Central European Variscan Basement in the Outer Carpathians: A Case Study from the Magura Nappe, Outer Western Carpathians, Poland

: Exotic crystalline blocks within the Outer Carpathian ﬂysch have the potential to establish the nature of their eroded basement source(s) and thus to reconstruct the paleogeography of the Outer Carpathians. Petrological investigations (including mineral analyses) coupled with zircon and apatite U-Pb dating were performed on an exotic crystalline block within Eocene siliciclastic rocks in the Raˇca Zone of the Magura Nappe in the Outer Western Carpathians, Poland. This exotic block is a large (c. 1 m diameter) pink porphyritic granitoid block found in the Osielczyk Stream, southeast of Osielec village in the Makowski Beskid mountains. The timing of magmatic crystallization is constrained by a U-Pb zircon age of 315.9 ± 2.6 Ma (MSWD = 0.69), while inherited zircon cores yield Archean (c. 2780 Ma), Cadomian (541.8 ± 6.7 Ma; MSWD = 0.53), Devonian (417 ± 11 Ma; MSWD = 0.57) and Early Variscan (c. 374 Ma) ages. Apatites from the same sample yield a Tera Wasserburg lower intercept U-Pb age of 311.3 ± 7.5 (MSWD = 0.87). The granitoid exhibits geochemical characteristics typical of I-type granites and ε Nd (316 Ma) = 2.15 (with a T DM model age of 1.18 Ga) and 87 Sr/ 86 Sr (316 Ma) = 0.704710. These data suggest a likely source region in the Saxo-Danubian Granite Belt, which possibly formed the basement of the Fore-Magura Ridge.


Introduction
The Carpathians mountain chain in Central Europe stretches for more than 1300 km from the eastern Alps and the Vienna Basin to the iron Gate gorge on the river Danube. In the Central Carpathians, Variscan basement massifs are a defining characteristic, while the Outer Carpathians comprise a complex nappe system that formed from the Cretaceous through to Neogene time as a result of the collision of several microplates with the consolidated European Plate [1]. The Pieniny Klippen Belt separates the Central Carpathians from the Outer Carpathians. These nappes are built from sedimentary sequences deposited in the Carpathian basins in the western Tethys Ocean. The Carpathian basins themselves are comprised of two domains: the Silesian domain to the north and the Magura domain to the south, which includes the Magura Basin. The sedimentary sequences of the Magura Basin are now incorporated into the Magura Nappe, which is the largest and southernmost tectonic unit in the Outer Western Carpathians.
Detrital zircon and apatite dating are commonly employed in single-grain detrital provenance studies to yield information on the source area [2,3]. However, single-grain provenance studies often yield ambiguous information due to the presence of recycled components or far-traveled detritus and may not be representative of the region surrounding the depositional basin. Coarse blocks and cobbles in flysch deposits (e.g., transported

Microscopy
Petrographic analyses of thin sections were undertaken at the Institute of Earth Sciences in the University of Silesia in Katowice using an Olympus BX-51 microscope to constrain textural and microstructural relationships and to determine the presence of zircon. The petrographical observations were used to select representative samples for subsequent electron probe microanalysis and whole-rock geochemical analyses.

Microscopy
Petrographic analyses of thin sections were undertaken at the Institute of Earth Sciences in the University of Silesia in Katowice using an Olympus BX-51 microscope to constrain textural and microstructural relationships and to determine the presence of zircon. The petrographical observations were used to select representative samples for subsequent electron probe microanalysis and whole-rock geochemical analyses.

Whole-Rock Chemical and Isotope Analyses
Whole-rock analyses were undertaken by X-ray fluorescence (XRF) for major and large ion lithophile trace elements (LILE) and by fusion and ICP-MS for high field strength elements (HFSE) and rare earth elements (REE) at Bureau Veritas Minerals (Canada). Preparation involved lithium borate fusion and diluted digestions for XRF and lithium borate decomposition or aqua regia digestion for ICP-MS. Loss on ignition (LOI) was determined at 1000 • C. Uncertainties for most of the major elements are 0.01%, except for SiO 2, which is 0.1%. REE was normalized to C1 chondrite [18].
The Sm-Nd and Rb-Sr analytical work was performed at the Laboratory of Geochronology, Department of Lithospheric Research, University of Vienna. Results are based on IC-TIMS procedures. Sample digestion for Nd-Sr analysis was performed in Savillex ® beakers using an ultrapure 4:1 mixture of HF and HNO 3 for 10 days at 110 • C on a hot plate. For whole-rock powders, a minimum dissolution time of three weeks was applied to ensure maximum leaching of the REEs from a refractory material, such as zircon. After evaporating the acids, repeated treatment of the residue using HNO 3 and 6.0 N HCl resulted in clear solutions for all samples. The REE fraction was extracted using AG ® 50 W-X8 (200-400 mesh, Bio-Rad) resin and 4.0 N HCl. Nd was separated from the REE fraction using Teflon-coated HdEHP and 0.22 N HCl as the elution media. For Sr, element separation followed conventional techniques, using AG ® 50W-X8 (200-400 mesh, Bio-Rad) resin and 2.5 N HCl as eluants. Maximum total procedural blanks were <1 ng for Sr and 50 pg for Nd and were taken as negligible. Nd and Sr were run as metals on a Re double filament, using a ThermoFinnigan ® Triton MC TIMS. A 143 Nd/ 144 Nd ratio of 0.511841 ± 0.000005 (n = 5) and an 87 Sr/ 86 Sr ratio of 0.710259 ± 0.000005 (n = 5) was determined for the La Jolla (Nd) and the NBS987 (Sr) international standards, respectively, during the period of investigation. Within-run mass fractionation for Nd and Sr isotope compositions (IC) was corrected to 146 Nd/ 144 Nd = 0.7219 and 86 Sr/ 88 Sr = 0.1194, respectively. Uncertainties on the Nd and Sr isotope ratios are quoted typically as 2σ m .

Mineral Separation and Imaging
Zircon and apatite crystals were separated using standard density separation techniques (crushing, sieving, washing and panning). This separation was carried out at the Institute of Geological Sciences at the Polish Academy of Sciences, Kraków, Poland. The zircons were hand-picked under a binocular microscope, cast in 25 mm diameter epoxy resin mounts, and then ground and polished to expose the grain interiors. Mineral textures were then imaged using back-scattered electron (BSE) and cathodoluminescence (CL) detectors on a FET Philips 30 scanning electron microscope with a 15 kV accelerating voltage and a beam current of 1 nA at the Faculty of Natural Sciences, the University of Silesia in Katowice, Poland. LA-ICPMS U-Pb age data were acquired using a Photon Machines Analyte Excite 193 nm ArF excimer laser-ablation system with a HelEx 2-volume ablation cell coupled to an Agilent 7900 ICPMS at the Department of Geology, Trinity College Dublin. The instruments were tuned using NIST612 standard glass to yield Th/U ratios of unity and low oxide production rates (ThO + /Th + typically <0.15%). A repetition rate of 11 Hz and a circular spot of 24 µm were employed. A quantity of 0.4 L·min −1 He carrier gas was fed into the laser cell, and the aerosol was subsequently mixed with 0.6 L·min −1 Ar make-up gas and 11 mL·min −1 N 2 . Eleven isotopes ( 49 Ti, 91 Zr, 175 Lu, 202 Hg, 204 Pb, 206 Pb, 207 Pb, 208 Pb, 232 Th, 23 5U and 23 8U) were acquired during each analysis, which comprised 27 s of ablation and 12 s washout, the latter portions, of which were used for the baseline measurement. Data reduction of the raw U-Pb isotope data was performed through the "VizualAge" data reduction scheme [19] in the freeware IOLITE package [20]. Sample-standard bracketing was applied after the correction of downhole fractionation to account for long-term drift in isotopic or elemental ratios by normalizing all ratios to those of the U-Pb reference standards. Final age calculations were made using the Isoplot add-in for Excel [21]. 91500 zircon ( 206 Pb/ 238 U TIMS age of 1065.4 ± 0.6 Ma; [22]) was used as the primary U-Pb calibration standard. The secondary standards GZ-7 zircon ( 206 Pb/ 238 U TIMS age of 530.26 Ma ± 0.05 Ma; [23]), Plešovice zircon ( 206 Pb/ 238 U TIMS age of 337.13 ± 0.37 Ma; [24]) and WRS 1348 zircon ( 206 Pb/ 238 U TIMS age of 526.26 ± 0.70; [25]) yielded LA-ICPMS ages of 532.0 ± 2.2 Ma, 337 ± 1.6 Ma and 528.4 ± 3.2 Ma, respectively.

Apatite U-Pb Dating
Apatite crystals were as separates on polished epoxy mounts. U-Pb and REE data were acquired using a laser ablation system (Photon Machines Analyte Excite 193 nm ArF Excimer) coupled to an Agilent 7900 Q-ICPMS at the Department of Geology, Trinity College Dublin. Twenty-nine isotopes ( 31 P, 35 Cl, 43 Ca, 51 V, 55 232 Th and 238 U were acquired using a 60 µm laser spot, a 11 Hz laser repetition rate and a fluence of 2.5 J/cm 2 . A~1 cm sized crystal of Madagascar apatite, which has yielded a weighted average ID-TIMS concordia age of 473.5 ± 0.7 Ma, was used as the primary apatite reference material in this study. McClure Mountain syenite apatite (the rock from which the 40 Ar/ 39 Ar hornblende standard MMhb is derived) and Durango apatite were used as secondary standards. McClure Mountain syenite has moderate but reasonably consistent U and Th contents (~23 ppm and 71 ppm, [26]) and its thermal history, crystallization age (weighted mean 207 Pb/ 23 5U age of 523.51 ± 2.09 Ma) and initial Pb isotopic composition ( 206 Pb/ 204 Pb = 17.54 ± 0.24; 207 Pb/ 204 Pb = 15.47 ± 0.04) are known from high-precision ID-TIMS analyses [27]. NIST 612 standard glass was used as the apatite trace-element reference material, and a crushed aliquot of Durango apatite that has been characterized by solution quadrupole-ICP-MS analyses [28] was used as the apatite trace-element secondary standard.
The raw isotope data were reduced using a modified version of the "Vizual Age" data reduction scheme [19] of the freeware IOLITE package of [25]. This data-reduction scheme ("VizualAge_UcomPbine") can account for the variable common Pb in the apatite [29]. User-defined time intervals are established for the baseline correction procedure to calculate session-wide baseline-corrected values for each isotope. The time-resolved fractionation response of individual standard analyses is then characterized using a userspecified down-hole correction model (such as an exponential curve, a linear fit or a smoothed cubic spline). The data-reduction scheme then fits this appropriate session-wide "model" U-Th-Pb fractionation curve to the time-resolved standard data and the unknowns. Sample-standard bracketing is applied after the correction of down-hole fractionation to account for long-term drift in isotopic or elemental ratios by normalizing all ratios to those of the U-Pb reference standards. Common Pb in the apatite standards and unknowns was corrected using a 207 Pb-based correction in VizualAge_UcomPbine and included the propagation of the uncertainties in the age of the reference materials. Over the course of analyses, McClure Mountain apatite ( 207 Pb/ 235 U TIMS age of 523.51 ± 2.09 Ma; [27]) and Durango apatite (31.44 ± 0.18 Ma; [30]) yielded weighted average 207 Pb-corrected ages of 517.5 ± 3.5 Ma (MSWD = 2.3) and 31.82 ± 0.41 Ma (MSWD = 1.9), respectively. The McClure Mountain apatite age was anchored using a 207 Pb/ 206 Pb value of 0.88198 derived from an apatite ID-TIMS total U-Pb isochron [27]. All apatite REE contents were normalized to C1 chondrite [18].

Petrography, Mineral Chemistry and Whole-Rock Chemistry of Granitoid Exotic Block
Two samples of pink porphyritic granitoid (OS-1 and OS-2; Figure 2a) were collected from one block. The rock is composed of perthitic K-feldspar phenocrysts up to 5 cm long, which usually show twinning (Figure 2b). The barium content ranges from 0.56 to 2.06 wt % and shows oscillatory zonation, with a general decrease in Ba contents towards the rim (Figure 2b). Locally anti-rapakivi structures are observed, characterized by K-feldspar overgrowths on plagioclase. The plagioclase is oligoclase (An [11][12][13][14][15][16][17]. Biotite exhibiting green pleochroism is enriched in Mg (#mg = 0.54-0.57; Table 1) and weakly chloritized. No muscovite was noted, but amphibole (Mg-hornblende; Table 2) intergrown with REEbearing titanite (Table 3) is present. Accessory phases are represented by chemically zoned pyrite, mostly replaced by secondary hydroxides (Ca,F)-apatite enriched in REE and zoned in respect of these elements (Table S1) and zircon. Secondary epidote (Table 3) and hematite are also found.    The granitoid from Osielec is weakly peraluminous, with Aluminium Saturation Index (ASI) at 1.05 and 1.08; (Table 4) and plot in the Q-monzonite transitional to granite field and belong to the high-K calc-alkaline series (Figure 3a,b). It is enriched in REE (∑ REE = 248 and 351.69; Table 4) and REE patterns are steeply inclined (Ce N /Yb N = 24.81 and 36.38) with a very flat Eu anomaly (Eu/Eu* = 0.92 and 0.83; Table 5; Figure 3c). The Rb/Sr ratio is moderate (0.1 and 0.12), and thorium is strongly enriched over uranium (Th/U = 12.7 and 23.6). Zircon saturation temperatures calculated on the basis of the whole-rock Zr content [31] yield temperatures of 814 • C and 853 • C (Table 4), while amphibole thermometry [32] yields a temperature range of 745-780 • C at pressures from 730 to 920 MPa and a log O 2 of c. −13 (Table 2).     [34]; (c) chondrite (C1)-normalized REE patterns of the granitoid from Osielec and apatite from the sample (gray area); (d) primitive mantle normalized multielement patterns of the analyzed exotic block from Osielec stream. Normalization values after [18], gray field-analyses from [35].

Zircon Morphology and U-Pb Dating
Zircon crystals from sample OS-1 are clear, colorless or yellow to gray, with aspect ratios ranging from 1.5:1 to 3:1 and long axes ranging from 50 to 180 µm. Cathodoluminescence (CL) imaging reveals the presence of magmatic oscillatory zoning, locally overgrowing inherited cores showing bright luminescence ( Figure 4). Inherited zircon cores yield a large range in concordant ages. Single inherited cores yield 206 Pb/ 238 U ages of 2772 ± 59 Ma, 629 ± 11 Ma and 378.7 ± 4.8 Ma, while two small groups of three inherited cores each yield the concordia ages of 541.8 ± 6.7 Ma (MSWD = 0.53), and 417 ± 11 Ma (MSWD = 0.57; Figure 5a; Table 5). Three grains with oscillatory magmatic zonation and six oscillatory zoned rims on the inherited cores yield an age of 315.9 ± 2.6 Ma (MSWD = 0.69; Figure 5b; Table 5). One concordant analysis with large uncertainty was also determined but supported this late Variscan age. Th/U ratios range from 0.10 to 1.14 (   Table 6) are marked as circles.  Table 6) are marked as circles.

Petrogenetic Interpretation
The granitoid from Osielec belongs to the high-K-calc-alkaline series (Figure 3b) and plots in the Volcanic Arc Granite (VAG) field ( Figure 6). On a primitive mantle-normalized multielement diagram (Figure 3d (Table 6) imply a mantle-related affinity of the parent magma. The high Th/U ratio in the whole-rock samples, in zircon (Table 5) and in apatite (Table S1) suggests a Th-enriched mantle and/or fluid influence during magma formation [36]. The T DM model age of 1.18 Ga (Table 6) is younger than the crustal residence ages typical of the Variscan fold belt of Europe (1.4-1.8 Ga; [37]), as most of the post-tectonic granites in the Variscan belt of Europe reflect the mixture of Cadomian/Caledonian and Paleoproterozoic source involvement [38]. The presence of inherited cores in the zircon crystal population covers a wide age range from c. 2772 Ma to c. 417 Ma and support this interpretation. A minimum closure temperature of c. 900 • C is assumed for Pb diffusion in zircon, while the Pb partial retention zone is c. 450-550 • C in apatite [39][40][41]. Therefore, the zircon and apatite U-Pb ages overlap within age uncertainty suggesting relatively fast cooling, inconsistent with monotonic thermal relaxation of a pluton at depth. Therefore, the mantle-derived magma intrusion either intruded at a shallow crustal level and/or was rapidly exhumed during cooling. Such a scenario is typical of post-collisional mantle lithosphere delamination. This process is common in the late-Variscan evolution of the Central European Orogenic Belt ( [42,43] and references therein) and is assumed responsible for the emplacement of voluminous I-type granitoids associated with the rapid exhumation and a low-pressure-high-temperature metamorphic overprint. The high Th/U ratios found in the analyzed zircon crystals (Table 6), both in the magmatically zoned rims and in the cores, are typical of the magmatic process [44] and exclude metamorphic overprinting.

Source Region of the Exotic Clasts
Exotic blocks are only sporadically found within the Magura Nappe. The available age data include a metadiorite-metagabbro dated at c. 614 Ma [7,9], centimeter-scale mica-schist pebbles from the Tylicz and Krynica Zone dated at 310 ± 10 Ma using the U-Th-Pb CHIME method on monazite [45] and the porphyritic granite dated in this study at 315.9 ± 2.6 Ma. The presence of clasts of both Neoproterozoic ocean floor remnants (gabbro-diorite) and Late Variscan I-type granites and metapelitic rocks suggests that the Fore-Magura Ridge could contain fragments of the Neoproterozoic basement, locally intruded and thermally metamorphosed by the Variscan granites. The Cadomian age of the inherited zircon cores in the investigated granitoid (541.8 ± 6.7 Ma; Table 5, Figure 5a), together with the presence of blocks of Neoproterozoic age (c. 614 Ma; [7]), suggest that peri-Gondwana basement was incorporated within this Variscan tectono-magmatic belt, as has been documented in many segments of the Variscan orogen (cf. [46][47][48]). No granites with similar zircon U-Pb ages and petrological characteristics have been noted in the Central Western Carpathians, in the Silesian and Subsilesian Nappes of the Outer Carpathians, or in Brunovistulia and the Małopolska Block. This, together with the lack of detrital fragments from the Pieniny Klippen Belt [45], implies there was no link between the Central Carpathians and Outer Carpathian basins during the Cretaceous to Paleogene. There is also no correlation between the basement of the Magura Nappe and the Silesian and Subsilesian Nappes. Magura Ridge could contain fragments of the Neoproterozoic basement, locally intruded and thermally metamorphosed by the Variscan granites. The Cadomian age of the inherited zircon cores in the investigated granitoid (541.8 ± 6.7 Ma; Table 5, Figure 5a), together with the presence of blocks of Neoproterozoic age (c. 614 Ma; [7]), suggest that peri-Gondwana basement was incorporated within this Variscan tectono-magmatic belt, as has been documented in many segments of the Variscan orogen (cf. [46][47][48]). No granites with similar zircon U-Pb ages and petrological characteristics have been noted in the Central Western Carpathians, in the Silesian and Subsilesian Nappes of the Outer Carpathians, or in Brunovistulia and the Małopolska Block. This, together with the lack of detrital fragments from the Pieniny Klippen Belt [45], implies there was no link between the Central Carpathians and Outer Carpathian basins during the Cretaceous to Paleogene. There is also no correlation between the basement of the Magura Nappe and the Silesian and Subsilesian Nappes. Figure 6. Plot of the granitoid from Osielec stream on the discrimination diagram of [49]: VAGvolcanic arc granites; syn-COLG-syn-collisional granites, WPG-within-plate granites, ORGocean ridge granites.
Similar U-Pb ages and geochemical characteristics to the Osielec granitoid samples investigated in this study are exhibited by the Saxoturingian and Moldanubian granites in the Saxo-Danubian Granite Belt (SDGB), such as the Falkenberg and Liebenstein granites (dated at 330-310 Ma, [50,51] and references therein), the Strzelin granites (Oberc-Dziedzic et al. 2016 [52] and references therein) and the Karkonosze granite [53]. The Karkonosze granite is an unlikely source taking into account its paleogeographic position [54]. As the youngest varieties (315-310 Ma) of the SDGB granitoids are fine-to mediumgrained S-type migmatitic granites, we propose that a more likely source is the older (320-328 Ma), genetically mixed (S/I) type) coarse-grained granitoids with K-feldspar phenocrysts in the SDGB, with geochemical features indicative of mantle delamination or a slabbreak-off origin [35,52]. The first model is more preferred for the South Bohemian Massif, with assumed lithosphere thinning and extension, followed by mantle melting [54]. These processes produced mantle-type melts up to c. 305 Ma and were followed by transtension in the Central European segment of Variscides [55]. The metagabbro-metadiorite exotic blocks [7] could have counterparts in the Cadomian mafic intrusions, which are found at the Moldanubian-Moravian Unit boundary ( [51,56] and references therein). The Moldanubian zone, originally described in the southern part of the Bohemian Massif between the Vltava (Moldau) and Danube rivers, probably extended westwards into the Black Forest in Germany, the southern Vosges Massif, the Massif Central, Nort-sur-Erdre; the South Armorican unit in France and into the Galicia-Trás-os-Montes zone in Spain (Figure 7). It  [50,51] and references therein), the Strzelin granites (Oberc-Dziedzic et al. 2016 [52] and references therein) and the Karkonosze granite [53]. The Karkonosze granite is an unlikely source taking into account its paleogeographic position [54]. As the youngest varieties (315-310 Ma) of the SDGB granitoids are fine-to medium-grained Stype migmatitic granites, we propose that a more likely source is the older (320-328 Ma), genetically mixed (S/I) type) coarse-grained granitoids with K-feldspar phenocrysts in the SDGB, with geochemical features indicative of mantle delamination or a slab-break-off origin [35,52]. The first model is more preferred for the South Bohemian Massif, with assumed lithosphere thinning and extension, followed by mantle melting [54]. These processes produced mantle-type melts up to c. 305 Ma and were followed by transtension in the Central European segment of Variscides [55]. The metagabbro-metadiorite exotic blocks [7] could have counterparts in the Cadomian mafic intrusions, which are found at the Moldanubian-Moravian Unit boundary ( [51,56] and references therein). The Moldanubian zone, originally described in the southern part of the Bohemian Massif between the Vltava (Moldau) and Danube rivers, probably extended westwards into the Black Forest in Germany, the southern Vosges Massif, the Massif Central, Nort-sur-Erdre; the South Armorican unit in France and into the Galicia-Trás-os-Montes zone in Spain (Figure 7). It also includes Corsica and the external crystalline massifs of the Alps. The ophiolitic parts of the Moldanubian zone represent a probable oceanic realm, the so-called Galicia-Moldanubian Ocean, which connected the eastern and western parts of the Paleotethys Ocean [57,58]. also includes Corsica and the external crystalline massifs of the Alps. The ophiolitic parts of the Moldanubian zone represent a probable oceanic realm, the so-called Galicia-Moldanubian Ocean, which connected the eastern and western parts of the Paleotethys Ocean [57,58].   The exotic rocks deposited in the Magura Basin constituted part of the Alpine Tethys [14]. Based on models recently applied to the Alps, we can link the formation of this basin to strike-slip transform faulting, which occurs in the Early to Middle Jurassic that resulted in the opening of the South Penninic-Piedmont-Ligurian Ocean ( [59,60] and references therein). The Magura Ocean has been suggested to be an eastern prolongation of that ocean.
As a result of Alpine compression, the ridges separating the Carpathian subbasins were uplifted and inverted during the Late Cretaceous to Paleogene. These ridges from north to south comprise the Sub-Silesian, Silesian and Fore-Magura Ridges ( [60,61] and references therein) (Figure 8a,b). Intensive erosion of the ridges, driven by tectonic uplift, resulted in the transport of the crystalline basement as clastic material to the basins, locally as olistostromes.
The Fore-Magura Ridge developed within the northern part of the Magura Domain during the Late Cretaceous [14,62]. This ridge was eroded during the Paleogene, exposing the crystalline basement. In the Magura Basin, sediment transport was likely derived from the Fore-Magura Ridge (Figure 8c; [9,63,64]). The distribution of exotic crystalline clasts reflects the zonation of the Variscan orogen in the Outer Carpathians. The southern zone (Foremagura Ridge) represents the internal core of the Variscan collisional orogen, while the northern zone (Silesian Ridge and Outer Carpathian Basement) represents the Variscan foreland built of Neoproterozoic rocks. As the large exotic blocks are assumed to have not been transported for significant distances, we infer that the crystalline basement of the Fore-Magura Ridge is comprised of Moldanubian Unit rocks.

ocean.
As a result of Alpine compression, the ridges separating the Carpathian subbasins were uplifted and inverted during the Late Cretaceous to Paleogene. These ridges from north to south comprise the Sub-Silesian, Silesian and Fore-Magura Ridges ( [60,61] and references therein) (Figure 8a,b). Intensive erosion of the ridges, driven by tectonic uplift, resulted in the transport of the crystalline basement as clastic material to the basins, locally as olistostromes.

Conclusions
The main conclusions arising from this study are: (1) The exotic block from Osielec represents an I-type, oxidized mantle-related late Variscan (post-orogenic) granitoid, probably related to magmatic underplating. The timing of crystallization is constrained by a U-Pb zircon date of 315.9 ± 2.6 Ma, while a U-Pb apatite age of 311.3 ± 7.5 Ma, which overlaps within age uncertainty, implies rapid cooling.
(2) As the large exotic blocks are not far traveled, the presence of this late Variscan granite clast in the Fore-Magura Ridge implies an affinity with the Moldanubian Unit (Saxo-Danubian Granite Belt) in the Central European Variscides.