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Post-Caledonian Tectonics Along the Billefjorden Fault Zone, Svalbard, and Implications for the Arctic Region

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Post-Caledonian Tectonics Along the Billefjorden Fault Zone, Svalbard, and Implications for the Arctic Region Post-Caledonian tectonics along the Billefjorden fault zone, Svalbard, and implications for the Arctic region G. M. MANBY School of Earth Sciences, University of Greenwich, Bigland Street, London El 2NG N LYBERIS 1 T */-tTTorir\r^ri I Université Paris VI, DPtde Geotectonique, 4 Place Jussieu, 75252 Paris Cedex 05 J. CHUKUWtCZ, J F. THIEDIG Geologisch-Palaeontologisches Institute und Museum, Universität Münster, Corrensstraße 24 ABSTRACT tensor calculations computed for fault plane In most reconstructions for the North At- populations with slickensides using the lantic region in late Paleozoic time, the Bille- The north-south Billefjorden fault zone of method described by Etchecopar and others fjorden fault zone is interpreted to have been northern Spitsbergen in the Svalbard archipel- (1981). The results of these analyses form the a major left-lateral transform (Harland and ago has been widely regarded as one of the basis of a new interpretation of the displace- others, 1974; Harland and Wright, 1979; Zieg- classic areas for transpressional tectonics. The ments along the Billefjorden fault zone and its ler, 1982, 1988). The Billefjorden fault zone fault zone coincides with a late Caledonian evolution and wider regional significance. became active in mid-Devonian time when shear zone and presently constitutes the east- Svalbard, which lies on the extreme north- the Ny Friesland block was transported some ern boundary of the main Devonian basin of west corner of the Eurasian Plate, separated 200 km northward by sinistral strike slip into northern Svalbard. Fold axial traces and from North Greenland along the De Geer its present location (Friend and Moody-Stu- thrust faults that developed in the Devonian to Fracture Zone (DGFZ, Fig. la) with the art, 1972; Harland and others, 1974). As Permo-Carboniferous rocks parallel the strike opening of North Atlantic and Arctic Ocean much as 1,000 km of left-lateral motion took of the fault zone. There is no evidence for the basins. Separation of the two blocks began in place on the Billefjorden fault zone in Late rotation of fold hinges, and nonaxial planar, late Paleocene time (56 Ma), and the forma- Devonian time, and the (Svalbardian) defor- transecting cleavages are lacking. Folds and tion of the West Spitsbergen fold belt to- mation of the post-Caledonian rocks along thrusts with similar geometries aifect the whole gether with the Eurekan structures of North the Billefjorden fault zone and across the De- 60-km-wide Devonian basin fill. These obser- Greenland and the Canadian Arctic islands vonian basin was caused by sinistral vations, together with analyses of fault and fold are attributed to this motion (for example, transpression accompanying this motion patterns, indicate (A) pre-Devonian (Cale- Harland and Horsfield, 1974). The Green- (Harland and Wright, 1979; Harland, 1985). donian) left-lateral ductile shearing; (B) Late land-Svalbard margin was also subjected to Folds with axial traces oblique to the Bille- Silurian-Early Devonian extension; (C) Late an earlier sequence of mid- to late Paleozoic fjorden fault zone are not found, however, Devonian-early Carboniferous inversion ac- (Caledonian and Ellesmerian, respec- and McWhae (1953) proposed that the fault companied by folding of Devonian sedimen- tively) orogenic events that appear to have zone was dominated by contraction followed tary rocks; (D) early Carboniferous extension developed diachronously following the by extension rather than strike-slip displace- followed by platform-wide subsidence into late closure of an earlier ocean (compare Har- ments. Fold axial traces and thrust faults af- Mesozoic time; (E) Late Cretaceous-Pa- land and Gayer, 1972; Christie, 1979). Sev- fecting the Devonian rocks along the north- leocene, east-west contraction, thrusting, and eral major north-south fault zones transect ern part of the fault zone are largely parallel folding; and (E) post-Paleocene east-west ex- Svalbard (Fig. lb), of which the Billefjor- to the main faults (Lamar and others, 1986). tension. The Late Devonian deformation along den fault zone is the most important be- Although Lamar and others (1986) did not the Billefjorden fault zone is compared with cause it has influenced the sedimentary present any detailed structural analysis to the Late Devonian to early Carboniferous and tectonic evolution of central Svalbard support their interpretation, they concluded Ellesmerian orogeny of the Canadian Arctic. since late Caledonian (Late Silurian-Early that the folds and thrusts were formed by re- The Late Devonian megashear model for the Devonian) time (Harland and others, gional east-west contraction rather than by tectonic evolution of the North Atlantic region 1974). The Billefjorden fault zone sepa- sinistral transpression. Paleomagnetic data, is not supported by the evidence from rates the Devonian basin of northern Spits- although somewhat equivocal, suggest that Svalbard. bergen from the high-grade Caledonian the Billefjorden fault zone has not experi- gneisses of the Hecla Hoek succession enced any significant strike slip since Devo- INTRODUCTION (Fig. lb) in Ny Friesland. Recent geophys- nian time (Torsvik and others, 1985). ical investigations have established, how- This paper presents the results of new ever, that Devonian red-bed sequences are GEOLOGIC SETTING mapping and structural analyses of data from also present in the offshore basins south- the Billefjorden fault zone in central Spitsber- east of Svalbard (Skilbrei and Eiken, 1992, The Billefjorden fault zone (BFZ) is best gen. Structural data are combined with stress personal commun.). exposed in central Spitsbergen between Geological Society of America Bulletin, v. 105, p. 201-216, 13 figs., February 1994. 201 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/106/2/201/3381963/i0016-7606-106-2-201.pdf by guest on 26 September 2021 MANBY AND OTHERS Present Day Oceanic crust Continental crust Figure la. Present-day tectonic setting of Svalbard. DGFZ = De Geer Fracture Zone; KR = Knipovich Ridge. Austfjord and Billefjord where it parallels the striking, sinistral shear zone, 20 km east of steep limb at a high angle. On the shallow main Caledonian tectonic grain (Fig. 2). In the Billefjord fault zone, separates the limb of the fold, the cleavage is concentrated this area, it also coincides with a wide zone of high-grade Lower Hecla Hoek rocks from along and parallel to the dikes, but the cleav- metamorphic retrogression and intense the weakly to unmetamorphosed Middle age is only weakly developed or is not obvi- shearing in the Hecla Hoek gneiss (base- Hecla Hoek succession. ous a few meters away from the dikes. The ment). We have recognized that the gneiss in The Devonian basin west of the Billefjord- dikes are more competent than the sedimen- the fault zone displays a range of ductile, en fault zone consists of 8-9 km of fluviatile tary rocks, and they appear to have acted as semi-brittle to brittle shear structures, all of red beds (Manby and Lyberis, 1992) depos- "stress risers," accumulating the strain to which are consistent with left-lateral dis- ited during the 410 Ma to 360 Ma interval. produce the cleavage; away from the dikes, placement. The extensive replacement of the Although the Devonian rocks are locally the shortening may have been dissipated Caledonian amphibolite facies by greenschist folded (Friend and Moody-Stuart, 1972, and along the less-competent siltstone and shale facies mineral assemblages within the shear Harland and others, 1974), the entire basin fill layers. These relations suggest that the short- zone suggests that the shearing followed the is affected by west-vergent, kilometric scale, ening responsible for the cleavage formation peak metamorphism possibly in Late Silurian north-south-trending, box-shaped or kink- and, therefore, a part of the folding affecting to Early Devonian time. like folds that plunge gently to the south the basin fill postdated the intrusion of the North of the Billefjord-Austfjord area, the (Manby and Lyberis, 1992). The Devonian dikes (Manby and Lyberis, 1992). Early Car- fault zone is projected to cross Wijdefjord rocks on the southwest shore of Wijdefjord boniferous coal-bearing deltaic and lacustrine near to the western coast of Ny Friesland are cut by mid-Carboniferous (309 ± 5 Ma) sediments (Horbyebreen Formation, Fig. 2) (Fig. lb). Here, the high-grade basement monchiquite dikes (Gayer and others, 1966), crop out in a zone centered on the Billefjord- rocks are strongly sheared and retrograded one of which parallels the bedding in the en fault zone (Harland and others, 1974). over a 2- to 3-km-wide zone close to the steep western limb of a large anticline; others Overlying these rocks and the basement onshore projection of the fault zone (Har- cut the bedding on the long, east-dipping, along and east of the fault zone is a sequence land and others, 1974; Manby, 1990). In shallow limb of the adjacent syncline 300- of fault-controlled, coarse sandstone and addition, the Sorgfjord shear zone 400 m to the west (Manby and Lyberis, 1992). conglomerate (Svenbreen Formation, Fig. 2) (Manby, 1990; Manby and Lyberis, 1992), A well-developed pressure solution cleavage followed by mid- to late Carboniferous a similar 2- to 3-km-wide, north-south- cuts the Devonian rocks and the dike on the evaporites, carbonate rocks, red beds, and 202 Geological Society of America Bulletin, February 1994 Downloaded from http://pubs.geoscienceworld.org/gsa/gsabulletin/article-pdf/106/2/201/3381963/i0016-7606-106-2-201.pdf
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