122 L. BARATOUX ET AL.recrystallized plagioclase in middle or deepcrustal metabasic rocks are rare <strong>and</strong> restrictedto rocks with very high plagioclase modal abundancessuch as anorthosites (Ji et al. 1988).However, as mentioned by other authors (e.g.Brodie & Rutter 1985), b<strong>and</strong>ed metabasic mylonitesare common, which is confirmed by thiswork. We show that plagioclase may easilyform interconnected weak layer networks inhornblende gabbros under upper amphibolitefacies conditions.Our micro<strong>structural</strong> study <strong>of</strong> an amphibolitefacies metagabbro (650 _+ 50 ~ shows thatthe load-bearing framework structure (H<strong>and</strong>y1990, 1994) is restricted to the lowest deformationintensities. The non-deformed metagabbroshows coarse-grained ophitic structure composed<strong>of</strong> r<strong>and</strong>omly distributed hornblende <strong>and</strong> plagioclase,where amphibole grains are only locallyin contact. With ongoing strain, the deformationis mostly concentrated in the plagioclase, whichis at the transient region between brittle <strong>and</strong>plastic behaviour, leading to development <strong>of</strong> afine-grained matrix (Tullis & Yund 1987).Amphibole grains showing high internal strain<strong>and</strong> local fracturing behave as rigid bodies surroundedby interconnected layers <strong>of</strong> plagioclasegrains. Such microstructures may be interpretedas an interconnected weak layer structure(IWL) with a high viscosity contrast betweenrigid clasts <strong>of</strong> amphibole <strong>and</strong> weaker, finegrainedplagioclase layers (H<strong>and</strong>y et al. 1999).In the amphibolite facies metagabbroic mylohires,the monomineralic hornblende layers areobserved, while plagioclase-rich layers showalmost perfect mixing with hornblende. Thegrain size <strong>of</strong> plagioclase <strong>and</strong> amphibole in theplagioclase-rich matrix areas is fairly similar,the latter showing slightly higher elongation. Thephase distribution <strong>of</strong> plagioclase-hornblendemixture, the absence <strong>of</strong> CPO in plagioclase,<strong>and</strong> its aspect ratio suggest that the dominantmechanism is granular flow (grain boundarysliding). Based on this interpretation, wesuggest that the phase mixing is probably amechanical process. The microstructures <strong>and</strong>CPO <strong>of</strong> amphibole forming monomineraliclayers indicate either dislocation creep or cataclasticflow. The absence <strong>of</strong> boudinage <strong>and</strong> progressivemixing <strong>of</strong> plagioclase <strong>and</strong> amphibolesuggest that the diffusion-dominated flowprocess operating in plagioclase aggregates ismechanically as efficient as dislocation or cataclasticflow in the hornblende layers. The finalstructure resembles the interconnected weaklayer structure with low viscosity contrast(H<strong>and</strong>y 1994). A switch in deformation mechanismfrom dislocation creep towards a grain sizesensitive process is thought to be responsiblefor the convergence <strong>of</strong> mechanical properties <strong>of</strong>amphibole <strong>and</strong> plagioclase in the mylonite,resulting in a drop <strong>of</strong> bulk rock strength(Etheridge & Wilkie 1979; Kirby 1985; Rutter &Brodie 1988).Two deformation stages were observed in theupper amphibolite facies (750 -t- 50 ~ metagabbros:(1) augen mylonite with locally preservedporphyroclasts <strong>of</strong> both plagioclase <strong>and</strong> hornblende;<strong>and</strong> (2) b<strong>and</strong>ed mylonites with completelyrecrystallized amphibole <strong>and</strong> plagioclase,each arranged in monomineralic layers. Theinitial stages <strong>of</strong> deformation are characterizedby tectonic grain size reduction <strong>of</strong> plagioclasewhile hornblendes represent strong objects floatingin the weak plagioclase matrix. The deformation<strong>of</strong> the metagabbro is interpreted to haveoccurred via dislocation creep accompanied bydiffusion mass transfer mechanisms, responsiblefor moderate mixing <strong>of</strong> plagioclase <strong>and</strong> amphibole.The b<strong>and</strong>ed fabric, only developed at highstrains, can be defined as an interconnectedweak layer structure with low viscosity contrast(H<strong>and</strong>y et al. 1999). The layered structureshows that the strengths <strong>of</strong> amphibole monornineralicaggregates <strong>and</strong> plagioclase-rich b<strong>and</strong>sare similar, suggesting convergence <strong>of</strong> rheologies<strong>of</strong> both minerals at high strains (Jordan1988; H<strong>and</strong>y 1994).In conclusion, amphibolite <strong>and</strong> upper amphibolitefacies metagabbroic mylonites are characterizedby layered low-viscosity IWL structures.This indicates that at high strains this b<strong>and</strong>edstructure in metagabbros forms a so-calledsteady-state foliation (Means 1990). Mechanicalmixing <strong>of</strong> phases is more important in lowertemperature (eastern belt) than in higher temperature(western belt) amphibolite facies mylonites.The bulk strength <strong>of</strong> amphibolite <strong>and</strong>upper amphibolite facies mylonitic metagabbrosis controlled by an equal contribution <strong>of</strong> bothrock-forming minerals showing contrasting butequally efficient deformation mechanisms.We are indebted to D. Mainprice for his help with theEBSD <strong>analyses</strong>. Fruitful discussions with F. Holub, D. J.Prior, H. Stiinitz <strong>and</strong> J. Wheeler are gratefully acknowledged.We thank P. T~)cov~, J. Haloda, P. Gr<strong>and</strong>jean <strong>and</strong>P. Capiez for the help with microprobe <strong>and</strong> bulk rock <strong>analyses</strong>.K. Brodie, H. Van Roermund <strong>and</strong> D. Gapais arethanked for thorough reviews, which improved significantlythe original manuscript. The project was fundedby grants <strong>of</strong> Czech National Grant Agency No. 42-201-204 to K.S. <strong>and</strong> 42-201-318 to P. Stipskfi, by Czech GeologicalService assignment No. 6327 to P. Mixa, <strong>and</strong> by aPhD financial support attributed by the French governmentto L.B.274
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On the relationshipbetween deformation <strong>and</strong> metamorphism, withspecial reference to the behavior <strong>of</strong> basic rocks. In:THOMPSON, A. B. & RUBIE, D. C. (eds) MetamorphicReactions; Kinetics, Textures, <strong>and</strong> Deformation.Springer-Verlag, New York, MY, UnitedStates, 138-179.CARVER, N. L. & TSENN, M. C. 1987. Flow properties<strong>of</strong> continental lithosphere. Tectonophysics, 136,27-63.CUMBEST, R. J., DRURY, M. R., VAN ROERMUND,H. L. M. & S1MPSON, C. 1989a. Dynamic recrystallization<strong>and</strong> chemical evolution <strong>of</strong> clinoamphibolefrom Senja, Norway. Contributions to Mineralogy<strong>and</strong> Petrology, 101, 339-349.CUMBEST, R. J., Van ROERMUND, H. L. M., DRURY,M. R. & SIMPSON, C 1989b. Burgers vector determinationin clinoamphibole by computer simulation.American Mineralogist, 74, 586-592.DALLAIN, C., SCHULMANN, K. & LEDRU, P. 1999.Textural evolution in the transition from subsolidusannealing to melting process, Velay Dome, FrenchMassif Central. Journal <strong>of</strong> Metamorphic Geology,17, 61-74.DOLLINGER, G. & BLACIC, J. D. 1975. Deformationmechanisms in experimentally <strong>and</strong> naturally deformedamphiboles. Earth <strong>and</strong> Planetary ScienceLetters, 26, 409-416.ETHERIDGE, M. A. & WILKIE, J. C. 1979. Grainsizereduction, grain boundary sliding <strong>and</strong> theflow strength <strong>of</strong> mylonites. Tectonophysics, 58,159-178.FITZ GERALD, J. D. & STI)NITZ, H. 1993. Deformation<strong>of</strong> granitoids at low metamorphic grade; I, Reactions<strong>and</strong> grain size reduction. Tectonophysics,221, 269-297.FLIERVOET, T. F., DRURY, M. R. & CHOPRA, P. N.1999. Crystallographic preferred orientations <strong>and</strong>misorientations in some olivine rocks deformedby diffusion or dislocation creep. Tectonophysics,303, 1-27.FREER, R. 1981. Diffusion in silicate minerals <strong>and</strong>glasses: a data digest <strong>and</strong> guide to the literature.Contributions to Mineralogy <strong>and</strong> Petrology, 76,440-454.GAPAIS, D. 1989. Shear structures within deformedgranites; mechanical <strong>and</strong> thermal indicators.Geology, 17, 1144-1147.HACKER, B. R. & CHRISTIE, J. M. 1990. Brittle/ductile<strong>and</strong> plastic/cataclastic transitions in experimentallydeformed <strong>and</strong> metamorphosed amphibolite.In: DUBA, A. G., DURHAM, W. B., HANDIN, J. W.& WANG HERBERT, F. (eds) The Brittle-DuctileTransition in Rocks. American GeophysicalUnion, Washington DC, Geophysical Monograph,56, 127-147.HANDY, M. R. 1990. The solid-state flow <strong>of</strong> polymineralicrocks. Journal <strong>of</strong> Geophysical Research,B, 95, 8647 - 8661.HANDY, M. R. 1994. Flow laws for rocks containingtwo non-linear viscous phases; a phenomenologicalapproach. Journal <strong>of</strong> Structural Geology, 16,287-301.HANDY, M. R_, WISSING, S. B. & STREIT, L. E. 1999.Frictional-viscous flow in mylonite with variedbimineralic composition <strong>and</strong> its effect on lithosphericstrength. Tectonophysics, 303, 175-191.HELMSTAEDT, H., ANDERSON, O. L. & GAVASCI, A. T.1972. Petr<strong>of</strong>abric studies <strong>of</strong> eclogite, Spinel-Websterite, <strong>and</strong> Spinel-Lherzolite xenoliths fromkimberlite-bearing breccia pipes in SoutheasternUtah <strong>and</strong> Northeastern Arizona. Journal <strong>of</strong>Geophysical Research, 77, 4350-4365.HILLERT, M. & PURDY, G. R. 1978. Chemicallyinduced grain boundary migration. Acta Metallica,26, 333-340.HOLLAND, T. J. B. & BLUNDY, J. 1994. Non-idealinteractions in calcic amphiboles <strong>and</strong> theirbearing on amphibole-plagioclase thermometry.Contributions to Mineralogy <strong>and</strong> Petrology, 116,433 -447.JENSEN, L. N. & STARKLY, J. 1985. Plagioclase micr<strong>of</strong>abricsin a ductile shear zone from the JotunNappe, Norway. Journal <strong>of</strong> Structural Geology,7, 527-539.J~SSELL, M. W., KOSTEN~:O, O. & JAMTVEIT, B. 2003.The preservation potential <strong>of</strong> microstructuresduring static grain growth. Journal <strong>of</strong> MetamorphicGeology, 21, 481-491.JI, S. & MAINPRICE, D. 1988. Natural deformationfabrics <strong>of</strong> plagioclase; implications for slip systems<strong>and</strong> seismic anisotropy. Tectonophysics,147, 145-163.JI, S. & MAINPRICE, D. 1990. Recrystallization <strong>and</strong>fabric development in plagioclase. Journal <strong>of</strong>Geology, 98, 65-79.JI, S., MAINPRICE, D. & BOUDIER, F. 1988. 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