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NGT 66 1 017-043.Pdf Biostratigraphy of a Lower Cretaceous section from Sklinnabanken, Norway, with some comments on the Andøya exposure NILS AARHUS, JACOB VERDENIUS & TOVE BIRKELUND Aarhus, N., Verdenius, J. & Birkelund, T.: Biostratigraphy of a Lower Cretaceous section from Sklinnabanken, Norway, with some comments on the Andøya exposure. Norsk Geologisk Tidsskrift, Vol. 66, pp. 17-43. Oslo 1986. ISSN 0029-196X. Ryazanian black shales in a core dose to the eastern margin of the Trøndelag Platform offshore Hel­ geland, northern Norway are overlain by a condensed latest Ryazanian-Barremian sequence of grey and red Utvik Formation equivalent marls and mudstones. Palaeontological studies show that the 'Late Cimmerian Unconformity' represents only a minor hiatus in the Upper Ryazanian. Upper Val­ anginian-Lower Hauterivian beds seem to be absent. The generalized model for the North Sea and adjacent areas (Rawson & Riley 1982) thus seems applicable to more northern areas, as would be ex­ pected if sedimentation was mainly controlled by eustatic sea level changes. The section is compared to the Lower Cretaceous sequence at Andøya, the stratigraphy of which is revised. N. Aarhus & J. Verdenius, Inst. for kontinentalsokkelundersøkelser og petroleumsteknologi AlS, Post­ boks I883, 7001 Trondheim, Norway. T. Birkelund, Inst. for hist. geo/. og palæont., Københavns Universitet, Øster Voldgade JO, DK-1350, København K, Denmark. The major break interpreted from seismic pro­ Wire line coring with 100% recovery started at files and lithology at the base of the Valhall For­ 9.2 m and continued to the base at 28.55 m. The mation in the North Sea and adjacent areas also palynological slides with the figured palyno­ occurs on seismic profiles offshore Helgeland morphs are housed in the Paleontologisk Mu­ (Fig. l) in equivalent stratigraphic position. This seum, Oslo (PMO). 'Late Cimmerian Unconformity' appears on Fig. 2 as an erosional surface with no angular dis­ cordance between the two units. During the sum­ Core description mer of 1982 the beds around the boundary were cored at 65°06.0'N, 10°17.3'E by the drilling ship The interval 28.55-11.00 m in core 7B (Fig. 3) 'Pholas' in a shallow drilling programme along consists of black homogeneous organic-rich E-W seismic profiles in the area. The strata are claystones. Neither sedimentary structures nor dipping gently to the west. This drilling pro­ bioturbation were observed. Some specimens of gramme is part of a mapping programme run by the bivalve genus Buchia occur. Smectite is the IKU (Maisey & Wøien 1983, Bugge, Knarud & dominant clay mineral. The total organic carbon Mørk 1984). con tent varies from 4 to 11%, and the rock has a rich hydrocarbon potential. Immature unstruc­ tured organic material is dominant, but palyno­ Material morphs and woody material also occur. At 11.00 m there is an abrupt lithological l'wo cores were recovered from the same site due change at a planar boundary (as seen in a core 5 to technical problems in the first hole. The tech­ cm in diameter) to an approximately 20 cm thick nique involves sampling by mechanical hammer­ light grey and grey intraformational conglomer­ ing through the outer drill string. Wire line coring atic limestone. The clasts and matrix are differen­ can start when reasonably well consolidated tiated on their colours, but interfinger and may strata have been reached. Only three hammer­ be difficult to distinguish. samples are available from the 5. 1 m deep core­ Above there are 25 cm of calcareous mudstone hole 7. Seven hammersamples were collected below another more well cemented micritic lime­ from the upper part (4.5-9.2 m) of corehole 7B. stone without intraclasts at 10.55 m. The calcite 2 Geologisk Tidsskr. 1/86 18 N. Aarhus et al. NORSK GEOLOGISK TIDSSKRIFT 66 (1986) Fig. I. Sketch map showing location of boreholes in !KU shallow drilling programme 1982. Cores 7 and 78 (same location) are here studied. Roman numerals indicate seismic units. The location of Andøya is also shown. content is 90% at 10.45 m and decreases to 75% grey to redbrown associated with the disappear­ at 10.20 m from where it is further reduced to 15- ance of pyrite. 40%. Siderite and dolomite do not occur. At 7.30 Calcareous fossil fragments are few both in the m there is a colour change of the marl from light limestones and marls. A few Inoceramus frag- w 150 E Fig. 2. Shallow seismic line 878-103 with location of studied coreholes. Seismic interpretation by Tom Bugge. NORSK GEOLOGISK TIDSSKRIFT 66 (1986) Biostratigraphy Lower Cretaceous, Sklinnabanken 19 ments are found, some of them bored probably Gochteodinia vi/losa and Scriniodinium pharo by sponges (?Clionia). Fungal borings are pres­ which all are in accordance with a Ryazanian dat­ ent in woody fragments from all the nine very ing. S. grossii is common to abundant in the up­ small (except at 10.10 m) organic residues recov­ permost metre of the black shale, at 11.25 m to­ ered from the interval 10.30-9.35 m. These gether with Hysterichodinium voigtii. This is woody fragments may well be reworked from the probably a result of change in environment; the Ryazanian, whereas the rest of the reworked or­ luxuriance of these species is associated with the ganic material was less resistant and has not been incoming of a bivalve bottom fauna which pos­ preserved. sibly reflects improved circulation of water. Sam­ The redbrown calcareous claystone in the two ples at 12.60 and 11.51 m, however, do have high lower hammersamples (4.00-4.30 m and 5.00- proportions of phytane. Some workers take this 5.10 m) from corehole 7 is similar to that above as an indication of reducing depositional environ­ 7.30 m in corehole 7B. Reduction spots and In­ ment. The rich content of organic material (al­ oceramus fragments occur. There is a thin grey though unstructured) also suggests that reducing bed around 4.24 m. The redbrown hammersam­ or oxygen-poor bottom conditions still prevailed. ple at 2 m in hole 7 contains pebbles icedropped Possibly Buchia or some species of this genus in calcareous ela y similar to that below and repre­ could live in water with low oxygen content. But sents Quatemary cover consisting mostly of in we will not completely exclude the possibility situ or nearly in situ weathering products. that these shells may have been dropped into the sediment. 28.55-10.85 m Ryazanian Nannofossils Palynology Samples in the black claystone proved to be bar­ The occurrences of Batioladinium pomum (lam­ ren. The interval 10.95-10.85 m yielded a spe­ plughii zone, eastem England, but younger in the cies-poor nannofossil association dominated by Haldager borehole no. l) and B. radiculatum Ellipsagelosphaera spp. Of biostratigraphic sig­ (runctoni-icenii zones, eastem England) (Davey nificance is the presence of Palaeopontosphaera 1982) throughout the black shale unit point to an sa/ebrosa, Nannoconus colomi, Nannoconus glo­ age no older and hardly younger than Ryazanian. bu/us and Nannoconus steinmanni. Systematophora palmula, Stiphrosphaeridium ar­ Nannoconids have not been reported before bustum and Kleithriasphaeridum porosispinum from earliest Cretaceous strata of north-western from 23.32 m and upwards support a Ryazanian Europe. According to Deres & Acheriteguy dating. (1980), the above-mentioned nannoconids and Egmontodinium expiratum from the base to the absence of younger forms are characteristic 16.65 m, according to Davey, would restrict the for a Berriasian age. A remarkable element in age to the runctoni zone (earliest Ryazanian). both samples is Sol/asites arcuatus. In the Spee­ Other species in the core which occur consis­ ton Clay, this species is restricted to bed D6 (Ber­ tently and have extinctions similar to that of E. riasian) according to Black (1971) and our own expiratum are Stiphrosphaeridium dictyophorum observations. and Dingodinium spinosum. They are, however, not found below 25.60 m. We think they have Macrofossils some stratigraphic potential in the area. This is A fragment of an ammonite has been found at also the case for Systematophora palmula (pres­ 13.20 m and in the interval from 12.00-11.95m a ent in the albidum Zone in the Speeton Clay ac­ number of heavily crushed buchiid bivalves oc­ cording to Davey (1982)). In contrast to in Eng­ cur. In spite of the poor preservation, the mate­ land, it has a partly overlapping range with that rial gives a due as to the age of this part of the of E. expiratum and occurs to the top of the black core. shale. The recorded species thus conflict with some of the ranges in Davey (1982). Based on Surites sp. cf./aff. tzikwinianus (Bogoslovsky, macrofossil evidence, a middle Late Ryazanian 1897) tzikwinianus zone age seems likely at 13.20 m. 1897 0/costephanus tzikwinianus Bogoslov­ The unit is otherwise characterized by consis­ sky, p. 59, 141, pl. 2, figs. 6a-d. tently occurring Tubotuberel/a apate/a, Chlamy­ 1964 Surites tzikwinianus (Bogoslovsky): Do­ dophorella membranoidea, Sirmiodinium grossii, novan, p. 31, pl. 7, fig. l. 2' --- - <�C -�� �og�� !:5 g:�gM:co � RYAZANIAN >�:g����m � il"- "' l� ��l zm mm " � � ??: � � .� � � /!! .;;; ... :;: jO_ p .;; -;- "' �:D �"'... "" � �§� ""'-! eo ex l'l'':!il 1 1 1 1 1 1 , 1 li'i'i!:' !i':J' j l lllllll'llli!l ll jllll�l!ll'''lllll'''lllll'lll illill i'':j'':1 ! ::.:... w"'''''1111111!l!ilim:1111 111 1111 1111 ,11liii!i'1111111111!ii1111 1111l111111111111111!1�lli ll111111 1 11111fll11111 11111ll!liliiii'i1i!i!11111111111111111:i� 11,111!11:1:ww �ll><1Xll l l ::. 1 1 1 1 1 >< !��terii<: 6\ () Cl Cl ;;. �ru� � Rf2"'�i:>!l_ ��a� �h � � Black Grey --+ Redbrown -i 1 2-� il � "3 .
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