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Mineralogy and Geochemistry of Shales from the Late Jurassic-Early Cretaceous Transition

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Mineralogy and Geochemistry of Shales from the Late Jurassic-Early Cretaceous Transition NORWEGIAN JOURNAL OF GEOLOGY Fine-grained epicontinental Arctic sedimentation 65 Fine-grained epicontinental Arctic sedimentation – mineralogy and geochemistry of shales from the Late Jurassic-Early Cretaceous transition Henning Dypvik & Victor Zakharov Dypvik, H. & Zakharov, V.: Late Jurassic-Early Cretaceous fine-grained epicontinental Arctic sedimentation – mineralogy and geochemistry of shales from the Late Jurassic-Early Cretaceous transition. Norwegian Journal of Geology, Vol 92, pp. 65-87. Trondheim 2012, ISSN 029-196X. Late Jurassic and Early Cretaceous fine-grained siliciclastic formations from key Arctic localities have been analysed. In this study their mineral- ogical and geochemical (major, trace, REE elements) affinities have been compared and put into a sedimentological context. Compared to other regions the studied sections represent more ventilated and less anoxic conditions than other Late Jurassic black shale formations. The overall mineral ogical and geochemical composition is rather similar in the studied sections. This homogeneous appearance reflects the well-developed circulation of the shallow epicontinental sea of the region. The suspended material was repeatedly homogenised before final deposition and appears today to be relatively similar in composition over this wide area. In contrast, a basaltic source rock component (Siberian Traps?) is evident in the Siberian section (Nordvik). On large parts of the sea floor anoxic conditions prevailed, and in the Nordvik region this, in combination with slow and very fine-grained clastic sedimentation and high algal production, resulted in the formation of phosphate concretions. Henning Dypvik, Department of Geosciences, University of Oslo, P.O.Box 1047, Blindern, NO 0316 Oslo, Norway. E-mail: [email protected]. no; Victor Zakharov, Geological Institute, Russian Academy of Sciences. Pyzhevskij 7, Moscow, 109017 Russia. E-mail: [email protected] Introduction consisted of three Siberian branches which were sepa- rated by the Urals, the Novaya Zemlya islands and Tai- The Late Jurassic epicontinental sea covered large parts myr Island (Zakharov et al. 2002). These depositional of the present Arctic basin. In this paper, field sections basins are presently named the Barents Sea Basin, West of shale from the remote Nordvik area (North Siberian Siberian Basin and North Siberian Basin, where Nordvik Basin) will be compared with a composite of selected, is located (Figs. 2, 3a and 3b). The widespread fauna was more closely spaced locations from the Barents Sea dominated by, e.g., stenohaline molluscs, brachiopods, region (North Greenland, Svalbard and the southern foraminifers, radiolarians and dinoflagellates with high Barents Sea drillcore 7018/05-U-01) (Figs. 1 and 2). taxonomic diversity. Such fauna could only be kept in The aim is mainly to disclose compositional similari- balance in very large masses of water, of relatively stable ties or differences in order to shed light on basinal devel- salinities and temperatures (Zakharov et al. 2002). opments along with variations in weathering, sedimen- tation, geometry and tectonics of the area (Figs. 2, 3a Dypvik (1992), Zakharov et al. (1998) and Mørk & and 3b). The search for possible geochemical signals of Smelror (2001) demonstrated several eustatic, sequence- the Late Jurassic Mjølnir impact has also been an issue stratigraphic signals in the Jurassic and Lower Cretaceous (Zakharov et al. 1993; Dypvik, et al. 1996; Dypvik and successions, important controlling factors in the sedi- Zakharov 2010). mentation of the Arctic basins at that time. During this period, sedimentation in the Siberian basins took place Geological background information in a wide range of environments; from alluvial plains and lacustrine swamps in Early and Mid Jurassic time Overview and into open marine conditions in the Late Jurassic and The Jurassic to Cretaceous transition can be fairly well Early Cretaceous (Shurygin et al. 2000). The Lower and correlated in the area, forming the natural stratigraphical Middle Jurassic formations of Western Siberia are domi- base of this study (Figs. 3a and 3b). nated by sandy horizons with interlayered beds of clay- stone and shale. The number of marine beds generally The Mesozoic successions of the North Greenland, Sval- increases from south to north, and in the Upper Jurassic bard, Barents Sea, Kara Sea and Siberian Arctic represent sections marine claystones dominate in the region. A few the wide epicontinental paleo-Arctic sea. This seaway glauconitic sands are found dispersed in the lower part 66 H. Dypvik & V. Zakharov NORWEGIAN JOURNAL OF GEOLOGY Figure 1. Map of the present- day Arctic. The 7018/05-U- 01 locality is represented by a shallow core, the Svalbard sample comes from the Janus- fjellet section, whilst the North Greenland localities are a = East Peary land and b= Kilen. The Mjølnir impact structure (star) is also marked on the map. a North Greenland b Nordvik Svalbard Mjølnir 7018/05-U-01 150 Ma (Kimmeridgian-Volgian) Figure 2. A simplified Late (absolute frame) 150 Ma (Kimmeridgian-Volgian)Jurassic paleogeography of (absolute theframe) Arctic, based on the plate reconstructions of Lawver v v v v et al. (1990). Arrow along v7 v v v v the North Greenland paleo- NORTH SIBERIAN BASIN v v v v Figure 1 7 coastline shows the major Nordvik v v v v v v v vv v v v v NORTH SIBERIANDypvik BASIN and Zakharov, 2011 coast-parallel current trans- v Nordvikv v v v vv v v v v v v v Taimyr port direction measured v v v v v v v v v Taimyr (towards SE). Possible tidal v v v channel transportation direc- tions towards the south have been measured at right angles WEST SI BERI AN BASI N to this. Same locations as in WEST SI BERI AN BASI N Figure 1. Novya Zemlya Ural Novya Zemlya Ural Svalbard BARENTS SEA BASI N Svalbard Mjølnir a BARENTS SEA BASI N b Mjølnir a North Greenland 7018/05-U-01 b North Greenland 7018/05-U-01 Mjølnir impact structure Land Mjølnir impact structure Scandinavia Land Volcanics/ Scandinavia volc. clastics Volcanics/ v v v v Siberian traps volc. clastics Marine/ Lagoonal/v v v v Siberian traps Shallow marine Marine/ Lagoonal/ Shallow marine NORWEGIAN JOURNAL OF GEOLOGY Fine-grained epicontinental Arctic sedimentation 67 a STAGES NORTH GREENLAND SVALBARD BARENTS SHELF NORTH SIBERIA East Peary Land Kilen Central Spitsbergen Bjarmeland Platform Nordvik C ? ? Albian Kap Rigsdagen Gåseslette R beds Group ? ? E Aptian L Carolineellet a Formation T d Kolmule A e Formation Barremian g ? Helvetiaellet C å ? Galadriel Formation r Fjeld E Hauterivian R Ullaberget Kolje d Formation u Member Formation s O Lichen Ryg r Valanginian å Sand- Formation i Klipp- Knurr U e k Wiman - sk Fm. Fm. stone ellet Rya- n Member Dromledome f. S Formation Member Berri- zan- ian F Fm. H Paksa asian e < < < < < < < < < < < < < < < < < < < < < < < < Formation o Kuglelejet k r Formation A Slottsmøya Krill J k Tithon- Volg- m Splitbæk g Member i a n Member U ian ian a Formation t r g Birkelund d Oppdal- e i R Kimmeridgian Fjeld h såta Mb. n o Formation f. A n Lardy- F Alge ? Member Oxfordian F ellet Mb. m. S o Callovian r Oppdalen S m. Member Fuglen Formation I Bathonian Kapp Toscana C Group b Figure 3a Dypvik and Zakharov, 2011 9 2008) w unschensis . Figure 3a and 3b. 3a. Stratigraphic comparison figure with correlations between the N.Greenland, Svalbard, Barents Sea and East Siberian Basin - Nordvik stratigraphy. General lithological information is presented in standard signatures, while the thick black lines show sample levels. 3b. Correlation chart of the zonal successions around the Jurassic-Cretaceous boundary of Nordvik and Svalbard.Figure Not 3bto scale. Dypvik & Zakharov 2011 of the Upper Jurassic formations. In latest Jurassic time, It should be noted that the studied Jurassic and turbidites were deposited in the prodeltaic and deeper Cretaceous basins of North Greenland, Svalbard and the offshore regions of western and northern Siberia. The Barents Sea are rather closely located compared to the marine shelf sedimentation continued into the earliest Nordvik section. They were highly influenced by their Cretaceous. proximity to the tectonically active regions along the 68 H. Dypvik & V. Zakharov NORWEGIAN JOURNAL OF GEOLOGY neighbouring plate boundaries towards the Mohns and Oxfordian, black, silty claystones with carbonate con- Knipovich ridges in the south and west, in addition to cretions and an overall apparent thickness of 11 m. The the eustatic sea- level changes at the time (Lawver et al. rocks contain abundant pyrite nodules and glauconitic 1990; Faleide et al. 1993). grains. Taphocoenoses of bivalves show signs of both autochthonous and allochthonous burial, suggesting sed- Siberia imentation within the storm-wave zone. The well-known Bazhenov Formation of Western Sibe- ria is of Volgian (Tithonian) to Berriasian age, and made In the Nordvik Peninsula, Kimmeridgian overlies the up of black to brown, organic-rich shales (Vyshemirsky Oxfordian section at a sharp but conformable contact. 1986; Gavshin & Zakharov 1996a; 1996b). This confined The Kimmeridgian is represented by dark grey, silty clay- 5-6 million year period of dark grey, black to dark brown, stones with grains of glauconite and chlorite ; the over- organic-rich clay sedimentation is commonly repre- all thickness is 32 m. The middle part of the Kimmeridg- sented by 25 to 30 m-thick beds, which vary between 10 ian beds enclose carbonate concretions up to 1 m across. and 60 m in thickness. This famous petroleum source Macrofossils are dominated by rostra of belemnites. rock covers more than 1 mill km2, is normally buried Ammonites and bivalves are scarce in these lower sub- beneath 2000 to 3000 m of younger sediments and con- littoral sediments. In the Kheta River basin, the Upper tains on average 8 % TOC (Gavshin & Zakharov, 1996b), Oxfordian and Lower Kimmeridgian deposits are litho- typically with type II organic matter (Kontorovich et al., logically similar, with a gradual internal transition (Saks 1997).
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