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276 K. SCHULMANN ET AL.Moldanubian-LugianOROGENIC ROOTOrogenic upper crustProterozoic andPaleozoic sedimentsOrogenic middle crustMonotonous groupVaried groupGneissesOrogenic lower crust(Gföhl Unit in Moldanubian)Granulites, gneissesMetasedimentsOrdovician mafic lower crustLUGIANBELBE ZONEC′Fig. 7SilesianB’ B′MOLDANUBIAN0 20 40 60MAGMATIC ROCKSSyenitesTonalitesCMPAS outhernC entralNorthernCSvratk vratka aThay haya aA′Moravo-SilesianBRUNIABRUNIAFig. 6Fig. 5Foreland basinCulmPara-autochtonous unitsCoverBasementAlochtonous unitsCoverBasementMoravianMicaschist ZonePermian coverLate granitesLetovice ophioliteFig. 2. Map of the eastern margin of the Bohemian Massif to show inferred orogenic crustal levels and the locations of Figs 5, 6 & 7,which are indicated by rectangular boxes. Also shown are the positions of interpretative cross sections A–A¢, B–B¢ and C–C¢ presentedin Fig. 10.Ó 2007 Blackwell Publishing Ltd136
Probabi l irequencyProbabi l irequencyEXHUMATION IN LARGE HOT OROGEN 277underthrust to eclogite conditions as well (Konopa´ seket al., 2002).The orogenic rootThe Gföhl Unit and Lugian high-grade rocksThe Gfo¨ hl Unit (Fig. 2) is composed predominantly offelsic granulites (11–20 kbar, 800–1000 °C) and highgradegneisses (e.g. OÕBrien & Ro¨ tzler, 2003; Sˇtı´ pska´ &Powell, 2005b) that contain eclogite lenses of basalticcomposition, suggesting a crustal origin (18–19 kbar,800)900 °C, Fig. 4; e.g. Medaris et al., 1998; Sˇtípska´& Powell, 2005a and references therein). The eclogitesand granulites, as well as other lithologies of the Gfo¨ hlUnit, were overprinted at amphibolite facies conditions(4)12 kbar, 750)850 °C, Fig. 4; e.g. Petrakakis,1997; Hasalova´ et al., 2008b). The Gfo¨ hl Unit containsnumerous tectonically emplaced bodies of garnet andspinel peridotite (28–44 kbar, 900–1300 °C, Fig. 4),associated with lenses of eclogite (16–20 kbar, 800–950 °C) and clinopyroxenite, representing partial meltcrystallized in the upper mantle (Medaris et al., 1995).The Lugian eclogites and granulites (18–20 kbar, 800–900 °C, Fig. 4; e.g. Steltenpohl et al., 1993; Sˇtípska´et al., 2004) are considered to reflect UHP conditions(Kryza et al., 1996), but this has not been confirmed;they were re-equilibrated at variable P–T conditions(4)11 kbar, 700)800 °C, Fig. 4).Multigrain zircon and monazite fractions fromgranulites and high-grade gneisses of the Gfo¨ hl Unityielded conventional upper intercept U–Pb agesbetween 550 and 510 Ma, interpreted to date the formationof the protoliths (Fig. 3b; e.g. Van Breemenet al., 1982; Schulmann et al., 2005). In addition,xenocrystic cores and prismatic zircon from felsicgranulites and Gfo¨ hl gneiss yield Silurian to DevonianU–Pb ages also interpreted to date the formation of theprotoliths (Fig. 3b; Friedl et al., 2004). However, amajority of U–Pb zircon ages fall in the range360)340 Ma with a prominent peak at c. 340 Ma,which is interpreted to record the age of Variscanmetamorphism (Fig. 3d). Ultra-potassic syenites (durbachites)spatially related to Ky–Kfs granulites yieldages around 338 Ma and 325 Ma (Fig. 3e; Holubet al., 1997; Janousˇek & Holub, 2007).The Monotonous and Varied GroupsIn the Moldanubian domain, paragneisses of theMonotonous and Varied Groups generally recordmedium-pressure metamorphism (8)9 kbar, 610)660 °C) associated at higher temperatures with widespreadanatexis ( ~ 9 kbar, 700)800 °C), followed byre-equilibration in the sillimanite stability field atconditions around 4)6 kbar and 600)800 °C (Fig. 4;e.g. Petrakakis, 1997). The metamorphic conditionsof the Monotonous Group paragneisses aret y fBrunia and Moravo-Silesian0.7(a)503 Ma0.6580 Ma0.50.4684 Ma0.30.2Protolith0.1U–Pb0350 400 450 500 550 600 650 700 7504(b)3.532.521.510.5Orogenic middle crust503 MaLugian (60)Moldanubian (5)ProtolithU–Pb0350 400 450 500 550 600 650 700 750Orogenic lower crust0.7(c)0.6413 Ma0.5389 Ma0.4550 Ma0.3487 Ma430 Ma0.20.1Moldanubian (14)Lugian (9)ProtolithU–Pb0350 400 450 500 550 600 650 700 750t y f3.5(d)3 340 Ma2.520.510.5359 MaMoldanubian (22)Lugian (15)1.4(e)1.2MetamorphicMagma.0.2U–PbU–Pb00300 320 340 360 380 400 420 280 300 320 340 360 380 40010.80.60.4335 Ma324 Ma340 Ma353 MaFig. 3. Probability curves of age histograms to show existing zircon U–Pb ages. For the Brunia continent and the Moravo–SilesianZone (a), Moldanubian and Lugian domain (b, c & d) and intrusive rocks (e). BB1, Brunia basement south of the Elbe zone; BB2,Brunia basement north of the Elbe zone; MB1, Moravian domain basement rocks; MB2, Silesian domain basement rocks; MSZ,Moravian Micaschist Zone; ID, Mg-rich syenites (durbachites) of the orogenic lower crust; IMC, intrusive rocks of the middle crust;IT, tonalite–granodiorite intrusions; IUC, granites in upper crustal units. Numbers in parentheses stand for number of available ages.Ó 2007 Blackwell Publishing Ltd137
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“It strikes me that all our knowl
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Contentsviii4.7 Schulmann, Konopás
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Dedicated to my wife Markéta, daug
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Foreword 2First topic “Quantitati
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Foreword 4source and freely availab
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1. Quantitative analysis of deforma
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Chapter 2Mechanisms of lower crusta
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2. Mechanisms of lower crustal flow
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Chapter 3Quantitative analyses ofme
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3. Quantitative analyses of metamor
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Bibliography 42Culshaw, N., Beaumon
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Bibliography 44sources and trigger
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Bibliography 46Skrzypek, E., Štíp
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Journal of Structural Geology 23 20
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JOURNAL OF GEOPHYSICAL RESEARCH, VO
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ORIGIN OF FELSIC MIGMATITES 31Ó 20
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ORIGIN OF FELSIC MIGMATITES 39Grain
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ORIGIN OF FELSIC MIGMATITES 45Fig.
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ORIGIN OF FELSIC MIGMATITES 49stron
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ORIGIN OF FELSIC MIGMATITES 51Cmı
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104 J. FRANĚK ET AL.in terms of th
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106 J. FRANĚK ET AL.Fig. 2. Struct
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