Weichselian till stratigraphy and glacial history of finnmarksvidda, north Norway

Quaternary International, Vols 3/4, pp. 101-108, 1989. Printed in Great Britain. All rights reserved.

WEICHSELIAN

1040-6182/89 $0.00 + .50 (~) 1990 INQUA/Pergamon Press plc

TILL STRATIGRAPHY AND GLACIAL NORTH NORWAY

HISTORY

OF F I N N M A R K S V I D D A ,

L. O l s e n

Geological Survey of Norway, P.O. Box 3006 Lade, N-7002 Trondheim, Norway

During the last decade, the Geological Survey of Norway has performed surficial and stratigraphical mapping of the Quaternary geology in Finnmark, north Norway. This mapping has revealed a complex Late Pleistocene stratigraphy with tills and intercalated gravels and sands which indicate at least three stadials and two interstadials during the Weichselian. Older glacial events are also recognized. True in situ organic material from an old ice-free period was first found in this area during the 1988 field season. Preliminary pollen counts of this material indicate interglacial conditions of probable Eemian age. Based on all the available stratigraphic data, a model for the Late Pleistocene glacial history has been developed. The locations of the ice accumulation zones during the three recognized stadials were different. The first stadial had ice d o m e s in both the mountains and the lower inland area. The second stadial was mainly a mountain ice dome glaciation, whereas the last stadial or glaciation had mainly inland ice domes. T h e glacial record for northern Fennoscandia indicates that glacial expansion during the Early and Middle Weichselian did not reach a size comparable to that of the Weichselian m a x i m u m , ca. 20 ka BP.

INTRODUCTION During the last decade, Quaternary surficial and stratigraphic investigations have been carried out as a part of a mineral resource mapping programme, performed by the Geological Survey of Norway, in Finnmarksvidda, north Norway. The background data for this paper is information from approximately 160 stratigraphic sequences, in addition to striation and other surficial data (Olsen and Hamborg, 1983, 1984; Often and Olsen, 1986; Olsen et al., 1987; Olsen, 1988,

in prep.). Finnmarksvidda (Fig. 1) is a part of the low preCaledonian plateau. This also represents the northcentral area of maximum isostatic depression caused by •the Fennoscandian inland ice sheet. The Caledonian mountain range located in the north and northwest is a several hundred metre high barrier which the glacier ice had to cross on its way from the central area of glaciation to the coast. Of course, much of the ice drainage followed the main through-cutting valleys, but the low plateau and mountain topography were important factors controlling the ice thickness and ice movement pattern. The topographic conditions are also an important aspect in the initiation of glacial growth in the central areas.

Vuolgamasjohka In 12 sections along a profile of 1300 m length and about 50 m height (Fig. 2) along the river Vuolgamasjohka, all known stratigraphic units of the Late Pleistocene of Finnmarksvidda are represented. The succession is separated into three till sequences by intercalated waterlain sediments. The fourth and lowermost till sequence is assumed to be older than the Weichselian. The lowermost waterlain sediments are mainly glaciofluvial material, representing the initial part of an ice-free period named the Vuolgamasjohka thermomer. It is thought to correlate with the Eemian. This correlation is based on two thermoluminescence (TL) dates of the sediments, both with ages of 120 + 10 ka, and on lithostratigraphic correlation of the younger tills to those of north Finland (Olsen, 1988). The younger waterlain sediments represent Weichselian interstadials, named the Eiravarri and the Sargejohka interstadial, respectively. The former is TL dated to about 100 ka. The latter is inferred to be of Middle or late Early Weichselian age, based on one 14C and one T L date with apparent ages, and on correlation to the T~irend6 interstadial in northern Sweden (Lagerb~ick and Robertsson, 1988).

Sargejohka KEY LOCALITIES The investigations in Finnmarksvidda have revealed a complex Late Pleistocene stratigraphy and glacial history, which is illustrated in two key localities. These are located beside the rivers Vuolgamasjohka and Sargejohka in western and eastern Finnmarksvidda, respectively.

In the course of gold exploration, the 'Sargejohka placer gold field' has been mapped with the help of excavations and drill holes. A composite stratigraphy in a profile of 275 m length indicates at least 5 till units separated by waterlain sediments (Fig. 3). The waterlain sediments are mainly glaciofluvial sand and gravel, but the stratigraphy also involves fluvial and lacustrine sediments. A distinct gyttja silt-sand horizon, exceeding 1 m thick in some places, is interbedded in one of 101

L. Olsen

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FIG. 2. Profile through the loose deposits along the southern bank of the river Vuolgamasjohka, located in western Finnmarksvidda (see Fig. 1).

Till Stratigraphy and Glacial History of Finnmarksvidda -

103

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FIG. 3. Profile through the composite glaciofluvial terrace by the river Sargejohka, located in eastern Finnmarksvidda (see Fig. 1). the glaciofluvial-fluvial sequences. The preliminary pollen counts from the organic horizon indicate interglacial conditions. Small stripes of wood (<35 cm) and fossil imprints of leaves have also been found in the organic horizon. It is assumed that the sediments with the organics are of Eemian age, and therefore that three of the tills are Weichselian. Organic matter in the lower part of the youngest till is ~4C accelerator dated to about 35 ka (insoluble fraction), which suggests that the youngest till is of Late Weichselian age (Olsen, 1988).

SYNTHESIS AND FURTHER CORRELATION TO NORTHERN FINLAND AND NORTHERN SWEDEN A synthesis of the last glacial cycle in this area

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Provided that both the Sargejohka interglacial beds and the Vuolgamasjohka thermomer mentioned above correlate with the Eemian, the stratigraphic successions at Vuolgamasjohka and Sargejohka above this reference level are correlative (Fig. 4). Therefore, a regional Weichselian stratigraphy has been established.

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FIG. 4. Composite glacial stratigraphy at Vuolgamasjohka and Sargejohka and correlations between these stratigraphies.

104

L. Olsen

The Late Pleistocene Glacial History The stratigraphic data can be used to construct a model of the Late Pleistocene glacial history (Figs 6--8). In these figures, arrows indicate ice movement directions inferred mainly from till fabric analyses and stone counts. The location of the first Weichselian ice domes is indicated by apparent elevation curves on Fig. 6. In this model, the ice started to grow and expand to ice sheet dimensions after the Eemian from the mountainous area of northwest Sweden and from centres

involves tills from at least three stadials and intercalated waterlain sediments. The regionality of the glacial events may be illustrated through correlation with neighbouring areas of northern Finland and northern Sweden (Fig. 5; and Olsen, 1988). The character of the young ice-free period in north Finland has long been debated, however, and it is still not evident whether an interstadial younger than the Per/ipohjola ever existed in this area (Hirvas et al., 1988).

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66* FIG. 6. Ice movements (arrows) and inferred location of ice domes (1 to 4) during the first Weichselian glaciation. The eastern part of the Caledonides is indicated with parallel lines. Thick arrows in northernmost Finland imply a dome in the north (?). Glaciotectonic evidence (open arrow) for such a dome is found on Finnmarksvidda (shaded). After Olsen (1988; unpublished

data).

Till Stratigraphy and Glacial History of Finnmarksvidda

the ice mass (e.g. Boulton and Jones, 1979). Therefore, the ice-surface profile might have been steep northwest of the mountains and mostly gentle in the southeast. A gentle ice-surface profile, and therefore a highly lobate configuration of the ice sheet southeast of the mountains may also be inferred from other field evidence. For example, the large drumlins and the thick and composite basal tills from the first Weichselian glaciation in northeast Sweden (Lagerb/ick, 1988a; Lagerb~ick and Robertsson, 1988), northern Finland (Hirvas et al., 1988), and in Finnmarksvidda (Olsen, 1988), are best explained by postulating a very active, sliding glacier with abundant material supply from load concentrated in the basal parts. Such a glacier would probably have a fairly low ice-surface gradient, as suggested above. The glacier expansion after the Eiravarri interstadial commenced from ice growth in the mountain area in the southwest and west (Fig. 7). It continued to move from southwestern and later southern ice centres until its retreat during the next and youngest Weichselian interstadial. The subglacial bed conditions during this and the last glaciation over the Caledonides and the inland area were most likely similar to those of the first Weichselian glaciation. The differences in glacier sliding and ice-surface gradient in the northwest and southeast, however, are expected to have been much smaller for the two youngest glaciations, because the ice sheet expanded offshore during both these, but did not during the oldest Weichselian glaciation. In the fjord areas and on the shelf, the unlithified and deformable sediments would have had the same effect on ice movement and ice-surface gradient as in the inland area southeast of the Caledonides. This factor, together with the probable ice-stream behaviour of the ice flow (e.g. Denton et al., 1986) in and outwards from the fjords would tend

along the Caledonian mountain range in Norway. The initial Weichselian ice movement over Finnmarksvidda is indicated by glaciotectonic deformation of the inferred Eemian sediments and glacially-diverted drainage (Olsen, unpublished data, 1989). Subsequently, the ice accumulation area migrated towards the south and southeast and away from the Caledonides. An inland ice dome was then formed in north Finland, and the oldest recorded Weichselian ice movement indicated by tills in Finnmarksvidda was directed to the northwest from this dome or ice divide. All of these ice centres belong to the first Weichselian glaciation, bracketed in age between the Eemian and the oldest Weichselian interstadial, named Eiravarri in Finnmarksvidda, Per~ipohjola in Finland, and J~imtland in Sweden. Consequently, this glaciation had ice centres both in the mountain range and inland more than 100 km from the mountains. This pattern is in contrast to that of the last glaciation, which had mainly inland ice domes. The glaciation between these two events had an intermediate character as well with regard to the location and development of ice domes. The first Weichselian glaciation is not, except for small local ice caps, thought to have covered the coastal areas of north Norway. The extension far inland and away from the Caledonides is thought to have been much greater (Hirvas et al., 1988; Olsen, 1988). This apparent asymmetric configuration of the ice sheet may partly be due to the precipitation and thus to the atmospheric circulation of the period, but it may also be explained by an ice sheet dynamic response to different subglacial bed conditions. Whereas the dominant and mostly exposed crystalline bedrock in the Caledonides, including the coastal areas of north Norway, induced a retarding force on ice movement, the unlithified and deformable sediments overlying the bedrock far inland favoured smooth and rapid sliding of

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106

L. Olsen

to lower the ice-surface gradient in the northwest, and therefore would minimize the differences in profile between the northwest and southeast. The last glaciation commenced from an ice centre in the low plateau area of northern Finland and northern Sweden (Fig. 8), and continued to move from inland ice centres until its end. This conclusion follows from the associated northwesterly and northerly ice movements over Finnmarksvidda. It is not clear whether the initial ice growth followed a model described by the concept of instantaneous glacierization (Ives, 1957; Ives et al., 1975), perhaps combined with an initial growth of sea ice in the Barents Sea and the Baltic Sea (Hughes, 1986), or if ice movements commenced from reactivation of stagnant ice masses in the northernmost part of Finland. The latter model, however, is apparently well supported by current opinions regarding the stratigraphy of north Finland (Saarnisto and Hirvas, 1989) and the evidence of warm-based ice during an early part of the last glaciation in Finnmarksvidda (Olsen, 1988).

2J"

GLACIATION CURVE FOR THE N O R D K A L O T T AREA Stratigraphic data from five localities has been projected on a profile which runs approximately normal to the main ice-marginal zones during the last deglaciation (Fig. 9). Two of the localities have been investigated by the University of Troms0 (1, 2), while the others have been investigated by the Geological Surveys of Norway (3, 4) and Sweden (5). The resulting glaciation curve indicates one restricted Early Weichselian glaciation, possibly correlating with Marine Isotope Substage 5d. It also indicates a more extensive Early or Middle Weichselian glaciation, which may correlate with Substage 5b or perhaps Stage 4. The northern part of the Fennoscandian ice sheet had no phase of glacial expansion during the Early and Middle Weichselian that seems to have approached that of the Late Weichselian maximum, however. This is in concordance with some other ice margins, at least in the southwest, where the Fennoscandian ice sheet

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As would be expected from an area beneath an ice accumulation zone, very little basal till or other signs of active ice conditions from the Late Weichselian are commonly found in the northernmost and northeasternmost part of Sweden (Lagerb/ick, 1988b). In Finnmarksvidda, the tills of that age are commonly much thicker (Olsen, 1988). This difference in till thickness may, however, be even better explained by the prevailing cold-based ice conditions in the central areas during the last glaciation (Lagerb/ick, 1988b; Sollid and Sorbel, 1988), while Finnmarksvidda must have been covered by an at least partly warm-based ice sheet, as indicated by striations, subglacial waterlain sediments, and basal tills (Olsen, 1988).

prior to the Late Weichselian probably had an extent much less than during its maximum (Mangerud, 1988; Larsen and Sejrup, 1990). In the south the ice sheet configuration seems to have been rather complex. TL dates of glaciofluvial sediments indicate that a Scandinavian ice sheet reached almost to Denmark about 60-70 ka BP (Kronberg, 1988), whereas no Weichselian glaciation prior to the maximum reached the southernmost part of Sweden (Lundqvist, 1987; Lagerlund, 1987; Ringberg, 1988). The first Weichselian ice sheet as inferred from many TL dates on glacigenic deposits, reached Poland about 60 ka BP (Drozdowski and Fedorowicz, 1987). If all these dates and information are correct, and the

107

Till Stratigraphy and Glacial History of Finnmarksvidda

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FIG. 9. Above - - Map with location of profile and sites of stratigraphic information used in the glaciation curve below. The maximum extension of the Late Weichselian is indicated. After Olsen (1988). Below - - Glaciation curve for northern Fennoscandia during the Last Interglacial-Glacial Cycle. The letters S, T, E, P, J, V, T and L, as they are used in the central column, symbolize the local names and position of the interstadial and interglacials indicated in Fig. 5. After Olsen (1988).

associated events belong to one major stadial, then the Fennoscandian ice sheet around 60-70 ka BP had a southerly extension with major ice lobes filling the basins of Skagerrak in the west and the Baltic Sea in the east. This ice sheet configuration in the Baltic suggests an ice dome location far east of the mountain range, perhaps over the Gulf of Bothnia. With a classical ice divide without major domes and with a less lobate ice pattern, it would be difficult to explain why no Early or Middle Weichselian glaciation reached southernmost Sweden. The suggested lobate ice sheet configuration in the south would fit well with a late stage of the second Weichselian glaciation in northern Fennoscandia. It would also fit well with the inferred ice flow pattern for the early part of the last glaciation in the north. In view of the chronologic and stratigraphic framework used (Fig. 9), no suggested alternative correlation models are possible. ACKNOWLEDGEMENTS The background data for this paper was provided by the Geological Survey of Norway. In addition, the paper has profited from the collaboration between the Geological Surveys of Finland, Norway, and Sweden in the Nordkalott Project 1980-86. The manuscript has

been critically reviewed by colleagues at the Survey. The pollen counts referred to were done by P.U. Sandvik and S.F. Selvik. Drawing of the figures has been carried out by G. GrOnli. The author is grateful to all these institutions and persons.

REFERENCES

Boulton, G.S. and Jones, A.S. (1979). Stability of temperate ice caps and ice sheets resting on beds of deformable sediment. Journal of Glaciology, 24, 29-42. Denton, G.H., Hughes. T.J. and Karl6n, W. (1986). Global ice-sheet system interlocked by sea level. Quaternary Research, 26, 3-26. Drozdowski, E. and Fedorowicz, S. (1987). Stratigraphy of Vistulian glaciogenic deposits and corresponding thermoluminescence dates in the lower Vistula region, northern Poland. Boreas, 16, 139-153. Hirvas, H., Lagerb~ick, R., M~ikinen, K., Nenonen, K., Olsen, L., Rodhe, L. and Thoresen, M. (1988). The Nordkalott Project: studies of Quaternary geology in northern Fennoscandia. Boreas, 17, 431--437. Hughes, T J . (1986). The marine ice transgression hypothesis. Geografiska Annaler, 69 A (2), 237-250. Ives, J.D. (1957). Glaciation of the Torngat Mountains, northern Labrador. Arctic, 10, 67-87. Ives, J.D., Andrews, J.T. and Barry, R.G. (1975). Growth and decay of the Laurentide ice sheet and comparisons with FennoSkandinavia. Die Naturwissenschaften, 62. Kronborg, C. (1988). Senk vartwr stratigrafi baseret p~ TL. Abstract at

'XXIV Uppsalasymposiet Senkvarti~r Stratigrafi i Norden 150,00015,000 BP'. University of Uppsala, Abstracts. 27. Lagerb~ick. R. (1988a). The Veiki moraines in northern S w e d e n -

108

L. Olsen

widespread evidence of an Early Weichselian deglaciation. Boreas, 17, 469--486. Lagerb~ick, R. (1988b). Periglacial phenomena in the wooded areas of northern Sweden - - a relict from the T~irend6 Interstadial. Boreas, 17, 487-499. Lagerb~ick, R. and Robertsson, A.-M. (1988). Kettle h o l e s stratigraphical archives for Weichselian geology and palaeoenvironment in northernmost Sweden. Boreas, 17, 439-468. Lagerlund, E. (1987). An alternative Weichselian glaciation model, with special reference to the glacial history of Skhne, South Sweden. Boreas, 16, 433-459. Larsen, E. and Sejrup, H.P. (1990). Weichselian land-sea interactions; western Norway-Norwegian Sea. Quaternary Science Reviews, 9, 85-97. Lundqvist, J. (1987). Late Weichselian glaciation and deglaciation in Scandinavia. In: Sibrava, V., Bowen, D.Q. and Richmond, G.M. (eds), Quaternary Glaciations in the Northern Hemisphere. Quaternary Science Reviews, 5, 269-292. Mangerud, J. (1988). The Scandinavian ice-sheet through the last interglacial/glacial cycle. Palaoklimaforschung, 1, Academy of Science and Literature, Mainz. Often, M. and Olsen, L. (1986). Gold transport in till in the complex glaciated Karasjok greenstone belt area, Finnmark, Norway. In: Prospecting in Areas of Glaciated Terrain 1986, pp. 83-94. Institute of Mining and Metallurgy, London.

Olsen, L. (1988). Stadials and interstadials during the Weichsel glaciation on Finnmarksvidda, northern Norway. Boreas, 17, 517539. Olsen, L, (in prep.). Karasjok. Quaternary geological map, scale 1:250,000, air-photo interpreted, with description (in Norwegian) (abstract in English). Geological Survey of Norway. Olsen, L, and Hamborg, M. (1983). Morenestratigrafi og isbevegelser fra Weichsel, s~rvestre Finnmarksvidda, Nord-Norge. English summary. Norges geologiske undersckelse, 378, 93-113. Olsen, L. and Hamborg, M. (1984). Weichselian till stratigraphy and ice movements, a model based mainly on clast fabric, Finnmarksvidda, Northern Norway. In: K6nigsson, L.-K. (ed.), Ten Years of Nordic Till Research. Striae, 20, 69-73. Olsen, L., Hamborg, M., Bargel, T.H. and Alstads~eter, I. (1987). Enonteki~. Quaternary geological map, scale 1:250,000, air-photo interpreted, with description (in Norwegian) (abstract in English). Geological Survey of Norway. Ringherg, B. (1988). Late Weichselian geology of southernmost Sweden. Boreas, 17, 243-263. Saarnisto, M. and Hirvas, H. (1989). The Last Interglacial-Glacial Cycle in Finland. Terra, Abstracts 1, 1989, 63. Sollid, J.L. and S~rbel, L. (1988). Influence of temperature conditions in formation of end moraines in Fennoscandia and Svalbard. Boreas, 17, 553-558.