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The Emplacement of Peridotites and Associated Oceanic Rocks from the Lizard Complex, Southwest England.', Geological Magazine., 139 (1)

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The Emplacement of Peridotites and Associated Oceanic Rocks from the Lizard Complex, Southwest England.', Geological Magazine., 139 (1) Durham Research Online Deposited in DRO: 23 May 2008 Version of attached le: Published Version Peer-review status of attached le: Peer-reviewed Citation for published item: Cook, C. A. and Holdsworth, R. E. and Styles, M. T. (2002) 'The emplacement of peridotites and associated oceanic rocks from the Lizard Complex, southwest England.', Geological magazine., 139 (1). pp. 27-45. Further information on publisher's website: http://dx.doi.org/10.1017/S0016756801005933 Publisher's copyright statement: c Cambridge University Press 2002 Additional information: Use policy The full-text may be used and/or reproduced, and given to third parties in any format or medium, without prior permission or charge, for personal research or study, educational, or not-for-prot purposes provided that: • a full bibliographic reference is made to the original source • a link is made to the metadata record in DRO • the full-text is not changed in any way The full-text must not be sold in any format or medium without the formal permission of the copyright holders. Please consult the full DRO policy for further details. Durham University Library, Stockton Road, Durham DH1 3LY, United Kingdom Tel : +44 (0)191 334 3042 | Fax : +44 (0)191 334 2971 https://dro.dur.ac.uk Geol. Mag. 139 (1), 2002, pp. 27–45. © 2002 Cambridge University Press DOI: 10.1017/S0016756801005933 Printed in the United Kingdom 27 The emplacement of peridotites and associated oceanic rocks from the Lizard Complex, southwest England C. A. COOK*†, R. E. HOLDSWORTH*‡ & M. T. STYLES§ *Reactivation Research Group, Department of Geological Sciences, University of Durham, Durham DH1 3LE, UK §British Geological Survey, Keyworth, Nottingham NG12 5GG, UK (Received 5 March 2001; accepted 16 July 2001) Abstract – Upper mantle peridotites and associated oceanic rocks from the Lizard Complex, south- west England, preserve evidence for a multistage geological history. Steeply dipping pre-emplacement fabrics record high-temperature (900–1100 °C) shearing and exhumation of the mantle peridotites apparently formed during localized NE–SW rifting in a pull-apart basin setting (c. 400–390 Ma). Associated oceanic rocks (Landewednack amphibolites) preserve a pre-emplacement prograde brown amphibole-bearing metamorphic assemblage and steeply dipping fabric thought to have formed as the newly formed oceanic crust was juxtaposed with newly exhumed hot mantle peridotite during NE–SW rifting. In both the peridotites and Landewednack amphibolites, steep pre-emplacement structures are cross-cut by low-angle mylonitic fabrics thought to have formed during the initial phases of emplacement of mantle over crustal rocks in a partially intra-oceanic setting (c. 390–375 Ma). The fabrics in peridotites and amphibolites exhibit retrograde mineral assemblages (c. 500–800 °C), with the amphibolites preserving two superimposed assemblages, green amphibole + titanite and colourless magnesio-hornblende, respectively, that are thought to record progressive down-temperature deforma- tion during thrusting. Emplacement-related structures in both the basal peridotites and amphibolites consistently dip at low to moderate angles NW, with down-dip lineations and kinematic indicators showing consistent top-to-the-NW senses of shear. Syn-emplacement magmatism is recorded by intrusions of foliated Kennack Gneiss. Anastomosing serpentine-filled faults mark many existing low- angle contacts between the peridotites and Landewednack amphibolites and appear to represent the final, lowest-temperature (< 250 °C) stages of emplacement (c. 370 Ma). This study shows that ‘dynamothermal aureoles’ in ophiolites may preserve evidence for tectonothermal events that pre-date thrust emplacement. metamorphism and deformation during overthrusting 1. Introduction of hot lithospheric fragments either in an intra- Metamorphic soles have been described beneath ultra- oceanic setting (Church & Stevens, 1971; Williams & mafic rocks in orogenic peridotite massifs and ophio- Smyth, 1973; Searle & Malpas, 1980; Boudier, lite suites in many parts of the world (e.g. Williams & Ceuleneer & Nicolas, 1988; Cawood & Suhr, 1992; Smyth, 1973; Jamieson, 1980, 1986; Searle & Malpas, Fergusson & Cawood, 1995), or within orogenic belts 1980; Lippard, Shelton & Gass, 1986; Boudier, (e.g. Tubia, Cuevas & Gil Ibarguchi, 1997). The rela- Ceuleneer & Nicolas, 1988; Boudier et al. 1988). Such tively hot overriding ultramafic sheet is inferred to metamorphic soles are usually defined as thin zones of provide most of the heat necessary for the observed metamorphic rocks which show mylonitic fabrics, metamorphism in the cooler footwall rocks (Jamieson, polyphase deformation and an inverted sequence of 1980). In the better-preserved examples (e.g. Bay of metamorphic assemblages that decrease in grade from Islands Complex and Oman), mylonitic fabrics in the granulite–amphibolite facies immediately in contact metamorphic sole parallel those in the basal peridotite with overlying basal peridotites to greenschist facies at mylonites, and kinematic indicators show the same lower structural levels (Jamieson, 1980). In early inves- sense of shear (Boudier, Nicolas & Bouchez, 1982; tigations, the development of a metamorphic sole was Girardeau, 1982; Boudier et al. 1985; Boudier, interpreted to result from the thermal effect of associ- Ceuleneer & Nicolas, 1988; Cawood & Suhr, 1992; ated ultramafic rocks, which were regarded as hot Fergusson & Cawood, 1995). intrusions or diapirs (Green, 1964a; MacKenzie, The Lizard Complex has long been described as an 1960). Since the early 1970s, however, it has been ophiolite based on the intimate association of peri- shown that most metamorphic soles are related to dotites, gabbros and a mafic dyke complex (e.g. Thayer, 1969; Bromley, 1973). Geochemical studies have shown ‡ Author for correspondence: [email protected] that many of the mafic crustal rocks have compositions † Present address: Baker Atlas GeoScience, Baker Hughes, Kettock Lodge, Campus 2, Balgownie Drive, Bridge of Don, Aberdeen, typical of mid-ocean ridge basalts (MORB; e.g. Floyd, AB22 8GU Scotland, UK. Lees & Parker, 1976; Kirby, 1979). Previous studies 28 C. A . COOK, R . E . HOLDSWORTH & M . T. STYLES have proposed that the metamorphosed oceanic rocks Sill’: Flett, 1946; Green, 1964c; Sandeman et al. 1997; (known as the Landewednack amphibolites) underly- C. A. Cook, unpub. Ph.D. thesis, Univ. Durham, ing the Lizard Complex peridotites represent part of a 1999). This suggests that the volcano-sedimentary metamorphic sole formed due to peridotite emplace- rocks of the Old Lizard Head Series formed prior to c. ment, either as a diapir (Green, 1964a,b) or as a hot 499 Ma and that they may be broadly equivalent in age mantle thrust sheet during Variscan tectonics to the Man of War Gneiss. Whole-rock geochemical (Bromley, 1979; Styles & Kirby, 1980; Jones, 1997). data (Sandeman et al. 1997; Nutman et al. 2001) sug- This event was then followed by ‘cold’ emplacement of gest that these metamorphic basement rocks formed the Lizard Complex as a thrust sheet over the during a regional episode of late Cambrian to early Devonian continental margin rocks to the north, Ordovician mafic and felsic magmatism within an probably during earliest Carboniferous times (Barnes intracontinental or continental margin setting. The & Andrews, 1984). In this paper, the contacts between contact between the Old Lizard Head Series and the the Lizard peridotites and Landewednack amphibo- overlying Landewednack amphibolites is exposed at lites are re-examined in detail, together with shear Polbream Cove (Fig. 1) and has been interpreted to be zone fabrics and faults in the overlying peridotites and a thrust (Jones, 1997). underlying Landewednack amphibolites. Several The Devonian Gramscatho Group, which is phases of shearing are observed, each with distinct exposed to the north of the Lizard Complex (Fig. 1), is associated metamorphic mineral assemblages, sug- interpreted to be a flysch sequence (Holder & gesting that the emplacement of the Lizard Complex Leveridge, 1986) comprising cleaved units of mud- involved a progressive sequence of events (cf. Jones, stone with subordinate turbidite sandstones and silt- 1997; Vearncombe, 1980). stones. A unit of matrix-supported mélange up to 1500 m thick, the Meneage mélange, is assigned to the southernmost part of the Gramscatho Group and car- 2. Geological setting of the Lizard Complex ries clasts of mudstone, siltstone, sandstone, quartzite, The various components of the Devonian Lizard schist and igneous rocks. Some of these clasts are Complex collectively form the structurally highest, thought to be derived from erosion of the Lizard fault-bounded unit exposed in the late Palaeozoic Complex and associated Cambro-Ordovician meta- Variscan fold and thrust belt of mainland southwest morphic basement rocks as they were exposed in emer- England (Holder & Leveridge, 1986). To the south, gent thrust sheets prior to final emplacement (Holder the Lizard Complex structurally overlies Cambro- & Leveridge, 1986). Ordovician metamorphic basement rocks (c. 500 Ma) The Lizard Complex comprises three distinct whilst to the north, it overlies mid-Devonian, very groups of igneous rocks (Fig. 1; Flett & Hill, 1912; low-grade metasedimentary units of the Gramscatho Green, 1964c; Floyd, Exley & Styles, 1993): the mantle Group (Fig. 1). All units have been tectonically dis- units (Lizard peridotites: Cook, Holdsworth & Styles, rupted by top-to-the-NNW thrusts formed during the 1998; Cook et
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