Interpretation of depth to the magnetic basement in the northern Barents Sea (south of Svalbard)

Skilbrei, Jan Reidar

doi:10.1016/0040-1951(91)90010-p

Cited by 22 publications

(23 citation statements)

References 20 publications

Supporting

Mentioning

Contrasting

Order By: Relevance

“…Nonmagnetic Devonian rocks in the west and weakly magnetized gneisses in the east accompany the fault zone. Skilbrei [1991] concluded that anomaly M5 separates two distinct terranes juxtaposed by suturing along the Billefjorden Fault Zone. The concept of a north‐south trending main thrust was picked up by Gudlaugsson et al [1998].…”

Section: Discussionmentioning

confidence: 99%

Caledonian basement of the western Barents Sea

Ritzmann

Faleide

2007

Tectonics

View full text Add to dashboard Cite

Major crustal units in the western Barents Sea have been defined on the basis of depth‐converted seismic reflection data, gravity and magnetic anomaly data. The seismic data revealed three types of crustal reflectivity below the sedimentary rock units, i.e., transparency, strong lower crustal reflectivity, and thoroughly reflective. The crustal structures obtained from the seismic reflection data are supported by 2D density and magnetic modeling. Three NE‐SW‐striking crustal units have been observed south of Bjørnøya. Changes in reflectivity in southwestern Barents Sea are accompanied by gravity and/or magnetic anomalies. North of Bjørnøya, two basement provinces could be distinguished. The observed outlines of the crustal blocks in the southwestern Barents Sea match with Caledonian main thrusts onshore northern Norway. We were therefore able to outline the continuation of Scandian nappe complexes in the southwestern Barents Sea. The crustal unit to the west of the Loppa High region is supposed to be a fragment of Laurentia, since the Loppa High region aligns with the Uppermost Allochthon nappes onshore, and is therefore expected to be the collision zone between Baltica and Laurentia. The southeastern crustal unit aligns with the Lower to Upper Allochthons and their Fennoscandian basement onshore. A compilation of all known thrusts and sutures in the western Barents Sea revealed the complexity of the Iapetus closure. It challenges the concept of two Caledonian main branches (NE and N). The thrusts/sutures are fan‐shaped distributed across the western Barents Sea, resembling the structure of the Late Paleozoic–Mesozoic/Paleocene rift basins and basement highs in the southwestern Barents Sea.

show abstract

Section: Discussionmentioning

confidence: 99%

Caledonian basement of the western Barents Sea

Ritzmann

Faleide

2007

Tectonics

View full text Add to dashboard Cite

show abstract

“…The structural features of the area around Svalbard and Hopen are commonly discussed using the names Edgeøya platform (Bergsager, 1986;Gabrielsen et al, 1990;Doré, 1995) and Svalbard platform interchangeably (Skilbrei, 1991;Nøttvedt et al, 1992a;Gudlaugsson et al, 1998;Grogan et al, 1999;Worsley et al, 2001;Henriksen et al, 2011). This is likely due to the existence of the poorly visualised Edgeøya basin (Elverhøi et al, 1988;Doré, 1995), which separates the Edgeøya platform from the Hopen high ( Fig.…”

Section: Data For Line G-g' and Line H-h' The Locations Of The Linesmentioning

confidence: 99%

Regional tectono-sedimentary development of the highs and basins of the northwestern Barents Shelf

Anell¹,

Faleide²,

Braathen³

2016

NJG

View full text Add to dashboard Cite

While many structural elements on the northwestern Barents Shelf initiated early and have remained influential on accommodation and sediment ation, detailed seismic interpretation attests to the development of new structural elements, shifting locus of influence, and burial, reactivation and inactivation at different times of various highs and basins. NE-SWoriented structural elements such as the Gardarbanken and Hopen highs, and the Capria ridge (informally named herein), have old Carboniferous foundations and show signs of reactivation in the Early Triassic. Towards the southwest, the Capria ridge merges with the paleoStappen high, which is a N-S, tilted peneplaned, Late Carboniferous riftshoulder which deeply erodes the Carboniferous deposits, and is onlapped by Permian and Early Triassic sediments. The paleosurface is overprinted by the dominantly postCretaceous development of the Stappen High, which has a maximum uplift and extent south of Bjørnøya. The Sørkapp basin is the main depocentre on the northwestern Barents Shelf; however, the Storjorden, Edgeøya and Ora (informally named herein) basins all formed around the same time in the Carboniferous. While the Sørkapp basin remained a sag basin until the Ladinian, the Edgeøya basin, a narrow rift basin, became largely inactive following infill. As a result, the Hopen high and Edgeøya platform, which bounded the Edgeøya basin, merged to form the Svalbard platform. The Storfjorden basin was reactivated around the Mid Jurassic when the Sørkapp depression, forming west of the Sørkapp basin, was initiated. Both basins are asymmetrical and bounded by gentle anticlinal features on one side implying formation associated with contraction. Cretaceous sediments, largely eroded from the area, are found in basins such as the Olga basin, which formed between two anticlines. One of these anticlines is the Sentralbanken high, which contrary to most other highs in the area shows no signs of initiation in the Carboniferous, but rather appears to have been a depocentre which was inverted around the Cretaceous.

show abstract

“…Mid-Permian Brekhuntsov et al (2011) Southern Kara Sea Henriksen et al (2011b) Barents Sea Ivanova et al (2011) Barents Sea/Kara Sea Johansen (1992) Barents Sea Khutorskoi et al (2008) Barents Sea Nikishin et al (2011) Southern Kara Sea Piskarev and Shkatov (2012) Eastern Barents and Kara seas Top crystalline crust Aplonov et al (1996) Eastern Barents and Kara seas Drachev (2011) Eastern Barents and Kara seas Gramberg et al (2001) Western Barents Sea Hauser et al (2011) European Arctic Ivanova et al (2011) Barents and Kara seas Johansen (1992) Barents Sea Myklebust 1994) Barents Sea Barents Sea Skilbrei (1991) Barents Sea Moho Aplonov et al (1996) Eastern Barents and Kara seas Dahl-Jensen et al (2003) NE Greenland Hauser et al (2011) European Arctic Ivanova et al (2011) Barents Sea Kostyuchenko et al (2006) Eastern Barents and Kara seas Minakov et al (2012a) Northern Barents Sea Barents Sea…”

Section: Modelling Of the Upper Mantle Configurationmentioning

confidence: 99%

“…This deep thermal mantle anomaly is assumed to account for the anomalous shallow seafloor of the NE Atlantic Ocean ( Fig. 1; Skogseid, 2014).…”

Section: Earliest Eocene To Presentmentioning

confidence: 99%

A lithosphere-scale structural model of the Barents Sea and Kara Sea region

et al. 2015

View full text Add to dashboard Cite

Abstract. We introduce a regional 3-D structural model of the Barents Sea and Kara Sea region which is the first to combine information on the sediments and the crystalline crust as well as the configuration of the lithospheric mantle. Therefore, we have integrated all available geological and geophysical data, including interpreted seismic refraction and reflection data, seismological data, geological maps and previously published 3-D models into one consistent model. This model resolves four major megasequence boundaries (earliest Eocene, mid-Cretaceous, mid-Jurassic and mid-Permian) the top crystalline crust, the Moho and a newly calculated lithosphere-asthenosphere boundary (LAB). The thickness distributions of the corresponding main megasequences delineate five major subdomains (the northern Kara Sea, the southern Kara Sea, the eastern Barents Sea, the western Barents Sea and the oceanic domain comprising the NorwegianGreenland Sea and the Eurasia Basin). Relating the subsidence histories of these subdomains to the structure of the deeper crust and lithosphere sheds new light on possible causative basin forming mechanisms that we discuss.The depth configuration of the newly calculated LAB and the seismic velocity configuration of the upper mantle correlate with the younger history of this region. The western Barents Sea is underlain by a thinned lithosphere (80 km) resulting from multiple Phanerozoic rifting phases and/or the opening of the NE Atlantic from Paleocene/Eocene times on. Notably, the northwestern Barents Sea and Svalbard are underlain by thinnest continental lithosphere (60 km) and a low-velocity/hot upper mantle that correlates spatially with a region where late Cenozoic uplift was strongest. As opposed to this, the eastern Barents Sea is underlain by a thicker lithosphere (∼ 110-150 km) and a high-velocity/density anomaly in the lithospheric mantle. This anomaly, in turn, correlates with an area where only little late Cenozoic uplift/erosion was observed.

show abstract

Interpretation of depth to the magnetic basement in the northern Barents Sea (south of Svalbard)

Cited by 22 publications

References 20 publications

Caledonian basement of the western Barents Sea

Caledonian basement of the western Barents Sea

Regional tectono-sedimentary development of the highs and basins of the northwestern Barents Shelf

A lithosphere-scale structural model of the Barents Sea and Kara Sea region

Contact Info

Product

Resources

About