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Author's personal copyK. Schulmann et al. / C. R. Geoscience 341 (2009) 266–286 275marked by relics of Ordovician MORB eclogites andmetabasites locally associated with Ordovician sedimentsmetamorphosed under blueschist–eclogite faciesconditions indicating a Mid-Devonian oceanic subduction[34] and an existence of Lower PalaeozoicSaxothuringian oceanic domain (Fig. 3a). The exactage and size of the Saxothuringian ocean is not known,because the differences of Ordovician and LowerDevonian faunas between Saxothuringian and Barrandiancontinental domains are not confirmed, precludingan existence of large oceanic barrier of biogeographicalsignificance [10,52,106]. Therefore, the oceanic domainmust have been narrow and potentially short lived inorder not to be recorded by palaeobiogeographic faunalevidence. The only existing argument for larger oceanicseparation are from palaeomagnetic data of Tait et al.,[141] suggesting that the Saxothuringian and Tepla-Barrandian blocks rotated independently during Silurianand Devonian times.The hornblende and mica cooling ages of theVohenstraus–Erbendorf Zone, Mariánské Lázně complexand the Sovie Gory granulites cluster around380 Ma, which indicates early collision betweenthe Teplá-Barrandian and Saxothuringian domains(Figs. 3middle and 4B). This is also confirmed byFamennian flysh sediments of the Saxothuringian basinthat contain detrital zircons dated at 380 Ma [114]which is a direct evidence of mutual contact betweenthe Teplá-Barrandian and Saxothuringian domainsduring Famennian but most likely already during mid-Devonian. The Barrovian metamorphic zonation developedat the western flank of the Teplá-Barrandian domain(Figs. 3middle and 4B) is potentially related todeformation of the overriding Teplá-Barrandian continentalmargin and is consistent with a model ofextrusion of lower part of the Teplá-Barrandian crustduring Devonian shortening event [160,161]. The foldingof the eastern very low grade shales and volcanics of theNeoproterozoic sequences is interpreted as a supracrustalresponse to the same deformation event affecting highgrade rocks in the west [161]. Thus, the exhumation ofHP rocks in the Mariánské Lázně Complex and thedeformation of the Teplá-Barrandian basement arecoupled and related to convergent processes at theSaxothuringian plate boundary (Figs. 3middle and 4B).The strong argument for eastward subduction of theSaxothuringian ocean underneath the eastern Teplá-Barrandian continent is a Devonian–Lower Carboniferousmagmatic arc that is firmly founded on thecontinental crust. This arc, the Central BohemianPlutonic Complex, separated the Teplá-Barrandiandomain from the future Moldanubian domain and inthis model the former unit represented a fore-arc regionduring Devonian (Figs. 3middle and 4B). Thus, theposition of Devonian HP rocks thrust over theSaxothuringian basement, existence of the MariánskéLázně Complex – the oceanic fragment at sutureposition, and location of calc-alkaline magmatic rocksfurther east confirm a polarity of the oceanic subductionunderneath the eastern fore-arc and magmatic arcsystem during Late Devonian (Figs. 3middle and 4B).The distance between the arc and the trench arearepresented by the suture indicates that the dip ofsubduction zone was probably moderate (30–408,Fig. 4B). The temporal evolution of magma geochemistryfrom calc-alkaline to more potassic/shoshoniticaffinities (from 370 to 336 Ma) is compatible withflattening of the subduction zone and increased meltingof continental material during Early Carboniferous. TheBarrandian (Prague) Basin is interpreted as a part of thefore-arc basin marked by 380-Ma-old detrital zirconsfound in Mid-Devonian flyshoid sequences [135]suggesting early erosion of the eastern magmatic arc.The most problematic question in the Devoniansubduction model for the Bohemian massif is the role ofthe future Moldanubian domain as well as the positionof the Brunia continent. The amphibolites derived fromSiluro-Devonian tholeiitic basalts associated withcarbonates, widespread in Lower Austria and SouthBohemia, are interpreted as volcanic products of a relicFig. 3. Time slices maps showing the chronological and tectonic significance of the various units of the Bohemian Massif. Top: Ordovician timeslice showing the location of Ordovician MORB and deep marine sediments, and that of the Proterozoic units containing the Ordovician magmatism;middle: Devonian time slice showing the location of Devonian high pressure (HP) rocks, the passive margin sequences, the active marginmetamorphism, the fore-arc region, the magmatic arc, the location of Devonian infrastructure and sediments; bottom: Carboniferous time sliceshows the location of orogenic lower and middle crust belts in the Moldanubian domain, the metamorphism of the Moravian Zone, the MoravianMicaschist Zone, the HP units in Saxothuringian domain and the various types of magmatic rocks.Fig. 3. Cartes selon des tranches de temps montrant la signification chronologique et tectonique des diverses unités du Massif de Bohême. Enhaut : tranche de temps ordovicienne montrant la localisation du MORB ordovicien et des sédiments marins profonds et celle des unitésprotérozoïques incluant le magmatisme ordovicien ; au milieu : tranche de temps dévonienne montrant la localisation des roches de haute pression(HP) dévoniennes, les séquences de marge active, le domaine avant-arc, l’arc magmatique et la localisation de l’infrastructure et des sédimentsdévoniens ; en bas : tranche de temps carbonifère montrant la localisation des chaînes orogéniques crustales inférieure et moyenne du Domainemoldanubien, le métamorphisme de la zone moravienne, de la zone des micaschistes moraviens, des unités HP du domaine saxothuriningien et desdifférents types de roches magmatiques.168
Author's personal copy276K. Schulmann et al. / C. R. Geoscience 341 (2009) 266–286Fig. 4. Conceptual model of the geodynamic evolution of the Bohemian Massif shown as schematic cross sections through the orogen. A. Silurian–Early Devonian subduction setting with the beginning of arc and back-arc formation on upper plate. B. Onset of the Mid-Devonian continentalunderthrusting of Saxothuringian lithosphere, deformation of active margin, formation of magmatic arc and persistence of back-arc region on theupper plate. C. Crustal thickening processes marked by the influx of Saxothuringian crust and progressive individualization of the Brunia activemargin. D. Brunia continent indentation associated with the channel flow process, imbrications of underthrust Brunia and the formation of theMoravian Zone.Fig. 4. Modèle conceptuel de l’évolution géodynamique du Massif de Bohême représenté par des coupes schématiques au travers de l’orogène.A. Subduction Silurien–Dévonien inférieur se mettant en place avec le début de la formation de l’arc et de l’arrière-arc sur la plaque supérieure.B. Au Dévonien moyen, mise en place du sous-charriage continental et de la lithosphère saxothuringienne, déformation de la marge active, formationde l’arc magmatique et persistance de la zone d’arrière-arc sur la plaque supérieure. C. Processus d’épaississement crustal marqué par la venue decroûte saxothuringienne et individualisation progressive de la marge active de Brunia. D. Indentation de Brunia, associée à un processus de flux dechenal, imbrications du sous-charriage de Brunia et formation de la zone moravienne.169
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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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1. Quantitative analysis of deforma
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Chapter 2Mechanisms of lower crusta
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Bibliography 44sources and trigger
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Bibliography 46Skrzypek, E., Štíp
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