Polarforschung 68: 283 - 290, 1998 (erschienen 2000)

Late Mesozoic-Cenozoic Evolution of the and Continental Margins

By Eugeny E.Musatov l and Yulian E.Pogrebitskijl

THEME 14: Circurn-Arctic Margins: The Search for Fits and Baikalian inliers, Scandinavian - West Spitsbergen epi-Cale­ Matches donian, Polar Ural - Pai-Khoi, and Byrranga epi-Hercynian - Early Kimmerian orogens) and continental Summary: The most remarkable tectonic feature of Barents Sea and Kara Sea slopes and rises of Norwegian- (NGB) and Eurasian continental margins is a Cenozoic system of deep troughs anel grabens which (EB) basins. Young epicontinental Barents - northern Kara shelf follow Devonian-Jurassic paleorifts. These depressions are divided by a number of major domes and uplifts. The dominating tectonic process in the Barcnts-Kara marginal and Pechora, West Siberian intracontinental basins shelf was the successive degradation of an upliftedland within -Franz occur on the continental margin. Each structure of this Josef Land-Severnaya Zemlya zone, which served as a terrigcnic source for morphostructural assemblage is characterised by its own spe­ scdimentary basins of southern and central parts of the continental margin, The cific features of Cenozoic tectonic and geodynamic regime. general neotectonic regime of the continental margin has caused strong uplift of orogens and shields as weil as shelfic archipelagos Svalbard, and Severnaya Zemlya and predominantly subsidence of intracontinental and The giant oil and gas fields discovered in the Barents and Kara marginal shelf basins, In general, Cenozoic tectonics were favourable for pres­ Seas shelves yield evidence for huge reserves ofhydrocarbons. ervation and re-fonning of oil & gas resourees on the shelf. Late Crctaceous­ In this context, studies of Cenozoic structures on the continen­ Danian regressive, Paleocene-Eocene transgressive, Oligocene-Miocene regres­ sive, Pliocene-Pleistocene regressive-transgressive and Holocene transgressive tal margin are important for the reconstruction of crustal mo­ epochs of continental margin evolution are reeognized. Cenozoic development tion and recent geodynamics. The geological structure of the of Arctic was controlled by progressive penetration of processes of riftogene­ shelf shows three main units: folded basement, relics of sis and spreading frorn North Atlantic into the Norwegian-Greenland and Eura­ Paleozoic carbonaceous-terrigenous cover and Upper Paleozoic­ sian basins, which constrained the contrasting character and circurn-oceanic zoning of tectonic movements at continental margins. Cenozoic terrigenous unit of epicontinental shelf basins (GRAM BERG & POGREBITSKlJ 1984). Four major subunits are rec­ ognized in the composition of the upper terrigenous unit: Up­ INTRODUCTION per Paleozoic-Triassic (from 1-2 to 8-10 km in thickness), Jurassie-Lewer Cretaceous (0,5-3 km), Upper Cretaceous­ Theis paper is largely based on multi-channel seismic data pub­ Eocene (0-1 km) and Oligocene-Quaternary (0-0.5 km). A seis­ lished in Russia (BATURIN 1988, BEZMATERNYCH et al. 1993, mic section of Cenozoic cover of the southern Kara Sea shelf SENIN et a1.1989) and Norway (FALElDE et a1.1984, JOSEHANS et is shown in Figure 2; regional reflectors D 1 and D2 correspond al. 1993, SATTEM et al. 1994, SUNDVOR & AUSTEGARD 1990, to the base of Pliocene and Quaternary sequences respectively. V AGNES et al 1992) and single channel high resolution acoustic High industrial oil & gas prospectivity is proved (OSTISTY & profiling (Fig. 1) carried out by Russian (MUSATOV 1996) and FEDOROVSKY 1993) for both Paleozoic carbonaceous-terrigenous Norwegian expeditions (ANTONSEN et al. 1991, KNUTSEN et al. (large Prirazlomnoe oil field and Severo-Gulyaevskoe oil-gas 1993, SOLHEIM et al. 1998, VORREN et al. 1990). Ground evidence field) and Upper Permian-Mesozoic terrigenous units. The Up­ of the geological structure included gravity and piston coring per Perrnian-Triassie sequence contains the large Murmanskoe, (ELVERHOI & SOLl-IEIM 1987, GUREVICH 1995, STEIN et al. 1996), medium Severo-Kildinskoe and other gas fields; Jurassic-Lower shallow drillings (GRITSENKO & BONDAREV 1994, KRAPIVNER Cretaceous rocks contain the uniqe Shtockmanovskoe and 1986) and materials of deep wells on the shelf and adjacent is­ Ledovoe gas condensate fields and large Ludlovskoe, lands (ARMISHEV et al. 1988, GRAMBERG et al. 1985). Moreover, Rusanovskoe, Leningradskoe gas & gas condensate fields. the tectonic zoning provide evidence on tectonic settings in ad­ jacent islands (DIBNER 1998) and mainland areas (KUZIN 1983, Barents and Kara Seas margins exhibit the following anomalous VARLAMOV 1983). features: a unique extension (up to 750-1500 km); extremely dissected The Barents Sea and Kara Sea shelves occupy the main part of and contrasting relief (Fig. 3); the extended transitional zone between its continental frame higher thicknesses ofsedimentary cover (up to 18-20 km and (Baltic crystalline shield, Timan-Kanin and northern Taimyr even more in the southern Barents depression); peripheral shelfdomes of archipelagos, exposing Hercynian, I All-Russin Research Institute für Geology and Mineral Resources of the World Oeean. Caledonian and Precambrian folded basement; wide occur­ I, Angliysky Ave.. 190121, St.Petersburg, Russia rence (GRAMBERG 1988, ELDHOLM & TALWANI 1977) of deep­ Manuscript received 19 January 1999, accepted 12 Oetober 1999 sea rift grabens uncompensated by sedimentation;

283 o 150 3&J 450 6&J 750 Fig. 1: Seismic data map showing seismic acoustic lines available for this study area

70 72 74 76 78 ~o ~2 ~~ ~6 ~8 1,9 I I I I I I I I I II km km

200 200

400

i Q- Quatemary sequenee, N - Pliocene sequenee, K - P - Cretaceous - Paleogene sequence, to(ms) D - bottom ofQuaternary sequence, D - bottom ofPliocene sequence , to(ms)

Fig. 2: Sparker records on the southern Kara Sea shelf. Q =Quaternary seguence, N =pliocene seguence, K-P =Cretaceous-Paleogene scqucnce, D, =bottom of Quaternary seguence, D, = bottom of Pliocene seguence

284 60'

isobathes

KM 150 0 150 300 '150 600 KM Iw • • I ! II

Fig. 3: Bathymctry of the Barents Sea and Kara Sea shelves

- nongranitic crust inliers; of the Narth Eurasian continental margins to intense cornpres­ - higher seismicity (magnitudes up to 5-7), particularly near sion produeed by initial spreading in the NGB and EB. The main eontinental slopes and flanks of deep-sea grabens); phase of regional uplift took plaee during the end of the Late - manifestations of the Late Mesozoie (Franz Josef Land Ar­ Cretaeeous (Campanian-Maastrichtian) epoeh. Figure 4 dernon­ ehipelago and the northernmost Barents Sea Shelf), Late strates the character of the pre-Late Cenozoie erosion on the Cenozoie (Novaya Zemlya Archipelago) and recent (West narthern Kara Sea Shelf; reflectar D (the bottom of Upper Spitsbergen) basic magrnatism; Cenozoic veneer) forms a regional unconformity on single chan­ - and abundant normal and normal-lateral faults controlling nel seismic data. fjord grabens and deep-sea grabens edges (MUSATOV & MUSATOV 1992). The Paleocene-Eocene time was characterised by peneplanation of relief and local marine transgressions. The Arctie Paleocene­ Eocene were eharacterised by seafloor spreading (KRISTOFFERSEN THE LATE MESOZOIC-CENOZOIC EVOLUTION 1990) in NGB and vast basaltic flows in the Brito-Arctic Thule Provinee. At that time, the continental margins were tectonically The Early/Late Cretaceous boundary was a turning point passive and experienced moderate oscillatory movements, (POGREBITSKYI 1976) in the geologieal history of the Arctie. At whieh were the reason of shallow marine (under transgressive that time vast denudation areas that existed in the present loca­ eonditions) and deltaie sedimentation. Crusts of weathering are tion of the Arctic deep-sea basins were affected by rift-related recognized for this time in the Baltie shield, Kanin-Timan inlier destruetion. The Late Cretaceous-Danian phase was character­ of folded basement and Polar Ural - Pai-Khoi orogen. The ep­ ised by the largest regional uplift of Arctie continental margins, och of peneplanation of relief spanned most of Paleoeene time, partieularly along the periphery of the EB and NGB spreading when continental margin was dominated by denudation-accu­ basins. The top ofJurassie and sometimes Triassie (e.g., Perseus mulation plains, and marine transgressions developed there in in the Barents Sea) sedimentary sequences were exposed by the Eocene. Due to high sea-Ievel stand in the Eoeene, the trans­ intensive erosion at major anticlines and domes. Apparently, this gression, whieh propagated from the actively developed NGB epoch of regional uplifts was controlled by the erustal responce to the Bear and Nordcap trenehes, involved also the Barents-

285 KM 262 260 256 252 245 244 242 278 276 272 229 KM I I I I I I I II I I

200 ~. - 200

Fig. 4: Sparkor records on the northern Kara Sea shelf. Note unconfonnities (toplap and erosion truncation) at the reflector D,

Kara shelf; however, unlike the East Arctic shelf, its sediments - Severnaya Zemlya dome) under alternating conditions of ex­ were nearly all denudated there as a result of Oligocene-Miocene tension and compression. By their tectonic regime, the uplift­ uplift. The Central and Forlandsundet peri-oceanic basins of ing areas along the Spitsbergen-Severnaya Zemlya continental Svalbard Archipelago, parallel to NGB continental slope, are slope corresponded to a rift shoulder relative to EB. Major unique in thicknesses of their Paleogene cIastic sediments ex­ Cenozoic regressions (up to 300 m below modern sea level) are ceeding 2.5-3 km (DOWDESWELL 1988, DOWLING 1988). The fixed in Late Oligocene and in the end of Late Miocene (Fig. thickness of Paleocene-Eocene siliceous-argillaceous deposits 6) epochs. accumulated in the Western Siberian intracontinental plate amounts to 1 km and more. However, the transgression here Active EB development and destruction of continental rock propagated from the south through the Turgay basin and West­ masses at the Pliocene-Pleistocene stage led to degradation of ern Siberia was a shelf of Tethys oceanic basins. adjacent source areas near the Eurasian Basin continental slope dissected by Pranz-Victoria, Saint Anna, and Voronin deep-sea In the Arctic the Oligocene-Miocene stage is characterized by grabens, where widespread predominantly glacial-marine sedi­ a drastic change in paleogeographic settings. Spreading pro­ ments were deposited. Several regressive-transgressive cycles ces ses took place in the whole EB (JOKAT et al. 1995). Intensive during Pliocene and Pleistocene influenced to the interaction of uplifts of epiplatform orogens and shields, started in the marine transgressions and ground glaciations (SOLHEIM & Oligocene, revived low mountain relief. They were accompa­ KRISTOFFERSEN 1984) of highlands and adjacent shelves and is­ nied by first glaciations related to mountain growth. The West lands. The Holocene epoch is characterised by general subsid­ Siberian marine basin shoaled and gradually dried up, ac­ ence and marine transgression. Fragments of Paleogene pene­ cumulating lignite-bearing alluvial-Iacustrine deposits. plain broken up into separate blocks by younger tectonic dislo­ Oligocene-Miocene coarse-grained alluvial deposits on the shelf cations were partially buried on shelves in periods of transgres­ occur in deep erosional valleys (Fig. 5). Perioceanic Svalbard sion, and denudation of the surface occurred at regressions and basins cIosed and experienced compressional inversion, and the glaciations. The Pliocene-Quaternary cover is represented by next stage ofuplifting and development of tectonic deformations arenaceous-argillaceous, mostly glacial-marine deposits, sparker (ZARCHlDZE et al. 1991) is the most active in the whole platform records, single channel seismic data, coring and shallow drillings history of Svalbard Archipelago. At the western coast a Caledo­ suggest that its thickness is commonly 5-150 m on the Barents nian horst was thrusted over marginal shelf basin in the post­ and Kara Seas shelf (Fig. 7). In the Late Cenozoic period con­ Oligocene time. An uplifted land that afterwards became a tinental slopes experienced progradation due to intensive activity source area of sedimentary basins began to develope in periph­ of suspension flows and forming of fan deposits (EIDVIN et al. eral zone of the Barents-Kara basin (Svalbard - Franz JosefLand 1988) up to 1-2 km in thickness.

286 KM 276 2"78 2LiO 242 2Li6 248 250 252 2.5~ 25G 258 260 262 KM I I I I I I I I I I I II

~oo -

500 - 500

600

700 -700 ~ t 0 (Me)

Fig. 5: Seismic section of the upper Cenozoic cover in the St. Anna Trough. See deeply cut acient valley in the top of the Cretaceous rocks (N,).

STRAIIGRAPKY Deep troughs

V> (Franz-Victoria, St.Anna, Voronin, etc.) ~ ~ ffi f------+-----,--+------:.------,--+------,---1 ~ ~ :;l V> Vl

LAIE UJ ... Z UJ - - U MID ~ >-Q:: CJ) m fA'<' \ ~ -' D.. , Q:: UJ ~ ~ /' ----,j :::;) (J ~ ~ 8

UJ LAIE UJZ zUJ UJU ... 0Q / 0-' UJ D.. MID Z

fA'<'

!!' ... ~ , LAIE \ -- -- -_... Fig. 6: Sea level changes during the Late Cenozoic compiled from various sourees.

287 Fig. 7: The thickness of Pliocene-Quaternary KM 150 0 iso 300 450 000 lw wl I I I sediments of the Barents Sca and Kara Sea shelves

The last neotectonic rearrangement of Arctic margins occurred depressive factors, but Quaternary sheet glaciations increased at the end of Late Pleistocene, marking the onset of a new pressures due to ice weight. Pressures were maximally decreased paleogeographic stage. Neoteetonic activation was accompanied in neotectonic faults zones and in ancient paleovalleys of flu­ by a glacio-eustatic regression and the last glaciation (Late vialorigin (KUZIN 1983). Prospective oil and gas factors are an Wurmian in Alps, Late Weichselian in Europe, Late Valdai on inherity of structural features (VARLAMOV 1983), activation of the Russian platform, and Sartan in Western Siberia). Its extent, perspective structures, moderate neotectonic movements and estimated by different authors, is either different from or wholly their gradients. Negative factors are crucial changes ofstructural incompatible (KRAPIVNER 1986, KUZIN 1983) with the model of assemblages (Rns & JENSEN 1992, THEIS et al. 1993) and high a pan-Arctic glacier covering all Arctic shelves (GROSVALD gradients ofneotectonic movements. At the activated peripheral 1983) in Russia. Elevations of marine terraces in Russian Are­ shelf uplifts adjacent to Spitsbergen, Franz Josef Land and tic indicate that glacio-isostatic movements die out towards the Severnaya Zemlya archipelagos and in rift grabens Franz-Vic­ east of the region, where the last glaciation was minimal. At the toria, St. Anna and Voronin numerous neotectonic predomi­ Late Pleistocene-Holocene stage, intense crustal subsidences in nantly normal faults as weIl as strike-slip faults and thrusts were peripheral deep-sea grabens and glacio-isostatic coastal uplifts the reason of HC fields disturbance. This fact is the barrier for accomplished the formation ofthe present-day morphostructural oil & gas search (KNUTSEN et al. 1993, Loseth et al. 1993) at the pattern in Arctic transition zones. The contemporary seismicity edge of continental-margin plate. of continental slopes, fjord coasts, and some of rift grabens is the evidence for persisting tectonic activity of the transition zone. CONCLUSIONS

Late Cretaceous-Cenozoic tectonic activity was the reason ofthe Late Cretaceous-Cenozoic spreading of the sea floor in Norwe­ growth up of perspective structures, strong denudation and gian-Greenland and Eurasian oceanic basins was the reason for sometimes forming ofnew hydrocarbon (He) resources or their neotectonics and geodynamics of Barents and Kara Seas shelf destroying. Positive neotectonic movements as weIl as strong (Fig. 8). The results of these processes were a complicated al­ (up to 1-2 km) denudation ofthe top of Mesozoie rocks (SKAGEN teration of compression and extension conditions on the conti­ 1993) had caused decreasing rock pressure and HC migration nental margin. Five major stages of the Barents and Kara Seas from ancient reservoires. Re-forming of HC was also influenced margins evolution are recognized: by Cenozoic sea level changes. Major regressions were positive - Late Cretaceous-Danian regressive,

288 Fig. 8: Neoteetonics of the Barents Sea, Kara Sea 9 and shelves and adjacent areas. I = crys­ 0- talline shields; 2 = Cenozoic grabens within EJ -10 shields; 3 = Caldonian, Hercynian and Kimmerian 11 orogens; 4 = inliers of folded plate basement; 5 = 0- intracontinental basins; 6 = depressions within I:::-:::-! - 12 intracontinental basins; 7 = domes and horsts of shelf marginal basins; 8 = uncompensated grabens of continental margin; 9 = faults; 10 = boundaries of structures; II = flexure zones of the shelf break; KM 150 0 . 150 300 450 500 ,I ! le ,,, '" ! 12 = continental slopes.

Paleocene-Eocene transgressive, References Oligocene-Miocene regressive, Pliocene-Pleistocene regressive-transgressive and Antonsen, P., Elverhoi, A., Dypvik, H. & Solheim, A. (1991): Shallow bedrock geology of the Olga Basin area, northwestern Barents Sea.- Amer. Assoc. Holocene transgressive epochs. The NGB-EB transition Petrol. Geol. Bull. 75 (7): 1178-1194. zones characterise the earlier stage of the development of an Armishev, A.M., Borisov, A. v., Bro, EG. (1988): Geologicheskoye stroenie Atlantic-type margin. Zapadno-Arkticheskoy kontinentalnoy okrainy po dannym geofizicheskych nabludeniy I glubokogo burenia (Geological and deep-sea drilling con­ Cenozoic tectonics was dominated by sharp uncompensated straints on the geological structure ofthe West Arctic Continental Margin).­ Geologia morei I okeanov, Docl. Sov. Geol. 28 IGK, Leningrad, PGO subsidences of shelf basins reviving the intricate graben-rift "Sevmorgeologia", 195-204 (in Russian). systems of the Barents-northern Kara basin. The maximum of Baturin, D.G. (1988): Stroenie i evolutsia kontinentalnoi okrainy Evraziyskogo tectonic activity of the Barents-Kara Seas continental margin basseina mejdu archipel agam i Spitsbergen i Zemlya Franza-Iosifa (Struc­ was confined to the coastal belt, where uplifting involved Scan­ ture and evolution of the Continental Margin of the Eurasian Basin between the Spitsbergen and Franz JosefLand archipelagos).- Dokl. AN SSSR, 299 dinavia, the Kola Peninsula, Timan-Kanin inlier, Polar Ural ­ (2): 419-423 (in Russian). Pai-Khoi - Novaya Zem1ya and Byrranga orogens and the pe­ Bermaternych, E.F, Sen in, B. v., Shipilov, E V. et al. (1993): Osadochniy ripheral shelf uplift along the Spitsbergen - Sevemaya Zemlya chekchol Zapadno-Arkticheskoi metaplatformy (Sedimentary cover ofthe continental slope. The highest oil and gas perspective zones are Western Arctic metaplatform).- Munnansk, NIIMorgeophiziki, 184 pp. (in recognised in central parts of intracontinental and marginal ba­ Russian). Dibner; V.D. (ed.) (1998): Geology of Franz Josef Land.- Norsk Polarinstitutt sins, i.e. on slopes of horsts and grabens and local positive struc­ Meddelelser 146: 190 pp. tures of anticline and non-anticline type. Dowdeswell, EK. (1988): The Cenozoic stratigraphy and tectonic development ofthe Barents Shelf.- In: W.B.HARLAND & EX DOWDESWELL (eds.), Geological Evolution of the Barents Shelf Region, 131-155. ACKNOWLEDGMENTS Dowling, L.M. (1988): Cenozoic evolution of the western margin of the Barents Shelf.- In: W.B. HARLAND & E.K.DOWDESWELL (eds.), Geological Evolution ofthe Barents ShelfRegion, 157-169. 01'­ We offer our sincere thanks to Franz Tessensohn and other Eidvin, T., Jansen, E & Riss, F (1993): Chronology ofTertiary fan deposits off ganisers of the ICAM-III Conference for their significant sup­ the Western Barents Sea: Implications for the up1ift and erosion history of port, editing of manuscript and helpful comments. the Barents She1f.- Marine Geo1ogy 112: 109-131.

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290