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The Northern Bergen Are Shear Zone an Oblique-Lateral Ramp in the Devonian Extensional Detachment System of Western Norway

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The Northern Bergen Are Shear Zone an Oblique-Lateral Ramp in the Devonian Extensional Detachment System of Western Norway The northern Bergen Are Shear Zone an oblique-lateral ramp In the Devonian extensional detachment system of western Norway OLE PETTER WENNBERG, ALAN GEOFFREY MILNES & INGER WINSVOLD Wennberg, O. P., Milnes, A. G. & Winsvold, I. The northern Bergen Are Shear Zone - an oblique-lateral ramp in the Devonian extensional detaehment system of western Norway. Norsk Geologisk Tidsskrift, Vol. 78, pp. 169-184. Oslo 1998. ISSN 0029-196X. ISSN 0029-196X. Structural investigations in the northern part of the Bergen area (western Norway) have been earried out on the major, 2-3 km-thiek, late/post-Caledonian, extensional Bergen Are Shear Zone. This shear zone dips steeply SW with a ehange in strike from 115-120° in the northeast to 150-160° in the southwest, over a distance of 50 km. The footwall eonsists of the autochthonous Western Gneiss Complex and the lowermost Caledonian Nappes. The hanging wall eonsists of strueturally higher Caledonian Nappes uneonformably overlain by eoarse Devonian eonglomerates. The orientation of the mylonitic foliation within the shear zone, in addition to several types of shear-sense indieators, predominantly indieate a dextral shear component. The related stretehing lineation pl unges about 20° W to NW, implying a significant eomponent of normal slip, as indieated by the regional geology. The minimum displacement on the Bergen Are Shear Zone is approximately 16 km, with a normal dip slip eomponent of 8 km, and a dextral strike slip eomponent of 14 km. The Bergen Are Shear Zone post-dates all Caledonian eontraetional deformation in its vieinity. We suggest that the Bergen Are Shear Zone represents a braneh of the Nordfjord-Sogn Detaehment Zone, the main Devonian detaehment, developed as an oblique-lateral ramp. O. P. Wennberg,• A. G. Mi/nes & l. Winsvold, Geologisk Institutt, Universitet i Bergen, A/legt 41, 5007 Bergen, Norway. • Z & S Geologi ajs. Sverdrupsgate 23, N-4007 Stavanger, Norway. & Introduction 1988; Seranne et al. 1991; Fossen 1992; Wennberg Milnes 1994). The Nordfjord-Sogn Detachment Zone The Bergen Are Shear Zone (BASZ, Fig. l) has been (NSDZ, Fig. l) and BASZ cut through, on a regional suggested to represent the southward continuation of the scale, the Caledonian Nappe pile, which was formed well-known large-scale (displacement �50 km), Devo­ during the final collisional event of the Caledonian nian, extensional detachment system in western Norway Orogeny (the Scandian phase), which ended in early - the Nordfjord-Sogn Detachment Zone (Milnes et al. Devonian times (ca. 395 Ma; Milnes et al. 1997). The Fig. l. Tectonie overview map of SW Norway. Abbreviations: BASZ =Bergen Are Shear Zone; NSDZ =Nordfjord-Sogn Detaehment Zone; HFSD = Hardangerfjord Shear Zone; LGF = Lærdal-Gjende R�f�:..WiJDevonian sediments 1iiiiJC aledonian allochthon Fault; WGC =Western Gneiss Complex. Modified l iiii from Sigmond et al. (1984), Milnes et al. (1997) and Autochthon/Parautochthon ....&....o.L� Late-/post-Caledonian shear zone Wennberg (1996). 1::::::::::J 170 O. P. Wennberg et al. 78 (1998) NORSK GEOLOGISK TIDSSKR!Ff wsw ENE km � Fig. 4b: � � � � � � � � � � � � � � � � � � � � � � � � � � � � � � , , , , , , J'' '''''' ''' '''' '''''''' '''' ''''''' '''''''' 5krn ,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,,' ,,,,,,,,,,, ,,, , ,,,,,, ,,, ,,,,,, ,,,,, , ,,,, ,, ,,,,,, , ,,, , , , ,,,,,,,,, , , ,,,,,,,,,,,,,,,, ,,,,,,,,,,,,, lO km , , , , HANGING WALL FOOTWALL BASZ BASZ BASZ E2] Devonlan deposlts ---------------- �---------------- Fig. 2. Profile aeross the northem Bergen Are Shear Zone showing the main teetonie units. Line of profile is indieated in Fig. l. MaBA = Major Bergen Are zone; MiBA = Minor Bergen Are zone. downthrown hanging wall of the NSDZ, to the west, lochthons consist of nappe complexes derived from the mainly exposes upper units of the nappe pile (Upper ancient continent Baltica (west of the present Au­ Allochthon), characterized by ophiolites derived from the tochthonjParautochthon), whereas the overlying nappes Iapetus ocean, and forming the basement to post-oro­ of the Upper Allochthon contain units with oceanic genic Devonian clastic sequences (Norton 1987; Seranne affinities derived from the Caledonian ocean, Iapetus. & Seguret 1987; Andersen et al. 1990). The NSDZ These tectonostratigraphic units can be identified both footwall, in contrast, mainly exposes deep parts of the within the BASZ and in its footwall and hanging wall orogenic root-poly-deformed high-grade gneisses repre­ (Fig. 2), and provide a framework for the structural senting the westward continuation of the Baltic Shield analysis. (Milnes et al. 1997 and references therein). The shear zone follows Fensfjorden and is well ex­ From its regional setting and from an early reconnais­ posed for structural analysis in two areas, at Byrknes<!>y sance study (Wennberg & Milnes 1994), the steeply in the northwest, and along Osterfjord in the southeast SW-dipping northern BASZ was known to have a large (Fig. 3). Most of the structural data comes from these dextral strike-slip component and a smaller normal com­ areas, and have been summarized in two profiles, A-A' ponent of movement. Within this tectonic framework, we in the northwest and B-B' in the southeast (Fig. 4). focus on the structural relationships within the northern Profile A-A' exposes the lower part of the BASZ, and part of the BASZ, and their regional implications. profile B-B' represents an almost complete traverse through the shear zone with > 90% exposure. Details from A-A' are presented by Winsvold (1996), and from B-B' will be presented elsewhere (Wennberg & Milnes in Main rock units prep.; Wennberg et al. in prep.). In addition, more regional work has been carried out along the northern In southwestern Norway, the Caledonides consist of a segment of the BASZ. sequence of tectonostratigraphic units, which from the lowest to highest levels have been designated Au­ tochthonjParautochthon, Lower Allochthon, Middle Al­ Footwall lochthon and Upper Allochthon (Roberts & Gee 19 85). The AutochthonjParautochthon consists of Precambrian The AutochthonjParautochthon in the footwall of the basement rocks of the Baltic Shield, in addition to BASZ (Fig. 2) is represented by the Western Gneiss Paleozoic cover sediments preserved locally above a Complex (WGC). North of the investigated area, along stratigraphic unconformity. The Lower and Middle Al- Sognefjorden, Precambrian intrusive and metamorphic 78 (1998) Bergen Are Shear Zone, western Norway 171 NORSK GEOLOGISK TIDSSKRIFT Plunge of lineation 0-5° - 5-15° � - 15-25° 25-35° ._, >35° ._... 10km LEGEND liiillI l Devonian conglomerates c:=J Lindås. Complex Major Bergen Are - Kvalsida Gneiss zone X:X:•: Western Gneiss Region + + Ø l + + l ygarden Gneiss Complex --- Bjørillen syntorm ----- Base Devonian unconform ity ...L- ....&.. Basal thrust zone of the Caledonian allochthon Fig. 3. Tectonic map of northern segment of the BASZ. Arrows represent trend of stretching lineation (from Bøe 1978 and Henriksen 1979, in addition to own data). A1ong most of its 1ength, the northern BASZ is under water. It is best exposed to the northwest (profile A-A'; see Fig. 4A) and to the southeast (profi1e B-B'; see Fig. 48). relations are preserved in the east, and these are increas­ lineation under amphibolite facies conditions (Milnes et ing1y reworked and overprinted westwards by Ca1edo­ al. 1988; Andersen & Jamtveit 1990). nian po1yphase deformation and high-grade meta­ South of Sognefjord (Fig. 1), the WGC forms the morphism (Milnes et al. 1988). The earliest of these footwall of the BASZ and is composed of granitic, phases is marked by the formation of eclogites which migmatitic and banded gneisses with local quartzites and give Sm/Nd ages in the range of 407-425 Ma (e.g. amphibolites. The gneisses are commonly intruded by Griffin & Bruekner 1985; Mørk & Mearns 1986; Jamtveit granitic and pegmatitic veins, which are correlated with et al. 1991). Exhumation of the eclogite-bearing WGC the youngest Precambrian intrusive activity in the Sogne­ was accompanied by deformation and metamorphism fjorden and Eksingedalen areas (isotopic intrusion ages related to three processes: ductile flow in the lower crust, of 900-1000 Ma; Gray 1978; Milnes et al. 1988). The localized extensional faulting (e.g. along the Nordfjord degree of Caledonian deformation (i.e. ductile deforma­ Sogn Detachment Zone, NSDZ), and erosion (e.g. An­ tion which post-dates the veins and pre-dates the BASZ) dersen & Jamtveit 1990; Osmundsen & Andersen 1994; decreases southeastward in the footwall exposing increas­ Milnes et al. 1997). The first part of the decompression ingly higher levels. The deformation is characterized by of the high pressure rocks was associated with a slight the development of a foliation and a prominent stretch­ increase in temperature (Jamtveit 1987; Chauvet et al. ing lineation (Fig. 3). At A-A', a pervasive Caledonian 1992), and the development of a pervasive foliation and foliation is developed, and towards the southeast 172 O. P. Wennberg et al. 78 (1998) Homogeneous NORSK GEOLOGISKMigmatites TIDSSKRIFT and banded granite foliated gneisses cut by\ Banded gneisses Massive Banded gneisses Eclogite pegmatitic dyke CS-mylonites with deformed with deformed No data and mylonites pegmatites pegmatit(!s / l x � � � X X X X X X Zone of new folalion and Zone of reorientation Caledonian foliation Precambrian foliation stretching lineation of Galedonian folialion and stretching lineation Caledonian stretching lineation Fensfjord Earlier fabric obliterated and stretching Anastomosing
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