, as in Scotland whereglaciers grew in the west whereas the east was in theprecipitation shadow (Gray & Coxon 1991). Benn &Lukas (2006) found that precipitation in northwestScotland was c. 26% higher during the YD than today,whereas in the mountains further east it was close topresent-day levels (Benn & Ballantyne 2005). TheScandinavian Ice Sheet had its largest growth in itssouthwest sector, as a result of the underlying topo-graphy (Mangerud 1980) and, perhaps more impor-tantly, a larger winter precipitation than in other areas(Mangerud 2004). In our interpretation, Svalbardwould be almost a mirror image of Scotland: an icecap in the east and a precipitation shadow in the west.

The glaciers on Svalbard and the Barents Sea grew inconcert with the Scandinavian, British and Alp glaciersduring the period before and around the global LGM(Landvik et al. 1998), in contrast with what we havedescribed for the YD. This could indicate differenttypes of glacial climates between the two cold periods.However, it should be borne in mind that YD was ashort period of about 1300 yr, whereas the LGM wasalmost 10 times longer when the period of ice build-upis included. Conditions for snow accumulation couldtherefore have varied over time during the LGM.Nevertheless, if precipitation was the main factorcausing the difference between mainland Europe andSvalbard during the YD, then less difference in theprecipitation pattern during the LGM ice growthwould be expected. Open water, at least periodicallyand during summers, has been described during theLGM in the North Atlantic and the Norwegian Sea asa source for precipitation on the Scandinavian andBarents ice sheets (Hebbeln et al. 1994; Hald et al.2001). However, open waters have also been reportedfor the YD (Koc et al. 1993; Birgel & Hass 2004)and were probably required for the ice growth inScandinavia.

ELA

dep

ress

ion

(m)

4000 km

Fig. 6. Estimation of how muchlower the equilibrium line altitude(ELA) was during the Little IceAge and the Younger Dryas relativeto the present day ELA. Note thevery different situation inSpitsbergen compared withmainland western Europe.Modified from Mangerud &Svendsen (1990) and Svendsen &Mangerud (1992).

BOREAS 36 (2007) Younger Dryas cirque glaciers in western Spitsbergen 283

Dow

nloa

ded

By:

[Sw

ets

Con

tent

Dis

tribu

tion]

At:

10:0

0 20

Jun

e 20

07

Conclusions

. Scottbreen and other glaciers on western Spitsber-gen were smaller during the YD than the LIA(c. AD 1900), in contrast with all glaciers in westernEurope.

. The explanation for the small YD glaciers inSpitsbergen is starvation of precipitation (snowfall),although higher insolation may have contributed toincreased summer melting.

Acknowledgements. � J. M. thanks co-leaders and students on theUNIS excursion 1995 for help in digging and finding molluscs. Wealso thank John Inge Svendsen and Øystein Lohne, who gave criticalcomments on an earlier version of the manuscript, Jane Ellingsen,who completed the drawings, and Mike Talbot, who corrected theEnglish language. Comments from the journals editor, Jan A.Piotrowski, and reviewers, Jon Ove Hagen and Matthias Forwick,also improved the manuscript and are appreciated.

References

Andersen, B. G., Mangerud, J., Sørensen, R., Reite, A., Sveian, H.,Thoresen, M. & Bergstrøm, B. 1995: Younger Dryas ice-marginaldeposits in Norway. Quaternary International 28, 147�169.

Benn, D. & Ballantyne, C. 2005: Palaeoclimatic reconstruction fromLoch Lomond Readvance glaciers in the West Drumochter Hills,Scotland. Journal of Quaternary Science 20, 577�592.

Benn, D. I. & Lukas, S. 2006: Younger Dryas glacial landsystems innorth west Scotland: an assessment of modern analogues andpalaeoclimatic implications. Quaternary Science Reviews 25, 2390�2408.

Berger, A. & Loutre, M. 1991: Insolation values for the climate of thelast 10 million years. Quaternary Science Reviews 10, 297�317.

Birgel, D. & Hass, H. 2004: Oceanic and atmospheric variationsduring the last deglaciation in the Fram Strait (Arctic Ocean): acoupled high-resolution organic-geochemical and sedimentologicalstudy. Quaternary Science Reviews 23, 29�47.

Birks, H. H., Kristensen, D., Dokken, T. & Anderson, C. 2005:Exploratory comparisons of quantitative temperature estimatesover the last deglaciation in Norway and the Norwegian Sea.American Geophysical Union, Geophysical Monograph Series 158,341�355.

Bondevik, S., Mangerud, J., Birks, H. H., Gulliksen, S. & Reimer, P.2006: Changes in North Atlantic radiocarbon reservoir ages duringthe Allerød and Younger Dryas. Science 312, 1514�1517.

Denton, G. H., Alley, R. B., Comer, G. & Broecker, W. 2005: The roleof seasonality in abrupt climate change. Quaternary ScienceReviews 24, 1159�1182.

Førland, E., Hanssen-Bauer, I. & Nordli, P. 1997: Climate statisticsand longterm series of temperatures and precipitation at Svalbardand Jan Mayen. Norwegian Meteorological Institute, Report 21/97,1�72.

Forwick, M. & Vorren, T. 2005: Late Weichselian deglaciation historyof the Isfjorden area, Spitsbergen. In Forwick, M. (ed.): Sedimen-tary processes and palaeoenvironments in Spitsbergen fjords. Dr.Scient. Thesis, University of Tromsø.

Geirsdottir, A. 2004: Extent and chronology of glaciations in Iceland;a brief overview of the glacial history. In Ehlers, J. & Gibbard, P.(eds.): Quaternary glaciations � extent and chronology. Part I:Europe, 175�182. Elsevier, Amsterdam.

Gray, J. M. & Coxon, P. 1991: The Loch Lomond stadial glaciation inBritain and Ireland. In Ehlers, J., Gibbard, P. & Rose, J. (eds.):

Glacial Deposits in Great Britain and Ireland, 89�105. A. A.Balkema, Rotterdam.

Hagen, J. & Liestøl, O. 1990: Long-term glacier mass-balanceinvestigations in Svalbard. Annals of Glaciology 14, 102�106.

Hagen, J. O., Kohler, J., Melvold, K. & Winther, J. G. 2003a: Glaciersin Svalbard: mass balance, runoff and freshwater flux. PolarResearch 22, 145�159.

Hagen, J., Liestøl, O., Roland, E. & Jørgensen, T. 1993: Glacier atlasof Svalbard and Jan Mayen. Norsk Polarinstitutt, Meddelelser 129,1�141.

Hagen, J., Melvold, K., Pinglot, F. & Dowdeswell, J. 2003b: On thenet mass balance of the glaciers and ice caps in Svalbard,Norwegian Arctic. Arctic Antarctic and Alpine Research 35, 264�270.

Hald, M., Dokken, T. & Mikalsen, G. 2001: Abrupt climatic changeduring the last interglacial�glacial cycle in the polar NorthAtlantic. Marine Geology 176, 121�137.

Hebbeln, D., Dokken, T., Andersen, E. S., Hald, M. & Elverhøi, A.1994: Moisture supply for northern ice-sheet growth during theLast Glacial Maximum. Nature 370, 357�360.

Kerschner, H., Kaser, G. & Sailer, R. 2000: Alpine Younger Dryasglaciers as palaeo-precipitation gauges. Annals of Glaciology 31,80�84.

Koc, N., Jansen, E. & Haflidason, H. 1993: Paleoceanographicreconstructions of surface ocean conditions in the Greenland,Iceland and Norwegian seas through the last 14 ka based ondiatoms. Quaternary Science Reviews 12, 115�140.

Landvik, J. Y., Bolstad, M., Lycke, A. K., Mangerud, J. & Sejrup, H.P. 1992: Weichselian stratigraphy and paleoenvironments atBellsund, western Svalbard. Boreas 21, 335�358.

Landvik, J. Y., Bondevik, S., Elverhøi, A., Fjeldskaar, W., Mangerud,J., Salvigsen, O., Siegert, M. J., Svendsen, J. I. & Vorren, T. O. 1998:The last glacial maximum of Svalbard and the Barents Sea area: icesheet extent and configuration. Quaternary Science Reviews 17,43�75.

Landvik, J., Ingolfsson, O., Mienert, J., Lehman, S., Solheim, A.,Elverhøi, A. & Ottesen, D. 2005: Rethinking Late Weichselian icesheet dynamics in coastal NW Svalbard. Boreas 34, 7�24.

Landvik, J. Y., Mangerud, J. & Salvigsen, O. 1987: The LateWeichselian and Holocene shoreline displacement on the west-central coast of Svalbard. Polar Research 5, 29�44.

Larsen, E., Eide, F., Longva, O. & Mangerud, J. 1984: Allerød�Younger Dryas climatic inferences from cirque glaciers andvegetational development in the Nordfjord area, western Norway.Arctic and Alpine Research 16, 137�160.

Lefauconnier, B. & Hagen, J. 1990: Glaciers and climate in Svalbard:statistical analysis and reconstruction of the Brøggerbreen massbalance for the last 77 years. Annals of Glaciology 14, 148�152.

Mangerud, J. 1980: Ice-front variations of different parts of theScandinavian Ice Sheet, 13,000�10,000 years BP. In Lowe, J. J.,Gray, J. M. & Robinson, J. E. (eds.): Studies in the Lateglacial ofNorth-West Europe, 23�30. Pergamon Press, Oxford.

Mangerud, J. 2004: Ice sheet limits on Norway and the Norwegiancontinental shelf. In Ehlers, J. & Gibbard, P. (eds.): QuaternaryGlaciations: Extent and Chronology, Vol. 1 Europe, 271�294.Elsevier, Amsterdam.

Mangerud, J. & Gulliksen, S. 1975: Apparent radiocarbon ages ofrecent marine shells from Norway, Spitsbergen, and ArcticCanada. Quaternary Research 5, 263�273.

Mangerud, J. & Svendsen, J. I. 1990: Deglaciation chronologyinferred from marine sediments in a proglacial lake basin, westernSpitsbergen, Svalbard. Boreas 19, 249�272.

Mangerud, J., Bolstad, M., Elgersma, A., Helliksen, D., Landvik, J.Y., Lønne, I., Lycke, A. K., Salvigsen, O., Sandahl, T. & Svendsen,J. I. 1992: The last glacial maximum on Spitsbergen, Svalbard.Quaternary Research 38, 1�31.

Mangerud, J., Bondevik, S., Gulliksen, S., Hufthammer, A. &Høisæter, T. 2006: Marine 14C reservoir ages for 19th century

284 Jan Mangerud and Jon Y. Landvik BOREAS 36 (2007)

Dow

nloa

ded

By:

[Sw

ets

Con

tent

Dis

tribu

tion]

At:

10:0

0 20

Jun

e 20

07

whales and molluscs from the North Atlantic. Quaternary ScienceReviews, 25, 3228�3245.

Ottesen, D., Dowdeswell, J. A. & Rise, L. 2005: Submarine landformsand reconstruction of fast-flowing ice streams within a largeQuaternary ice sheet: the 2500-km-long Norwegian�Svalbardmargin (578�808N). Geological Society of America, Bulletin 117,1033�1050.

Renssen, H., Isarin, R. F. B., Jacob, D., Podzun, R. & Vandenberghe,J. 2001: Simulation of the Younger Dryas climate in Europe using aregional climate model nested in an AGCM: preliminary results.Global and Planetary Change 30, 41�57.

Salvigsen, O. 1979: The last deglaciation of Svalbard. Boreas 8, 229�231.

Salvigsen, O., Elgersma, A. & Landvik, J. Y. 1991: Radiocarbondated raised beaches in northwestern Wedel Jarlsberg land,Spitsbergen, Svalbard. In Repelewska-Pekalowa, J. & Pekala, K.

(eds.): Polar Session. Arctic Environment Research, 9�16. Instituteof Earth Sciences, Marie Curie-Sklodowska University, Lublin.

Sissons, B. 1980: Palaeoclimatic inferences from Loch Lomondadvance glaciers. In Lowe, J. J., Gray, J. M. & Robinson, J. E.(eds.): Studies in the Lateglacial of North-West Europe, 31�44.Pergamon Press, Oxford.

Svendsen, J. I. & Mangerud, J. 1992: Paleoclimatic inferences fromglacial fluctuations on Svalbard during the last 20 000 years.Climate Dynamics 6, 213�220.

Svendsen, J. I., Gataullin, V., Mangerud, J. & Polyak, L. 2004: Theglacial history of the Barents and Kara sea region. In Ehlers, J. &Gibbard, P. (eds.): Quaternary Glaciations: Extent and Chronology,Vol. 1 Europe, 369�378. Elsevier, Amsterdam.

Vorren, T. O. & Plassen, L. 2002: Deglaciation and palaeoclimateof the Andfjord-Vagsfjord area, North Norway. Boreas 31,97�125.

BOREAS 36 (2007) Younger Dryas cirque glaciers in western Spitsbergen 285