ИСТИНА

Petroleum potential of Cretaceous succession in the Barents Sea is confirmed by the presence of uncommercial fields in Lower Cretaceous clastic wedges along the flanks of the Hammerfest basin, Loppa high and Tromso basin [Sattar et al, 2012, Seldal et al, 2005] and gas shows in the Cretaceous strata of the Ludlovskoe gas field in the South Barents trough [Borisov et al, 1995]. The Cretaceous sedimentary succession is divided into various sequences which are controlled by main sedimentary cycles: Upper Jurassic-Berriassian (sequence S0), Valanginian (S1), Hauterivian-Barremian (S2), Lower Aptian (S3), Aptian-Lower Albian (S4), Albian (S5) and Albian-Cenomanian (S6). These sequences are of regional character and could be recognized from Western Barents to Kara Sea and Western Siberia. Late Jurassic deep basin formed on the huge shelf area of West Siberia, Kara Sea, Barents Sea and Russian platform due to tectonic subsidence and uncompensated sedimentation [Suslova et al, 2010]. In the Eastern Barents Sea the basin was gradually filed by Berriassian and Valanginian clastic wedges from Novaya Zemlya archipelago, Persey high and Admiraltey high and by shelf clinoforms from the North Kara paleo land. More localized sediment sources include Fedinsky high, Kola monocline and perhaps Baltic shield. The deep basin has increased to the beginning of Aptian. Shallow marine and coastal sedimentation prevailed on the South Barents trough meanwhile the North Barents trough was the transitional zone for clastic material and represented by deltaic and fluvial plane. In the Aptian and in the first half of Albian there was a further reduction of marine basin due to normal regression which was changed by slow transgression in the middle of the Albian. Sea level rise resulted to marine condition in the Eastern Arctic in the Late Albian and Cenomanian. In the Neocomian clinoforms of Shtokmanovskoe, Ludlovskoe and Ledovoe fields sandstone layers are found based on well-log interpretation and correlation. These reservoirs can be saturated by gas and gas condensate due to dissipation of primary Jurassic reservoirs or contain hydrocarbons generated by Upper Jurassic and Lower Cretaceous source rocks [Stoupakova et al, 2015].