Lead isotope evolution of the Central European upper mantle: Constraints from the Bohemian Massif

Research Paper Lead isotope evolution of the Central European upper mantle: Constraints from the Bohemian Massif Simona Krmí ckov a a , b , Luk a s Krmí cek a , b , c , * , Rolf L. Romer d , Jaromír Ulrych b a Department of Geological Sciences, Faculty of Science, Masaryk University, Kotl a rsk a 2, CZ-611 37, Brno, Czech Republic b Institute of Geology of the Czech Academy of Sciences, Rozvojov a 269, CZ-165 02, Prague 6, Czech Republic c Brno University of Technology, Faculty of Civil Engineering, AdMaS Centre, Veve rí 95, CZ-602 00, Brno, Czech Republic d Deutsches GeoForschungsZentrum GFZ, Telegrafenberg, D-144 73, Potsdam, Germany ARTICLE INFO Handling Editor: Christopher J Spencer Keywords: Lead isotopes Lamprophyres Volcanic rocks Mantle components Bohemian massif Variscan orogeny ABSTRACT The Pb isotope composition of the upper mantle beneath Central Europe is heterogeneous due to the subduction of regionally contrasting material during the Variscan and Alpine orogenies. Late Variscan to Cenozoic mantlederived melts allow mapping this heterogeneity on a regional scale for the last ca. 340 Myr. Late Cretaceous and Cenozoic anorogenic magmatic rocks of the Bohemian Massif (lamprophyres, volcanic rocks of basanite/ tephrite and trachyte/phonolite series) concentrate mostly in the Eger Rift. Cretaceous ultramafic lamprophyres yielded the most radiogenic Pb isotope signatures reflecting a maximum contribution from metasomatised lithospheric mantle, whereas Tertiary alkaline lamprophyres originated from mantle with less radiogenic 206 Pb/ 204 Pb ratios suggesting a more substantial modification of lithospheric source by interaction with asthenosphericderived melts. Cenozoic volcanic rocks of the basanite/tephrite and trachyte/phonolite series define a linear mixing trend between these components, indicating dilution of the initial lithospheric mantle signature by upwelling asthenosphere during rifting. The Pb isotope composition of Late Cretaceous and Cenozoic magmatic rocks of the Bohemian Massif follows the same Pb growth curve as Variscan orogenic lamprophyres and lamproites that formed during the collision between Laurussia, Gondwana, and associated terranes. This implies that the crustal Pb signature in the post-Variscan mantle is repeatedly sampled by younger anorogenic melts. Most Cenozoic mantle-derived rocks of Central Europe show similar Pb isotope ranges as the Bohemian Massif. 1. Introduction Central Europe has been affected by two major extensional events of Permo-Carboniferous and Tertiary age (e.g., Meier et al., 2016). Permo-Carboniferous extension began in Central Europe because of post-collisional changes in the kinematics between the Laurussia and the Gondwana plates (Kroner et al., 2016) and resulted in the formation of the Central European Extensional Province (CEEP) with numerous volcano-sedimentary basins in Europe as well as the Oslo Rift (e.g., Neumann et al., 2004; Wilson et al., 2004). This extension was coeval with the opening of the Palaeo-Tethys Ocean farther to the east and the closure of the remaining Rheic Ocean farther to the west (Kroner and Romer, 2013). Late Cretaceous to Tertiary lithospheric extension was initiated as a response to the tensional reactivation of Variscan Permo-Carboniferous fracture systems by the Alpine collision, eventually resulting in the formation of a vast rift system in Western and Central Europe. The European Cenozoic rift system includes the following individual rifts: Valencia Trough in Spain, the Gulf of Lions, the Sa^ one, Limagne and Bresse grabens in south-eastern France, the Rhine, Ruhr and Leine grabens in Germany, and the Eger Rift in the Bohemian Massif (Ziegler, 1992,Fig. 1). Formation of continental rift systems associated with horizontal movements of plates and subsequent lithosphere thinning is commonly accompanied with magma generation by decompression melting of lithospheric and asthenospheric mantle that is passively upwelling beneath the thinned lithosphere (e.g., Berkesi et al., 2019). Melts generated in rifts by decompression are separated from their residue and ascend from the zone of melting in the upper mantle and are emplaced within the overlying continental crust or are extruded as lava flows. The volume of the produced melts depends on the amount of lithospheric * Corresponding author. Institute of Geology of the Czech Academy of Sciences, Rozvojov a 269, CZ-165 02, Prague 6, Czech Republic. E-mail address: [email protected] (L. Krmí cek). Peer-review under responsibility of China University of Geosciences (Beijing). HOSTED BY Contents lists available at ScienceDirect Geoscience Frontiers journal homepage: www.elsevier.com/locate/gsf https://doi.org/10.1016/j.gsf.2019.09.009 Received 27 April 2019; Received in revised form 2 August 2019; Accepted 25 September 2019 Available online 23 October 2019 1674-9871/©2019 China University of Geosciences (Beijing) and Peking University. Production and hosting by Elsevier B.V. This is an open access article under the CC BY-NC-ND license (http://creativecommons.org/licenses/by-nc-nd/4.0/). Geoscience Frontiers 11 (2020) 925–942 extension and on the temperature of the asthenosphere. The primary products of volcanic activity in rifts are mainly basaltic. Continental intra-plate rifting produces predominantly olivine/nepheline-bearing alkaline basalts (e.g., White and McKenzie, 1989; Wilson and Downes, 1992; Lustrino and Wilson, 2007; Haase and Renno, 2008). For the Cenozoic rift system of the Central European Volcanic Province (CEVP), there are two end-member type models. Some authors favour asthenospheric melting in response to large-scale upwelling of mantle plumes or small-scale plumelets (e.g., Wilson and Downes, 1991; Hegner et al., 1995). Other studies favour derivation of the intraplate volcanic rocks from the metasomatised lithospheric mantle, either by preferential melting of phlogopite/amphibole-bearing vein assemblages hosted in lherzolitic mantle or by very low degree melting of highly metasomatised domains, resulting in the generation of strongly SiO 2 -undersaturated melts (Hegner et al., 1995; Jung et al., 2005; Pf€ ander et al., 2018). Late Variscan to Cenozoic mantle-derived rocks, such as lamprophyres, lamproites, and alkali-basalts, largely sampled the same mantle on a regional scale and at variable depth during above mentioned extensional events (e.g., Mayer et al., 2014; Krmí cek et al., 2016; Ulrych et al., 2018). Although mantle-derived lamprophyres and associated intrusive rocks are relatively rare within the volcanic complexes, these small-volume melts are particularly important for studying processes and geochemical heterogeneities of the upper mantle beneath Central Europe as they preferentially sample the metasomatic component, which was induced during the Variscan orogeny when continental collision brought continental crust to mantle depth (e.g., Kroner and Romer, 2013; Borghini et al., 2018; Pf€ ander et al., 2018). The Sr, Nd, and Pb isotope composition of mantle-derived rocks may identify contributions from different mantle sources, such as depleted asthenospheric and enriched lithospheric upper mantle and lower mantle, to the generated magmas (e.g., White and McKenzie, 1989; Zou et al., 2000). Isotope constraints on the mantle sources of Mesozoic and Cenozoic volcanic rocks of the Bohemian Massif largely rely on Sr–Nd isotope data (e.g., Alibert et al., 1983, 1987; Blusztajn and Hart, 1989; Bendl et al., 1993; Vokurka, 1997; Ulrych et al., 2002, 2008, 2011, 2013, 2016, 2018; Haase and Renno, 2008; Cajz et al., 2009; Sk ala et al., 2014, 2015). In contrast, Pb isotope data are rare (Blusztajn and Hart, 1989; Fig. 1. (A) Distribution of major volcanic areas within Central Europe (modified after Blusztajn and Hegner, 2002); EL –Elbe Line, OFZ –Odra Fault Zone. (B) Map of volcanic centres in the Eger Rift with sampling areas (modified after Zachari a s et al., 2008). Abbreviations: BRB –Berzdorf Radomierzyce Basin; CDG –Cheb–Doma zlice Graben; CSVC –  Cesk e St redoho rí Volcanic Complex; DHVC –Doupovsk e Hory Volcanic Complex; MB –Most Basin; RPVC – Ralsk a Pahorkatina Volcanic Complex; SB –Sokolov Basin; ZB –Zittau Basin. S. Krmí ckov a et al. Geoscience Frontiers 11 (2020) 925–942 926 Haase and Renno, 2008; Ulrych et al., 2016). As typical mantle has low Pb contents, the Pb isotope composition of the mantle is readily affected during metasomatism. Because of the contrasting Pb contents in crust and mantle rocks, small contributions of continental material are more sensitively recorded in the Pb isotope composition than in the Sr and Nd isotope composition (Cohen and O’Nions, 1982; Davies and Macdonald, 1987; Sun and McDonough, 1989; Conticelli et al., 2002). Our paper focuses on Pb isotope data and whole-rock geochemistry of intrusive and extrusive volcanic rocks of the Bohemian Massif that sampled the upper mantle. We pay special attention whether Late Palaeozoic to Quaternary Central European mantle-derived rocks sampled different mantle sources on a local to regional scale and through time. 2. Geological setting The upper mantle beneath Central Europe is heterogeneous, which is largely due to Variscan and Alpine subduction events during which regionally contrasting subducted material of both continental and oceanic crust metasomatically modified the upper mantle (e.g., Witt-Eickschen and Kramm, 1997; Downes, 2001; Ackerman et al., 2009; Kroner and Romer, 2013; Pf€ ander et al., 2018). Older tectonic structures reactivated during the late Variscan to Alpine events were associated with asthenospheric upwelling and subsequent extension-related magmatism that sampled this modified mantle (Wilson and Downes, 1991). 2.1. Variscan to post-Variscan development The Variscan orogen is the result of the Devonian–Carboniferous collision of Gondwana with Laurussia that started with the collision of the Armorican Spur, which is part of segmented peri-Gondwana. The collision of the Armorican Spur with Laurussia resulted in the closure of the Rheic Ocean in the area of future Central Europe (Kroner and Romer, 2010, 2013). The subducted material consisted primarily of relative thin lithosphere covered by Palaeozoic volcano-sedimentary rocks (Kroner et al., 2007). In contrast, the unsubductable parts of the peri-Gondwana (Cadomian) magmatic arc (i.e., thick crustal fragments of the Armorican Spur) caused reorganisation within the plate boundary zone (Kroner and Romer, 2013). The Bohemian Massif consists of highand low-strain domains that behaved differently during the Variscan orogeny. The Tepl a-Barrandian Unit and Lusatia (parts of Gondwana) and the Brunovistulian Terrane (part of Laurussia) are low-strain domains that collided during the closure of the Rheic ocean (e.g., Kalvoda et al., 2008; Kalvoda and B abek, 2010). The Saxo-Thuringian and Moldanubian Zones are high-strain domains that represent former Gondwana shelf and that were subducted and exhumed during the Variscan orogeny (e.g., Kroner and Romer, 2013; Krmí cek et al., 2016;  Z ak and Sl ama, 2018). Plate tectonic processes that may have changed the composition of the upper mantle of the Bohemian Massif include (i) Cadomian subduction followed by Late Neoproterozoic back-arc spreading and early Palaeozoic rifting in northern peri-Gondwana, (ii) intra-oceanic subduction and formation of oceanic arcs that were later accreted to form part of Variscan Europe, (iii) possible subduction beneath the northwards migrating terranes, (iv) subduction and collision at the southern margin of Laurussia, and (v) Carboniferous extension of Central Europe (Wilson et al., 2004; McCann et al., 2006; Pin and Waldhausrov a, 2007; Timmerman, 2008; Abdelfadil et al., 2013; Dostal et al., 2019a,b). Subduction of both oceanic and continental crust peaked at 340 Ma and led to the establishment of isotopically contrasting domains in the metasomatised lithospheric mantle (Krmí cek et al., 2016). During the late stage of the Variscan orogeny, these metasomatised mantle domains underwent partial melting resulting at ca. 340–300 Ma in the intrusion of potassic to ultrapotassic dykes (lamprophyres and lamproites) along deep-fault zones related to initial crustal extension eventually leading to the formation of the CEEP (Awdankiewicz, 2007, 2009; Krmí cek et al., 2011, 2014, 2016; Abdelfadil et al., 2013; Hrouda et al., 2016). Post-Variscan magmatic activity throughout Variscan Europe was associated with the extension of thickened Variscan crust and accompanied by progressively increasing contributions from the asthenospheric mantle (Lorenz and Nicholls, 1984; Timmerman et al., 2009). Permian extension led to the formation of rift basins, such as the North Germany Basin or the Oslo Rift (Benek et al., 1996; McCann et al., 2006). 2.2. Mesozoic to Cenozoic development Within the framework of the African–Eurasian plate collision, the extensive European Cenozoic Rift System (ECRIS) formed in Western and Central Europe stretching from Spain and France through Germany to the Czech Republic and Poland (Prodehl et al., 2006). The ECRIS recorded intermittent sub-volcanic/volcanic activities that started in the Late Cretaceous and have lasted to the present (Lustrino and Wilson, 2007). Episodic volcanism occurred mainly in the Oligocene to Miocene with waning phases of anorogenic volcanic activity reaching to the Plio-Pleistocene (Nowell et al., 2006). Magmatic activity in the ECRIS is concentrated in intrusive complexes and volcanic fields within the grabens and their shoulders (Fig. 1A). Rifts formed at reactivated Variscan suture zones separating large different lithospheric segments, indicating structural control on the location of Cenozoic volcanic activity (D ezes et al., 2004). The Bohemian Massif is transected by the nearly 300 km long ENE–WSW trending Eger Rift, by the transverse NW–SE striking Elbe/ Labe–Odra Fault System in the north (Fig. 1A), and by the NW–SE trending Cheb–Doma zlice Graben in the west (  Spa cek et al., 2011). The Eger Rift represents the easternmost part of the Cenozoic rift system of the Central European Volcanic Province (e.g., Ziegler, 1994; Lustrino and Wilson, 2007). The magmatic rocks of the Eger Rift are predominantly SiO 2 -undersaturated alkaline rocks of intra-plate origin (Ulrych et al., 2002,2011;Lustrino and Wilson, 2007; Dostal et al., 2017). The volcanic activity is a result of reactivation of Variscan structures in the Bohemian Massif during the Alpine orogeny (Babu ska and Plomerov a, 1992, 2001, 2010). Whether the model of mantle plumes sensu Wilson and Paterson (2001), with Alpine flexure and lithospheric extension followed by adiabatic decompression, decompression melting, and injection of mantle-derived magmas into the crust, played a major role is debated (Wilson and Downes, 1991; Wedepohl et al., 1994; Lustrino and Wilson, 2007; Ulrych et al., 2011) and is reflected in terms like Common Mantle Reservoir (CMR –Lustrino and Wilson, 2007) or European Asthenospheric Reservoir (EAR –Cebri a and Wilson, 1995) used to characterise magmas from a possible sub-lithospheric source region. Ulrych and Pivec (1997) and Ulrych et al. (2011) defined three phases of Cenozoic volcanic activity based on K–Ar dating and palaeostress mapping: (i) a pre-rift period (~80–49 Ma), (ii) a syn-rift period (42–16 Ma) and (iii) a late-rift period (16–0.26 Ma). Ulrych and Pivec (1997) also defined two coeval alkaline series: (i) a volumetrically dominant nephelinite–basanite–tephrite–phonolite series of strongly to mildly alkaline rocks and (ii) a subordinate and only locally occurring weakly alkaline alkali basalt–trachybasalt–trachyandesite–trachyte–rhyolite series. The Eger Rift comprises several volcanic centres (Fig. 1B), namely the  Cesk e St redoho rí Volcanic Complex (CSVC), the Doupovsk e Hory Volcanic Complex (DHVC; access to volcanic edifice exposures is restricted as they are predominately located in the Doupovsk e Hory military training zone), the Ralsk a Pahorkatina Volcanic Complex (RPVC) and a great number of isolated volcanoes in the western part of the Bohemian Cretaceous Basin and in the Cheb–Doma zlice Graben (CDG). The youngest volcanoes occur in the Cheb/Eger Basin, a sub-basin of the Eger Rift. The first manifestation of volcanic activity in the Eger Rift is Late Cretaceous ultramafic lamprophyres and related melilitic rocks associated with subsurface intrusion of melilitolite composition that occur near the intersection of the marginal fault of the Eger Rift and the Lusatian Fault within the future RPVC in the northern part of the Bohemian Cretaceous Basin (Ulrych et al., 2014). Most of the Cenozoic volcanic rocks, predominantly of basanitic composition, are concentrated in the S. Krmí ckov a et al. Geoscience Frontiers 11 (2020) 925–942 927 CSVC and DHVC, whereas hypabyssal intrusions spatially associated with alkaline lamprophyre dykes of Cenozoic age are restricted to the CSVC and RPVC (Sk ala et al., 2014). Sr-Nd-(Pb)-isotope compositions of rocks from the western Eger Rift, i.e., the DHVC and CDG, were recently published by Ulrych et al. (2016) and Haase et al. (2017). For locations of investigated samples and characteristics of sampled areas see Fig. 1B and Supplement A. 3. Methods Representative samples of the studied volcanic and subvolcanic rocks are described petrographically using conventional optical microscopy and characterised geochemically by whole-rock and mineral composition using ICP-ES, ICP-MS, and electron microprobe, respectively. Whole-rock chemical analyses from fresh samples lacking signs of alteration or wall-rock assimilation were carried out at Bureau Veritas (former ACME) Analytical Laboratories Ltd. (Vancouver, Canada) using inductively coupled plasma emission spectrometry (ICP-ES; major oxides, Ba, Ni, Cu, Pb, Zn) and inductively coupled plasma mass spectrometry (ICPMS; Co, Cs, Hf, Nb,Rb, Sr,Ta, Th, U, V, Zr, Y andREE). Loss on ignition(LOI) was determined by weight difference after ignition at 1000 C. The Pb, U, and Th concentrations are used to recalculate the initial Pb isotope composition. The errors for the Pb, U and Th concentrations correspond to 0.1 ppm, 0.1 ppm, and 0.2 ppm, respectively. For further analytical details and detection limits see www.acmelab.com. The composition of characteristic dark minerals (amphibole, clinopyroxene, and mica) was analysed using a CAMECA SX 100 electron microprobe (Institute of Geology of the CAS, Prague) operated in wavelengthdispersive mode. Measurements were performed using a 15 keV acceleration voltage, 10 nA beam current and 2 μ m beam diameter. Both natural and synthetic minerals were used as reference standards. Concentrations of following elements were measured (standard, spectrometer crystals and detection limit for analysed elementsare given in parentheses):Si (diopside, LTAP, 222 ppm), Ti (rutile, LPET,357 ppm), Al(jadeite, LTAP, 272 ppm), Cr (Mn–Cr spinel, LIF, 910 ppm), Fe (haematite, LIF, 1047 ppm), Mn (rhodonite, LIF, 965 ppm), Ni (Ni 2 Si, LTAP, 1404 ppm), Mg (periclase, LTAP, 422 ppm), Ca (diopside, LPET, 341 ppm), Na (jadeite, LTAP, 262 ppm), K (leucite, LPET, 300 ppm), F (fluorite, PC0, 1575 ppm), Cl (tugtupite, LPET, 320 ppm), Rb (RbCl, LTAP, 217 ppm) and Ba (barite, LPET, 503 ppm). Countingtimeson peaks were 10 s for Mg,Al,K, Ca, Cl, Ti; 20 s for Na, Si, Rb, Ba, Ni and Mn, Ni;and 30 s for Cr, Caand Al. TheX-phi correction procedure (Merlet, 1992) was used for spectra processing. The Pb isotope compositions were determined at Deutsches GeoForschungsZentrum (GFZ), Potsdam, Germany. Powders from representative unaltered samples of volcanic and subvolcanic rocks were dissolved in concentrated HF for four days on a hot plate at 160 C. Samples were dried, re-dissolved in 2 N HNO 3 and dried slowly at 80 C overnight to convert fluorides to nitrates. Finally, the samples were taken up in 6 N HCl to convert nitrates to chlorides. Lead was separated in columns using ion exchange resin Bio Rad AG-1-X8. Procedures for the separation and purification of Pb are described in detail by Romer et al. (2005). The ion exchange procedure was repeated to purify Pb elutes. Lead was loaded together with H 3 PO 4 and silica-gel emitter on single Re-filaments. The Pb isotope ratios were measured using a ThermoFinnigan Scientific TRITON TIMS multi-collector mass-spectrometer operated in static multi-collection mode. The obtained Pb isotope ratios were corrected for instrumental fractionation of 0.1%/a.m.u. as determined from repeated measurement of Pb reference material NBS 981. Total procedural blank is between 15 and 30 pg Pb, thus, negligible. Accuracy of the determined Pb data is better than 0.1% at the 2 σ level. 4. Results 4.1. Field and petrographic descriptions The studied volcanic rocks were mainly taken from exposures and quarries (Fig. 2A and B), whereas lamprophyres and related dykes were mostly collected as loose angular blocks in the field (Fig. 2C). Melilitolite sample (OC-12) originates from a 271 m deep Holi cský vrch borehole near Ose cn a(Table 1). Late Cretaceous ultramafic lamprophyres, such as polzenite and aln€ oite dykes and the melilitolite of the Ose cn a intrusion, were sampled in the RPVC. Polzenites and aln€ oites generally have a fine-grained greyish groundmass and microporphyritic textures. They contain abundant partially serpentinised olivine phenocrysts/xenocrysts in a finegrained poikilitic groundmass containing microphenocrysts of phlogopite, which may be variably chloritised, flow-oriented melilite laths, feldspathoids, apatite and abundant Ti-rich magnetite (Fig. 2D). Aln€ oites contain, in contrast to polzenites, also phenocrysts of clinopyroxene. Tertiary basaltic volcanic rocks predominantly have microporphyritic textures with a fine-grained groundmass. Basanite samples are generally dominated by clusters of slightly serpentinised olivine along with elongated brownish, rarely corroded clinopyroxene crystals with oscillatory and/or hour-glass zoning. Twinned clinopyroxene forms isolated crystals or larger glomerophyres. The basanite fine-grained groundmass contains tiny plagioclase laths irregularly distributed together with smaller clinopyroxene columns (Fig. 2E). Most of the tephrite samples are characterised by the presence of both euhedral and partially corroded kaersutite with apatite inclusions. Kaersutite is surrounded by a very fine-grained hypocrystalline groundmass. Tertiary alkaline lamprophyres, such as camptonite, monchiquite and more alkaline leucocratic microsyenite, are especially common in the Roztoky Intrusive Complex of the CSVC. A special form of camptonite to monchiquite dykes occurs in the RPVC. The alkaline lamprophyres typically contain macroscopic amphibole phenocrysts in a fine-grained groundmass. The amphibole phenocrysts typically show corrosion rims comprising Ti-rich magnetite. Clinopyroxene in camptonites forms oscillatory and hour-glass zoned phenocrysts and smaller tabular crystals in a fine-grained plagioclase-rich groundmass. A typical accessory mineral is apatite, which is commonly associated with amphibole and/or clinopyroxene, titanomagnetite and feldspathoids. Zeolites are rare and form vesicular fillings (Fig. 2F). Camptonite to monchiquite samples from RPVC are characterised by amphibole that is rimmed by distinct dark mica, strongly serpentinised olivine and rare oscillatory-zoned clinopyroxene in a glassy matrix. Leucocratic microsyenite samples contain glomerophyres of amphibole and alkaline feldspar in a fine-grained feldspar-rich matrix (Fig. 2G). Amphiboles have inclusions of apatite and ilmenite. The groundmass consists primarily of glass, plagioclase and rare sodalite. Vesicles are filled by hydrothermal calcite. Very finegrained chilled margins of the leucocratic microsyenite dyke show flow-aligned alkali feldspar microphenocrysts (Fig. 2A). Additionally, two areas with nephelinte to melilitite occurrences are included in this study. Cretaceous intrusive melilitite from the Great Devil’s Wall in the RPVC is spatially related to ultramafic lamprophyres and forms a spectacular wall with horizontal columnar jointing (Fig. 2H). It contains mildly corroded olivine often forming clusters, and strongly zoned brown Ti-rich clinopyroxene commonly displaying characteristic twinning. Opaque minerals and flow-oriented thin laths of clinopyroxene occur in a melilite-bearing groundmass. In contrast, the Quaternary melilitite effusion from the youngest volcanic field in the Bohemian Massif, i.e., Cheb Basin, is characterised by the mineral association olivine (with thick, corroded rims) and large, kink-banded phlogopite flakes distributed in a vesicular glassy groundmass. For detailed petrographical characteristic of individual studied samples see Supplement B. 4.2. Mineral chemistry of amphibole, clinopyroxene and dark mica Chemical compositions of amphibole, clinopyroxene and dark mica from camptonite/monchiquite, leucocratic microsyenite and polzenite samples are listed in Supplement C available in the electronic appendix. Analysed minerals have relatively homogenous compositions without significant variation between cores and rims. S. Krmí ckov a et al. Geoscience Frontiers 11 (2020) 925–942 928 Amphibole phenocrysts from both camptonite/monchiquite and leucocratic microsyenite samples have relatively uniform contents of CaO (11.6–12.8 wt.%) and Na 2 O (1.9–2.5 wt.%). Amphibole from leucocratic microsyenite has higher concentrations of FeO tot (13.6–15.3 wt.%) and TiO 2 (4.6–5 wt.%) and lower contents of MgO (10–11.2 wt.%) and Al 2 O 3 (12–13.4 wt.%) than those from camptonite/monchiquite samples that have concentrations of MgO ¼13–15.2 wt.%, Al 2 O 3 ¼ 13.6–14.6 wt.% and TiO 2 ¼3.6–4.1 wt.%, except for three analyses that yielded very high TiO 2 contents of 6–6.5 wt.%. Concentrations of FeO tot in amphibole from camptonite/monchiquite samples are between 7.4 wt.% and 10.4 wt.%. All analysed amphibole crystals have high Mg/(Mg þFe) atomic ratios between 0.54 and 0.82 and have ~6 Si atoms per formula unit (apfu) and ~2 Ca apfu, respectively (Supplement C.1). Analysed amphiboles correspond both to pargasite and kaersutite (Fig. 3A). Clinopyroxene phenocrysts from camptonite/monchiquite and leucocratic microsyenite samples have similar compositions (Supplement C.2). They are Ca-rich with a relatively narrow range of CaO contents (22.4–24.8 wt.%; ~1 Ca apfu) along with variable concentrations of MgO (7.8–14.2 wt.%), Al 2 O 3 (4.8–13.1 wt.%), FeO tot (5.6–10.4 wt.%) and TiO 2 (1.4–5.1 wt.%). They have only minor MnO (up to 0.4 wt.%) and Na 2 O (below 1 wt.%) contents. Their Fe/(Fe þMg) atomic ratios range between 0.19 and 0.43. All analysed clinopyroxene phenocrysts fall in the diopside field (Fig. 3B). Dark mica from the polzenite sample shows a broad variation in MgO (16.8–22.2 wt.%; ~1.8–2.4 Mg apfu) and Al 2 O 3 (11–16.3 wt.%), and plots in two compositional fields (see Fig. 3C). In contrast, dark mica from camptonite/monchiquite is relatively uniform, having MgO and Al 2 O 3 contents in the ranges of 16.3–17.3 wt.% and 15.9–16.4 wt.%, respectively. The K 2 O contents are more variable in mica from polzenite Fig. 2. Field appearances and petrographic features of intrusive (lamprophyric) and extrusive volcanic rocks from the  Cesk eSt  redoho rí (CSVC) and Ralsk a Pahorkatina (RPVC) volcanic complexes. (A) Contact of a leucocratic microsyenite dyke in basanite host, characterised by a very fine-grained chilled margin (CSVC). (B) Columnar jointing of sandstone (see Vel azquez et al., 2008) at the contact to a camptonite dyke (RPVC). (C) Polzenite with characteristic warty surface (RPVC). (D) Partly serpentinised olivine (Ol) within fine-grained groundmass with slightly chloritised phlogopite (Phl), melilite (Mll) and Ti-rich magnetite (Mag) in polzenite (PPL; RPVC). (E) Cluster of olivine (Ol) and clinopyroxene (Cpx) displaying hour-glass zoning in groundmass composed of smaller plagioclase (Plg) laths and tiny clinopyroxene in basanite (PPL; RPVC). (F) Large amphibole (Amp) phenocryst surrounded by corrosion rim with Ti-rich magnetite (Mag) which encloses rounded vesicles filled with zeolite (Zeo) in camptonite (PPL; RPVC). (G) Glomeroporphyritic amphibole (Amp) and plagioclase (Plg) in aphanitic groundmass in leucocratic microsyenite (XPL; CSVC). (H) The Great Devil’s Wall melilitite dyke displaying horizontal columnar jointing (RPVC). S. Krmí ckov a et al. Geoscience Frontiers 11 (2020) 925–942 929 (~8.6–10.8 wt.%; ~0.8–1.0 K apfu) than in mica from camptonite/ monchiquite (8.8–9.4 wt.%; ~0.8–0.9 K apfu). The latter also contains mica that is relatively poor in BaO (max. 1.8 wt.% BaO). FeO tot concentrations range between 6 wt.% and 10.2 wt.%, except for few dark mica analyses from polzenite that show higher contents of 14.1–15.6 wt.%. Tetrahedral Al ranges between 0.94 and 1.41 apfu along with Mg/ (Mg þFe) atomic ratio of 0.66–0.88. Dark mica from polzenite falls in the phlogopite and Mg-biotite fields, whereas dark mica from camptonite/ monchiquite samples falls in the phlogopite field (Fig. 3C). Moreover, phlogopite from polzenite with very high Mg/(Mg þFe) shows an evolutionary trend towards tetra-ferriphlogopite, which is attested by deficient tetrahedral Al in recalculated analyses (Supplement C.3). 4.3. Whole-rock geochemistry 4.3.1. Major elements The SiO 2 and MgO contents of a representative set of 36 samples were recalculated on a volatile-free basis and range from 33 wt.% to 61 wt.% and 0.1 wt.% to 18 wt.%, respectively (Fig. 4,Table 2). The most ultrabasic rocks are Cretaceous ultramafic lamprophyres (SiO 2 ~36 wt.%) followed by associated melilitic rocks (SiO 2 ~40 wt.%). Tertiary volcanic rocks compositionally range from ultrabasic nephelinite and basic tephrite/basanite (majority of the samples with SiO 2 ~43 wt.%) to more acidic rocks of phonolite composition. Tertiary alkaline lamprophyres are basic (SiO 2 ~46 wt.%) with highly variable contents of alkalies. One sample of leucocratic microsyenite plots in the tephriphonolite field (Fig. 4). The various samples define a coherent trend in binary variation diagrams, using SiO 2 as differentiation index, that may be interpreted as (i) fractionation trend or (ii) mixing/assimilation trend or (iii) superposition of both (Fig. 5). Generally, Al 2 O 3 contents correlate positively, whereas CaO and MgO are negatively correlated. In contrast, TiO 2 contents behave differently. TiO 2 contents in Cretaceous ultramafic lamprophyres and melilitic rocks are in the range of 2–3 wt.% and correlate positively with SiO 2 . Contrary to that, TiO 2 contents in the most primitive members of the Tertiary volcanic rocks and alkaline lamprophyres reach ~4 wt.% and correlate negatively with increasing SiO 2 . FeO tot behaves similarly as TiO 2 (Fig. 5). K 2 O contents are ~2 wt.% in the majority of ultramafic lamprophyres and associated melilitic rocks. In the most primitive members of Tertiary volcanic samples, K 2 O contents are below 1.5 wt.% and correlate positively with increasing SiO 2 . An extremely high K 2 O content of 8.3 wt.% was found in a leucocratic microsyenite (sample KK7A). 4.3.2. Trace elements The samples generally have highly variable transition metal contents and a slightly variable enrichment of large-ion lithophile elements (LILE) and light rare earth elements (LREE) relative to high-field strength elements (HFSE) and heavy rare earth elements (HREE). This is clearly visible both in binary variation diagrams and in primitive mantle normalised trace and chondrite normalised rare earth element abundance plots (Figs. 5 and 6A–F). The highest Cr concentrations (up to 800 ppm) occur in Cretaceous ultramafic lamprophyres and associated melilitic rocks. Chromium correlates negatively with increasing SiO 2 , reaching levels as low as 2 ppm Cr in differentiated trachyte (Fig. 5,Table 2). Cretaceous ultramafic lamprophyres show the highest degree of LREE enrichment. La, Ce and Ce/Yb show a negative correlation with increasing SiO 2 for ultramafic Table 1 List of mantle-derived rocks of the Bohemian Massif selected for Pb isotope determination, sample location, petrographic types and field characteristics. No. Sample Locality Area Rock type Age (Ma) Latitude (N) Longitude (E) Outcrop characteristic 1 1_1367 V sechlapy CSVC basanite 41.9 5037.10001347.7670Quarry 2 4_New Radobýl CSVC basanite 30 5031.85001405.7170Abandoned quarry 3 5_New Sout esky CSVC basanite 30 5044.88301416.0170Quarry 4 8_1299  Zandov CSVC basanite 25.4 5042.48301423.8170Quarry 5 12_1295 Rade sín CSVC trachybasalt 26.8 5041.88301403.5670Abandoned quarry 6 14_1358 Valke rice CSVC trachybasalt 24.7 5042.11701419.7170Rock exposure 7 15_1359 Chlum CSVC tephrite 26.6 5044.81701413.5830Abandoned quarry 8 17_BM-8 Rýde c CSVC phonolite 25.8 5036.43301409.3000Abandoned quarry 9 18_BM-16  Strbický vrch CSVC phonolite 30 5033.46701350.5170Rock exposure 10 19_BM-48 Bo re n CSVC phonolite 30 5031.61701345.7170Rock exposure 11 20_BM-13 Lhenice CSVC trachyte 30 5034.50001352.1830Rock exposure 12 21_BM-51 Mile sovský Kloc CSVC trachyte 30 5032.35001355.0670Rock exposure 13 23_BM-4 Kalich CSVC trachyandesite 31 5036.18301412.5670Abandoned quarry 14 25_BM-60 Bore c CSVC trachyandesite 30 5030.85001359.2670Rock exposure 15 CS-30 Dobkovice I CSVC monchiquite 30 5042.63301411.5670Dyke in old quarry 16 CS-31 Dobkovice II CSVC camptonite 30 5042.64001411.5490Dyke in old quarry 17 CS-43 Le stina CSVC camptonite 30 5039.36701412.3000Abandoned quarry 18 KK1 Komorní Hůrka CHB melilitite 1 5006.02001220.1660Rock exposure 19 KK2  Ríp CSVC tephrite 25.6 5023.23001417.3200Angular blocks 20 KK3 Pansk ask  ala CSVC basanite 29.7 5046.14601429.1020Abandoned quarry 21 KK4 Tlustec RPVC basanite 30 5043.53501444.6490Angular blocks 22 KK5 St ríbrník RPVC tephrite 30 5043.93601450.9250Rock exposure 23 KK6 JanůvDůl RPVC camptonite/monchiquite 28.7 5042.10201457.3790Abandoned quarry 24 KK7A P rední Lhota I CSVC leucocratic microsyenite 30 5042.52901412.0310Dyke in quarry - centre 25 KK8 P rední Lhota II CSVC camptonite 30 5042.55701412.0180Dyke in quarry 26 KK9 Sv arov RPVC polzenite 70 5042.31301453.4500Angular blocks 27 KK10 Velk a  Certova ze  d RPVC melilitite 70 5040.41401456.7250Dyke exposure 28 KK11 Hamerský  Spi c ak I RPVC polzenite 70 5041.33601450.9890Angular blocks 29 KK12 Pta cí vr sek RPVC basanite 70 5040.50901440.7820Dyke in old quarry 30 ME-3/13 Krkav cí sk ala I CSVC nephelinite 27 5035.15001404.7830Rock exposure 31 ME-4/13 Krkav cí sk ala II CSVC basanite 30 5035.11701404.7170Rock exposure 32 OC-1 Veselí RPVC camptonite/monchiquite 30 5038.28001438.4600Angular blocks 33 OC-2 Pelousek RPVC polzenite 70 5040.68001458.2000Abandoned quarry 34 OC-9 Vesec RPVC polzenite 68.4 5042.18001458.9800Angular blocks 35 OC-10 Nový Luhov RPVC aln€ oite 70 5042.48001445.0000Angular blocks 36 OC-12 Holi cský vrch RPVC melilitolite 70 5040.80001453.8200Borehole CSVC –  Cesk eSt  redoho rí Volcanic Complex; RPVC –Ralsk a Pahorkatina Volcanic Complex; CHB –Cheb Basin. Ages are taken from Ulrych et al. (1998, 2002, 2013, 2014, 2018), Skala et al. (2014), Ackerman et al. (2015), Dostal et al. (2017). S. Krmí ckov a et al. Geoscience Frontiers 11 (2020) 925–942 930 lamprophyres towards tephritic and basanitc rocks (Fig. 5). The Cretaceous ultramafic lamprophyres and associated melilitic rocks are characterised by troughs for K and Pb in primitive mantle normalised trace element plots (Fig. 6A). Tertiary alkaline lamprophyres show slightly negative or even positive anomalies for K along with Pb enrichment and P depletion. The leucocratic microsyenite has the most pronounced anomalies among the analysed alkaline lamprophyres and related rocks (Fig. 6C). Absolute trace element concentrations in Tertiary volcanic samples differ from those of the basanite/tephrite samples and the more evolved trachytic/phonolitic samples. However, they define the same trends in primitive mantle normalised trace element plots. Tertiary volcanic samples show variable Rb depletion, K and Pb depletion or enrichment, as well as troughs for P and Ti that markedly increase from basanite/tephrite to trachyte/phonolite samples (Fig. 6E). There are two geochemical types of phonolite in the representative sample set: type A (Sr-rich) and type B (Sr-poor), first characterised by Ackerman et al. (2015). Whereas the samples of type A phonolite compositionally resemble other types of evolved volcanic rocks, type B phonolite is prominent by extreme depletion of Ba, Sr, P, and Ti along the most pronounced Cs, U, and Pb enrichments among all Tertiary volcanic rocks (Fig. 6E). The samples show variable REE contents and generally lack pronounced Eu anomalies (Fig. 6B, D, F). Cretaceous ultramafic lamprophyres have the highest total REE contents (ΣREE ~500 ppm), whereas Tertiary trachytic/phonolitic samples have the lowest total REE contents οf ~270 ppm. Ultramafic lamprophyres together with associated melilitic samples are prominent by the highest enrichment in LREE over HREE with Ce N /Yb N of ~30 and Lu N of ~7, whereas Tertiary volcanic samples have contrasting enrichment trends in LREE/HREE (Ce N /Yb N ~21 in basanite/tephrite samples, and ~31 in more differentiated trachyte/ phonolite samples). Type B phonolite is prominent by its U-shaped REE normalised pattern (Fig. 6F). Ultramafic lamprophyres, associated melilitic rocks, the majority of alkaline lamprophyres and basanite/tephrite volcanic rocks all have Lu N <10 indicating the presence of garnet in the mantle source of their parent melts (see Wilson and Downes, 1991). Fig. 3. Classification of amphibole, clinopyroxene and dark mica from camptonite/monchiquite, leucocratic microsyenite, and polzenite. All chemical elements are given in apfu (atoms per formula unit). (A) Analyses of amphibole phenocrysts from camptonite/monchiquite samples plot in the fields of both pargasite and kaersutite, whereas amphibole in leucocratic microsyenite falls in the kaersutite field of the amphibole classification scheme of Leake (1997). (B) Clinopyroxene from both camptonite/monchiquite and leucocratic microsyenite samples is diopside (Morimoto, 1988), diagram adopted from Rapprich (2005). (C) Dark mica from camptonite/monchiquite and polzenite corresponds to phlogopite. Dark mica from camptonite/monchiquite is compositionally rather homogeneous, whereas dark mica from polzenite falls in two groups ranging from phlogopite to Mg-biotite. Classification diagram after Rieder et al. (1998). Fig. 4. Total Alkali-Silica (TAS) diagram showing the chemical composition of analysed samples (after Le Maitre, 2002). S. Krmí ckov a et al. Geoscience Frontiers 11 (2020) 925–942 931 Table 2 Major oxide (wt.%) and trace element compositions (ppm) of mantle-derived rocks of the Bohemian Massif. No. 1 a 2 a 3 a 4 a 5 a 6 a 7 a 8 a 9 a 10 a 11 a 12 a 13 a 14 a 15 b 16 b Sample 1_1367 4_New 5_New 8_1299 12_1295 14_1358 15_1359 17_BM-8 18_BM-16 19_BM-48 20_BM-13 21_BM-51 23_BM-4 25_BM-60 CS-30 CS-31 SiO 2 40.2 40.4 42.3 41.6 47.0 45.2 42.2 55.8 55.2 54.2 59.1 56.8 53.9 54.6 45.9 47.8 TiO 2 2.65 3.73 3.3 2.8 2.97 3.59 3.92 0.14 0.59 0.28 0.57 0.45 1.27 0.86 3.22 2.13 Al 2 O 3 11.1 12.1 14.7 13.5 15.2 15.5 13.6 21.4 20.3 21.7 19.8 20.2 18.9 19.7 15.0 16.2 Fe 2 O 3 tot 12.5 14.0 12.1 11.5 9.6 10.8 11.5 2.3 3.63 2.2 3.22 3.11 5.66 4.36 11.1 8.34 MnO 0.19 0.19 0.19 0.19 0.16 0.18 0.33 0.28 0.23 0.26 0.23 0.22 0.2 0.2 0.16 0.16 MgO 12.9 8.91 8.4 9.87 4.57 5.4 6.53 0.08 0.43 0.23 0.21 0.34 1.32 0.67 4.91 2.48 CaO 12.5 12.5 11.8 12.6 9.85 10.6 13.5 0.95 4.15 1.8 3.4 3.59 5.4 4.42 8.79 7.35 Na 2 O2.73 1.85 2.25 1.84 3.67 3.38 2.61 9.9 6.85 9.11 5.0 6.47 6.47 5.94 2.92 3.7 K 2 O0.66 1.47 1.63 1.31 2.31 1.96 1.38 5.46 5.05 4.73 5.69 5.39 3.84 5.06 4.09 4.07 P 2 O 5 0.79 0.68 0.54 0.54 0.49 0.51 0.65 0.02 0.1 0.03 0.08 0.07 0.35 0.15 0.47 0.52 LOI 2.61 3.2 2.69 2.99 3.62 3.27 4.31 1.79 2.16 5.52 2.47 3.22 2.77 4.51 3.44 6.86 Total 98.8 99.1 99.9 98.7 99.4 100.4 100.5 98.2 98.7 100.1 99.8 99.8 100.1 100.5 99.9 99.6 Mg# 67 56 58 63 49 50 53 6 19 17 11 18 32 23 47 37 Cr 350 210 140 320 50 40 70 10 10 2 2 10 20 10 27 16 Ni 280 170 120 190 10 70 90 10 10 10 10 10 20 10 22 15 Co 51 45 40 44 26 30 34 1 14 4 5 7 14 7 31 17 Sc 26 29 30 32 20 24 30 1 1 1 0 0 4 1 24 10 V281 336 345 317 336 378 436 23 71 18 60 57 108 100 367 212 Cu 70 60 70 90 40 60 180 5 10 5 5 5 10 5 –– Zn 110 110 100 100 90 110 120 150 130 175 118 110 130 120 –– Rb 10 36 33 29 144 84 44 371 123 219 184 153 98 121 81 117 Cs 0.5 0.5 0.0 1.7 1.7 1.4 1.2 9.9 1.4 4.78 5.45 2.0 1.70 2.5 0.9 1.5 Ba 643 600 494 700 992 776 752 17 1880 620 1870 1730 1400 1420 781 937 Sr 981 1260 1290 1000 937 904 1070 21 2070 433 1830 1560 1570 1410 641 1000 Ga 18 19 19 18 20 24 24 53 27 25 41 27 29 26 –– Ta 4.6 7.1 4.5 5.7 4.4 5.5 5.7 2.02 5.5 7.2 8.56 4.1 6.9 5.0 4.84 6.13 Nb 68 70 66 79 70 78 76 138 140 447 198 113 127 110 94 123 Hf 5.0 6.2 8.0 5.3 6.7 8.1 7.9 21.2 10.2 22.2 11.1 10.0 13.1 10.4 9.2 12.4 Zr 228 232 211 218 324 329 323 1200 543 1650 634 568 615 562 359 576 Y23 27 22 22 22 22 24 16 24 24 29 20 27 22 21 25 Pb 4 4 3 4 7 7 7 34 9 12 25 11 15 11 6 7 Th 7.5 4.2 5.0 6.5 7.9 8.9 9.0 49.7 14.8 28.8 15.4 15.3 17.9 14.6 8.9 11.8 U1.9 1.1 1.4 1.6 2.3 3.1 5.7 18.6 3.8 16.6 4.0 3.9 4.1 3.4 2.0 3.4 La 68 46 44 60 58 51 69 139 124 115 148 112 108 110 49 77 Ce 124 96.7 87.7 112 112 105 133 146 210 160 216 178 186 181 101 147 Pr 13.7 12.3 10.3 12.3 12.9 12.4 15.4 8.5 19.5 22.0 13.0 15.9 18.7 17.6 11.8 16.4 Nd 50.2 49.2 39.4 43.8 48.2 47.4 57.6 17.3 56.1 45.8 67.3 44.0 60.9 54.4 45.8 59.3 Sm 9.2 10.1 7.5 7.9 8.6 8.5 10.4 1.61 6.8 6.72 8.2 5.6 9.3 7.5 8.58 9.84 Eu 2.92 3.21 2.35 2.5 2.49 2.53 3.08 0.32 2.01 1.34 2.06 1.56 2.71 2.18 2.48 2.89 Gd 7.7 8.4 6.3 6.5 6.5 6.5 8.2 1.13 4.9 3.9 4.4 3.7 6.9 5.4 8.21 9.88 Tb 1.0 1.2 0.9 0.9 0.9 0.9 1.1 0.22 0.7 0.69 0.8 0.5 0.9 0.7 1.03 1.23 Dy 5.1 5.8 4.7 4.8 4.6 4.6 5.3 1.56 3.7 5.3 5.7 3.0 5.0 3.9 4.84 5.62 Ho 0.9 1.0 0.9 0.9 0.8 0.8 0.9 0.41 0.7 0.9 0.9 0.6 0.9 0.8 0.85 1.0 Er 2.3 2.6 2.2 2.3 2.2 2.2 2.3 1.6 2.4 2.8 2.8 2.0 2.7 2.2 2.35 2.88 Tm 0.3 0.34 0.29 0.29 0.29 0.3 0.32 0.34 0.36 0.45 0.52 0.32 0.39 0.33 0.28 0.36 Yb 1.8 1.9 1.9 1.8 1.9 1.8 1.8 2.98 2.4 3.94 2.88 2.3 2.6 2.2 1.81 2.37 Lu 0.25 0.26 0.28 0.27 0.28 0.26 0.26 0.52 0.4 0.61 0.48 0.37 0.41 0.35 0.27 0.34 No. 17 b 18 19 20 21 22 23 24 25 26 27 28 29 30 c 31 c 32 d 33 d 34 d 35 d 36 d Sample CS-43 KK1 KK2 KK3 KK4 KK5 KK6 KK7A KK8 KK9 KK10 KK11 KK12 ME-3/13 ME-4/13 OC-1 OC-2 OC-9 OC-10 OC-12 SiO 2 42.7 38.2 39.2 42.4 41.7 40.6 44.9 52.8 45.2 33.8 39.9 33.1 41.3 36.8 39.9 38.9 34.0 30.6 34.1 31.5 TiO 2 2.97 3.1 3.4 3.17 3.73 3.22 2.62 1.45 3.25 2.62 2.96 2.47 3.08 3.07 2.63 3.43 2.57 2.28 2.1 2.57 Al 2 O 3 13.8 11.5 11.8 13.6 14.5 14.7 13.0 17.8 15.8 7.88 9.99 7.74 14.5 12.6 12.2 13.7 8.96 7.38 8.24 8.65 (continued on next page) S. Krmí ckov a et al. Geoscience Frontiers 11 (2020) 925–942 932 Table 2 (continued) No. 17 b 18 19 20 21 22 23 24 25 26 27 28 29 30 c 31 c 32 d 33 d 34 d 35 d 36 d Sample CS-43 KK1 KK2 KK3 KK4 KK5 KK6 KK7A KK8 KK9 KK10 KK11 KK12 ME-3/13 ME-4/13 OC-1 OC-2 OC-9 OC-10 OC-12 Fe 2 O 3 tot 11.6 13.2 15.6 12.4 12.5 13.3 11.9 5.58 10.4 11.7 11.5 10.8 13.0 13.6 12.9 12.3 12.1 11.6 13.7 10.7 MnO 0.19 0.23 0.33 0.18 0.2 0.22 0.23 0.15 0.17 0.2 0.18 0.19 0.21 0.22 0.18 0.16 0.2 0.2 0.2 0.17 MgO 7.88 12.1 7.15 9.15 7.07 8.36 5.94 1.79 4.71 15.3 15.7 16.9 7.90 11.4 13.6 11.0 15.1 17.0 16.5 13.4 CaO 10.5 12.4 12.0 12.0 11.8 12.4 11.8 4.28 8.07 16.1 13.0 18.6 12.7 14.7 12.1 13.2 14.1 21.1 16.4 17.9 Na 2 O3.03 3.71 4.39 3.13 3.03 2.92 2.62 3.79 4.03 1.02 2.31 1.59 3.3 3.19 2.02 0.89 2.16 0.52 2.01 0.22 K 2 O2.15 2.15 1.1 1.57 1.75 1.53 1.67 7.97 4.17 1.72 1.41 1.25 1.33 1.5 0.96 1.9 1.85 0.75 1.66 1.98 P 2 O 5 0.6 0.92 1.41 0.73 0.77 1.09 1.23 0.32 0.52 1.24 0.75 1.30 0.87 1.5 0.63 0.53 1.07 1.12 1.09 0.95 LOI 4.57 1.8 3.0 1.1 2.3 1.2 3.6 3.7 3.2 7.6 1.4 5.2 1.4 1.8 3.5 5.18 7.4 6.3 4.9 12.0 Total 100.0 99.4 99.3 99.4 99.4 99.5 99.5 99.6 99.5 99.2 99.2 99.2 99.5 100.4 100.6 101.1 99.6 98.8 100.4 100.0 Mg# 57 65 48 59 53 56 50 39 47 72 73 76 55 63 68 64 71 74 71 71 Cr 70 431 27 294 144 130 55 14 34 602 842 746 192 197 486 262 749 810 623 700 Ni 75 147 25 98 41 54 27 5 12 317 339 336 56 132 239 134 327 330 253 216 Co 37 56 37 46 40 43 31 9 28 53 59 60 43 55 60 51 56 59 61 47 Sc 30 29 21 27 26 27 17 5 20 22 30 26 24 27 31 45 33 23 30 22 V345 304 275 289 348 336 269 141 341 252 308 210 315 378 334 ––252 –– Cu –48 38 70 61 47 38 9 46 52 76 48 56 ––––30 –– Zn –63 150 90 100 88 91 77 82 86 72 65 84 ––––70 –– Rb 38 54 21 35 64 37 48 222 118 49 51 47 32 29 35 154 64 26 48 65 Cs 1.3 0.4 1.0 0.4 0.6 0.2 1.2 1.80 1.2 0.9 1.0 0.8 0.4 0.8 0.5 1.89 2.9 0.5 0.93 3.03 Ba 654 965 1030 717 791 591 541 1070 868 737 807 968 726 1470 651 1610 1980 717 1380 754 Sr 920 807 1580 937 1700 940 1230 757 890 866 873 1420 1140 1770 963 854 2000 1800 1780 1280 Ga –21 25 19 22 20 17 21 21 13 14 12 19 ––––18 –– Ta 4.9 6.8 10.1 4.5 4.8 5.7 5.7 5.2 5.1 8.5 5.1 6.9 5.3 5.8 4.1 3.49 5.5 10.7 7.80 7.73 Nb 95 122 168 87 78 88 96 107 82 129 84 134 90 141 96 79 188 151 183 125 Hf 8.1 6.7 14.7 5.8 8.2 6.3 7.0 9.7 8.2 5.5 5.7 4.6 6.1 8.5 7.1 10.2 7.5 5.5 6.3 7.8 Zr 313 299 616 233 351 256 290 461 340 251 224 197 243 333 259 301 357 247 292 345 Y24 27 42 25 29 28 30 23 23 30 19 24 27 34 21 21 26 29 28 29 Pb 1725 64 24 15853 4 2 10 3 4 6 4 6 4 Th 7.6 11.3 13.8 6.9 6.6 7.1 8.0 18.4 10.0 16.1 6.4 12.7 6.9 17.0 7.0 12.3 15.0 23.0 17.0 10.2 U2.1 3.1 3.9 1.5 1.8 1.6 2.0 5.2 2.5 3.9 1.6 2.9 1.5 3.7 1.7 1.45 3.9 4.83 4.8 2.49 La 62 89 125 58 63 67 73 80 57 124 52 106 62 165 64 51 103 163 130 84 Ce 128 168 249 110 132 136 144 145 115 248 104 201 125 289 117 104 186 304 235 177 Pr 14.6 18.9 28.7 12.1 15.4 15.4 16.9 14.8 13.0 28.2 11.9 22.2 14.7 28.0 13.0 12.5 21.0 33.8 25.0 19.9 Nd 56.9 69.3 110 46.1 61.5 59.6 61.5 50.4 50.4 106 46.1 84.3 56.9 102 48.0 50.6 79.0 120 90.0 77.2 Sm 10.3 11.4 18.0 8.5 11.0 10.7 10.4 7.69 8.4 17.1 8.61 13.9 9.67 16.0 8.4 9.27 13.0 18.4 14.0 13.4 Eu 3.02 3.33 5.01 2.52 3.3 3.11 3.13 2.06 2.42 4.73 2.56 3.92 3.07 4.5 2.5 2.74 3.6 5.13 3.9 3.85 Gd 9.74 9.34 14.2 7.51 9.39 8.98 9.05 6.11 6.97 12.7 7.06 10.6 8.29 15.0 8.1 8.61 10.0 12.9 13.0 13.9 Tb 1.22 1.16 1.75 0.98 1.2 1.11 1.16 0.83 0.9 1.52 0.86 1.23 1.08 1.7 1.0 1.03 1.30 1.53 1.5 1.62 Dy 5.51 5.88 8.98 5.13 6.31 6.35 6.50 4.58 4.93 7.69 4.28 6.03 5.88 7.6 4.8 4.77 6.6 7.08 6.3 6.28 Ho 0.96 0.95 1.52 0.88 1.02 1.04 1.07 0.75 0.84 1.12 0.67 0.91 0.94 1.3 0.85 0.82 1.10 1.11 1.0 0.97 Er 2.72 2.46 3.93 2.29 2.83 2.86 2.83 2.31 2.28 2.66 1.67 2.18 2.53 3.6 2.3 2.19 2.6 2.61 2.6 2.87 Tm 0.33 0.31 0.56 0.28 0.35 0.38 0.37 0.32 0.31 0.32 0.19 0.25 0.33 0.42 0.27 0.26 0.33 0.3 0.3 0.29 Yb 2.05 1.89 3.33 1.89 2.16 2.15 2.46 2.30 1.94 1.84 1.26 1.49 1.92 2.6 1.7 1.92 1.9 1.63 1.8 1.82 Lu 0.29 0.26 0.49 0.25 0.33 0.34 0.35 0.33 0.3 0.25 0.16 0.19 0.29 0.36 0.23 0.22 0.25 0.21 0.23 0.25 LOI - loss on ignition; Mg# ¼100 Mg/(Mg þFe tot ). a Analyses adopted from Dostal et al. (2017). b Analyses adopted from Sk ala et al. (2014). c Analyses adopted from Sk ala et al. (2015). d Analyses adopted from Ulrych et al. (2014). S. Krmí ckov a et al. Geoscience Frontiers 11 (2020) 925–942 933 (3) Generally, off-rift volcanic/subvolcanic rocks are derived from a mantle source with higher 206 Pb/ 204 Pb than corresponding rocks from axial parts of the rift, possibly indicating that the low 206 Pb/ 204 Pb component is derived from the mantle source influenced by asthenosphere upwelling. (4) The majority of Cenozoic mantle-derived rocks of Central Europe show similar Pb isotope variations as those of the Bohemian Massif. Acknowledgments This research was financially supported by the institutional project RVO 67985831 of the Institute of Geology of the Czech Academy of Sciences, as well as by the Brno University of Technology project LO1408 “AdMaS UP –Advanced Materials, Structures and Technologies”, supported by the Ministry of Education, Youth and Sports of the Czech Republic under the “National Sustainability Programme I”. S.K., L.K. and J.U. thank Jaroslav Dostal (Saint Mary’s University, Canada) and Martin J. Timmerman (University of Potsdam, Germany) for discussion. The authors greatly appreciate an anonymous reviewer and Dr. C. Spencer for their very constructive and helpful comments and suggestions. Appendix A. Supplementary data Supplementary data to this article can be found online at https://doi. org/10.1016/j.gsf.2019.09.009. References Abdelfadil, K.M., Romer, R.L., Seifert, T., Lobst, R., 2013. 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