Svalbard’s post-Caledonian strata — an atlas of sedimentational patterns and palaeogeographic evolution

Steel, Ronald J.; Worsley, David

doi:10.1007/978-94-009-5626-1_9

Cited by 206 publications

(290 citation statements)

References 27 publications

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“…[64] In Spitsbergen, normal faulting during Carboniferous times has been described by, for example, , Gjelberg and Steel [1981], Steel and Worsley [1984], Ringset and Andresen [1988], Johannessen and Steel [1992], Dallmann [1992], Dallmann et al [1993a], McCann and Dallmann [1996], and CASE Team [2001]. The most prominent structures are the Billefjorden Fault Zone and Lomfjorden Fault Zone in the east (Figure 19a), the Inner Hornsund Fault in the south, and additional fault bounded basins in the west [e.g., Maher and Welbon, 1992;Welbon and Maher, 1992;.…”

Section: Block Faultingmentioning

confidence: 99%

Eurekan transpressive deformation in the Wandel Hav Mobile Belt (northeast Greenland)

Gosen

Piepjohn²

2003

Tectonics

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Besides the ∼W‐E trending Kap Cannon Thrust Zone and Harder Fjord Fault Zone, the 300 km long and NW‐SE striking Wandel Hav Mobile Belt represents the third major fault zone in north Greenland. Structural analyses in several areas of this belt suggest that compressive deformation is characterized by transpressive dextral strike‐slip kinematics. This is demonstrated by a combination of folding around ∼W‐E axes, approximately north and south directed reverse faulting, and dextral strike‐slip displacements along NW‐SE trending fault lines. The initial formation of the long, linear faults is interpreted to be related to deformational events in Late Paleozoic, Triassic‐Jurassic, and Late Cretaceous times. Due to the lack of structural evidence, we assume that deformations led to the generation of extension faults which probably were reactivated during dextral strike‐slip tectonism. It is suggested that dextral transpressive deformation was coeval with ∼N‐S compression at the Harder Fjord Fault Zone and Cap Cannon Thrust Zone and took place during Eocene (Eurekan) times. Dextral strike‐slip tectonism in the Wandel Hav Mobile Belt was the result of ∼N‐S compression due to a general northward movement of the Greenland plate. As a zone of crustal weakness, the belt can be interpreted as the onshore equivalent of the main transcurrent fault zone (De Geer Fault) which caused the intracontinental dextral slip of Svalbard (Barents Shelf) relative to north Greenland during Early Tertiary (Eurekan) times and prior to their separation. In this configuration, it represents one part of the belt of Eurekan deformation which extends from the Canadian Arctic islands over north Greenland to the Barents Shelf where compressive deformation is recorded in the West Spitsbergen Fold‐and‐Thrust Belt.

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Section: Block Faultingmentioning

confidence: 99%

Eurekan transpressive deformation in the Wandel Hav Mobile Belt (northeast Greenland)

Gosen

Piepjohn²

2003

Tectonics

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“…Section Tålmodryggen is located on the Nordfjorden High, which was a persistent positive feature (horst block) during the Carboniferous-Permian. This also explains why the sedimentary successions record shallower-water conditions in comparison with other sections (Steel & Worsley, 1984;Ehrenberg et al, 2001). During the deposition of the Kapp Starostin strata (S2, S3 & S4), the main depocentre was located near section Kapp Fleur de Lys that contains a thick succession of deep-water microfacies such as bedded cherts (MFT-12).…”

Section: Correlation In Central Spitsbergenmentioning

confidence: 72%

“…6). The Permian is characterised by a period of tectonic quiescence on Svalbard (Steel & Worsley, 1984;Dallmann et al, 1999). The local differences in accommodation space and facies may be linked to the older, pre-existing, structural elements, inherited from the reactivation of the main tectonic lineaments throughout the Carboniferous (Ehrenberg et al, 2001;Blomeier et al, 2013).…”

Section: S2 S3 and S4mentioning

confidence: 99%

“…During the Mid/Late Artinskian, a major transgression flooded the shelf margins and structural highs resulting in the deposition of extensive carbonates along the northern margin of Pangea (Steel & Worsley, 1984;Blomeier et al, 2011). The upper parts of unit L-8 (Isbjørn Formation) of the Finnmark Platform and the Great Bear Cape Formation within the Sverdrup Basin are considered to correlate with the Vøringen Member on Spitsbergen (Stemmerik & Worsley, 2005).…”

Section: Vøringen and Kapp Starostin Stratamentioning

confidence: 99%

“…The Franklinian shelf, located on the northern rim of the supercontinent Pangea, preceded the formation of basins in Arctic Canada (the Sverdrup Basin), the Barents Sea (the Finnmark Platform, the Hammerfest Basin and onshore Svalbard), Greenland (the Wandel Sea Basin), and Russia (the Timan-Pechora Basin) (Scotese & Langford, 1995;Golonka, 2002). During the Late Palaeozoic, the sediments within these basins recorded a gradual cooling from warm and arid to cold-water conditions and an associated deepening of the depositional environments (Steel & Worsley, 1984;Beauchamp, 1994;Beauchamp & Desrochers, 1997;Ehrenberg et al, 1998).…”

Section: Introductionmentioning

confidence: 99%

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Facies arrangement and cyclostratigraphic architecture of the Templet Member and the Kapp Starostin Formation (Permian) on Spitsbergen, Svalbard

Jafarian¹,

Groen²,

Nooitgedacht³

et al. 2017

NJG

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Because of outstanding outcrops, Spitsbergen (Svalbard archipelago) provides unique opportunities to investigate the whole Upper Palaeozoic succession in great detail. This study can help to interpret the stratigraphic history and depositional evolution at other locations exposing coeval shelf strata along the northern margin of Pangea, e.g., the southern Barents Sea and Arctic Canada. Bed-scale outcrop observations are combined with microfacies studies to interpret the sedimentary settings and depositional environment of the Upper Palaeozoic strata. A sequencestratigraphic analysis has been carried out to evaluate the relative timing of sediment facies deposition in response to sea-level changes. The Early Artinskian to Kazanian successions of the Templet Member and the Kapp Starostin Formation were divided into five parasequences that are superimposed on a long-term, second-order, sea-level fall. These parasequences record a fundamental change of the sedimentary setting, from a restricted-marine, warm-water carbonate platform to an open-marine, cold-water, biosiliceous-carbonate ramp system. A cross-section across Svalbard comprising nine onshore sections shows that during deposition of the Kapp Starostin Formation a major depocentre marked by thick parasequences and a higher proportion of deep-water facies (bedded cherts) is located in the southwest of Spitsbergen (at Akseløya), whereas northeastern Svalbard records shallow-water microfacies. Svalbard was tectonically passive during the Permian; the local differences in accommodation space and facies were most likely linked to the rejuvenation of pre-existing structural elements, inherited from the Carboniferous. A deepening of the depositional environment combined with cold-water climatic conditions as recorded in our study area has also been documented in other Upper Palaeozoic successions around the Arctic, such as the Finnmark Platform (Norwegian Barents Sea) and the Sverdrup Basin (Arctic Canada). This transition in the depositional environment along the northern margin of Pangea is the result of large-scale changes in oceanic circulation patterns and local palaeogeographic changes during the northward movement of Pangea.

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Diagenetic Alterations Related to Falling Stage and Lowstand Systems Tracts of Shelf, Slope and Basin Floor Sandstones (Eocene Central Basin, Spitsbergen)

Mansurbeg

Morad

Plink‐Björklund

et al. 2013

Linking Diagenesis to Sequence Stratigraphy

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Svalbard’s post-Caledonian strata — an atlas of sedimentational patterns and palaeogeographic evolution

Cited by 206 publications

References 27 publications

Eurekan transpressive deformation in the Wandel Hav Mobile Belt (northeast Greenland)

Eurekan transpressive deformation in the Wandel Hav Mobile Belt (northeast Greenland)

Facies arrangement and cyclostratigraphic architecture of the Templet Member and the Kapp Starostin Formation (Permian) on Spitsbergen, Svalbard

Diagenetic Alterations Related to Falling Stage and Lowstand Systems Tracts of Shelf, Slope and Basin Floor Sandstones (Eocene Central Basin, Spitsbergen)

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