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Reinterpretation of Finnmarkian Deformation on Western Sørøy, Northern Norway: a Comment

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Reinterpretation of Finnmarkian Deformation on Western Sørøy, Northern Norway: a Comment Discussion Reinterpretation of Finnmarkian deformation on western Sørøy, northern Norway: a comment BRIAN A. STURT & DONALD M. RAMSA Y Sturt, B. A. & Ramsay, D. M.: Reinterpretation of Finnmarkian deformation on western Sørøy, northern Norway: a comment. Norsk Geologisk Tidsskrift, Vol. 68, pp. 213--219. Oslo 1988. ISSN 0029-196X. The postulate by Krill and Zwaan (1987) that the magmatic rocks of the Seiland Province are uniquely pre-orogenic based on dyke relationships on Western Sørøy is rejected, as also are the stratigraphic implications made by those authors from that area. 8. A. Sturt, Norges geologiske undersøkelse, Postboks 3006, 7002 Trondheim, Norway; D. M. Ramsay, Department of Geology, University of Dundee, Dundee, Scotland, U.K. We have read with interest but with a strong consistent sense of younging from the Klub­ measure of bewilderment the contribution by ben Group through a transition zone into Krill & Zwaan (1987) to this journal concerning the micaschists of the Storelv Group per se. the relationships between stratigraphy, tectonic Other such transitions are well marked, e.g. structures, dykes and possibly plutons on Sørøy, at Storelv (Ramsay & Sturt 1963) and in the western Finnmark. Langstrand area (Roberts 1968a). At many The basis of their argument is as follows: places along this contact, however, the strains (i) The described stratigraphy of Sørøy is not a may be higher and sedimentary structures are continuous sequence as considered by difficult to tind, although the characteristic Roberts (1968a), Ramsay (1971), lithologies of the transition zone can be Speedyman (1972, 1983), Sturt et al. (1978). unequivocally identified in most cases. (ii) The contact between the Storelv and Fal­ (ii) Dyke and fold relationships on W. Sørøy · kenes Groups is also transitional in nature, show unequivocally that the dykes are pre- and generally the lithological sequence is fold and hence pre-tectonic. comparable in different areas. Sedimentary (iii) Folds preserved in contact aureoles have a structures, however, are only sporadically unique fiow-fold mechanism in their pro­ preserved, owing to the nature of the original duction. lithologies and orogenic strains. This leads Krill & Zwaan (op. cit.) to the con­ (iii) The contact between the Falkenes Group and clusion that the igneous rocks of the Seiland Prov­ the Aafjord Group is again transitional in ince are uniquely of pre-tectonic emplacement. nature and similar sequences are preserved This view we refute for the following reasons: in different areas, while the lithologies rarely preserve any sedimentary structures. (i) The stratigraphy of Sørøy is in our view well (iv) The contact between the rocks of the Aafjord established, and a clearly marked sedi­ and Hellefjord Groups is somewhat more mentary transition can be seen between the abrupt over much of the area, though as Klubben and Storelv Groups on the road Roberts (1968a, 1968b) shows there is a clear section, 2 km east of Sørvær, and in innumer­ transition between those groups in the Lang­ able other localities along the extent of this strand-Finfjord area. Locally abundant boundary. In the Sørvær ro ad section the sediment structures in the HG consistently transition is perfectly exposed both at road young away from the Aafjord Group. leve! and on the coast. This particular section is characterized by low strains and, as a result, We thus see no compelling reason or evidence to sedimentary structures, especially current suspect that there is any major stratigraphic or bedding, abound. These structures show a tectonic break within this sequence. A similar 214 B. A. Sturt & D. M. Ramsay NORSK GEOLOGISK TIDSSKRIFT 68 (1988) b Fig. la. Basic dyke cutting asymmetrical second generation F,-folds. Note folded and boudined earlier basic sheet in centre-right of photo (ED 460203). b. Basic dykes cutting asymmetrical F2-folds. Note chilled margin to the thicker dyke (ED 454276). c. Thin basic dyke cutting F2-folds. The light­ coloured hands dose to hammer-handle are folded granitic sheets (ED 462278). d. Basic dyke cutting strongly attenuated and folded (F2) banding. Note the pre-dyke deformed pegmatite (ED 460203). lithostratigraphic succession has been observed in Speedyman (1968, 1972, 1983) demonstrated how several nappes in the Kalak Nappe Complex the various gabbros, diorites and nepheline syen­ across a wide areal extent of Finnmark and N. ite pegmatites intrude through the entire Sørøy Troms (Ramsay et al. 1985). stratigraphic sequence from the Klubben through In their note, Krill & Zwaan (op. cit. , p. 16) to the Hellefjord Group. The contact relations of east doubts upon the relationships between the the Husfjord Plutonic Complex are well marked major plutons and the Sørøy stratigraphy and and in places well exposed and there can be no advance the view that 'the Falkenes Marble is doubt conceming the intrusive nature through its too young to have undergone Finnmarkian stratigraphically almost complete sidewall. This deformation or to have been intruded by rocks of complex is replete with xenoliths and rafts derived the Seiland Province'. This we must treat as a from the metasedimentary carapace. These 'view' not based on critical assessment of evidence clearly demonstrate the imprint of contact meta­ available in the literature or from Field morphism and are now well-developed hom­ observations. In the Husfjord area (S. Sørøy) felses. It is also clear that these contact meta- NORSK GEOLOGISK TIDSSKRIFT 68 (1988) Discussion - comment 215 c d morphic effects were superimposed upon at !east section from Donnesfjord to Kipperfjord simila1 one phase of penetrative folding/foliation. Simi­ materials derived fromthe Klubben, Storelv, Fal­ Iar features can be se en in other plutons on Sørøy. kenes and Aafjord Groups (Bjærknes 1975; Hol­ The Hasvik gabbro, for example, in its upper land & Sturt 1970). Similarly, basic dykes/sheets portion (Robins & Gardner 1975) contains abun­ may be observed at all levels of the stratigraphy, dant inclusions of previously deformed, now although, depending on the host-lithology, they hornfelsed, material derived from the psammites, may have undergone deformation and meta­ semipelites and quartzites of the Klubben Group, morphism which render them superficially dif­ which can be matched with xenolithic matenals in ficult to identify. the Breivikbotn Gabbro (Sturt & Ramsay 1965). The Storelv Gabbro, in the Burfjord area, con­ (ii) With regard to the relationships between tains abundant xenoliths/rafts of previously basic dykes and sidewall tectonic elements, deformed rocks derived from the Klubben and which is the basic theme of Krill & Zwaan's Storelv Groups (Sturt & Taylor 1971) and in the (op. cit.) thesis, we consider that their con- 216 B. A. Sturt & D. M. Ramsay NORSK GEOLOGISK TIDSSKRIFT 68 (1988) clusions are simply wrong. In establishing obvious in portions which are dyke-free. unequivocal relationships between dyke and (g) The preservation of current bedding in sidewall structure it is necessary to establish metamorphic rock systems does not the nature of the structural state of the host imply an absence of penetrative rock. This we consider has not been done deformation, but rather that the strains in the case in question. Where dykes do in metamorphic rock sequences defor­ predate folds, as reported by Krill & Zwaan, med at middle crustal levels are notably it is important to establish the age of these inhomogeneous. folds. We have recently had the opportunity (h) Dykes, now in amphibolite facies, but to re-examine the sections described by Krill with well-preserved igneous form & Zwaan and would make the following including chilled margins, cut older bla­ observations: stomylonitic fabrics (Fig. 2). (a) The folds which they describe as post­ datir.g dyke emplacement are in fact The features and relationships outlined above are second-generation (F2) structures, and incompatible with the model of Krill & Zwaan congruous with large-scale F2 folds in (op. cit.). the region. (b) They fold a previous near bedding foli­ (iii) Many of the best preserved dykes in western ation (Sl) and the axial plane cleavage Sørøy occur within the contact metamorphic is always a crenulation cleavage (S2). aureoles to the Breivikbotn and Hasvik gab­ The sole cleavage observed in the dykes bros and smaller plutons. This is closely is generally margin-parallel and essen­ related to the more competent nature of tially parallel to the axial planes of the hornfelses and their ability to propagate F2 folds, i. e. Sl dyke = S2 meta­ joints over long distances during the regional sediment. The near bedding nature of deformation and intrusion hydrofracturing Sl is a regional feature related to the attending magma injection. This is the case recumbent large-scale folds and Sl is for dykes which are either syn-genetic with a only observed as a markedly oblique major pluton or intruded subsequently. structure in the hinges of Fl folds. Dykes and inclined sheets of basic rock, (c) The folds figured, by Krill & Zwaan, 'granite' and pegmatite are spectacular fea­ also fold the S0/S1 intersection lineation tures intruding the contact metamorphic and in some cases a stretching lineation rocks around the Breivikbotn and Hasvik consisting of elongated retrograded sil­ gabbros. Primary features such as chilled limanite pods. margins, horns, matching marginal irregu­ (d) Many basic dykes are markedly oblique larities and other indications of dilation and to the axial planes of F2 folds and other xenoliths are generally well preserved, and dykes with variable orientation may many of the dykes show low effects of tec­ trend up to 90° in the axes of such folds. tonic strains, particularly in the inner parts of (e) Fl folds the well-developed Sl axial the aureoles (Fig. 3). Further out, however, plane cleavage are transected by dykes, they demonstrate an increasing degree of and a number of these are in turn folded tectonic strain. These dykes and sheets cut by F2 fold structures (Figs. la, b, c, d).
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