294 K. SCHULMANN ET AL.at 330–325 Ma <strong>and</strong> was associated with exhumation <strong>of</strong>HP metamorphic rocks to the surface, as demonstratedby sedimentation <strong>of</strong> granulite pebbles <strong>and</strong> metamorphicmuscovite in the forel<strong>and</strong> basin. The earlier agesclustering around 340 Ma correspond to D 2 event, i.e.to the vertical material transfer associated with crustalscalefolding, evidence <strong>of</strong> which is partially preservedin flat-lying migmatites.The structure <strong>of</strong> the Moldanubian domain is consistentwith the Ôstage 3Õ <strong>of</strong> the channel-flow model – thehot fold nappe (Beaumont et al., 2006; Culshaw et al.,2006). In these channel-flow models, stage 3 coincideswith the arrival <strong>of</strong> a lower crustal block that forces weakmiddle <strong>and</strong> lower crust into large-scale gently inclinedfold nappes rooted in the thickened Moho.The hot fold nappe model can be applied to theMoldanubian root system, keeping in mind that themodel represents the result <strong>of</strong> a continuous 2D historywhereas the Moldanubian root system comprises anexhumation history in two stages that are kinematicallyindependent. Nevertheless, the hot fold nappemodel simulates well the relatively weakly deformedNE part <strong>of</strong> the Moldanubian system with well-preservedD 2 fabric, which reaches shallow crustal levels<strong>and</strong> ultimately the surface (Figs 8 & 11). To the south,the extruded nappes were derived from more internal<strong>and</strong> hotter parts <strong>of</strong> the orogen. Increasingly largevolumes <strong>of</strong> weak lower crust were gradually transportedsouthwards over the Brunia continent leadingto an increase in the amount <strong>of</strong> lower crustal materialat the surface.The channel flow is heterogeneous, as predicted byBeaumont et al. (2001, 2006), because <strong>of</strong> the previoushistory, which generates important crustal strengthvariations. The implication <strong>of</strong> this model is that theheterogeneous crust makes the geometry <strong>and</strong> composition<strong>of</strong> the channel flow similarly heterogeneous. Inthe Moldanubian case, the channel transportsdetached blocks <strong>and</strong> boudins <strong>of</strong> distinctly differentcompositions such as HP granulites <strong>and</strong> mid-crustalsegments that still preserve relicts <strong>of</strong> the D 2 fabric. Inthis southern part <strong>of</strong> the channel all isotopic systemsare re-equilibrated <strong>and</strong> the cooling ages are younger incomparison with the non-uniformly reset isotopicsystems in the north.CONCLUSIONSThis study has shown that exhumation <strong>of</strong> the orogeniclower crust in the eastern sector <strong>of</strong> the Variscan orogenicbelt is characterized by two independent stages.(1) The first stage is best preserved in the Lugi<strong>and</strong>omain, where it is characterized by an intra-crustalfolding that is responsible for vertical material transferassociated with exhumation <strong>of</strong> the deep orogenic lowercrust to shallower crustal levels corresponding topressures around 10 kbar at about 350 to 340 Ma. Thefolding <strong>and</strong> vertical extrusion events are followed by avertical shortening leading to development <strong>of</strong> subhorizontalfabrics at medium to low pressures. Theearly horizontal shortening was probably triggered bythe existence <strong>of</strong> a rigid Ordovician block, part <strong>of</strong> whichis preserved at the eastern boundary <strong>of</strong> the Lugi<strong>and</strong>omain. We suggest that this early exhumation eventwas related kinematically to Saxothuringian continentalsubduction to the east, creating a convergentcontinental accretionary wedge – the Lugian domain.Mechanical interactions with the large Brunia continentduring the exhumation process remain unconstrained.(2) The Moldanubian domain has steep fabrics insimilar orientations to those preserved in the Lugi<strong>and</strong>omain. Vertical material transfer during the LowerCarboniferous led to the development <strong>of</strong> alternations<strong>of</strong> steeply inclined domains <strong>of</strong> lower <strong>and</strong> middle orogeniccrust, similar to Lugian domain. However, thistectonic event was followed by a NNE-directed subhorizontalshearing at about 330–325 Ma resultingfrom subsurface indentation by the Brunia continentalpromontory into the Moldanubian domain. The arrival<strong>of</strong> the Brunia continent is responsible for the progressiveemplacement <strong>of</strong> hot fold nappes <strong>and</strong>heterogeneous channel flow in the rear (western) part<strong>of</strong> the system generating mixtures <strong>of</strong> middle <strong>and</strong> lowercrustal units with preserved early exhumation fabrics.ACKNOWLEDGEMENTSThis study was made possible thanks to the ANRproject ÔLFO in orogensÕ funding as well as to financialsupport <strong>of</strong> CNRS (UMRs 7516 <strong>and</strong> 7517) <strong>and</strong> theCzech Science Foundation (GACR 205 ⁄ 05 ⁄ 2187 <strong>and</strong>GACR 205 ⁄ 04 ⁄ 2065). Ondrej Lexa is indebted to theUniversite´ Louis Pasteur for covering his salary. Weare grateful to J. Platt, D. Grujic <strong>and</strong> an anonymousreviewer for constructive reviews. The editorial work<strong>of</strong> M. Brown is highly appreciated.REFERENCESAllem<strong>and</strong>, P. & Lardeaux, J. M., 1997. Strain partitioning <strong>and</strong>metamorphism in a deformable orogenic wedge: Applicationto the Alpine belt. Tectonophysics, 280, 157–169.Andersen, T. B., Jamtveit, B., Dewey, J. F. & Swensson, E.,1991. Subduction <strong>and</strong> eduction <strong>of</strong> continental crust: majormechanisms during continent–continent collision <strong>and</strong>orogenic extensional collapse, a model based on the southNorwegian Caledonides. Terra Nova, 3, 303–310.Baratoux, L., Schulmann, K., Ulrich, S. & Lexa, O., 2005.Contrasting microstructures <strong>and</strong> deformation mechanisms inmetagabbro mylonites contemporaneously deformed underdifferent temperatures (c. 650 °C <strong>and</strong> c. 750 °C). In: DeformationMechanisms, Rheology <strong>and</strong> Tectonics: From Minerals tothe Lithosphere, Special Publication 243 (eds Gapais, D., Brun,J.-P. & Cobbold, P. R.), pp. 97–125. Geological Society,London.Beard, B. L., Medaris, L. G., Johnson, C. M., Brueckner, H. K.&Mı´ sarˇ, Z., 1992. Petrogenesis <strong>of</strong> Variscan high-temperaturegroup–A eclogites from the Moldanubian zone <strong>of</strong> the BohemianMassif, Czechoslovakia. Contributions to Mineralogy <strong>and</strong>Petrology, 111, 468–483.Ó 2007 Blackwell Publishing Ltd154
EXHUMATION IN LARGE HOT OROGEN 295Beaumont, C., Jamieson, R. A., Nguyen, M. H. & Lee, B., 2001.Himalayan tectonics explained by extrusion <strong>of</strong> a low-viscositycrustal channel coupled to focused surface denudation.Nature, 414, 738–742.Beaumont, C., Nguyen, M. H., Jamieson, R. A. & Ellis, S., 2006.Crustal flow modes in large hot orogens. In: Channel Flow,Ductile Extrusion <strong>and</strong> Exhumation in Continental CollisionZones, Special Publication 268 (eds Law, R. D., Searle, M. P.& Godin, L.), pp. 91–145. Geological Society, London.Bro¨ cker, M. & Klemd, R., 1996. Ultrahigh-pressure metamorphismin the Snieznik Mountains (Sudetes, Pol<strong>and</strong>): P–Tconstraints <strong>and</strong> geological implications. Journal <strong>of</strong> Geology,104, 417–433.Brueckner, H. K., Medaris, L.G. & Bakun-Czubarow, N., 1991.Nd–Sm age <strong>and</strong> isotope patterns from Variscan eclogites <strong>of</strong>the eastern Bohemian Massif. Neues Jahrbuch fu¨r MineralogieAbh<strong>and</strong>lungen, 163, 169–196.Burg, J.-P., 1999. Ductile structures <strong>and</strong> instabilities: theirimplication for Variscan tectonics in the Ardennes. Tectonophysics,309, 1–25.Burg, J.-P. & Podladchikov, Y., 1999. Lithospheric scale folding:<strong>numerical</strong> <strong>modelling</strong> <strong>and</strong> application to the Himalayan syntaxes.International Journal <strong>of</strong> Earth Sciences, 88, 190–200.Burg, J. P., Davy, P., Nievergelt, P. et al., 1997. Exhumationduring crustal folding in the Namche-Barwa syntaxis. TerraNova, 9, 53–56.Carswell, D. A. & O¢Brien, P. J., 1993. Thermobarometry <strong>and</strong>geotectonic significance <strong>of</strong> high-pressure granulites: examplesfrom the Moldanubian Zone <strong>of</strong> the Bohemian Massif inLower Austria. Journal <strong>of</strong> Petrology, 34, 427–459.Chemenda, A. I., Mattauer, M., Malavieille, J. & Bokun, A. N.,1995. A mechanism for syn-collisional rock exhumation <strong>and</strong>associated normal faulting: results from physical <strong>modelling</strong>.Earth & Planetary Science Letters, 132, 225–232.Culshaw, N.G., Beaumont, C. & Jamieson, R.A., 2006. Theorogenic superstructure–infrastructure concept: revisited,quantified, <strong>and</strong> revived. Geology, 34, 733–736. doi:10.1130/G22793.1.Dallmeyer, R. D., Neubauer, F. & Hock, V., 1992. Chronology<strong>of</strong> late Paleozoic tectonothermal activity in the southeasternBohemian Massif, Austria (Moldanubian <strong>and</strong> Moravo–Silesianzones): 40 Ar ⁄ 39 Ar mineral age controls. Tectonophysics,210, 135–153.Dewey, J. F., C<strong>and</strong>e, S. & Pitman, W. C., 1989. Tectonic evolution<strong>of</strong> the India ⁄ Eurasia Collision Zone. Eclogae GeologicaeHelvetiae, 82, 717–734.Don, J., 1964. The Zlote <strong>and</strong> Krowiarki Mountains as <strong>structural</strong>elements <strong>of</strong> the Snieznik metamorphic massif. GeologiaSudetica, 1, 79–117.Duchene, S., Lardeaux, J. M. & Albarede, F., 1997. Exhumation<strong>of</strong> eclogites: insights from depth–time path analysis. Tectonophysics,280, 125–140.Dudek, A., 1980. The crystalline basement block <strong>of</strong> the OuterCarpathians in Moravia. Rozpravy Cˇeskoslovenske´ AkademieVeˇd, 90, 1–85.Dudek, A. & Fediukova´ , E., 1974. Eclogites <strong>of</strong> the BohemianMoldanubicum. Neues Jahrbbuch fu¨r Mineralogie Abh<strong>and</strong>lungen,121, 127–159.Dumicz, M., 1979. Tectogenesis <strong>of</strong> the metamorphosed series <strong>of</strong>the Klodzko district: a tentative explanation. GeologicaSudetica, 14, 29–44.Edel, J. B., Schulmann, K. & Holub, F. V., 2003. Anticlockwise<strong>and</strong> clockwise rotations <strong>of</strong> the Eastern Variscides accommodatedby dextral lithospheric wrenching: palaeomagnetic <strong>and</strong><strong>structural</strong> evidence. Journal <strong>of</strong> the Geological Society, 160,209–218.Engl<strong>and</strong>, P. C. & Houseman, G. A., 1988. The mechanics <strong>of</strong> theTibetan Plateau. Philosophical Transactions – Royal Society <strong>of</strong>London, Series A, 326, 301–320.Feehan, J. G. & Br<strong>and</strong>on, M. T., 1999. Contribution <strong>of</strong> ductileflow to exhumation <strong>of</strong> low-temperature, high-pressure metamorphicrocks: San Juan–Cascade nappes, NW WashingtonState. Journal <strong>of</strong> Geophysical Research B: Solid Earth, 104,10 883–10 902.Finger, F., Tichomirowa, M., Pin, C. & Hanzˇl, P., 2000. Relics<strong>of</strong> an early Panafrican metabasite–metarhyolite formation inthe Brno Massif, Moravia, Czech Republic. InternationalJournal <strong>of</strong> Earth Sciences, 89, 328–335.Francu˚, E., Francu˚, J., Kalvoda, J., Poelchau, H.S. & Otava, J.,2002. Burial <strong>and</strong> uplift history <strong>of</strong> the Palaeozoic Flysch in theVariscan forel<strong>and</strong> basin (SE Bohemian Massif, CzechRepublic). In: Continental Collision <strong>and</strong> the TectonosedimentaryEvolution <strong>of</strong> Forel<strong>and</strong>s, Stephen Mueller Special PublicationSeries (eds Bertotti, G., Schulmann, K. & Cloetingh, S.),pp. 167–179. European Geophysical Society, Berlin.Franeˇk, J., Schulman, K. & Lexa, O., 2006. Kinematic <strong>and</strong>rheological model <strong>of</strong> exhumation <strong>of</strong> high pressure granulites inthe Variscan orogenic root: example <strong>of</strong> the Blanský les granulite,Bohemian Massif, Czech Republic. Mineralogy <strong>and</strong>Petrology, 86, 253–276.Franke, W., 2000. The mid-European segment <strong>of</strong> the Variscides:tectonostratigraphic units, terrane boundaries <strong>and</strong> plate tectonicevolution. In: Orogenic Processes: Quatification <strong>and</strong>Modelling in the Variscan Belt, Special Publication 179 (edsFranke, W., Haak, W., Oncken, O. & Tanner, D.), pp. 35–63.Geological Society, London.Friedl, G., Finger, F., Paquette, J.L., von Quadt, A.,McNaughton, N. J. & Fletcher, I. R., 2004. Pre-Variscangeological events in the Austrian part <strong>of</strong> the Bohemian Massifdeduced from U–Pb zircon ages. International Journal <strong>of</strong> EarthSciences, 93, 802–823.Fritz, H., Dallmeyer, R. D. & Neubauer, F., 1996. Thick-skinnedversus thin-skinned thrusting: rheology controlled thrustpropagation in the Variscan collisional belt (the southeasternBohemian Massif, Czech Republic–Austria). Tectonics, 15,1389–1413.Fuchs, G., 1986. Zur Diskussion um den Deckenbau der Bo¨ h-mischen Masse. Jahrbuch der Geologischen Bundesanstalt, 129,41–49.Gerya, T. & Stockhert, B., 2006. Two-dimensional <strong>numerical</strong>modeling <strong>of</strong> tectonic <strong>and</strong> metamorphic histories at activecontinental margins. International Journal <strong>of</strong> Earth Sciences,95, 250–274.Godin, L., Grujic, D., Law, R.D. & Searle, M.P., 2006. Channelflow, ductile extrusion <strong>and</strong> exhumation in continental collisionzones: an introductionIn: Channel Flow, Ductile Extrusion <strong>and</strong>Exhumation in Continental Collision Zones, Special Publication268 (eds Law, R. D., Searle, M. P. & Godin, L.), pp. 1–23.Geological Society, London.Grujic, D., Casey, M., Davidson, C. et al., 1996. Ductile extrusion<strong>of</strong> the Higher Himalayan Crystalline in Bhutan: evidencefrom quartz micr<strong>of</strong>abrics. Tectonophysics, 260, 21–43.Harrison, T. M., Duncan, I. & McDougall, I., 1985. Diffusion <strong>of</strong>40 Ar in biotite; temperature, pressure <strong>and</strong> compositionaleffects. Geochimica et Cosmochimica Acta, 49, 2461–2468.Hartley, A. J. & Otava, J., 2001. Sediment provenance <strong>and</strong> dispersalin a deep marine forel<strong>and</strong> basin: The Lower CarboniferousCulm Basin, Czech Republic. Journal <strong>of</strong> the GeologicalSociety, 158, 137–150.Hasalova´ , P., Schulmann, K., Lexa, O. et al., 2008a. Origin <strong>of</strong>migmatites by deformation enhanced melt infiltration <strong>of</strong>orthogneiss: a new model based on quantitative micro<strong>structural</strong>analysis. Journal <strong>of</strong> Metamorphic Geology, 26, 29–53.Hasalova´ , P., Sˇtı´ pska´ , P., Powell, R., Schulmann, K., Janousˇek,V. & Lexa, O., 2008b. Transforming mylonitic metagranite byopen-system interactions during melt flow. Journal <strong>of</strong> MetamorphicGeology, 26, 55–80.Hensen, B.J. & Zhou, B., 1995. Retention <strong>of</strong> isotopic memory ingarnets partially broken down during an overprinting granulite-faciesmetamorphism: implications for the Sm–Nd closuretemperature. Geology, 23, 225–228.Holub, F. V., Cocherie, A. & Rossi, P., 1997. Radiometric dating<strong>of</strong> granitic rocks from the Central Bohemian Plutonic Complex(Czech Republic): constraints on the chronology <strong>of</strong>Ó 2007 Blackwell Publishing Ltd155
- Page 3:
“It strikes me that all our knowl
- Page 8 and 9:
Contentsviii4.7 Schulmann, Konopás
- Page 11:
Dedicated to my wife Markéta, daug
- Page 14 and 15:
Foreword 2First topic “Quantitati
- Page 16 and 17:
Foreword 4source and freely availab
- Page 18 and 19:
1. Quantitative analysis of deforma
- Page 20 and 21:
1. Quantitative analysis of deforma
- Page 22 and 23:
1. Quantitative analysis of deforma
- Page 24 and 25:
1. Quantitative analysis of deforma
- Page 26 and 27:
1. Quantitative analysis of deforma
- Page 28 and 29:
1. Quantitative analysis of deforma
- Page 31 and 32:
Chapter 2Mechanisms of lower crusta
- Page 33 and 34:
2. Mechanisms of lower crustal flow
- Page 35 and 36:
2. Mechanisms of lower crustal flow
- Page 37 and 38:
2. Mechanisms of lower crustal flow
- Page 39 and 40:
2. Mechanisms of lower crustal flow
- Page 41 and 42:
Chapter 3Quantitative analyses ofme
- Page 43 and 44:
3. Quantitative analyses of metamor
- Page 45 and 46:
3. Quantitative analyses of metamor
- Page 47 and 48:
3. Quantitative analyses of metamor
- Page 49 and 50:
3. Quantitative analyses of metamor
- Page 51:
3. Quantitative analyses of metamor
- Page 54 and 55:
Bibliography 42Culshaw, N., Beaumon
- Page 56 and 57:
Bibliography 44sources and trigger
- Page 58 and 59:
Bibliography 46Skrzypek, E., Štíp
- Page 61 and 62:
Journal of Structural Geology 23 20
- Page 63 and 64:
J. KonopaÂsek et al. / Journal of
- Page 65 and 66:
J. KonopaÂsek et al. / Journal of
- Page 67 and 68:
J. KonopaÂsek et al. / Journal of
- Page 69 and 70:
J. KonopaÂsek et al. / Journal of
- Page 71 and 72:
J. KonopaÂsek et al. / Journal of
- Page 73 and 74:
J. KonopaÂsek et al. / Journal of
- Page 75 and 76:
J. KonopaÂsek et al. / Journal of
- Page 77 and 78:
J. KonopaÂsek et al. / Journal of
- Page 79 and 80:
J. KonopaÂsek et al. / Journal of
- Page 81 and 82:
JOURNAL OF GEOPHYSICAL RESEARCH, VO
- Page 83 and 84:
SCHULMANN ET AL.: STRAIN DISTRIBUTI
- Page 85 and 86:
SCHULMANN ET AL.: STRAIN DISTRIBUTI
- Page 87 and 88:
SCHULMANN ET AL.: STRAIN DISTRIBUTI
- Page 89 and 90:
SCHULMANN ET AL.: STRAIN DISTRIBUTI
- Page 91 and 92:
SCHULMANN ET AL.: STRAIN DISTRIBUTI
- Page 93 and 94:
SCHULMANN ET AL.: STRAIN DISTRIBUTI
- Page 95:
SCHULMANN ET AL.: STRAIN DISTRIBUTI
- Page 98 and 99:
5 - 2 LEXA ET AL.: COLLISION IN WES
- Page 100 and 101:
5 - 4 LEXA ET AL.: COLLISION IN WES
- Page 102 and 103:
5 - 6 LEXA ET AL.: COLLISION IN WES
- Page 104 and 105:
5 - 8 LEXA ET AL.: COLLISION IN WES
- Page 106 and 107:
5 - 10 LEXA ET AL.: COLLISION IN WE
- Page 108 and 109:
5 - 12 LEXA ET AL.: COLLISION IN WE
- Page 110 and 111:
5 - 14 LEXA ET AL.: COLLISION IN WE
- Page 112 and 113:
5 - 16 LEXA ET AL.: COLLISION IN WE
- Page 114 and 115:
156O. Lexa et al. / Journal of Stru
- Page 116 and 117: 158O. Lexa et al. / Journal of Stru
- Page 118 and 119: 160O. Lexa et al. / Journal of Stru
- Page 121 and 122: DTD 5ARTICLE IN PRESSJournal of Str
- Page 123 and 124: DTD 5ARTICLE IN PRESSL. Baratoux et
- Page 125 and 126: DTD 5ARTICLE IN PRESSL. Baratoux et
- Page 127 and 128: DTD 5ARTICLE IN PRESSL. Baratoux et
- Page 129 and 130: DTD 5ARTICLE IN PRESSL. Baratoux et
- Page 131 and 132: DTD 5ARTICLE IN PRESSL. Baratoux et
- Page 133 and 134: DTD 5ARTICLE IN PRESSL. Baratoux et
- Page 135 and 136: Table 1Statistical values of the qu
- Page 137 and 138: DTD 5ARTICLE IN PRESSL. Baratoux et
- Page 139 and 140: DTD 5ARTICLE IN PRESSL. Baratoux et
- Page 141 and 142: Table 2Summary of parameters derive
- Page 143 and 144: DTD 5ARTICLE IN PRESSL. Baratoux et
- Page 145 and 146: J. metamorphic Geol., 2008, 26, 273
- Page 147 and 148: EXHUMATION IN LARGE HOT OROGEN 275m
- Page 149 and 150: Probabi l irequencyProbabi l ireque
- Page 151 and 152: EXHUMATION IN LARGE HOT OROGEN 279y
- Page 153 and 154: EXHUMATION IN LARGE HOT OROGEN 281N
- Page 155 and 156: EXHUMATION IN LARGE HOT OROGEN 283w
- Page 157 and 158: EXHUMATION IN LARGE HOT OROGEN 285a
- Page 159 and 160: EXHUMATION IN LARGE HOT OROGEN 287w
- Page 161 and 162: EXHUMATION IN LARGE HOT OROGEN 289T
- Page 163 and 164: EXHUMATION IN LARGE HOT OROGEN 291O
- Page 165: EXHUMATION IN LARGE HOT OROGEN 293r
- Page 169: EXHUMATION IN LARGE HOT OROGEN 297R
- Page 172 and 173: Author's personal copyK. Schulmann
- Page 174 and 175: Author's personal copyK. Schulmann
- Page 176 and 177: Author's personal copyK. Schulmann
- Page 178 and 179: Author's personal copyK. Schulmann
- Page 180 and 181: Author's personal copyK. Schulmann
- Page 182 and 183: Author's personal copyK. Schulmann
- Page 184 and 185: Author's personal copyK. Schulmann
- Page 186 and 187: Author's personal copyK. Schulmann
- Page 188 and 189: Author's personal copyK. Schulmann
- Page 190 and 191: Author's personal copyK. Schulmann
- Page 193 and 194: J. metamorphic Geol., 2011, 29, 79-
- Page 195 and 196: HEAT SOURCES AND EXHUMATION MECHANI
- Page 197 and 198: HEAT SOURCES AND EXHUMATION MECHANI
- Page 199 and 200: HEAT SOURCES AND EXHUMATION MECHANI
- Page 201 and 202: HEAT SOURCES AND EXHUMATION MECHANI
- Page 203 and 204: HEAT SOURCES AND EXHUMATION MECHANI
- Page 205 and 206: HEAT SOURCES AND EXHUMATION MECHANI
- Page 207 and 208: HEAT SOURCES AND EXHUMATION MECHANI
- Page 209 and 210: HEAT SOURCES AND EXHUMATION MECHANI
- Page 211 and 212: HEAT SOURCES AND EXHUMATION MECHANI
- Page 213 and 214: HEAT SOURCES AND EXHUMATION MECHANI
- Page 215 and 216: HEAT SOURCES AND EXHUMATION MECHANI
- Page 217 and 218:
J. metamorphic Geol., 2011, 29, 53-
- Page 219 and 220:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 221 and 222:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 223 and 224:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 225 and 226:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 227 and 228:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 229 and 230:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 231 and 232:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 233 and 234:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 235 and 236:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 237 and 238:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 239 and 240:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 241 and 242:
EXTRUSIONOFLOWERCRUSTINVARISCANOROG
- Page 243 and 244:
J. metamorphic Geol., 2005, 23, 649
- Page 245 and 246:
CONTRASTING TEXTURAL RECORD OF TWO
- Page 247 and 248:
CONTRASTING TEXTURAL RECORD OF TWO
- Page 249 and 250:
CONTRASTING TEXTURAL RECORD OF TWO
- Page 251 and 252:
CONTRASTING TEXTURAL RECORD OF TWO
- Page 253 and 254:
CONTRASTING TEXTURAL RECORD OF TWO
- Page 255 and 256:
CONTRASTING TEXTURAL RECORD OF TWO
- Page 257 and 258:
CONTRASTING TEXTURAL RECORD OF TWO
- Page 259 and 260:
CONTRASTING TEXTURAL RECORD OF TWO
- Page 261 and 262:
Contrasting microstructures and def
- Page 263 and 264:
TEXTURES OF NATURALLY DEFORMED META
- Page 265 and 266:
TEXTURES OF NATURALLY DEFORMED META
- Page 267 and 268:
TEXTURES OF NATURALLY DEFORMED META
- Page 269 and 270:
TEXTURES OF NATURALLY DEFORMED META
- Page 271 and 272:
TEXTURES OF NATURALLY DEFORMED META
- Page 273 and 274:
1.0--0.9__Mg~(Mg2++Fe2+)9 Core of p
- Page 275 and 276:
TEXTURES OF NATURALLY DEFORMED META
- Page 277 and 278:
' ~'-----2~--~----TEXTURES OF NATUR
- Page 279 and 280:
TEXTURES OF NATURALLY DEFORMED META
- Page 281 and 282:
TEXTURES OF NATURALLY DEFORMED META
- Page 283 and 284:
TEXTURES OF NATURALLY DEFORMED META
- Page 285 and 286:
TEXTURES OF NATURALLY DEFORMED META
- Page 287 and 288:
TEXTURES OF NATURALLY DEFORMED META
- Page 289:
TEXTURES OF NATURALLY DEFORMED META
- Page 292 and 293:
B10210ZÁVADA ET AL.: EXTREME DUCTI
- Page 294 and 295:
B10210ZÁVADA ET AL.: EXTREME DUCTI
- Page 296 and 297:
B10210ZÁVADA ET AL.: EXTREME DUCTI
- Page 298 and 299:
B10210ZÁVADA ET AL.: EXTREME DUCTI
- Page 300 and 301:
B10210ZÁVADA ET AL.: EXTREME DUCTI
- Page 302 and 303:
B10210ZÁVADA ET AL.: EXTREME DUCTI
- Page 304 and 305:
B10210ZÁVADA ET AL.: EXTREME DUCTI
- Page 307 and 308:
ClickHereforFullArticleJOURNAL OF G
- Page 309 and 310:
B10406SCHULMANN ET AL.: RHEOLOGY OF
- Page 311 and 312:
B10406SCHULMANN ET AL.: RHEOLOGY OF
- Page 313 and 314:
B10406SCHULMANN ET AL.: RHEOLOGY OF
- Page 315 and 316:
B10406SCHULMANN ET AL.: RHEOLOGY OF
- Page 317 and 318:
B10406SCHULMANN ET AL.: RHEOLOGY OF
- Page 319 and 320:
B10406SCHULMANN ET AL.: RHEOLOGY OF
- Page 321 and 322:
B10406SCHULMANN ET AL.: RHEOLOGY OF
- Page 323 and 324:
B10406SCHULMANN ET AL.: RHEOLOGY OF
- Page 325 and 326:
B10406SCHULMANN ET AL.: RHEOLOGY OF
- Page 327 and 328:
J. metamorphic Geol., 2008, 26, 29-
- Page 329 and 330:
ORIGIN OF FELSIC MIGMATITES 31Ó 20
- Page 331 and 332:
ORIGIN OF FELSIC MIGMATITES 33durin
- Page 333 and 334:
ORIGIN OF FELSIC MIGMATITES 35(a)Ty
- Page 335 and 336:
ORIGIN OF FELSIC MIGMATITES 37(a)Pl
- Page 337 and 338:
ORIGIN OF FELSIC MIGMATITES 39Grain
- Page 339 and 340:
ORIGIN OF FELSIC MIGMATITES 41(a)(b
- Page 341 and 342:
ORIGIN OF FELSIC MIGMATITES 43(a)(b
- Page 343 and 344:
ORIGIN OF FELSIC MIGMATITES 45Fig.
- Page 345 and 346:
ORIGIN OF FELSIC MIGMATITES 47produ
- Page 347 and 348:
ORIGIN OF FELSIC MIGMATITES 49stron
- Page 349 and 350:
ORIGIN OF FELSIC MIGMATITES 51Cmı
- Page 351:
ORIGIN OF FELSIC MIGMATITES 53easte
- Page 354 and 355:
104 J. FRANĚK ET AL.in terms of th
- Page 356 and 357:
106 J. FRANĚK ET AL.Fig. 2. Struct
- Page 358 and 359:
108 J. FRANĚK ET AL.(a)perthite po
- Page 360 and 361:
110 J. FRANĚK ET AL.(a)(b)(c) (d)
- Page 362 and 363:
112 J. FRANĚK ET AL.Table 1. Repre
- Page 364 and 365:
114 J. FRANĚK ET AL.at these P-T c
- Page 366 and 367:
116 J. FRANĚK ET AL.(a)(b)Fig. 10.
- Page 368 and 369:
118 J. FRANĚK ET AL.(a)(b)Fig. 11.
- Page 370 and 371:
120 J. FRANĚK ET AL.Table 2. Quant
- Page 372 and 373:
122 J. FRANĚK ET AL.(a)(b)Fig. 15.
- Page 374 and 375:
124 J. FRANĚK ET AL.Fig. 16. Inter
- Page 376 and 377:
126 J. FRANĚK ET AL.development of
- Page 378 and 379:
128 J. FRANĚK ET AL.Behrmann, J.H.
- Page 380:
130 J. FRANĚK ET AL.Southern Bohem
Change language