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Stratigraphy and Sedimentology of Middle to Upper Pleistocene Sediments in the New Grødeland Borehole at Jæren, SW Norway

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Stratigraphy and Sedimentology of Middle to Upper Pleistocene Sediments in the New Grødeland Borehole at Jæren, SW Norway Stratigraphy and sedimentology of Middle to Upper Pleistocene sediments in the new Grødeland borehole at Jæren, SW Norway JURAJ JANOCKO, JON Y. LANDVIK, EILIV LARSEN & HANS PETTER SEJRUP Janocko, J., Landvik, J. Y., Larsen, E. & Sejrup, H. P.: Stratigraphy and sedimentology of Middle to Upper Pleistocene sediments in the new Grødeland borehole at Jæren, SW Norway. Norsk Geologisk Tidsskrift, Vol. 77, pp. 87-100. Oslo 1997. ISSN 0029-196X. The new Grødeland borehole penetrates 124.5 m of Pleistocene sediments at the coast of Jæren. Amino-acid analysis suggests that the succession is of Saalian to Weichselian age. Six major units dominated by tills, glaciomarine and marine deposits were recovered: Unit l rests on crystalline bedrock and comprises 42 m of subglacial till. Unit 2 comprises silty and sandy sediments deposited in a glaciomarine environment, grading into normal marine and back to glaciomarine conditions before deposition of the overlying till (unit 3). Unit 3 is 32 m thick subglacial till. Unit 4 was deposited in a shallow glaciomarine environment. The succession is capped by the uppermost subglacial till (unit 5) of assumed Early Weichselian age, and a Holocene beach deposit. The stratigraphy is compared with the classic results fr om the Grødeland coring carried out at this site in i874. Jura} Janocko, University of Tromsø, Department of Geology, IBG, N -9037 Tromsø, Norway; Jon Y. Landvik, The University Courses on Svalbard (UNJS), PO Box 156, N-9170 Langyearbyen, Norway; Eiliv Larsen, Geological Survey of Norway, PO Box 3006, N-3006 Trondheim, Norway; Hans Petter Sejrup, University of Bergen, Department of Geology, A/legt. 41, N-5007 Bergen, Norway. Relatively long and complex Quaternary stratigraphic in April 1993 and presented here, was located 50 m from records are documented from many parts of western the modem beach (UTM 32VLK021045) only 20 m Norway and from the North Sea (e.g. Andersen et al. southeast of the 1874 drilling that recorded 92 m of 1981; Mangerud et al. 1981; Landvik & Hamborg 1987; sediments (Bjørlykke 1908). Larsen et al. 1987; Larsen & Mangerud 1989; Larsen & The main objective of this article is to document the Sejrup 1990; Sejrup et al. 1987, 1989, 1991, 1994). The lithostratigraphy of the thick sedimentary succession at Jæren region (Fig. l) has a thick Quaternary cover, in Grødeland and reconstruct the depositional environ­ contrast to the rest of mainland Norway. The region has ments. Some preliminary results of chronological and been extensively studied since the turn of the century biostratigraphical work are also presented. (Bjørlykke 1908; Grimnes 1910; Feyling-Hansen 1964, 1966, 1971, 1974; Wangen 1968; Østmo 1971; Andersen et al. 1981, 1987; Fugelli 1992; Fugelli & Riis 1992). Methods Correlation between studied sites reveals a complex stratigraphy in the area (Andersen et al. 1987). The drilling was performed using a rotary system from a The Jæren region represents a border zone between the truck-mounted rig. Sampling by a wire-line system was North Sea shelf region and the Norwegian mainland, carried out in the fine-grained sediments. A stee1 sampler extending from Stavanger in the north to Ogna in the with plastic core barrel 150 cm long and 10 cm in south (Fig. 1). The region is divided into Lågjæren diameter was fixed in the front part of the drill string and (Lower Jæren) to the west, with elevations below 100 m, pushed down without rotation during drilling. After 150 and Høgjæren (Upper Jæren) to the east (Fig. l), reach­ cm of penetration, the coring was stopped and the sam­ ing up to 250 m a.s.l. In some areas the two parts are pler recovered using a wire-line retriever. Different core separated by a morphologically conspicuous step (Fig. catchers were used to prevent samples from sliding out of 2). The area east of a line passing through Ålgård, Lake the plastic barrel. Recovery in the fine-grained sediments Storamos and Brusand is dominated by exposed bedrock was 42%. During retrieval, sorted sand and silt some­ (Fig. 1). This crystalline basement comprises Precam­ times escaped from the sampler. On most occasions, a brian gneisses and granites ( anatexites ), anorthosites, fist-sized, often disturbed sample was preserved in the phyllites, mica schists and mica gneisses (Birkeland core catcher itself. In bouldery diamictons, a rock drill 198 1). bit was used and cores were not collected. Information Several coal exploration boreholes made in the second on these units was obtained by cutting samples from drill half of the last century revealed thick Quaternary de­ mud collected during every 3 m run. Sudden changes in posits (Bjørlykke 1908). The Grødeland borehole, drilled drill penetration indicate lithological changes, probably 88 J. Janocko et al. NORSK GEOLOGISK TIDSSKRIFT 77 (1997) 5°30' 5°45' ,......-----,------=-------.--=-�59°00' Norwegian Sea NORTH SEA Areas covered by Quatemary sediments Areas with exposed bedrock Grødeland drilling * Old Grødeland drilling Roods O Houses Fig. l. Map of the Jæren area showing the location of the new Grødeland borehole. The indicated boreholes at Auestad, Elgane and Habberstad were drilled in 1994-95, and will be reported in future articles. The map showing areas with predominantly Quatemary deposits and exposed bedrock is constructed after Andersen et al. ( 1987). NORSK GEOLOGISK TIDSSKRIFT 77 (1997) Pleistocene stratigraphy and sedimentology, Jæren, SW Norway 89 Fig. 2. Oblique air photograph of southem Jæren showing its typical lowland character. Lågjæren area is separated from Høgjæren by the morphological step to the east of the town of Varhaug. See Fig. l for location. between zones with diamictic and hetter sorted sedi­ Lithostratigraphy and interpretation ments. The unsplit core barrels were X-rayed while moving The drilling penetrated 124.5 m of Quaternary sediments them along their lang axis and rotating them, giving a befare encountering mica schist or mica gneiss of Pre­ three-dimensional image of sedimentary structures and cambrian age. The sedimentary succession is divided into contained clasts. The X-ray data were recorded on video six lithological units, numbered from bottom to top (Fig. tape and computer disks. After the cores were split, 3). The borehole contains two fine-grained sediment units sediments were visually described and photographed. separated by three thick diamictons. The succession is Samples were taken for determination of water content, capped by Holocene beach sediments. The different fa­ preconsolidation pressure (Hernes 1995), total carbon, cies are indicated in the log (Fig. 3) using lithofacies total organic carbon and CaC03, foraminifera, molluscs, codes (Table l) slightly modified after Eyles et al. (1983). grain-size analysis and palaeomagnetism (Løvlie 1994). Selected core intervals were sliced, transferred to plexi­ glass trays and X-rayed for more detailed inspection. Unit l Amino acid samples were prepared after the method described by Miller et al. ( 1983) and then run on an Description. - Unit l is the lowermost 42 m thick automatic ion exchange amino acid analyser at the diamicton (D) extending from 124.5 m to 82.2 m (Fig. 3). Bergen Amino Acid Laboratory (BAL). Two samples It has not been cored, and the information about de­ were dated by the AMS method at the Laboratory for posits comes from cutting samples and drilling log. Radiological Dating in Trondheim. Changes in penetration speed, observed during drilling, Clast fabric, shape and roundness (25 per sample) indicated boulders 'floating' in a finer matrix. The unit were measured in the uppermost 2.2 m of the succession consists of crystalline clasts up to boulder size, supported in a shallow pit next to the drilling site. Clast fabric was by a fine-grained matrix. Cutting samples occasionally measured on rock fragments between 2 and l O cm lang, contained mollusc fragments. However, their strati­ having an a/b-axis ratio of at least 1.5. Clast shape was graphic position is uncertain because they may have been calculated after Zingg ( 1935, in Pettijohn 1975). Round­ washed out from overlying deposits by the rising drill ness was estimated visually after Folk (1951). mud. 90 J. Janocko et al. NORSK GEOLOGISK TIDSSKRIFT 77 (1997) 0.0 9.5 51.5 6 o\ Fm ,-=-=--::::--=-=--=-::1. ® o ® Sh Fl {)rm 52.0 5 _1_ 10.0 �JSm • • ' ·�Gmm 52.5 +-___;;;....__--,_..--, ..- -� 5.0 �m o J Sg l Sm 10.5 53.0 ----------t t -- Fl no recovery SI 11.0 10.0 -'l. o Gmm Sg l*51 775�5145 oaooooøo�ooo_Q_o Gcm _ 3110 _'\"'Sg "-Gcm � •O. 087 11.5 o l 54 5 13.0 Cj o � �n . EiE��� 3 c sand gr011el 42.0 D '=:f::::::K/ Fl ._Q_ <> oJ - ss.o r-"· --�----"l cloy sil sand gravet 45.0 o "' Sm © 77.0 © 50.0 •===--==/ -'l. l���FISh ---- A ----- •=�=� �Fl ----------- Fl J�Sm 9 i -��"'i�,._ -'l. • o. 107 77. 7 .5 ::::;;::::.i. Fl • D. 153 osJ:===�Sh lf:ll..... ;;;;., ��- � l \.. 55.0 F o � Sm no recovery Oo oooaoooooo"'i;\ · --j,). Sh Fl ._ n 9 -1----,----,-'-I Sm • o. 124 . ___, 80.5 Fm � �n �nd Fm Fl c • o. 134 Fl ---------c 153 • o. o Gmm 81_5 �=====:i�"; • 148 o. Fm • O. 078,0. 051 82.0 -E§�Fl *42 635± \6�g cloy sin 65.0 1':�-'l.Fm .o.�s �------------;:::::::::::::::::::::::::::::::::::::::::::::::::::� l·.·:� -'l-Fl Leg end rJI==::::r.J\ -'l.Fl, Fm �==\o\ Massive strucltre Outsized clasts 70.0 Fl. Fm l­ D Horizontal lamlnaflon Mud l- • o. 142 § Faint lamlnaflon Sand • o. 166 Malrlx-supported 75.0 Trough cross-straflficaflon � grave! • o. 147 �-···GmmSh �__Æ; � Shell layer Clast-supported r1 grave! l-ll���t-..........-�� .f! • •• Gmm -,l 130 -----�·:.J -'l. .o. B Gravel layer Diamicton 80.0 m • � _j© ·-···· 136 Bed rock ,Fl Gmm • O. EJ Water escape structure ·i � •0.128 Boundary: 84.0 0 � Softsediment deformaflon a) shaiP D b) eroslve o = Moffied, bloturbated c) loaded l Core l\.,\., Preconsolldafion test � Core catcher mean Alle/lie raflo • o.
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