Supplementary material
Analytical techniques
Whole-rock geochemistry
After the conventional crushing and homogenization of the freshest samples (Fig. A.1, Table A.1) with minimal weight of 15 kg, the powders produced under acetone in agate mill have been analysed in Acme Analytical Laboratories Ltd., Vancouver. The contents of major and minor elements were determined by ICP-OES and most trace elements (Ba, Cs, Ga, Hf, Nb, Rb, Sr, Ta, Th, U, V, Zr, Y, and REE) by ICP-MS. The dissolution of the rock powders in both cases followed fusion with a LiBO2/Li2B4O7 flux. The analyses of remaining trace elements, and transition metals in particular (Cu, Pb, Zn, Cr and Ni), were carried out by ICP-MS following leaching with a HCl–HNO3–H2O mixture at 95 ºC for 1 hour. Recalculation and visualization of geochemical data were facilitated using the R software package GCDkit (Janoušek et al. 2006).
Radiogenic isotopes (Sr–Nd)
The peridotites were leached with hot 6M HCl overnight to remove as much olivine-held Mg as possible; after centrifuging of the beakers, the supernatant was pipetted off and stored. Followed by dissolution of the residue in HF and HCl on a hotplate, the two fractions were then recombined, mixed and spiked with 85Rb–84Sr and 149Sm–150Nd tracers.
External precision for peridotite measurements (MC-ICP-MS, University of Melbourne) are 87Rb/86Sr = ± 0.5% and 147Sm/144Nd = ± 0.2%. Values of 87Sr/86Sr were corrected for mass bias by normalizing to 88Sr/86Sr = 8.37521; reported relative to SRM 987 = 0.710230. Values of 143Nd/144Nd were corrected for mass bias by normalizing to 146Nd/145Nd = 2.0719425 (equivalent to 146Nd/144Nd = 0.7219, Vance & Thirlwall 2002) and reported relative to La Jolla Nd = 0.511860. Internal precision (± 2σ) is ≤ ± 0.000020 for 87Sr/86Sr and ≤ ± 0.000012 for 143Nd/144Nd. External precision (2s of multiple runs of same Sr or Nd) is ≤ ± 0.000040 for 87Sr/86Sr and ≤ ± 0.000020 for 143Nd/144Nd. The results for USGS standard basalt BCR-2 are consistent with TIMS reference values (e.g. Raczek et al. 2003).
For the Sr and Nd isotope determinations of granulites, samples were dissolved using a combined HF–HCl–HNO3 digestion. Strontium and neodymium were isolated from the bulk matrix by the exchange chromatography techniques using Eichrom/Triskem Sr.spec, TRU.spec and Ln.spec resins (Míková & Denková 2007 and references therein). Isotopic analyses of Sr and Nd were performed on a TIMS instrument housed at Czech Geological Survey in dynamic mode using a single Ta filament and double Re filament assembly, respectively. The 143Nd/144Nd ratios were corrected for mass bias to 146Nd/144Nd = 0.7219, 87Sr/86Sr ratios assuming 88Sr/86Sr = 8.375209. Internal precision (±2σ(M)) was ≤ ± 0.000014 for both 87Sr/86Sr and 143Nd/144Nd. External precision is given by averaged NBS 987 measurements (0.710246 ± 0.000026, 2s) for 87Sr/86Sr and JNdi-1 (0.512100 ± 0.000022, 2s) for 143Nd/144Nd. 
Although reference values from the two laboratories are not identical (143Nd/144Nd value 0.51186 for La Jolla is equivalent to 0.51212 for JNdi-1, Tanaka et al. 2000) the difference is within the range given by reported external reproducibility. The difference between used 88Sr/86Sr normalizing values is negligible relative to measurement uncertainties.
Sensitive high-resolution ion-microprobe (SHRIMP) U–Pb zircon dating
In order to constrain the timing of orogenic root processes, in situ zircon samples from different generations in of granulite and amphibolite microstructures were acquired. First, the zircons were identified in polished thick sections (100 µm) using Back-Scattered Electron (BSE) attachment on scanning electron microscope CamScan 4 at Charles University, Prague (accelerating voltage 30 kV). Targeted zircons were then micro-drilled from the sections under optical microscope (Fig. A.4) and mounted together with the Temora zircon standard (Black et al. 2003) with 206Pb/238U IDTIMS age of 416.8 ± 1.1 Ma. Reflected and transmitted light photomicrographs were obtained for all zircons. Cathodoluminescence (CL; Fig. A.5) and BSE (Fig. 7) images were used to decipher the internal structures of the sectioned grains and to ensure that the 10–30 µm SHRIMP spot was completely within a single compositional domain within the sectioned grains.
The U–Th–Pb analyses were made using the SHRIMP II at the Research School of Earth Sciences, The Australian National University, Canberra, following procedures given in Williams (1998) and references therein. Each analysis consisted of 6 scans through the mass range, with a U–Pb reference grain analysed for every three unknown analyses. The data have been reduced using the SQUID Excel Macro of Ludwig (2001). For the zircon analyses, the U/Pb ratios have been normalized relative to a value of 0.0668 for the Temora reference zircon, equivalent to an age of 417 Ma (see Black et al. 2003). Uncertainties in the U–Pb calibration were 0.61 % for analytical sessions. Correction for common Pb for the U/Pb data has been made using the measured 238U/206Pb following Tera and Wasserburg (1972) as outlined in Williams (1998). Weighted average of all Temora standard measurements in course of the present study has been 416.0 ± 2.4 Ma (2σ, n = 15). Uncertainties given for individual isotopic ratios are at the one sigma confidence level; errors of the quoted ages are 2 sigma, if not stated otherwise.

Least-squares estimates of the modal compositions of the serpentinized peridotites
Modal abundances of individual mineral phases in variously serpentinized Mohelno peridotites were estimated by Least-squares modelling with Monte Carlo approach (LS modelling) (Fig. A.6) using previously measured mineral compositions (appendix A in Medaris et al. 2005; table 1–5 in Kamei et al. 2010) and the newly obtained whole-rock analyses (Table A.2). For each modelling run, a random set of individual mineral compositions was selected and the modal abundances calculated using constrained least-squares method (Albarède 1996) as implemented by the ModeC function of the GCDkit package (Janoušek et al. 2006). Mineral densities used for recalculation from wt.% to vol.% were as follows: olivine (Fo93Fa7) – 3.311 g/cm3 (Kumazawa & Anderson 1969); orthopyroxene (En80Fs20) – 3.354 g/cm3 (Frisillo & Barsch 1972); clinopyroxene (diopside) – 3.289 g/cm3 (Levien et al. 1979).
The most depleted sample (WKG6) has the highest inferred modal volume of Ol and minimal of Opx, Cpx and Spl among the spinel peridotites, and vice versa. This pattern is valid also for garnet peridotite samples, if taking in account the fact that part of the olivine was generated (and pyroxenes consumed) bypinernet Grt equilibrium reaction:
orthopyroxene + clinopyroxene + spinel → olivine + garnet (Webb & Wood 1986).
References
Albarède, F. 1996. Introduction to Geochemical Modeling. Cambridge University Press, Cambridge.
Black, L.P., Kamo, S.L., Allen, C.M., Aleinikoff, J.N., Davis, D.W., Korsch, R.J. & Foudoulis, C. 2003. TEMORA 1: a new zircon standard for Phanerozoic U–Pb geochronology. Chemical Geology, 200, 155–170.
Frisillo, A.L. & Barsch, G.R. 1972. Measurement of single-crystal elastic constants of bronzite as a function of pressure and temperature. Journal of Geophysical Research, 77, 6360–6384.
Janoušek, V., Farrow, C. & Erban, V. 2006. Interpretation of whole-rock geochemical data in igneous geochemistry: introducing Geochemical Data Toolkit (GCDkit). Journal of Petrology, 47, 1255–1259.
Kamei, A., Obata, M., Michibayashi, K., Hirajima, T. & Svojtka, M. 2010. Two contrasting fabric patterns of olivine observed in garnet and spinel peridotite from a mantle-derived ultramafic mass enclosed in felsic granulite, the Moldanubian Zone, Czech Republic. Journal of Petrology, 51, 101–123.
Kumazawa, M. & Anderson, O.L. 1969. Elastic moduli, pressure derivatives, and temperature derivatives of single-crystal olivine and single-crystal forsterite. Journal of Geophysical Research, 74, 5961–5972.
Levien, L., Weidner, D. & Prewitt, C. 1979. Elasticity of diopside. Physics and Chemistry of Minerals, 4, 105–113.
Ludwig, K. 2001. SQUID 1.02, A user's manual. Berkeley Geochronology Center Special Publication No. 2.
Medaris, L.G., Wang, H., Jelínek, E., Mihaljevič, M. & Jakeš, P. 2005. Characteristics and origins of diverse Variscan peridotites in the Gföhl Nappe, Bohemian Massif, Czech Republic. Lithos, 82, 1–23.
Míková, J. & Denková, P. 2007. Modified chromatographic separation scheme for Sr and Nd isotope analysis in geological silicate samples. Journal of Geosciences, 52, 221–226.
Raczek, I., Jochum, K.P. & Hofmann, A.W. 2003. Neodymium and Strontium Isotope Data for USGS Reference Materials BCR-1, BCR-2, BHVO-1, BHVO-2, AGV-1, AGV-2, GSP-1, GSP-2 and Eight MPI-DING Reference Glasses. Geostandards Newsletter, 27, 173–179.
Tanaka, T., Togashi, S., Kamioka, H., Amakawa, H., Kagami, H., Hamamoto, T., Yuhara, M., Orihashi, Y., Yoneda, S., Shimizu, H., Kunimaru, T., Takahashi, K., Yanagi, T., Nakano, T., Fujimaki, H., Shinjo, R., Asahara, Y., Tanimizu, M. & Dragusanu, C. 2000. JNdi-1: a neodymium isotopic reference in consistency with LaJolla neodymium. Chemical Geology, 168, 279–281.
Tera, F. & Wasserburg, G. 1972. U–Th–Pb systematics in three Apollo 14 basalts and the problem of initial Pb in lunar rocks. Earth and Planetary Science Letters, 14, 281–304.
Vance, D. & Thirlwall, M. 2002. An assessment of mass discrimination in MC-ICPMS using Nd isotopes. Chemical Geology, 185, 227–240.
Webb, S.A.C. & Wood, B.J. 1986. Spinel–pyroxene–garnet relationships and their dependence on Cr/Al ratio. Contributions to Mineralogy and Petrology, 92, 471–480.
Williams, I. 1998. U–Th–Pb geochronology by ion microprobe. In: McKibben, M., Shanks III, W. & Ridley, W. (eds) Applications of Microanalytical Techniques to Understanding Mineralizing Processes. Reviews in Economic Geology, 7, 1–35.
Figure captions
Fig. A.1 Localization of the geochemical and dated zircon SHRIMP samples in close vicinity of the Mohelno peridotite.
Fig. A.2 Characteristic textures of Náměšť granulites (A–C) and Mohelno peridotites (D–E). (A) Coarse grained Ky–ternary Fsp granulite WK188A, (B) mylonitic Ky-bearing granulite WKG16, (C) retrogressed Bt–Sil granulite WKG3, (D) garnet peridotite WKG5, (E) spinel peridotite WKG6. Images are composed from scans of thin sections in plane- and cross-polarized light.
Fig. A.3 Back-scattered electron (BSE) images of characteristic microstructure of Náměšť granulites. (A) Coarse grained Ky–ternary Fsp granulite WK188A, (B) mylonitic Ky-bearing granulite WKG16, (C) retrogressed Bt–Sil granulite WK201.
Fig. A.4 Overview of mounted micro-drilled cores (Grt – garnet, Zrn – zircon).
Fig. A.5 Cathodoluminescence (CL) images of zircon grains drilled from different structural positions. Shown are the measured spots with inferred 206Pb/238U age at the two sigma level and U abundance. Individual measurements are colour coded according to the latter value (red – high, yellow – medium, white – low). (A) Zircon grains from granulitic coarse-grained S1 fabric sample (WK188A, B). (B) Zircon grains from ultramylonitic granulite S2 fabric samples (WK196AB and WK177L2). (C) Zircon grains from retrogressed S3 fabric samples (WK201).
Fig. A.6 Modal compositions of the studied Mohelno peridotite reconstructed from published mineral analyses (Medaris et al. 2005; Kamei et al. 2010) and our whole-rock geochemical dataset by Least-squares modelling with Monte Carlo approach (LSModel). Calculated modal abundances (obtained from 1000 randomly combined mineral assemblages) are visualized with set of boxplots for each peridotite sample. For garnet peridotite samples WKG5 (5□) and WKG4 (4□) a mineral assemblage olivine + orthopyroxene + clinopyroxene + spinel + garnet is considered. For spinel peridotite samples WKG6 (6◊), WKG7 (7◊) and WKG10 (10◊) same garnet-free mineral assemblage is assumed. (A)–(E) Wt.% of olivine, orthopyroxene, clinopyroxene, spinel and garnet in calculated assemblage. (F) Binary diagram Ti/(FeOT + Ti) vs. Km. Colour coding of samples according to the bulk magnetic susceptibility Km (see Fig. 6.A).
Table captions
Tab. A.1 List of samples from the Náměšť Granulite Massif
Tab. A.2 Major-element whole-rock geochemical analyses from the Náměšť Granulite Massif (wt.%)
Tab. A.3 Trace-element whole-rock geochemical analyses from the Náměšť Granulite Massif (ppm)
Tab. A.4 Whole-rock Rb–Sr and Sm–Nd isotopic data for rocks of the Náměšť Granulite Massif
Tab. A.5 Bulk susceptibility of the serpentinized peridotite (1000×SI)
Tab. A.6 Summary of SHRIMP U–Pb results for zircon grains micro-drilled from thin sections
Sample descriptions 
WKG2 
(N 49°5'55.5'' E 16°11'38.16'', WK199, right bank of the Jihlava river, 30 m upstream from the bridge over river on the Mohelno–Dukovany road 392) 
Felsic granulite with fine-grained (< 0.2 mm) mylonitic quartz – K-feldspar – plagioclase matrix, small porphyroclasts of garnet (< 1 mm) without inclusions and biotite. Evenly distributed biotite flakes are associated with large quartz disc-like grains (length up to 2 mm) and together are forming well-defined foliation. In discrimination according Kusbach et al. (2012) this microstructure corresponds to S2–S3 transition.

WKG3
(N 49°6'2.33'' E 16°11'39.46'', next to the Mohelno–Dukovany road 392, close to the car accident tombstone) 
The retrogressed S3 granulite at this locality is dark and very massive without any strong fabric, sometimes alternating with lighter layers rich in plagioclase. The basis of the microstructure is intermixed fine-grained mylonitic intermixed quartzo–feldspathic matrix (< 0.2 mm). Often the fine-grained microstructure is annealed to microstructure with regular triple points and large lobate neoblasts of quartz and plagioclase (> 1 mm). Large garnet crystals (~ 1 mm) with irregular shapes rich in inclusions of quartz and plagioclase are distributed evenly in the rock. Large biotite flakes occur in close vicinity of garnet and small crystals are widely distributed along matrix minerals' triple points throughout the rock volume.

WKG4 
(N 49°5'57.09'' E 16°11'46.98'', WK25, outcrop with cabin 08, left bank of the Jihlava river, 50 m downstream from the bridge on the Mohelno–Dukovany road 392) 
Sample is characteristic example of the Mohelno garnet peridotite. Peridotite is highly serpentinized, with mylonitic olivine–orthopyroxene matrix (fine-grained < 100 µm) with rare presence of clinopyroxene. Small orthopyroxene (~ 1 mm) and large garnet porphyroclasts (> 5 mm) with spinel inclusions are aligned within mylonitic fabric. Macroscopically banded appearance of the rock is caused by distribution of serpentine minerals with different proportions of opaque minerals and submicroscopic pigment of iron oxides dispersed in serpentine minerals. Talc and chlorite are present as accessories.

WKG5 
(N 49°5'36.54'' E 16°11'58.79'', WK142, in the gorge with a small brook, next to the Mohelno–Dukovany road 392) 
Black massive garnet peridotite from this locality has strong ultra-mylonitic fabric with serpentinized olivine–orthopyroxene matrix. Large garnet porphyroclasts (>1 cm) with olivine and pyroxene inclusions surrounded by coarse-grained microstructure are rarely preserved. Visible shaded banding is caused by different colouring of the serpentine minerals (due to pigment of iron oxides) and thin bands of recrystallized orthopyroxene porphyroclasts.

WKG6
(N 49°6'21.81'' E 16°11'13.26'', WK3, large outcrop on the left bank of the Jihlava river next to river weir for the Mohelno mill)
Sample WKG6 is highly serpentinized greenish spinel peridotite. Spinel (> 1 mm) and orthopyroxene porphyroclasts (~ 2 mm) are aligned in fine-grained mylonitic olivine–orthopyroxene matrix with rare clinopyroxene. At this locality orthopyroxene bands, several centimetres wide, are very common and sample was taken to avoid them.

WKG7 
(N 49°6'19.41'' E 16°11'20.64'', WK56, in the road cutting towards Mohelno, in the serpentinite above Mohelno mill) 
Similar characteristics as other samples of spinel peridotite. Massive greenish serpentinized spinel peridotite with abundant large orthopyroxene porphyroclasts (~ 3 mm). Spinel is homogenously distributed in the mylonitic matrix. Systems of polygonal fractures are perpendicularly cutting orthopyroxene bands and are filled with serpentine minerals.

WKG8 
(N 49°5'56.71'' E 16°12'14.43'', WK7, sample from the vertical fold cropping out in the slopes above the campsite)
Granulite is characteristic for the retrogression from the S2 to the S3 fabric. Light felsic granulite is associated with darker bands rich in biotite. Garnet porphyroclasts with common crystallographically oriented rutile rods and also quartz and feldspars inclusions are surrounded by the fine-grained quartzo-feldspathic groundmass. Biotite replaces garnet and also small biotite flakes are evenly distributed along the foliation defined mostly by alignment of the elongated quartz grains.

WKG10 
(N 49°5'58.87'' E 16°10'39.46'', WK127, close to the stream entry into dam at the bottom of gorge) Spinel peridotite, which is slightly banded due to the coloured serpentine minerals. Fine-grained olivine–orthopyroxene groundmass is intensively serpentinized with abundant occurrence of the opaque minerals. Large orthopyroxene porphyroclasts with olivine inclusions and randomly oriented fractures annealed with serpentine are preserved.

WKG11
(N 49°6'6.61'' E 16°10'51.85'', WK171, outcrop next to the southern end of the Mohelno barrage, disused small quarry)
Ultimate example of the so-called “Weisstein”. S1(?) Granulite composed almost exclusively of quartz and feldspars, with minimum proportion of garnet and biotite. Needles of biotite are not preferentially oriented, weak alignment can be observed for small garnet remnants only. Grain boundaries are lobate both for quartz and feldspars. Felsic matrix is fine-grained with occasionally larger elongated quartz grains. Euhedral crystals of accessory opaque mineral (magnetite?) are common.

WKG13
(N 49°6'0.21'' E 16°10'41.08'', WK106, at the bottom of the gorge, between road and dam bank) 
Felsic S3 granulite with typical layering of several millimetres thin dark bands rich in biotite alternating with layers composed predominantly from quartz and feldspars. Garnet porphyroclasts with quartz and feldspar inclusions are evenly distributed throughout the rock. Both quartz and feldspars comprise the intermixed mylonitic matrix, while only quartz forms long recrystallized disc-shaped porphyroclasts aligned into foliation. Kyanite is replaced by sillimanite in the foliation defined by quartz discs and biotite.

WKG15
(N 49°6'9.18'' E 16°9'29.39'', WK179, outcrop in the forest road cutting on the left bank of the dam lake)
Light felsic S2 granulite sample with typical thin biotite-rich bands has almost a migmatitic appearance in hand specimen. Peak granulite mineral assemblage quartz + ternary feldspar + garnet and kyanite is slightly retrogressed. Garnet porphyroclasts with large inclusions of quartz and feldspar in quartzo-feldspathic matrix are consumed by biotite. Foliation is defined by elongation of garnet porphyroclasts, alignment of kyanite needles and biotite flakes growing along parallel grain boundaries.

WKG16 
(N 49°6'3.27'' E 16°9'46.49'', WK177, outcrop on the left dam bank, small cliff in the middle of the slope) 
Extra ultramylonitic felsic S2 granulite with intermixed quartz and feldspars matrix; average grain size ~ 50 μm. Garnet porphyroclasts (~ 0.5 mm) with quartz and feldspar inclusions are slightly retrogressed into biotite rims. Foliation is marked by biotite flakes evenly distributed in the matrix and also oriented non-retrogressed kyanite grains.

WKG17 
(N 49°6'10.91'' E 16°9'13.87'', WK101, outcrop on the left dam bank, large cliff in the slope) 
Darker variety of the felsic S3 granulite with granulite-facies mineral assemblage quartz + feldspars + garnet + kyanite + biotite. Strong foliation fabric is caused primarily by alignment of the garnet porphyroclasts, which are retrogressively consumed by biotite. Garnet forms often atoll structures with enclosed grains of quartz and plagioclase. Quartzo-feldspathic mylonitic groundmass is annealed into larger elongated crystals, from which lobate quartz grains are forming monomineralic elongated aggregates.