The Quaternary Record of Eastern Svalbard - an Overview

The Quaternary record of eastern Svalbard - an overview

JON Y. LANDVIK, CHRISTIAN HJOKT. JAN MANGERUD, PER MOLLER and OTTO SALVIGSEN

Landvik, J. Y., Hjort, C., Mangerud. J.. Mdler, P. & Salvigsen. 0. 1995: The Quaternary record of eastern Svalbard - an overview. Po/ar Research /4(2),Y5-103. The eastern part of the Svalbard archipelago and the adjacent areas of the Barents Sea were subject to extensive erosion during the Late Weichselian glaciation. Small remnants of older sediment successions have been preserved on Edgeoya, whereas a more complete succession on Kongsoya contains sediments from two different ice-free periods, both probably older than the Early Weichselian. Ice movemeht indicators in the region suggest that the Late Weichselian ice radiated from a centre east of Kong Karls Land. On Bj~rnOya,on the edge of the Barents Shelf, the lack of raised shorelines or glacial striae from the east indicates that the western parts of the ice sheet were thin during the Late Weichselian. The deglaciation of Edgeoya and Barentsoya occurred ca 10,300 BP as a response to calving of the marine-based portion of the ice sheet. Atlantic water, which does not much influence the coasts of eastern Svalbard today, penetrated the northwestern Barents Sea shortly after the deglaciation. At that time, the coastal environment was characterised by extensive longshore sediment transport and deposition of spits at the mouths of shallow palaeo-fjords. Jon Y. Lundoik. The University Courses on Svalbard (UNIS), P.O. BOX 156. N-9170 Longyearbyen, Norway; Christian Hjort and Per Moller, Department of Quaternary Geology. Lund Uni~~ersity,Solvegatan 13, S-223 62 Lund, Sweden; Jan Mangerud, Department of Geology, University of Bergen, Alkgr. 41, N- 5007 Bergen, Norway; Otto Saloigsen, Norwegian Polar Institute, P. O. Bor 5072 Majorsnra, N-0301 Oslo, Norway.

the surrounding land mass. Thus, the eastern Introduction islands of the Svalbard archipelago can now con- The Quaternary geology of the Svalbard archi- tribute towards an integrated understanding of pelago (Fig. 1) has been the subject of extensive the Quaternary development along a profile from research during the last three decades. The inves- the central Barents Sea to the continental shelf tigations have concentrated in particular on the west of Svalbard. In this paper we summarise the largest island, Spitsbergen (Fig. 2), and models main results obtained from the PONAM have been developed for the Late Quaternary expeditions to Edgeoya. Barentsaya, Kongsoya glaciations (Boulton 1979; Miller 1982; Landvik and Bjomoya, and use the new data to compare et al. 1992a; Mangerud & Svendsen 1992), glacio- and modify the present models of the Quaternary isostatic rebound (Schytt et al. 1968; Forman history of Svalbard and the Barents Sea. 1990; Forman et al. 1995) and the Holocene marine conditions of both Svalbard and the adjacent seas (Salvigsen et al. 1992). However. due to the more difficult accessibility, less progress has The Late Quaternary record been made in understanding the Quaternary geo- The pre-Late Weichselircn logy of the eastern islands of the archipelago such as Edgeoya, Barentsaya and Kong Karls Land Sediments which record the Late Quaternary ice (Fig. 2). These islands, however, are critical for growth and decay have been preserved in several the understanding of the geology of the northern sections on Spitsbergen (Boulton 1979; Troitsky Barents Sea, and their geological history is fun- et al. 1979; Miller 1982; Miller et al. 1989; Landvik damental for the development of regional models. et al. 1992a; Mangerud & Svendsen 1992; Man- As a result of both the PONAM programme gerud et al. 1992) and an updated glaciation curve (Polar North Atlantic Margins. Late Cenozoic for the last intergIacial/glacial cycle of Svalbard Evolution) and hydrocarbon exploration in the and the northern Barents Sea was recently sug- Barents Sea, renewed interest has been expressed gested by Mangerud et al. (1996), based on cor- in the Quaternary geology of the sea floor and relation of the different sediment successions. 96 J. Y. Landuik et al.

Fig. I. Regional map showing the main areas discussed in the text. The present oceanic surface circulation is indicated.

These studies inferred from the Spitsbergen sites deposited along the northern valley slope at a that the northern Barents Sea was covered by ice time when the seal level was >57m above the sheets during most of the Weichselian. except for present, and these were later covered by sub- two intervals at around 80 ka and 30-50 ka. The glacial till (Moller et al. 1995). Sub-till sediments Barents Sea part of this reconstruction is based have also been reported from the adjacent Rosen- on the assumption that high relative sea levels bergdalen by Boulton (1990). Unfortunately. during ice free periods on Spitsbergen were neither of these latter units could be dated. caused by glacial loading in the northern Barents The islands of Kong Karls Land (Fig. 2) hold Sea. a key position with regard to understanding the During the PONAM expeditions. pre-Late last interglacial/glacial cycle of the northern Weichselian sediments were found on Edgesya Barents Sea. Shells from Svenskoya have been and on Kong Karls Land (Fig. 2). On northeastern dated to 40,000~~and older, and four drift- Edgesya. ice-free conditions are reflected by shell wood logs from Kongsoya were more than 40,000 fragments embedded in beach sediments (Bon- years old (Salvigsen 1981). One whalebone from devik et al. 1995). The fragments yield infinite eastern Kongseya was dated to 33,600 ? 970 radiocarbon ages. and mean amino acid ratios which was considered to be a minimum age by (aIle/Ile total) of 0.082 t- 0.019 (n = 6). These Salvigsen (1981). From northwestern Kongsoya, ratios are similar to those from the oldest ice- Ingolfsson et al. (1995) report sediment suc- free period on Kongsoya (Ingolfsson et al. 1995). cessions from two ice-free periods older than the which are postulated to be of pre-Eemian age. Late Weichselian. Biostratigraphical studies sug- In Visdalen on western Edgeoya (Fig. 2). gest that the climate then was similar to or slightly coarse-grained fan delta sediments were warmer than the present (Ingolfsson et al. 1995). Quaternary record of eastern Soalbard 97

80 I 1.5. 21' 4

Fig. 2. Deglaciation dates from Edgeoya and Barentscdya. The two oldest dates have been listed from most of the study areas. Details are given in Table 1. The insert map also shows the location of Kongsfjorden (K), Isfjorden (I), Van Mijenfjorden (VM) and Agardhbukta (A). The glaciers on Edgeoya and Barentscdya are shaded. 98 J. I'. Lardilik et al.

The older period is characterised by amino acid However, less is known about the exact timing ratios (aIle/Ile total) of 0.W ? 0.009. and coin- and dynamics of the ice sheet. parison with the amino acid ratios in the Eeniian The pattern of glacioisostatic rebound shows a deposits at Kapp Ekholm (Mangerud & Svendsen centre of maximum uplift in the northern part of 1992) and luminescence dates. both support a pre- the Barents Sea (Schytt et al. 1968; Forman 1990). Eemian age. The vounger period. with amino acid Bondevik et al. (1995) present detailed relative ratios of 0.043 ? 0.008. is interpreted to be of sealevel curves from Edge~yaand Barents~ya, either Earlv Weichselian or Eemian age (Ingolfs- and their revised isobase map for 10,000 "'C years son et al. 1995). BP suggest a centre of uplift southeast of Kong Several scenarios for the progression of the last Karls Land (Fig. 2). This compares with the iso- interglacial/glacial cycle of Svalbard and static models of Lambeck (1995, 1996) who also the northern Barents Sea have been suggested suggested that the ice sheet had its maximum ice (Lindner et al. 1984; Larsen et al. 1991; Landvik thickness southeast of Kongsaya. Glaciological et al. 1997a: Mangerud Xr Svendsen 1992; Man- modelling of the ice sheet (Siegert & Dowdeswell gerud et al. 1996). Through time, these models 1995) suggests a similar location for the maximum have evolved a better foundation for recon- ice thickness. Based on reconstructions of ice flow structing the area of the Barents Sea proper. directions, it has been suggested that the Svalbard Previous models (Larsen et al. 1991; Mangerud and Barents Sea Ice Sheet consisted of several & Svendsen 1992) suggested almost contem- confluent ice domes and not only one single ice poraneous glacials and interstadials over Spits- dome centered over the Barents Sea (Landvik & bergen and the Barents Sea. whereas the later Salvigsen 1985; Mangerud et al. 1992). However, ones (Landvik et al. 1992a; Mangerud et al. 1996) this ice flow pattern may represent only phases of suggest a long period of ice cover over the sea to growth. or decay, of the ice sheet. the east of the Svalbard islands during the Early In the peripheral region of the former ice sheet, Weichselian. If the younger ice-free period on ice streams have been shown to drain along the Kongs~ya(Ingolfsson et al. 1995) is of an Early Bjsrnaya and Storfjorden troughs on the Barents Weichselian age. we assumed that the whole Bar- Shelf (Elverhoi et al. 1993), and along Van ents Sea must have been deglaciated. However, Mijenfjorden and Isfjorden on Spitsbergen (Man- the time control so far is too rough to justify any gerud et al. 1992). Different sets of ice movement revision of the latest models (Mangerud et al. indicators (see review by Salvigsen et al. 1995) 1996) for the last interglacial/glacial cycle of the show phases when ice flow radiated from a centre Svalbard/Barents Sea region. east of Svalbard. Evidence for an ice sheet centred east of Kong Karls Land is also found on Kongs- sva. where the sediments from the younger ice- The dwrrmics of rlw Lorp Weichselian ire sheet free period were deformed by a topographically The extent of the ice sheet over Svalbard and the independent glacier moving from the northeast Barents Sea during the Late Weichselian has been (Ingolfsson et al. 1995). Even if these sediments the subject for debate for three decades (e.g. are of an Early Weichselian age, we assume that Schvtt et al. 1Y68; Boulton 1979: Salvigsen 1981; such an ice movement must be attributed to the Mangerud et al. 1992; Elverhai et al. 1993). Based large Late Weichselian ice sheet. on the post glacial uplift pattern (Salvigsen 1981; On a larger scale, there is a systematic variation Forman 1990). and the distribution of sea floor in the sediment distribution on the Barents Sea sediments. moraine ridges. and subglacially floor that fits the theoretical zonation of glacial formed flutes (Eherhsi ct al. 1993). there is a erosion and deposition under an ice sheet as pro- consensus today that the ice sheet covered at least posed by Sugden (1977,1978). The shallow banks the northern Barents Sea. For a short period. north of 74". where bedrock is exposed over outlet glaciers adwnced to the continental shelf ca 50% of the area and sediment thickness is \vest of Spitsbergen (Manperud et al. 1992; Svend- <25 ni (Solheim & Kristoffersen 1984), can be sen rt :it. 1992) and to the western Barents Sea ascribed to a zone of erosion. This contrasts with shelf (Elverhmi et al. 1993). Recent models of ice the zone of deposition to the southwest, where sheet extent based on uplift data also suggest that large sedimentary wedges increase in thickness the ice sheet extended to the shelf edge to the towards the shelf margin, e.g. in the Bj~rn- west and north of Svalbard (Lambeck 1995,1996). 0yrenna and Storfjordrenna troughs (Solheim & Quuternary record of eastern Siialb~itd 99

Kristoffersen 1984; Vorren et al. 1990). Also the al. 1995). We assume that the rapid emergence distribution of pre-Late Weichselian sediments between 10,000 and 9000 BP. (Salvigsen 1981; on the Svalbard islands fits such a model. As Bondevik et al. 1995) is as a response to a major reported here. Edgeoya and Barentsoya were unloading just prior to 10,000~~.The cor- subjected to extensive glacial erosion during the respondence in time between the deglaciation last glaciation, whereas most sediment accumu- dates of ca 10,000 BP for both Agardhbukta (Fig. lations of pre-Late Weichselian age are found on 2) on the western side of Storfjorden (Salvigsen western Spitsbergen (Landvik & Salvigsen 1985; & Mangerud 1991) and on Kongs~ya(Salvigsen Miller et al. 1989; Lonne & Mangerud 1991; 1981) also suggests that the marine part of the ice Landvik et al. 1992a; Mangerud & Svendsen sheet vanished due to rapid calving. At this time, 1992). Several of these accumulations are in glac- the nature of the ice flow across high areas thus ially-shaped fjord and valley basins or on the changed from being regionally governed by the strandflat, and show that the Late Weichselian configuration of the Barents Ice Sheet, to being glacial erosion was probably less important in more locally affected by the topography beneath forming the glacial topography of western Spits- the last ice remnants on the islands. On Bj~rnoya bergen, (Fig. l), glacial striae reflect only a local ice cap centred on the southern and middle part of the island (Salvigsen & Slettemark 1995). The ice cap The Late Weicliselian deglaciation may also have been a remnant of the ice sheet, The western margin of the Barents Ice Sheet formed by rapid withdrawal of the western margin reached the shelf break to the west during the of the Barents Ice Sheet. Basal dates from lake Late Weichselian (Elverhoi et al. 1993; Mangerud sediments on the island show that most of the et al. 1992), and the glacier must also have sur- local glaciers had vanished before 9800 BP rounded or covered BjQrnQya on the south- (Wohlfarth et al. 1995). western margin of Spitsbergenbanken. As indicated by many radiocarbon dates, the ice The Holocene sheet started to recede from the outer coast of Spitsbergen at 13,000 BP (Forman 1990; Man- The sediment records of Edgeoya and Barents~ya gerud et al. 1992), whereas the central fjord show that the physical environment at the region first became ice free ca 10,000 BP (Man- Weichselian/Holocene transition was different gerud et al. 1992). From the eastern part of the from today. The large transverse ridges found at archipelago, the timing of the deglaciation had the mouths of several valleys were interpreted by before the PONAM expeditions been based on Biidel (1968) to have been formed by longshore only a few dates from Edgeoya and Barentsoya currents. They were later reinterpreted by Nagy (Knape 1971: Nagy 1984; Forman 1990) and from (1984) as ice contact deltas, and taken as evidence Kongsoya (Salvigsen 1981). There were no satis- for a halt in the deglaciation, called the “Visdalen factory date$ for the deglaciation of Bjorn~ya event”. New investigations of the sediment suc- until the studies of Wohlfarth et al. (1995). cessions in Visdalen on Edgecdya (Fig. 2) (Moller Dating of the local deglaciation has been an et al. 1995) support Biidel’s view, and show that aim of the PONAM studies, and a regionally well- thick piles of sediments were deposited as fan distributed set of new dates from Edgeoya and deltas which also fed longshore currents, Barents~yais now available (Table 1, Fig. 2). depositing large ridge-formed spits at the mouths These indicate a contemporaneous deglaciation of inundated valleys between 10,000 and at around 10,300~~along both the eastern and 9000 BP. The elevations of other similar ridges at western coasts of the islands. However, dating of the mouths of shallow paleo-fjords on Edge~ya the oldest part of the sea level curves from the and Barentsoya, suggest that these are of the area (Bondevik et al. 1995), indicates that the same age as the one in Visdalen. deglaciation occurred ca 500 radiocarbon years The formation of large spits (Miiller et al. 1995) later. The deglaciation probably progressed by during a period of rapid regression (Bondevik et rapid calving in both Storfjorden and Olgastretet al. 1995), suggests that the longshore sediment (Fig. 2), and remnants of the glacier remained in transport during the Preboreal was considerably the interior of Spitsbergen (Mangerud et al. 1992) greater than today. In the situation immediately and Edgeoya (Landvik et al. 1992b; Moller et following the deglaciation, we assume that uncon- lY75)

Frankcnhalvava 7X034'N 21"20'F. IO.265 2 YS X7-776 I.andvrk CI al (1992h) 9450 t I I0 X7-7711 Landvrk ct al. (IY92h) Kdpp Zichcn 78'33" ?1"5X'E Y615 5 1111 x7-x 15 Umdcvik CI ;II (lYY5) YSO5 2 7(1 XX-2MI Bondcvik ct ;iI (lYY5) lladalcn 7X"ll'N 2I"SS'E X77(1 i 50 (1BI Ih Forrnun (1090) Humh 7H"I:'N 23"(WI'E YXXS 5 13(1 XX-S?SA Hondevik ct at. (1995) 9620 -c 1311 XX-527 Hondcvik ct al. (1995) Blifjorddalcn 77"SY)'N 22"SY'E l(1.330 -c I l(1 xx-5x3 Landvik ct al. (IYYZh) YSYO f YII XX-56X Landvik ct al. (1992h) Alhrcchthrccn 77"57'N 23Y15'E Y405 2 711 X7-Xl(l Ronncrt d L.;indvik ( IYY3) 0360 f l(15 X7-XO6 Konncri d l.;indvik (1993) Dianadalen 77%" 23"lh'E 10.2(Ml % Y5 X6-706 Ihindevik ct al. (lYY5) 959.5 t 105 X6-705 Dondcvik et al. (1995) Dyrdalen 77045" 22"45'E 9x40 t 130 xx-737 Adriclsson et al. (IYYZh) Guldalen 77"53'N 21"3Y'E Y705 ? 135 86-418 Hansen & Knudsen (IYYS) 9675 2 50 X 6- 4 2( ) Hanscn & Knudrcn (1995) Srnelledalcn 7757" 22"ZX'E YYYO ? 80 GBXS Fvrrnan (IYYO) Raddedalen 78"00'N 21"36'E 10.015 lr 75 86-572A Bondcvik ct al. (lY95) 9565 -c 80 86.5728 Bondevik ct al. (1995) Visdalen 78"03'N 21"IS'E l(l.lY0 f 320 - Nagy (1984)

9820 f 130 88-675 AAR-908 Mtiller et al. (1995) 9810 2 200 87-702 AAR-838 Moller et al. (1995) Talavera 78"15'N 21"07'E 10.370 lr 60 GB123 SRR-2204 Forrnan (1990) Quaternary record of eastern Svalbard 101 solidated glacial sediments deposited on unstable periods, with climates similar to or slightly slopes were the most important source for the warmer than the present on Kong Karls Land, sediments deposited in the alluvial fans and fan show periods when the Barents Sea was corn- deltas. The latter process may have been pletely deglaciated. enhanced by an early Holocene hydrographic 3. Both the improved isobase reconstructions regime which was different from the present. The and isostatic modelling suggest that the Late Svalbard waters experienced a stronger influx of Weichselian ice sheet had its maximum thicknes, Atlantic water during the early and middle southeast of Kong Karls Land. Holocene as reflected by the influx of thermo- 4. Detailed relative sea level curves from philous molluscs already around 9500 BP (Sal- Edge~yaand Barentsaya show that the glacio- vigsen et al. 1992). However, a detailed Preboreal isostatic uplift 10,000-9000 BP was rapid, climatic record based on foraminifera from raised responding to a major unloading just prior to glacimarine deposits at eastern Edgeoya suggests 10,000 BP. that the steady amelioration of the marine con- 5. During the last deglaciation, the marine- ditions was interrupted by a short cooling between based part of the ice sheet over eastern Svalbard 9600 and 9400~~(Hansen & Knudsen 1995). underwent rapid calving, and most of the glacier From findings of subfossil Mytilus edulis, a mini- fronts receded beyond the present day coasts of mum age of 8800~~was obtained for the first Edge~yaand Barentscbya before 10,300BP. major influx of Atlantic water reaching Edgecbya 6. The coastal environment immediately after (Hjort et al. 1995). This shows that the circulation the deglaciation was characterised by extensive in the northwestern part of the Barents Sea was longshore sediment transport. Large spit ridges different during the early Holocene, and it poss- were formed at the mouths of several valleys. ibly may also have influenced the strength and 7. Subfossil Mytilus edulis indicate a major pattern of the near-shore currents in the area. influx of Atlantic water into the northwestern At the same time, during the Preboral, the Barents Sea between ca 8800 and SO00 BP. glaciers on Edgeoya receded beyond their present Acknowkdgemeni.s. - This paper is mainly the result of the limits (Ronnert & Landvik 1993) and the modern expeditions within the PONAM (Polar North Atlantic Margins. flora of the area was established (Bennike & Late Cenozoic Evolution) programme in IYYI and 1993. Fund- Hedenas 1995). Most glacier margins in the area ing for the fieldwork was provided by the research councils in are today characterised by the retreat from young Denmark, Norway, Sweden and the U.K., as well as by the participants own institutions. The Norwegian group also moraines formed by stacking of sheets of sedi- received financial support from Norsk Hydro. Saga Petroicurn. ments during the Little Ice Age (Adrielsson et al. Statoil and the Norwegian Petroleum Directorate. and the 1992; Ronnert & Landvik 1993; Dowdeswell & Swedish group from the Polar Research Secretariat Helicopter Bamber 1995). transport in the field was made possible by a grant from the European Commission to the European Science Foundation The Norwegian Polar Institute provided log~sticsupport, and the use of R/V LANCE during initial reconnaissance work and for transport to and from eastern Svalbard. Norwegian Polar Conclusions Institute expedition leaders T. Siggerud (1991) and J. Hdugland (1993) were most helpful to the two PONAM expeditions. In The collaborative efforts during the PONAM 1991, B. Torgerhagen (pilof) and K. Nilsen (engineer) skillfully expeditions to eastern Svalbard and Bjorncbya operated the helicopter from a base camp at Kapp Lee at resulted in a new understanding of the geological Edgeoya. H. Eggenfellnet assisted in base operations. The Norwegian Coast Guard transported two field parties to development of this part of the Svalbard archi- Bjornoya in 1993. All operattons in eastern Svalbard werc pelago and the Barents Sea. The main results are made possible through kind permissions from the Governor summarised below. on Svalbard, who also assisted with helicopter transport from Kongsoya in 1993. To all these persons and institutions we offer 1. Glacial erosion during the Late Weichselian our sincere thanks Anally. all parttctpants in the PONAM removed most of the older sediments from the project are thanked for the open communication. and all the eastern parts of the Svalbard archipelago and lively discussions that have contributed to the results we sec today. adjacent parts of the Barents Sea. The erosion in this region was more extensive than on the western coast of Spitsbergen. where several older References sediment successions have been preserved. Adnelsson, L , Johansson. K & Hjort, C 1992 Deglaciation 2. Deposits from two pre-Late Weichselian and Holocene stratigraphy tn a Llttle Ice Age comporite 102 J. Y. Lnndiiik er al

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