Late Cretaceous – Early Tertiary Deformation, North Greenland

Okulitch, A V; Trettin, H P

doi:10.1130/dnag-gna-e.467

Cited by 11 publications

(12 citation statements)

References 10 publications

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“…2). This is supported by Soper & Higgins (1991b), who found no evidence that the fault zone, as now seen, was in existence during the Ellesmerian deformation. In this case, the northernmost parts of North Greenland would represent a terrane and the Harder Fjord Fault Zone a terrane boundary (Soper & Higgins, 1991b).…”

Section: B Devonian To Early Carboniferous (Ellesmerian Deformation)mentioning

confidence: 50%

“…Surlyk, Hurst & Bjerreskov (1980), , 1984 and , 1984 suggested that the fault zone already controlled the platform margin in Early Cambrian times. In contrast, Soper & Higgins (1987, 1991b pointed out that the position of the lineament does not coincide with the facies changes in the Lower Cambrian sediments which define the trough-platform transition. In the study areas the almost identical Frigg Fjord mudstones on both sides of the Harder Fjord Fault Zone indicate that it was not active during Early Palaeozoic times because no effect on sedimentary facies in the Franklinian Basin could be observed.…”

Section: Discussion and Synthesis Of Structural Evolution 4a Pre-dementioning

confidence: 94%

“…In Nansen Land, Soper & Higgins (1987, 1991b structures and stratigraphic boundaries along the western segment of the Harder Fjord Fault Zone which indicate 20 km of dextral strike-slip movements. Although we found no clear structural evidence of lateral displacements in the study areas, a post-late Santonian phase of dextral strike-slip along the fault zone, which accommodated crustal extension in the north during the emplacement of the N-S dyke swarms (Soper & Higgins, 1991b), seems to be likely (Fig. 15b).…”

Section: E Late Cretaceousmentioning

confidence: 99%

“…As the F1 and F2 fold structures and related cleavage planes (S1, S2) do not affect the Wandel Sea Basin deposits or do not pass through the unconformity into the overlying Cretaceous sediments, their Ellesmerian age is evident. Soper & Higgins, 1991b). 12 top profile -left).…”

Section: B Devonian To Early Carboniferous (Ellesmerian Deformation)mentioning

confidence: 99%

“…The orientations of the B1 fold axes do not coincide with the overall ENE-WSW trend of the Ellesmerian structures and can be compared with W-and S-directed imbricate thrusts south of the Harder Fjord Fault Zone southwest of Frigg Fjord (Fig. In this case, the northernmost parts of North Greenland would represent a terrane and the Harder Fjord Fault Zone a terrane boundary (Soper & Higgins, 1991b). Håkansson & Pedersen (1982) and Pedersen (1986) interpreted these structures as being related to the Caledonian orogenic belt in Kronprins Christian Land (eastern North Greenland) during the Early to Middle Devonian 'Vølvedal orogeny' and suggested large-scale (?about 700 km), pre-Ellesmerian sinistral strike-slip displacements along the fault zone during that time.…”

Section: B Devonian To Early Carboniferous (Ellesmerian Deformation)mentioning

confidence: 99%

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Polyphase deformation at the Harder Fjord Fault Zone (North Greenland)

Piepjohn

Gosen²

2001

Geol. Mag.

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In North Greenland, the E-W-trending Harder Fjord Fault Zone represents a major lineament which cuts through Cambrian to Silurian deep-water sediments of the Franklinian Basin over a distance of 300 km. On both sides of the fault zone, these successions were affected by two stages of folding (F1, F2) during Devonian to Early Carboniferous (Ellesmerian) deformation. No field evidence was found that the Harder Fjord Fault Zone was active prior to Ellesmerian folding. Early movements along the fault zone are indicated by post-Ellesmerian sedimentation of coarse red-beds (Depot Bugt conglomerate) which represent the oldest of the Wandel Sea Basin sediments. They were probably deposited in narrow, fault-controlled (?)Late Carboniferous basins similar to those described from Svalbard. During Late Cretaceous times, 500 m thick fluvial and marine clastic sediments were unconformably deposited over the folded Cambro-Ordovician units. Although no direct field evidence suggests that sedimentation was controlled by displacements along the Harder Fjord Fault Zone, the intrusion of Upper Cretaceous mafic sills and dykes indicates a phase of important crustal extension related to reactivation of the fault zone during this period of time. This stage was followed by post-late Santonian (Eurekan) N-S compression (D3) which affected the Franklinian Basin deposits, Wandel Sea Basin sediments and mafic intrusions. In general, it was concentrated along the Harder Fjord Fault Zone and probably caused the reactivation of pre-existing (?)Carboniferous and younger fault lines. The entire deformation and its timing are comparable with the Eurekan structures found at the Kap Cannon Thrust Zone in northernmost Greenland and are related to intracontinental compression prior to the separation of Svalbard from Greenland.

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Section: B Devonian To Early Carboniferous (Ellesmerian Deformation)mentioning

confidence: 50%

Section: Discussion and Synthesis Of Structural Evolution 4a Pre-dementioning

confidence: 94%

Section: E Late Cretaceousmentioning

confidence: 99%

Section: B Devonian To Early Carboniferous (Ellesmerian Deformation)mentioning

confidence: 99%

Section: B Devonian To Early Carboniferous (Ellesmerian Deformation)mentioning

confidence: 99%

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Polyphase deformation at the Harder Fjord Fault Zone (North Greenland)

Piepjohn

Gosen²

2001

Geol. Mag.

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Tectonic inversion in the Wandel Sea Basin: A new structural model of Kilen (eastern North Greenland)

2016

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The seminunatak Kilen in eastern North Greenland, with its complexly deformed Carboniferous‐Cretaceous strata, is a key area to understand the tectonic history of the transform plate boundary between eastern North Greenland and Svalbard. Detailed 3‐D geological mapping from oblique photogrammetry along with limited ground fieldwork and interpretation of previously published data forms the basis for a new structural model of Kilen. Previous structural models interpreted rhombic‐shaped fault patterns as the evidence for strike‐slip tectonics. These structures are here interpreted to be the result of a post‐Coniacian NE‐SW extension with NW‐SE trending normal faults followed by later, N‐S compression of presumable Paleocene‐Eocene age, folding the faults passively and suggesting the presence of a basal detachment. Furthermore, two thrust sheets have been distinguished on Kilen: a lower Kilen Thrust Sheet and an upper Hondal Elv Thrust Sheet separated by a subhorizontal fault: the Central Detachment. The style of deformation and the structures described are interpreted as the result of Paleocene‐Eocene N‐S directed compression resulting in basin inversion with strike‐slip faults only having minor status. This indicates that the Greenland margin as exposed on Kilen and the conjugate Svalbard margin in the West Spitsbergen fold‐and‐thrust belt are more similar than previously anticipated.

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