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Holocene Shorelevel Displacement in Telemark, Southern Norway

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Holocene Shorelevel Displacement in Telemark, Southern Norway Holocene shorelevel displacement in Telemark, southern Norway BJØRG STABELL Stabell, B.: Holocene shorelevel displacement in Telemark, southem Norway. Norsk Geologisk Tidsskrift. Vol. 60, pp. 71411. Oslo 1980. ISSN 0029-196X. Diatom analysis has been used to construct two radiocarbon dated shorelevel displacement curves for the Porsgrunn and KragerØ areas in Telemark county. No transgressions have been demonstrated, but the curves show a fairly slow regression in the Tapes period. B. Stabell, Institutt for geologi, Universitetet i Oslo, Postboks 1047, Blindern, Oslo 3, Norway. The aim of this investigation has been to de­ part, however, belongs to the Oslo Region with termine the Holocene shorelevel displacement in its Cambro-Silurian sedimentary rocks and Per­ Telemark county, Norway. Two areas centered mian volcanic rocks. around the towns of Kragerø and Porsgrunn The shorelevel curve from the Kragerø district have been investigated. Separate shorelevel dis­ is thus based solely on localities within the placement curves for each area have been con­ Precambrian area, whereas the Porsgrunn curve structed. The two areas investigated were cho­ is based mainly on localities within the Oslo sen in collaboration with archaeologists, as the Region. shorelevel curves form part of the Telemark The Holocene marine limit in the KragerØ archaeological project. district is at approximately 120 m a. s.l. (Hen­ Shorelevel displacement in Telemark, based ningsmoen, pers. comm. 1978), while that in the on the study of sub-fossil shell-banks, has earlier Porsgrunn district is at approximately 150 m been investigated by Keilhau (1838), BrØgger a.s.l. (Holtedahl 1953, pl. 19). (1900-1901, 1905), Øyen (1906) and others. More recently TrØmborg (1974) has published a paper on marine limits in which he also briefly discus­ sed shorelevel displacement. Field and laboratory work Major works on shorelevel displacement in the Oslofjorden area (Fig. l) based on isolation-con­ This investigation uses diatom analysis to de­ tacts dated by pollen analysis of basins at differ­ termine isolation contacts which are then ent 1eve1s above present sea-1evel have been radiocarbon dated. The 1ocalities have been cho­ published by Hafsten (1956) (the Oslo area) and sen in collaboration with Helge l. HØeg, who has Danielsen (1970) (Østfold county). A shorelevel undertaken the pollen analysis investigation for curve from the Ski area (southeast of Oslo) is the Telemark project. His work, which will be given by SØrensen (1979). This curve is quite published elsewhere, gives pollen based dates on similar to Hafsten's curve from Oslo. An in­ all isolation contacts in addition to the vestigation from Vestfold, the county bordering radiocarbon datings. Telemark to the northeast, will shortly be All dates are given in uncorrected 14C-years published by Henningsmoen. The shorelevel with a 14C half life of 5570 years. All radiocarbon curve, however, is already published by Hen­ analyses were carried out at Laboratoriet for ningsmoen (1979). SØrensen (1979) and Hen­ radiologisk datering, NTH, Trondheim, Nor­ ningsmoen (1979) also use 14C dating. way. The field work for this investigation started in 1974. Seventeen lakes and bogs in the Porsgrunn and Kragerø areas were sampled (Fig. l). The Geology of the area stratigraphy of the basins was studied and the The bedrock is of Precambrian age in the greater altitude of their overflow thresholds were de­ part of the investigated area. The northeastern termined mainly by leveling. Samples were col- 72 B. Stabell NORSK GEOLOGISK TIDSSKRIFT l (1980) ' ' Oslo / (( {ø old �sttotdst'; �olm Kristiansh\Hbnd lia TELEMARK •5 \ ' � ør ' ' •6 •7. ' �V'JKRf<fhø ' \ tJ C!'g\/ C-J N l 11 1 � l • � l •3 •12 \ • 2 ?.1 o 10 20 l '--, Fig. l. Locations of the basins ...... in Telemark and map showing ·8- km ' other areas mentioned in the ' text. lected by a Russian type sampler, except at Polyhalobous taxa: marine taxa with an optimum Locality 13, where a Hiller sampler was used. range of 30%o S and more. The samples used for diatom analysis were Mesohalobous taxa: brackish water taxa with treated with 30% hydrogen peroxide, and the their optimum and lower tolerance limit within residue mounted with Hymount and counted in the range 30-0.2%o S. phasecontrast at 1250 x magnification. The Oligohalobous taxa: taxa living in both brackish identification of the different diatom taxa was and fresh water. carried out mainly with reference to Hustedt halophilous taxa: optimum in slightly brackish (1930, 1931-62) and Cleve-Euler (1951-55). In­ water. formation about the salinity requirements of the (salinity-)indifferent taxa: optimum in fresh different taxa was mainly obtained from the water. above references and in addition from Simonsen Halophobous taxa: exclusively fresh water taxa, (1962), Cholnoky (1%8), and Edsbagge (1968). strongly averse to Cl-ions. Two diagrams have been constructed for each basin. The first diagram shows the percentage of The diatom diagrams the diatom flora for each salinity group, while In the diagrams the different taxa have been the second shows percentages for each taxon in grouped conventionally with regard to their pre­ detail. In this paper a selection of 8 diagrams ference for the salt content of the water, accord­ from five basins are presented. The construction ing to the redefined halobion system of Hustedt of the diagrams are based on Florin (1946), with (1957), originally proposed by Kolbe (1927). The the exception that the taxa are grouped alpha­ salinity (S) is expressed as percentage by weight. betically within each salinity group. The four main groups are: Levels above and below those included in the NORSK GEOLOGISK TIDSSKRIFT l (1980) Holocene shorelevel displacement 73 LANGVANN BOG 99 ma.s.l. uE c a. HALOPHOBOUS "' o ---"'"""' •;. 914 9040BP :t210 918 � FINE DETRITUS GVTTJA D CLAY Fig. 2. Langvann bog. Stratigraphy and diatom content in salinity groups. Hl= Halophilous. diagrams have been diatomologically checked, Three levels, at 918, 916, and 914 cm, were but not counted. analysed, Fig. 2. The lowermost level contains The calculation sum for each sample can be mostly polyhalobous and mesohalobous diatom found in the diagrams. For practical reasons the taxa, with some indifferent taxa. In the middle Fragilaria taxa have not been included in this level the polyhalobous taxa disappear, the sum because of the high frequencies of these mesohalobous decrease, and there is a sharp taxa in some of the samples. increase in indifferent and halophobous taxa. The topmost level contains more than 90% indif­ ferent and halophobous taxa. Fig. 3 shows the distribution of the taxa in Description of localities 1-17 detail. The lower lev el contains small amounts of Locality l, Langvann bog (58°57' N, several polyhalobous taxa and is dominated by 9°/6' E), 99 m a.s.l. mesohalobous Nitzschia species. The flora in both the middle and top level is totally domi­ Stratigraphy: nated by Fragilaria construens. Apart from F. 800-911 cm Fine detritus gyttja construens, however, the middle level is domi­ 911-916 cm Gyttja with alternating layers of clay nated by the indifferent taxon Amphora ovalis 916-931 cm Clay with alternating layers of gyttja and the top level is dominated by the halophob­ 931-950 cm Clay ous taxa Tabellaria fenestrata and Tabellaria LANGVANN BOG 99ma.s.l. E u .!: � a... o 914 916 918 � FINE DETRITUS GVTTJA c::J cLAV Fig. 3. Langvann bog. Stratigraphy and diatom con tent. 74 B. Stabell NORSK GEOLOGISK TIDSSKRIFT l (1980) E PØDDETJØNN 50.5 ma.s.l. u c: POLYHALOBOUS 50 75 � GYTTJA WITH SAND D CLAY Fig. 4. PøddetjØnn. Stratigraphy and diatom content in salinity groups. M = Mesohalobous. flocculosa. Isolation from the sea must have struens in the middle and top leve!. Level 664 cm taken place between leve! 916 cm and 914 cm. is dominated by the polyhalobous Melosira Sediment from this part of the core was dated sulcata, while there is no dominating taxon and gave an age of 9040±210 years BP (T-1968). among the indifferent and halophobous taxa. Isolation from the sea must have taken place between leve! 663 cm and 661 cm. Sediment Locality 2, Kolbjørnsmyr (58°48' N, from this part of the core was dated at 8820± 300 9°17' E), 82 m a.s.l. years BP (T-1967). Stratigraphy: 150-525 cm Coarse detritus gyttja Locality 4, Storkjenn (58°50' N, 9°26' E), 43 525-690 cm Fine detritus gyttja m a.s.l. 690--825 cm Clay with molluscs Stratigraphy: Four levels, at 700, 697.5, 695, and 692.5 cm, 500 -555 cm Coarse detritus gyttja fining were analysed. The diatom content is similar to downwards that of Loe. Isolation from the sea took place l. 555 -555.5 cm Clay between 700 cm and 697.5 cm and was dated at 555.5-558.5 cm Fine detritus gyttja 9180± 340 years BP (T-24 15). 558.5-560.5 cm Clay 560.5-561.5 cm Fine detritus gyttja 561.5-575 cm Alternating narrow layers of Locality 3, Pøddetjønn (58°49' N, 9°14' E), gyttja and clay 50.5 m a.s.l. 575 -650 cm Clay Stratigraphy: Three levels, at 560, 557.5, and 555 cm, were 525-648 cm Fine detritus gyttja analysed. The diatom content is similar to that of 648-663 cm Fine detritus gyttja with sand Loe. l, but with a smaller percentage of 663-750 cm Clay mesohalobous taxa. Isolation from the sea took place between 560 cm and 557.5 cm and was Three levels, at 664, 662, and 660 cm, were dated at 8500± 180 years BP (T-1966). analysed. As seen in Fig. 4, the transition from marine to fresh water happened very fast. In level 664 cm, almost 90% of the valves belong to Locality 5, Lille Neslandskjenn (5S057' N, polyhalobous taxa, while in leve! 660 cm almost 9°17' E), 38 m a.s.l.
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