In the Bergen Area, the Existence Has Long Been Known Both of Fossil-Bearing Tills and of Marine Sediments Underlying Till (Rekstad 1900, Kolderup 1908, Pp

INTERGLACIAL SEDIMENTS AT FJØSANGER, NEAR BERGEN, WITH THE FIRST EEMIAN POLLEN-SPECTRA FROM NORWAY

JAN MANGERUD

Mangerud, J.: Interglacial sediments at Fjøsanger, near Bergen, with the first Eemian pollen-spectra from Norway. Norsk Geologisk Tidsskrift. Vol. 50, pp. 167-181. Oslo 1970. A description is given of marine sediments which were somewhat deplaced by the ice during the Last Glaciation. Of macro-fossils, finds were made of seal-bones, fragments of molluscs and remnants of wood. Radiocarbon datings gave an age of more than 40,000 years. The foraminiferal fauna shows northerly boreal conditions, with a neritic facies. Pollen analyses indicate a dense forest of Picea, Pinus, Betula, Alnus and Corylus. Picea is of special interest, as it does not grow in the area today. On the basis of the pollen analyses, the sediments are presumed to be of Late Eemian age.

l. Mangerud, Geological Institute, Dept. B, University of Bergen, Olaf Ryes vei 19, 5000 Bergen, Norway.

In the Bergen area, the existence has long been known both of fossil-bearing tills and of marine sediments underlying till (Rekstad 1900, Kolderup 1908, pp. 55-66, Undås 1942 and 1963, p. 13, H. Holtedahl 1964). Radiocarbon datings (Nydal 1960, pp. 88-89, 1962, pp. 171-172) have hitherto shown a Late Weichselian age. The present author has made a systematic investiga tion of these sediments. During the work with fabric analyses of a deposit of this nature at Fjøsanger (Fig. 1 ), fossils were found which suggested a greater age. This was subsequently confirmed by two Ca-datings, which showed an age of over 40,000 years. The present paper contains the results of investigations made in a small natural section alongside the road. It is hoped that the opportunity will at some later date present itself for the boring, or preferably the excavation, of a deeper section, and that it will thereby perhaps be possible to obtain a more complete stratigraphy.

Petrography of the sediments

Situation and extension The deposit is situated at Fjøsanger, immediately south of the Bergen city boundary (Fig. lb). Here unconsolidated sediments are found covering an area 50 m in breadth and 400-500 m in length along the north-western bay 168 JAN MANGERUD

Youngest < GLACIAL STRIAE Oldest

4km Fi .lb

Fig. la. Key map of Southern Norway. The occurrence of Picea is indicated according to Gelting (Cit. Fægri 1950, Fig. 1). Hatching: continuous occurrence. Dots: isolated stands. B. - Bergen. Fig. lb. The Bergen district. Contour interval 90 m. Maximum deeps in the fiords (in meters). The locality discussed is marked by a broken line at Fjøsanger. Main directions of glacial striae are marked. of the Nordåsvannet inlet. No section occurs throughout the deposit, but the thickness is assumed to be 5-10 m. On the upper side of the road the material is situated at a maximum stable slope gradient, and it appears that it consists wholly of clayey and silty sediments; it is, however, unclear to what extent the whole deposit has the same origin. Sedimentological and palaeontological investigations have been carried out in only one section (Fig. 2), which has been excavated by a small brook alongside the road.

Grain-size distribution The greater part of the sediment is more or less unsorted, and conveys an immediate impression of till or landslide deposit (Fig. 3). The same sediment contains some cobbles and boulders (Figs. 2, 3). The grain size analyses of the material under 2 cm in diameter (samples 3 and 4, Fig. 5) show a high content of clay and silt, but do not give an indisputable solution as to the origin. However, considering also the high occurrence of shell-fragments, INTERGLACIAL SEDIMENTS 169

Fig. 2. The section described. The spade is 1 m long, and is situated in the excavation where fabric analyses were carried out. In the small excavation were found the seal bones and the wooden sticks. The silt-lenses in Fig. 3 are indicated by a white cross.

the analyses would suggest a marine origin for the fine material. The presence of a lump of marine clay gyttja, about 5 cm in diameter, also points in the same direction.

Structures The greater part of the section lacks visible structures. Fig. 3, however, shows a 2-cm-thick sand bed (sample 5, Fig. 5) which dips 40° towards SW, and approximately parallel to this in other parts of the section occur two zones with lenses of silt (Fig. 4). These structures must have been formed by sorting of the material in water. The rare occurrence of the layers may suggest that water was present only temporarily during the final deposition. The structures fit into the present writer's general interpretation through a supposition that they were formed in water, below the ice. By the same interpretation it is possible to explain their steep dip towards SW.

Roundness and lithology Roundness analyses of 111 pebbles (axes 4-10 cm) have been carried out according to the definitions of Pettijohn (1957, pp. 58-59). The results were: angular 59 'J'o; subang�lar 32 'J'o; subrounded 6 'J'o; rounded 1 %; well rounded 2 'J'o. As the stones have an unweathered surface, the roundness shows the stone material to be glacial in origin. A lithological investigation was carried out on the same stone material as was used for the roundness analyses. The results were: mica schists 33 %; green schists and hornblende- 170 JAN MANGERUD

Fig. 3. The inner wall of the excavation, showing a typical section of the sedi ments. The upper knife is 20 m long, and marks the thin sand bed mentioned in the text.

Fig. 4. Zone with silt-lenses (light) of uncertain genesis. INTERGLACIAL SEDIMENTS 171

% CLAY SILT SAND GRA VEL lO o ,_ p- /l::=f:== f.="""' o � o . -::� 3Y. � /5 70 � o l j' l o /.'/ 1/ o ,Y l o V o � / � / / o -

o ,., 2J.1 ,., a� 11JJ 31J.1 Uf' 0.125mm 025mm 0.5mm 1mm 2mm 4mm lmm 16mm

Fig. S. Grain size distribution. Samples 3 and 4 are typical of the sediments described. Sample 5 is from the sand bed marked by the knife in Fig. 3.

schists 31 %; quartzites 26 %; Bergen-Jotun rocks 10 %- The Bergen-Jotun rocks occur extensively in the Bergen area, and it is therefore difficult to deterrnine their direction of transport. It is overwhelrningly probable that the remainder (90 %) originate from the valley in which Bergen is situated (Kol derup and Kolderup 1940), and their length of transport may then vary from 0-4 km. No finds were made of granite, which does occur in the mountain slopes above the described locality. This proves both that the material has not been deposited by slides from the valleyside above, and also that it is not intermixed with material from older deposits from this side of the valley.

F abric of the pebbles Investigations of the orientation of length axes have been carried out on 140 stones, between 2 and 20 cm in diameter - the majority of them, however, being 4-10 cm. The directions show such great dispersion (Fig. 6) that a definite interpretation is not possible. It may, however, be pointed out that both alongside and at right angles to the slope of the vallyside there are minimal values. This is again an indication that the material is not a land slide deposit. The maximum to be shown by the analysis (130°-220°) runs parallel to the youngest glacial striae found nearby (Fig. 6), and it is reason able to presume that it is the corresponding ice movement which has caused the orientation of the material.

Conclusion The sediment consists of components with varying origin, which were finally intermixed and deposited by ice during the Last Glaciation. However, the presence of the sealbones - which lay in a concentrate:d area - and of the molluscs and the lump of clay gyttja, demonstrates that no Iong glacial trans port has taken place, and that parts of the sediment must have been very little disturbed by the ice. 172 JAN MANGERUD

GLACIAL STRIAE

Slope of lhe Youngest, Oldest, Bones 15 pct mo u ntaln side Fana roklubb Fana roklubb

90° 120° 150° 180° 210° 2�0· 270°

Fig. 6. Fabric analyses of 140 pebbles, represented as percentage of pebbles at to• intervals. Orientation of glacial striae in the vicinity, and direction of the slope in which the sediments occur, are indicated above.

The fossils show that marine sediments must have constituted a major part of the original material. This appears in particular to be the case for the fine material (clay-silt), an assumption which is supported by the fact that the foraminifers are of a neritic facies. It is not possible as yet to determine to what proportion of the sediment this applies. The sediment can be classified as fossil-bearing, short-transported till, or as parautochthonous, marine sediments.

Macro-fossils and radiocarbon datings A number of well-preserved bones, which lay together, were found (Fig. 7). These were identified by Curator Håkon Olsen as seal Phocaidae, without it being possible to determine the species. A large number of small fragments of shells were found. Some of these are possibly identifiable through careful ex;amination, but this has not as yet been carried out. Fragments of shells were collected, both in the section described and at other localities along the road, in order to obtain sufficient material for a C14-dating. If all the shells were of the same age, it would thus be possible to date large parts of the sediment. The dating (T- 749) gave an age of + 5'000 + 17,000 46 ' 000 or with two standard deviations: 46' 000 - 3,000 - 5,000 INTERGLACIAL SEDIMENTS 173

Fig. 7. The bones of seal.

Apart from the above margin of error, there are two conditions which necessitate a careful interpretation of the dating. It has been mentioned above that the shells were taken from different parts of the sediment. It is thus possible that these differ widely in age, and that the dating provides an average. The other possible source of error is that younger carbon may have been introduced. The shell-samples were taken at a depth of 1-3 m, and the foraminifers (see below) showed considerable corrosion. The dating must be assumed to provide a definite minimum age of 40,000 years, and an indi cation of a maximum age of approximately 65,000 years. Several pieces of wood were found, the !argest of them almost 10 cm in length. One of these has been identified by Prof. Knut Fægri as spruce (Picea). The wood samples gave a radiocarbon age of more than 40,000 years (T- 748).

Pollen and spores Description of the samples Sample 1 was taken from material which lay in immediate contact with seal bones. Sample 2 was taken from a 5-cm lump of clay gyttja which was found in the sediment. Sample 3 was taken in the deepest part of the excavated section (Fig. 2). Grain size analyses were also carried out on this sample (sample 3, Fig. 5). All three samples indicate a marine depositional environ ment, with respectively 83, 50 and 23 %Hystrix calculated as sum AP. In addition all contained foraminifers. Both samples 1 and 2 were taken from parts which are presumed to be undisturbed remains of the original marine sediments. These should therefore 174 JAN MANGERUD

A p TOTAL NAP SPORES

o 10'1. 20'1. 30'/. 40% AP NAP Sp o 10'/. o 10'1.

Pie.a Cyp�raeHJ• Sphagnum Plrtus Cromintat f- l.ycopadium � - Bttuta - Ericolts "' 1423 102 .. , 1---- FWcts f-- J .. Atnus - l[ ,.,., .. Corylus - 68·1. . 15'/. "' Qutrcus

lltx 10.9) Compositot

Pie.a Cyp. $ph. - Pinus - N C ram. Lye. Btt. Eric. � 1500 34 184) Fil. .. Afn. - l[ f- lsotlts .. , .,, Car. - 10'1. 26'1. "' �J::�g��s au. Plan/aga morltJmo

ic P to CJp. f- Sph. Pin us C ram. t---1- Lye. � Btt. "' 1317 125 64) Eric. f-- Fil. .. A In. Jsotlts " 25'/. .. Cor. - 63'1. 13'1. Rub;octot "' au. Comp. Ilu lo.& l Arttmisia r

Fig. 8. Pollen diagram. Calculation basis is sum AP for the AP-diagram, and sum AP+ NAP+Sp for the other diagrams. In the total diagram, num ber of pollen and spores are given in brackets.

provide a picture of the pollen rain at a definite point of time. Sample 3, on the other hand, may be a mixture of pollen rain from various periods of time.

Vegetation Sample 1 indicates the presence of a dense forest of conifers (Fig. 8). Since Picea (spruce) produces less pollen than Pinus (pine), it must be assumed that Picea has been the more important species. The forest floor vegetation is dominated by heather and bracken. Of great significance for an evaluation

of the climate is the relatively high frequency of /lex (0.9% = 4 pollen grains). This is the highest frequency found in Norway, even though a large number of pollen analyses have been carried out within the present area of occurrence of /lex (e.g. Fægri 1944, Hafsten 1965). Sam ple 2 represents the densest forest of all, with only 4 % NAP. This has been a mixed forest, with Picea and Pinus as the most important conifers, and with Betula and Alnus as the most important deciduous trees. The forest floor vegetation has consisted almost entirely of bracken and Sphagnum. In this sample was found one pollen grain of Plantago coronopus, which does not exist in Norway today. Sample 3 contains considerably more deciduous trees than the other samples. This more open forest also contains a somewhat richer undergrowth, especially of grass.

Picea

Of special interest is the large amount of Picea-pollen, since spruce has not

grown in the area since the Last Glaciation (Fig. 1 ) . Picea may therefore be a characteristic fossil for other possible finds of the same age. INTERGLACIAL SEDIMENTS 175

INTER Allerød Denekamp Eemian STADIALS 8Q'IIing Heng elo lnterg la c ial

� 20°C------��--�------z� �� 15�--��------��<7�--�------ :J:." ...... r Vll\------".------:..------i---\-1---\,.---.J----.-..::S::::h :;:ub:_-� und�rt :::o _ � � 10,+------fo.sl !;(: ! � 5 Polar d�� ' ...... undrat :i)� '"'.. �-----...... ,,_ ---- 0+-----�----,-----�-----r----�------YEARS B.P.-+ 10000 20 000 30000 40000 50 000 > 70000

Fig. 9. Climatic curve and interstadials of the Weichselian in the Netherlands. Modified from Hammen et al. (1967, Fig. 8).

The question has been discussed as to whether the western geographical limit of the Picea has been determined climatically or historically (e.g. Fren zel 1967, p. 42 and Fægri 1950, pp. 48-49). If one considers the current distribution of Picea and Ilex in NW Europe, there is virtually no overlapping of their areas of occurrence. In the Eemian Interglacial, Picea and Ilex occur together, and this fact is used by Iversen (1944, p. 477) as an argument for the contention that the present western limit for Picea is not climatically determined. This is supported by the present author's pollen analyses, where Ilex occurs in considerable quantities in the Picea forest (samples l and 3, Fig. 8).

Age The late Pleistocene is well covered with regard to pollen diagrams from Northern Europe.From the Fjøsanger locality only three pollen spectra were obtained, their age relationship not being known. However, it does seem possible to compare the types of vegetation with the development in known are as. Fig. 9 shows a climate diagram for the Weichselian, which seems to be fairly representative of the present view (Morner, 1969, p. 38). It is only the Brørup Interstadial which has been sufficiently warm to have conceivably produced the vegetation shown by the finds at Fjøsanger. This alternative will be discussed first. In Denmark the vegetation in the Brørup Interstadial is well known (S.Th. Andersen 1961). The forest is here completely dominated by Pinus and Betula, with some Picea. Now S. Th. Andersen (1961, p. 121) maintains that ' ...it appears that the temperate deciduous trees were absent mainly because they had not had time to immigrate. A similar vegetation may have prevailed in Scandinavia. However, species of trees (Picea? Alnus?) may have immi grated to that area from the east'. This can hardly be the case for Corylus (Frenzel 1967, p. 219), which occurs in considerable numbers at Fjøsanger. If J. Lundqvist (1967, pp. 227-228) is correct in his parallelisation of the Jamtland Interstadial with Brørup, then it is likewise not very probable that Alnus has immigrated into Scandinavia from the east. As mentioned above, 176 JAN MANGERUD

the pollen frequency (in all 6 pollen grains) of !lex at Fjøsanger is high in comparison with the very small amount of pollen produced by the tree; and it is therefore improbable that this is secondary pollen. !lex is a very reliable climate indicator (Iversen 1944), and as Fjøsanger today Iies dose to the boundary for its area of occurrence (Fægri 1960, Pl. 24), it seems to be out of the question that it can have grown here during the Brørup Interstadial. The conclusion must therefore be that the Fjøsanger vegetation does not originate from the Brørup Interstadial, a conclusion which would seem to be fairly certain. The next alternative further back in time is the Eemian Inter glacial. During the last part of the Eemian the forest in Denmark (Andersen 1965, p. 499) was dominated by Pinus, Picea, Betula and Alnus. There was very little pollen of mixed-oak forest, despite the fact that the climate was suf ficiently favourable. The pollen spectra from Fjøsanger show the same principal features, and if we assume that the development of vegetation in Denmark and Norway has been roughly parallel during the Eemian, in the same way as in the Flandrian (Holocene), it is very pro bable that the Fjøsanger vegetation stems from Late Eemian. It may also be mentioned that !lex had a greater extension during the Eemian than during the Flandrian (Frenzel 1967, p. 111), and that it occurs frequently in Danish pollen diagrams from this interglacial.

Foraminifera

In the same three samples from which the pollen was taken, Dr. R. W. Fey ling-Hanssen has carried out a preliminary investigation of Foraminifera with the following results: Sample l. All foraminifers are strongly corroded, and it must be assumed that they represent only remains of the original fauna. Several species of Foraminifera were identified, but for the above-mentioned reason these have not been included in the present material. Sample 2. Likewise in this sample the calcareous material has been cor roded, and the fauna is therefore not discussed further. It may nevertheless be mentioned that many specimens of Bu!imina gibba and same of Bulimina marginata were found. Sample 3. Rich fossil-bearing sample. Here too corrosion has possibly taken place, but to a far smaller degree than in the two other samples. Hitherto the following species have been observed. Very frequent: Elphidium hugesi, E. bartletti, E. subarcticum, Protelphi dium orbiculare, P. anglicum, Nonion labradoricum, Nonionella auricula, lslandiella teretis. Frequent: Bulimina gibba, B. marginata. Sparse: Angulogerina ssp., Elphidium incertum, E. clavatum, E. excava tum, Lagena acuticosta, lslandiella islandica. Very sparse: Elphidiella arctica, lslandiella norcrossi, Nonionella aff. au- INTERGLACIAL SEDIMENTS 177 ricula, Guttulina sp., Polymorphina sp., Buccella frigida, Cibicides loba tulus(?). The fauna, which belongs to the neritic facies, indicates northerly boreal climatic conditions presumably somewhat colder than is the case in the area to-day. It seems clear that glacial environments have not existed. On the basis of these preliminary investigations of Foraminifera, it is not possible to make any definite statement concerning the age.

Conclusions and discussion

Age The results can be summarized as follows: l. The sediments were deplaced and disturbed by the ice during the Weichs elian, and it is the age of the primary marine sediments which is under discussion here. 2. The sediments are situated close to the surface, and the underlying material is unknown. Thus, a fuller picture of the stratigraphy cannot be ascertained. 3. The radiocarbon datings give a definite minimum age of 40,000 years. The dating of the shell remnants (T-749) indicates an early Weichselian age. 4. The foraminifers show that the sediments were not deposited under glacial conditions, but warm interstadials cannot be excluded. 5. The pollen analyses provide a definite minimum age of older than Late Weichselian, and a presumable interglacial age. As the vegetation tallies very well with the vegetation in Denmark during the Late Eemian, the author assumes that the Fjøsanger sediments date from the Late Eemian, even though it is impossible to exclude a still greater age.

Sea-leve l The sediments are found up to a level of 10-15 m above present sea-level, but it is possible that the ice has carried them up from a level of 10 m below sea-level. The threshold of the Nordåsvann inlet is shallow, and today the water is brackish. The sediments under discussion are marine, and the for arninifers show a neritic facies. The sea-level must therefore have been higher than is the case today; bow much, it has not yet been possible to determine.

Climate As mentioned above, both the general picture of the vegetation and the presence of /lex show that the climate can only have been slightly less fa vourable than at present. The foraminiferal fauna does, however, suggest that the water was somewhat colder than is the case today. Considering that this is a marine sediment, with but little influence from Iocally-produced pollen, there is a high content of Sphagnum spores, the 178 JAN MANGERUD

X S•dlm•nts contalnlng marine fossils

A Mammoth remalns in glaclal sedlments

• _., __ "_ river-�nks

O Musk-olt vertebrae

• Str.atified silt and cliiy

l l

\ l l l l l , ,-- 1

Fig. 10. Sediments and fossils of supposed pre-Late Weichselian age in Southern Norway.

presence of which indicates an advanced paludification, and thus a humid climate.

Glacial-geological aspects The sediments are situated in an area strongly influenced by glacial erosion, bare rock being almost everywhere exposed. The Nordåsvann inlet has over deepening of more than 80 m below its threshold, and just outside Bergen to the north the fjord is almost 400 m deep. It is therefore very surprising that unconsolidated sediments have been preserved in this area during the whole of the Weichselian Glaciation. Nor is it possible to point out any ob vious reason as to why the sediments have been preserved at this locality, in contrast to other sites in the area.

Correlation with other sediments in Norway Very few sediments or fossils of pre-Late Weichselian are known from Nor way. The most indisputable among them are discussed below (Fig. 10). Eastern Norway. From Eastem Norway, particularly from the valley of Gudbrandsdalen, several finds of mammoth bones and teeth are known (Heintz 1962, Mangerud 1965). All these fossils were, however, found in a INTERGLACIAL SEDIMENTS 179 secondary position, in glacial sediments or in recent alluvium (Fig. 10). One of the teeth has been Cwdated, the age being 19,000 ± 1200 (Heintz 1965). However, as suggested by Heintz ( op. cit., p. 229), this da ting must be er roneous. Finds have also been made of a vertebra of musk-ox at Inset (oyen 1913, p. 204) (Fig. 10). This was found in a deposit of stratified sand and grave! of somewhat disputable genesis, below 3-4 m thickness of till (oyen 1913, Reusch 1913, Bjorlykke 1913). Since no other fossils were found, the age cannot be ascertained with greater accuracy than pre-Late Weichselian. At Skåbu (Mangerud 1965, p. 201) and at Folldal (Streitlien 1935, pp. 60-61), stratified clay and silt occurs below a great thickness of till. In the opinion of the present author these sediments must be older than the last ice cover of the Weichselian Glaciation, but a more accurate dating has hitherto not been possible. Karmoy. On the istand of Karmoy (Ringen 1964) there occurs a silty and clayey till containing a large number of shell fragments, mainly of Mya truncata. The shells have a C14-age (T - 140) of 34,000 ± 3,000 years. Thus Ringen (1964, pp. 216-217) assumes the shells to be from the Paudorf or Gottweig Interstadial. Jæren. At Jæren are found great thickness of sediments below till from the Weichselian Glaciation (boring having been carried out down to a depth of 92 m). The sediments consist of layered sand and gravet and fossil-bearing marine clay. The age and origin of these deposits is very ambiguous and has lately been discussed by O. Holtedahl (1960, pp. 362-364), B. G. Andersen (1964) and Feyling-Hanssen (1964b and 1966). Large numbers of molluscs, indicative of arctic or boreo-arctic conditions, have been found in the clay. On some of these, radiocarbon datings have been carried out (Nydal 1960) and gave more than 36,000 years (T -116) and more than 23,000 years (T - 148). The foraminifers in the clays from Sandnes have been investigated by Feyling-Hanssen (1966). These are dominated by coldwater fauna, notably Elphidium clavatum and Cassidulina crassa (op. cit., p. 35 and 42), and he therefore assumes that the clays originate from an interstadial during the Weichselian. The foraminiferal faunas at Sandnes show much colder con ditions than do the Fjøsanger fauna described above. B. G. Andersen (1964, p. 10) presumes that the clays were deposited at the end of the Riss Glaciation, mainly on account of the fact that the high level of the clays presupposes a great isostatic depression of the area. Later, Andersen (1965, p. 113) suggests that the clays and the fossils originate from the Riss-Wtirm Interglacial or from the Gottweiger Interstadial. Conclusion. Sediments and fossils of pre-Late Weichselian age are known from various localities in Norway. In the case of the majority of these, the age is not accurately determined. Those here described from Fjøsanger, near Bergen, are the first to show with a certain degree of assurance conditions sufficiently warm as to suggest a definite interglacial age. The pollen-spectra 180 JAN MANGERUD described are likewise the first from Norway to indicate an age greater than Late Weichselian. Acknowledgements. I gratefully record my obligation to several people, who in various ways have contributed to the present paper with most valu able help. For the determinations carried out on the Foraminifera and bone remnants respectively, my thanks are due to Dr. Rolf Feyling-Hanssen, Uni versity of Aarhus, and to Mr. Håkon Olsen, Curator of the University of Bergen. Professor Knut Fægri made a species identification of the fragment of wood and, moreover, in conjunction with the other pollen-analysts of the University of Bergen Botanical Museum, provided valuable help in connec tion with the pollen analyses. Professor Hans Holtedahl read through the manuscript, and to him and other colleagues in the Geology Department I am grateful for the fruitful discussion of various problems. Mr. Kjell Sognen provided useful assistance both during the fieldwork and in the laboratory. The figures were drawn by Miss Ellen Irgens. The manuscript was translated by Wendy Holtedahl, M. A. To all these persons I proffer my sincere thanks.

JO October 1969

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ADDENDUM

During the printing of the present article, a stump of spruce from a sand pit in south eastern Norway has been C14-dated, the age being 48,000 �i:: years (I. L. Sollid 1969: A 48,000 year old tree stump, presumably of spruce, found in Ringerike, South Norway. Norsk Geogr. Tidsskr. 23, 131-133). A mammoth-tusk from Kvam in Gudbrandsdalen has a1so recent1y been C14-dated, this dating giving the age of 24,400±900 years B. P. (A. Heintz 1969: Two new mam moth-fragments from Norway and age determination of one of them. Norsk Geo/. Tidsskr. 49, 437-438).