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Middle Jurassic–Early Cretaceous Rifting of the Danish Central Graben

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Middle Jurassic–Early Cretaceous Rifting of the Danish Central Graben Middle Jurassic – Early Cretaceous rifting of the Danish Central Graben Jens J. Møller and Erik S. Rasmussen During the Jurassic – Early Cretaceous, the Danish Central Graben developed as a N–S- to NNW– SSE-trending graben bounded by the Ringkøbing–Fyn High towards the east and the Mid North Sea High towards the west. The graben consists of a system of half-grabens and evolved by fault- controlled subsidence; three main rift pulses have been recognised. The first pulse ranged from the Callovian to the Early Oxfordian, the second pulse was initiated in the latest Late Kimmeridgian and lasted for most of the Early Volgian, and the third and final pulse occurred within the Ryazanian in the Early Cretaceous. The first pulse was characterised by subsidence along N–S-trending faults. The most pro- nounced fault-controlled subsidence occurred in the east, especially along N–S-striking segments of the boundary fault to the Ringkøbing–Fyn High. During this period, minor salt movements occurred with the development of salt pillows. The activity along the N–S-trending faults ceased during the Oxfordian. During the second pulse, in Early Volgian times, subsidence was concen- trated along new NNW–SSE-trending faults and the main depocentre shifted westward, being most marked within the Tail End Graben, the Arne–Elin Graben, and the Feda Graben. This tec- tonic event was accompanied by the accumulation of a relatively thick sediment load resulting in the development of salt diapirs, especially within the Salt Dome Province. The third tectonic pulse was essentially a reactivation of the NNW–SSE-trending structures and there is clear evi- dence of subsidence controlled by faulting and salt movements. Despite the overall extensional tectonic regime, local compressional tectonics resulted in thrusting. For instance, the Gert Ridge is interpreted to have formed by readjustment at the boundary fault between two subsiding blocks. The structural framework during graben evolution controlled, to some degree, the distribution of reservoir sandstones. Reservoir sandstones associated with periods of rotational tilt include Middle Jurassic deposits referred to the Bryne and Lulu Formations, and Upper Jurassic sandstones referred informally to the ‘Fife Sandstone Formation’. Sands deposited during tectonic relaxation are repre- sented by the Heno Formation and Upper Jurassic turbidites interbedded in the Farsund Formation. Sea-level changes were probably most important during periods of tectonic relaxation, particularly with respect to the deposition of lowstand sandstones in basinal areas. Keywords: North Sea, Danish Central Graben, Middle Jurassic – lowermost Cretaceous, 3D seismic data, struc- tural evolution, reservoir sandstone distribution Geological Survey of Denmark and Greenland, Geocenter Copenhagen, Øster Voldgade 10, DK-1350 Copenhagen K, Denmark. E-mail: [email protected] The structural development of the Danish part of the (1985), Møller (1986), Cartwright (1987), and Korstgård Central Graben during the Jurassic has previously been et al. (1993). The structural evolution of the Norwegian described by Andersen et al. (1982), Gowers & Sæbøe Central Trough (Graben) has been presented by Gowers Geological Survey of Denmark and Greenland Bulletin 1, 247–264 (2003) © GEUS, 2003 247 et al. (1993). These papers are based on interpretation cence prevailed during the Early Jurassic and a uniform of 2D multichannel seismic data acquired during the early succession of marine mudstones accumulated (Michelsen 1980s. Despite the relatively high quality of these data, 1978; Andsbjerg & Dybkjær 2003, this volume). Middle new information has come to light as a result of recently- Jurassic updoming of the Central Graben area (Ziegler acquired 3D seismic data and information from wells 1982) resulted in significant erosion of Triassic and Lower drilled in the late 1980s and in the early part of this Jurassic sediments. Following Middle Jurassic uplift, a decade. The purpose of this paper is to present our inter- stretching phase caused rapid fault-controlled subsidence, pretation of the evolution of the Danish Central Graben, particularly in the Tail End Graben area (Vejbæk 1992). on the basis of these new data. Furthermore, mapping This mainly Late Jurassic rifting ceased during the Early of oil and gas fields demonstrates a close link between Cretaceous and it has been proposed that subsequent the structural framework and the location of reservoir subsidence was controlled by a combination of thermal rocks, in this case, sandstones. Therefore, the influence relaxation and gabbro–eclogite phase transformation, the of the structural framework on the distribution of reser- latter process explaining the increased subsidence rate dur- voir sandstones is discussed. ing the Cenozoic (Vejbæk 1992). Kooi et al. (1991), on the other hand, suggested that increased compressional stresses within the North Sea region were the main cause of accelerated subsidence in the late Cenozoic. Geological framework Structural development The Danish Central Graben is a major east-dipping half- Structural elements graben system bounded towards the east by the Ring- The complex pattern of the Danish Central Graben has købing–Fyn High and towards the west by the Mid North made it necessary to name the most important struc- Sea High (Fig. 1). The half-graben consists of a series of tural elements (Fig. 1); the following usage is based on minor NW–SE-trending half-grabens mainly dipping east- Britze et al. (1995) and Japsen et al. (2003, this volume). wards. The graben formed between the Middle Jurassic Towards the east, the Danish Central Graben is bounded and the earliest Cretaceous by the interaction of base- by a segment of the Ringkøbing–Fyn High termed the ment faulting and mobilisation of Zechstein and Trias- East North Sea High. The eastern part of the graben is sic(?) salt (Gowers & Sæbøe 1985; Møller 1986; Cartwright subdivided into the Søgne Basin towards the north, the 1987; Korstgård et al. 1993). Locally, stretching factors Tail End Graben in the central part, and the Salt Dome have been calculated to be up to two (Vejbæk 1992). The Province and the Rosa Basin in the south. Minor ele- faulting and salt mobilisation resulted in a complex con- ments such as the Poul Plateau constitute the transition figuration of highs and graben features, the most distinct between the main boundary fault and the graben itself. of which have been named (Andersen et al. 1982; Møller Towards the west, the Tail End Graben passes into the 1986; Vejbæk 1986; Japsen et al. 2003, this volume). Heno Plateau. In the northern part of the graben, a Tectonic movements in the Central Graben area have more complex development occurred involving the been recognised to have occurred as early as the Permian evolution of a series of grabens, the Arne–Elin, Gertrud (Ziegler 1975; Gowers & Sæbøe 1985); indeed, Rotliegen- and Feda Grabens. The Søgne Basin is separated from des strata in the Danish sector record rifting and associ- the Gertrud Graben by the Mandal High and the Piggvar ated volcanism although not restricted to the Central Terrace. The Mid North Sea High forms the eastern limit Graben area (Stemmerik et al. 2000). Zechstein deposits of the Danish Central Graben; at the transition this is are present in the northern and southern parts of the segmented into the Mads and Inge Highs. Danish Central Graben (e.g. the Søgne Basin and the Salt Dome Province) but are probably absent in the central part. There may have been a connection between the southern and northern Permian basins through the Tail Stratigraphic evolution of the End Graben during Zechstein times although evidence Danish Central Graben (e.g. salt structures) is lacking. Triassic sediments were more widespread and relatively thick Triassic deposits were Pre-Middle Jurassic probably laid down, as indicated by the U-1 well (Jacobsen The P-1 well located on the Mads High terminated in 1982) and discussed by Vejbæk (1992). Tectonic quies- Caledonian basement of greenschists. The oldest sedi- 248 Cleo-1 4°E Fig. 5 Reverse fault Mandal Piggvar TerraceHigh Normal fault Søgne Basin Fig. 13 Salt diapir Salt pillow Gert-4,-1,-3,-2 Gert Well Ridge Gertrud Graben Fault plane Ål Basin Jeppe-1 Feda Graben Gwen-2 Tail End Graben Ringkøbing–Fyn High Fig. 7 East North Sea High A Inge High r P-1 n e Fig. 4 Mid North – E li Sea High n 56°N G r Nora-1 a Heno b Tordenskjold-1 e Plateau n Coffee Soil Fault Outer Rough Ravn-1 Basin Ravn-2 N. Jens-1 Mads High Elly-1,-2 Poul Plateau Rosa Basin Salt Dome Province N Igor Basin N U-1 UK DK Fig. 3 NL G 20 km 500 km Fig. 1. Location map and structural elements of the Danish Central Graben. Wells referred to in the text are indicated, together with the location of the geosections in Figs 3–5 and the seismic lines in Figs 7, 13. Position of additional wells named on Figs 3–5 is also shown. National sectors of the North Sea: DK, Denmark; G, Germany; N, Norway; NL, the Netherlands; UK, United Kingdom. mentary deposits known in the Danish Central Graben lian deposits and sabkha sediments of the Rotliegendes are of Carboniferous age, as encountered in the P-1 Group (Jacobsen & Larsen 1982; Stemmerik et al. 2000). well (Michelsen 1982) and in the Gert-2 and Gert-3 Transgression of the northern and southern parts of the wells. Thick Carboniferous sections are known both Danish Central Graben in the Late Permian resulted in south and north of Danish territory (Michelsen 1982) the deposition of carbonates and evaporites referred to and the Carboniferous is believed to have been dis- the Zechstein Group. Triassic sedimentation occurred tributed over most of the area, but was probably eroded in basinal areas inherited from the Permian, but elevated during later tectonic events. The Lower Permian sec- areas were also periodically areas of deposition.
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