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Biostratigraphy of Some Callovian and Oxfordian Cores Off Vega, Helgeland, Norway

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Biostratigraphy of Some Callovian and Oxfordian Cores Off Vega, Helgeland, Norway Biostratigraphy of some Callovian and Oxfordian cores off Vega, Helgeland, Norway NILS ÅRHUS, TOVE BIRKELUND & MORTEN SMELROR Århus, N., Birkelund, T. & Smelror, M.: Biostratigraphy of some Callovian and Oxfordian cores off Vega, Helgeland, Norway. Norsk Geologisk Tidsskrift, Vol. 69, pp. 39-56. Oslo 1989. ISSN 0029-196X. Four shallow cores drilled on an E-W trending seismic line on the Trøndelag Platform 35-40km to the west of Vega, Helgeland, Norway are described and their dinoflagellate cysts, ammonites and bivalves studied. Two new dinoflagellate cyst species, Crussolia perireticulata and Glomodinium cerebraloides, are formally described, and one new combination, Glomodinium granulatum (Pocock) n. comb., is proposed. Ammonites and bivalves of the genera Pseudocadoceras, Longaeviceras, Amoeboceras, Prae­ buchia and Buchia are systematically described and figured. The recorded fossils are used for a bio­ stratigraphical interpretation. The cores represent parts ofthe Callovian and a nearly complete Oxfordian section. Lowermost Kimmeridgian strata are also represented. N. Århus & M. Smelror, /KU, Postboks 1883, N-7002 Trondheim, Norway. Tove Birkelund died in lune 1986. During the summer of 1982 the drilling ship micaceous grey siltstone. Calcite cement occurs 'Pholas' drilled 14 shallow coreholes between 65° in variable amounts. XRD analyses do not reveal and 66°N on offshore Norway. Most of the sta­ any dolomite't>r siderite. The main clay minerals tions are located along two E-W running sei smie are kaolinite, chlorite and mica/illite, but some lines (the strata dipping gently to the west) and mixed layer minerals also occur. the cores examined here are all from the northern The visually examined samples have a total of these lines 3� kilometres to the west of the organic carbon con tent slightly above l%, with island of Vega (Fig. 1). The cores are treated here woody material as the most important in order of decreasing age (Fig. 2). Between the constituent. Cuticles, pollen and spores constitute top of core 4B and the base of core 3 there is an 30-40% of the organic residue with Cerebro­ undrilled interval of about 38 m, between 3 and pollenites macroverrucosus, Cal/ialasporites spp. 3B an interval of 32 m and between 3B and 5 the and Cyathidites minor as the most common taxa. interval is 48 m (Tom Bugge, pers. comm. 1987). Rock-Eva! data show that immature type IV Bugge, Knarud & Mørk (1984) published gen­ kerogen (Tmax 425-427) is dominant and the rock eral geological information from IKU's mapping has only a poor potential for gas. programme in the area and Århus, Verdenius & Birkelund (1986) gave details from a Lower Cretaceous core from the southern seismic line. Core 3 The core recovery from this hole is dose to 100% although there is some uncertainty with respect to the exact depth at the bottom of the hole. Lithology, vis u al kerogen and The penetrated strata consist mainly of micaceous organic geochemical data non-calcareous grey siltstones similar to core 4B, but with fine sand particularly in the lower part . Core 4B Heavy bioturbation by Macaronichnus occurs This core consists of 5 up to 25 cm long hammer throughout and some terrestrial plant material is samples from the interval 2.0-5.91 m below the observed. The total organic carbon content varies sea ftoor. The samples from the bottom of the between 0.6 and 0.9%. hole to the boundary with the Quaternary over­ Technical problems caused termination of the burden at 3.8 m consist of bioturbated very piggyback drilling operation in an at !east 1.3 m 40 N. Århus et al. NORSK GEOLOGISK TIDSSKRIFT69 (1989) Fig. l. Sketch map showing location of boreholes in IKU shallow drilling programme 1982. Cores 4B, 3, 3B and 5 are studied here. Roman numerals indicate seismic units. Fig. 2. Shallow seismic line B78-109 with location of studied coreholes. Seismic interpretation by Tom Bugge. thick brown calcite and siderite cemented bed The nine organic geochemically analysed with some dolomite cement in the upper part. samples from this core have a total organic carbon Two other brown carbonate cemented beds also content of between 0.60 and 0.93%, with woody occur in this approximately 18 m long core, one material dominant. However, the amount of about 0.3 m thick siderite and calcite cemented cuticles, pollen (mainly bisaccates), to a lesser and the other of at !east 0.7 m thick calcite extent spores and in some samples in the middle cemented at the top of the core. The carbonate is and upper part of the core also dinoflagellate micritic with microspa1itic and even some sparitic cysts, is large enough to influence the Rock­ patches. All three carbonate cemented beds are Eva! data and give a mixed type III/IV kerogen. very similar to the intervening siltstones in all Cerebropollenites macroverrucosus and partly aspects other than diagenesis. also Cal/ialasporites spp. occur in large numbers NORSK GEOLOGISK TIDSSKRIFT 69 (1989) Biostratigraphy of some Callovian cores 41 throughout the core. One sample at 12.4 m is pristane to phytane ratio in this sample. Tmax particularly rich in cuticles. values, which vary from 410 to 427 together with The reliable Tmax values vary between 419 and an R0 value of 0.37% at 24.44 m, indicate 428 and a Ro measurement of 0.34% at 8.15 m immaturity. The samples have poor to fair hydro­ and 0.35% at 15.8 m also implies immaturity. The carbon potentials based on sl+ s2. drilled interval would have only a poor potential The interval 20.1-17 m is transitional between as a source rock for gas. the beds below and above with respect to silt content, colour and degree of bioturbation and consists of micaceous non-calcareous grey silty Core 3B claystone. Only three 5 to 15 cm long hammer samples from Two samples between 20 and 18 m from the a drilled section of 4 m comprise this core. They intermediate lithology have a rich abundance of consist of micaceous non-calcareous grey silt­ organic carbon (12.59 and 6.91%). Rock-Eva! stones similar to those found in cores 4B and 3. pyrolysis indicates that this is type IV kerogen, The mineralogy is very uniform throughout with but transmitted light microscopy reveals abundant kaolinite, chlorite and mica/illite as the quanti­ bisaccate pollen and also quite rich spore floras. tatively most significant clay minerals. Although these immature samples (Tmax 413-415) One organic geochernically analysed sample are rich in organic material, the hydrocarbon contains 1.37% total organic carbon of mixed potential would on! y be for gas due to the kerogen type III/IV kerogen composition with Tmax of 427. type. Woody material is quantitatively most significant Around 17 m there is a mineralogical change in two of the three samples studied in transmitted associated with the income of non-calcareous dark light, whereas the uppermost sample contains grey shales with some mica and occasional slightly more cuticles than woody material. Bisac­ bioturbations. Such beds occur towards the top cates, other gymnosperm pollen and spores are of the core at 9.5 m. The main clay minerals in abundant throughout. The samples could have a the lower part of the core are kaolinite, chlorite fair potential for gas. and illite, but there are also considerable amounts of quartz and mixed layer minerals. Above about 17 m smectite is the dominant mineral, although Core 5 fair amounts of kaolinite, chlorite, illite and Coring stopped due to technical problems in a quartz still occur. siderite bed at 28.20 m, and drilling problems The change in lithology is associated with a caused uncertainties with respect to correct depth change in the composition of the organic material below 20 m. Drilling data suggest that the rec­ as observed in Rock-Eva! pyrolysis data, but not orded si deri te fragments fromthe lowermost part so easily seen in transmitted light except for a of the hole represent beds in an interval domi­ reduction in the number of spores. This may be nated by poorer consolidated sediments. Car­ due to difficulty in distinguishing between algal bonate beds do not occur above about 24.5 m and degraded woody material. A sample at from where bioturbated non-calcareous grey 17.58 m contains a type Ill (with type Il?) clayey siltstones with wood fragments are kerogen. Mixed type II/III occurs throughout retrieved. the rest of the core with type Ill dominating at Three samples between 24.5 m and 20 m con­ 17.05 m, 15.55, 14.30, 12.14 and 11.55 m and tain between 1.26 and 2.74% total organic carbon more equal amounts of type Il and Ill at 13.82, with blade opaque woody particles as the domi­ 12.75 10.50 and 9.55 m. The organic richness is nant constituent. Dinoflagellate cysts also con­ fairly uniform in these samples with TOC values tribute significantlyto the organic residues. Rock­ varying between 6.54 and 8.46%. Tmax values Eva! pyrolysis hydrogen and oxygen indices sug­ from 409 to 416 are evidence of immaturity. The gest that the kerogen is type IV, except for the samples at 17.05 and 9.55 m show a long-ranging lowermost analysed sample at 24.44 m which is aliphatic homology (C7 to C25), indicating a lipid very rich in cysts and contains a rnixedtype 11/III input with a high abundance of aromatics. In the kerogen. The long-ranging aliphatic homology latter sample spores are again abundant, whereas (C7 and C25 with a high abundance of aromatics) the 17.05 m sample has not been examined in may be due to the lipid rich cysts.
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