Geochemistry of granitoids from the Austroalpine Seckau Complex: a key for revealing the pre-Alpine evolution of the Eastern Alps

Recent studies revealed that the calc-alkaline metagranitoids of the Seckau Complex comprise both (1) a Late Cambrian to Early Ordovician and (2) a Late Devonian to Early Carboniferous (early Variscan) intrusive complex. The older rocks of the Hochreichart Plutonic Suite reflect I to S-type affinity and are peraluminous and characterized by a general decrease in TiO2, Al2O3, MgO, CaO, P2O5, FeOt and MnO with increasing SiO2. Chondrite-normalized rare earth element (REE) plots display a slight enrichment in light rare earth elements (LREE) relative to heavy rare earth elements (HREE) as well as negative Eu anomalies ((Eu/Eu*)N = 0.15- 0.77). The whole-rock initial 87Sr/86Sr ratios calculated back to the time of emplacement (~ 496 Ma) vary between 0.7056 to 0.7061. The early Variscan rocks of the Hintertal Plutonic Suite can be subdivided into (a) the meta- to peraluminous granodioritic suite of the Pletzen Pluton and (b) the peraluminous granitic suite of the Griessstein Pluton. The Pletzen Pluton shows typical magmatic fractionation trends for most of the major oxides and trace elements plotted against SiO2. On a chondrite-normalized diagram, metagranitoids are strongly enriched in LREE and show no significant negative Eu anomaly. Metagranitoids of the Griessstein Pluton have a more peraluminous character and similar major and trace element fractionation trends compared to the Pletzen Pluton. However, the contents in SiO2, major and trace elements clearly point towards a more evolved melt with generally lower TiO2, Al2O3, MgO and CaO values and higher K2O content. Metagranitoids of the Griessstein Pluton are additionally characterized by a slight negative Eu anomaly of about 0.81 on a chondrite-normalized REE plot. Initial 87Sr/86Sr values calculated back to the time of emplacement (~ 353 Ma) of the Pletzen Pluton and the Griessstein Pluton vary between 0.7051—0.7061 and 0.7054—0.7063, respectively, and suggest the same magmatic source for both units. Application of rhyolite-MELTS modelling to the Hintertal Plutonic Suite revealed that the Griessstein Pluton formed by fractional crystallization (~ 30%) from the more primitive Pletzen Pluton. Our geochemical data from the Hochreichart Suite granitoids suggest the existence of a Late Cambrian to Early Ordovician active margin with its remnants now exposed in the Seckau Complex. The early Variscan grainitoids of the Seckau Complex are inferred as part of a magmatic arc along the southern Bohemian active continental margin that was related to the subduction of differently termed oceanic domains (Galicia-Moldanubian Ocean or Paleotethys), prior to the final collision of Gondwana and Laurussia. The general paleogeographic position of the Seckau Complex during the Variscan orogeny is considered to be south to southeast of the Bohemian Massif, adjacent to the eastern Hohe Tauern, the Schladming Tauern, and the Western Carpathians.


Introduction
The Variscan orogen formed through long and diachronous convergence and collision of Gondwana lithospheric fragments with Laurussia that finally amalgamated during the Carboniferous. Individual orogenic phases are known to expand from early to mid-Devonian to Pennsylvanian times and were associated with the emplacement of numerous granitoids, which are heterogenous in terms of ages, Editorial handling: X. Xu geochemistry, source and regional distribution .
In contrast to the well-studied plutons of the northern and central European Variscides, only few data exist from the re-worked intra-Alpine granitoids originating from the former southern part of the Variscan orogen. Granitoids of the Seckau Complex (Eastern Alps), now observed as metagranitoids, were generally considered to be part of these intra-Alpine Variscan intrusive suites. Recent studies, however, revealed that the metagranitoids of the Seckau Complex are part of both a late Cambrian to Early Ordovician, and Late Devonian to Early Carboniferous (early Variscan) intrusive complex (Mandl et al. 2018). While the older intrusives comprise primarily peraluminous granitoids with I-to S-type characteristics, the early Variscan granitoids represent meta-to peraluminous granitoids, which represent mostly I-type characteristics.  Finger et al. 1997Finger et al. , 2003Finger et al. , 2009Franěk et al. 2011 Yuan et al. 2020) Based on the geochronological results of Mandl et al. (2018) new geochemical data as well as recalculated Sr isotope data from literature (Pfingstl et al. 2015) were used in order to (1) better understand and constrain the evolution of Variscan magmatism and magmatic differentiation of the Seckau Complex and (2) characterize the older late Cambrian to Early Ordovician plutonic suite of the Seckau Complex.

Geological setting
The nappe systems of the Eastern Alps ( Fig. 1) comprise widely exposed pre-Alpine basement units that are covered by Upper Carboniferous to Eocene sedimentary sequences (for summary, see Schmid et al. 2004).
Large parts of Variscan and pre-Variscan crust, including its sedimentary cover, were incorporated into the Alpine orogen during the continuous convergence of the African and European continental plates from Late Jurassic times onwards. Several oceanic basins and microcontinents were involved in this collision event at different times (Schmid et al. 2004). The Eastern Alps (Figs. 1, and 2) are basically the product of two orogenic collision events: (1) the Eo-Alpine event (Frank 1987) and (2) the Alpine event (e.g., Froitzheim et al. 1996). The Eo-Alpine event is basically related to the closure of the Meliata Ocean. The subsequent Alpine event (Late Cretaceous to Paleogene) followed the subduction of the Penninic oceans (Piemont-Ligurian and Valais Ocean), due to the collision of Europe and Adria (Froitzheim et al. 1996;Schmid et al. 2004;Schuster 2004). Accordingly, the nappe stack in the (Eastern) Alps can be subdivided into three main structural units: (1) the Helvetic realm and sub-Penninic nappes, representing the former southern European continental margin, (2) the Penninic nappes, comprising oceanic (Piemont-Ligurian Ocean and Valais Ocean) and continental crust (e.g., Brianconnais) and (3) the Austroalpine nappes, representing continental crust from the northern part of former Adria (Fig. 2a) (Schuster 2003;Schmid et al. 2004;Froitzheim et al. 2008).
Basement units within the Austroalpine nappe system consist of Cadomian continental crust with Paleozoic metasedimentary sequences, and magmatic rocks related to rifting and subduction processes lasting until Carboniferous times (for summary, see von Raumer and Neubauer (1993);von Raumer et al. 2013). During the Variscan orogeny large parts of this crust were affected by metamorphic overprint and synorogenic magmatism.
The Lower Austroalpine basically derived from the northern continental margin of Adria facing towards the Piemont-Ligurian Ocean (e.g., Schmid et al. 2004). The Upper Austroalpine Subunit, widely exposed in the Eastern Alps, is mainly shaped by the Eo-Alpine collision event (Eo-Alpine as term for the Early Cretaceous to early Late Cretaceous orogeny). It comprises Paleozoic and Mesozoic cover units along the northern margin of the Eastern Alps (Northern Calcareous Alps) and Paleozoic metasediments and metavolcanics of the Graywacke Zone. In the central and southern part, pre-Alpine crystalline basement units such as (from bottom to top) the Silvretta-Seckau-, the Koralpe-Wölz-, the Ötztal-Bundschuh-and Drauzug-Gurktal Nappe Systems are mostly covered by Late Carboniferous-Permian to Mesozoic metasediments (Schmid et al. 2004;Froitzheim et al. 2008).
The Silvretta-Seckau Nappe System (Fig. 2), being the focus of this study, consists of a pre-Alpine metamorphic and magmatic basement and remnants of Carboniferous to Triassic cover sequences. The Seckau Nappe, as part of the Silvretta-Seckau Nappe System, was overprinted by subgreenschist to greenschist facies metamorphic conditions during the Eo-Alpine event (Schuster et al. 2013;Faryad and Hoinkes 2003), as indicated by Rb-Sr biotite ages in the range of 85 to 82 Ma (Pfingstl et al. 2015). The main area of exposure extends from the Bösenstein Massif (Pölsenstein Massif in Metz 1976) to the Seckau Tauern (Fig. 2). The Seckau Nappe comprises several pre-Alpine basement complexes ( Fig. 2b): Seckau Complex, Amering Complex, Gleinalm/Gleinalpe and Rennfeld Complex as well as Permian to Lower Triassic metasediments summarized as Rannach-Formation (Metz 1967;Flügel and Neubauer 1984;Faryad and Hoinkes 2001;Gaidies et al. 2006;Pfingstl et al. 2015). The Seckau Complex is dominated by paragneisses (partly migmatitic) and micaschists being intruded by large volumes of meta-to peraluminous granitoids. Together, the granitoids make up about 90% of the Seckau Complex . Whereas the paleogeographic and tectonic position of these basement complexes during Alpine evolutionary steps is ascertained, their plate tectonic arrangement during Cambrian and Late Devonian / Mississippian times remains unclear and is focus of this study.
Recent studies revealed a more distinct subdivision of the Seckau Complex based on petrological, geochemical and geochronological data (Mandl et. al. 2018) (Fig. 3). The Glaneck Metamorphic Suite comprises paragneisses with U-Pb ages of originally detrital zircons in the range from Neoarchean (ca. 2.7 Ga) to Ediacaran (ca. 559 Ma) with distinct frequency peaks between ca. 572 ± 7 Ma and 559 ± 11 Ma. Highly fractionated peraluminous granites of the Hochreichart Suite indicate a magmatic event between 508 ± 9 Ma and 486 ± 9 Ma that may also have caused migmatisation of distinct domains in the paragneisses of the Glaneck Metamorphic Suite. The Hintertal Plutonic Suite displays a second intrusion event ranging from 365 ± 8 Ma to 343 ± 12 Ma and comprises meta-to peraluminous granodiorites (Pletzen Pluton) as well as peraluminous granites (Griessstein Pluton).

Analytical methods
Forty-eight samples, up to 10 kg each. representing the metagranitoids of the Seckau Complex were taken and analyzed for this study. All analyses were conducted at the Institute of Earth Sciences, NAWI Graz Geocenter, University of Graz, Austria. All samples were cut with a rock saw and the thin sections were prepared and examined by optical microscopy. The remaining major parts of the samples were crushed and for major and trace element analysis, a representative aliquot was milled to a homogenous powder in a tungsten carbide vibratory disc mill. Before further preparation the powder was dried at 105 °C for 2 h. 1 g of the dried powder was used for Loss on ignition (LOI) by heating the samples to 1030 °C for 1 h. Fused glass discs of ~ 4 cm diameter, were produced with 1 g of rock powder and a mixture of 4.62 g of lithium tetraborate and 2.38 g of lithium metaborate powder.
Major-and selected trace-element concentrations (Rb, Sr, Zr and Ba) of whole-rock samples were determined by a Bruker Pioneer S4 X-ray fluorescence (XRF) spectrometer on fused glass discs (see Mandl et al. 2018 for details). The reproducibility of major elements was better than 1% and for  Mandl et al. 2018). The study area (part of the Seckau Nappe System) is marked with a dotted rectangle trace elements within 3-5%. Detection limits for major, minor and trace elements determined by XRF are 0.01 wt%, 0.005 wt% and 20 μg/g, respectively. International standards as e.g., AC-E, MA-N, GSP-2 were routinely measured to ensure analytical accuracy. Trace elements and rare earth elements were determined by inductively coupled plasma mass spectrometry (ICP-MS, Agilent 7500) at the Institute for Analytical Chemistry, University of Graz (Austria). For the analytical procedure about 50 mg of powdered sample were placed in a Teflon beaker and dissolved in concentrated nitric (HNO 3 ) and hydrofluoric (HF) acid mixture with a volumetric ratio of 1:2. The uncapped beakers were placed on a hot plate at 100 °C for 30 min, then tightly capped and returned to the hot plate at 180 °C for at least 48 h. After dissolution and evaporation, samples were extracted with 7.5 N HNO 3 and diluted 1500 times. The analytical results for standards GSP-2, JR-2, BCR-2, BHVO-2 were for most elements within the specified uncertainty. Detection limits for trace and rare earth elements determined by ICP-MS are 0.05 μg/g.

Sample description
Sample locations of the Seckau Complex metagranitoids are displayed in Fig. 3; coordinates of sample sites are listed in supplementary Table S1. Based on field observations and petrographic characteristics, the granitoid intrusions of the Seckau Complex, now mostly observed as metagranitoids, can be distinguished into two plutonic suites.
The granite gneisses of the Hochreichart Plutonic suite usually display S-type to minor I-type affinity. The magmatic mineral assemblage predominantly consists of quartz, K-feldspar, plagioclase (with partial saussuritization), muscovite, biotite (orange colored). Zircon, apatite, garnet and opaque phases are common as accessory minerals. Chlorite, titanite, epidote/zoisite, and calcite formed during Eo-Alpine low to medium grade metamorphic overprint. Large Geierhaupt, Gr. Grst: Großer Griessstein, Pltz: Pletzen, Rk: Rosenkogel, SZ: Seckauer Zinken. Sample MM16 is a reference sample for the chemical composition of paragneisses K-feldspar idiocrysts, up to several cm in size, as well as quartz aggregates occur in a fine-grained groundmass of equigranular quartz and feldspar (Fig. 4a, b). The dominance of muscovite over biotite and a hiatial texture are observed in most samples. The modal composition comprises approximately 35-40 vol% quartz, 25-20 vol% K-feldspar, 20 vol% plagioclase, 5 vol% biotite (brownish to orange colored) and around 15-20 vol% muscovite.

Dikes
Granitic, leucogranitic and pegmatitic dikes intruded into paragneisses of the Glaneck Metamorphic Suite and metagranitoids of the Hochreichart Pluton. They show variable orientation and occur as both concordant and discordant dikes with respect to the penetrative paragneiss foliation. They are summarized in a "dike" group and are discussed separately. Sample locations are marked in Fig. 3. Finegrained granitic occur concordantly within the paragneisses (MM14, MM15) or penetrate them discordantly (MM54). Another granitic dike (MM69) was sampled within a biotite granodiorite gneiss. MM3 represents a leucogranitic dike intruded within a granite gneiss. Similar to the granites of the Griessstein Pluton the dike rocks are characterized by a fine-grained texture with the dominance of K-feldspar and muscovite and rare biotite. They also show, compared to the Griessstein Pluton, a similar modal composition of 35-30 vol% quartz, 25-20 vol% K-feldspar, 30-25 vol% Fig. 4 Representative photomicrographs of (a, b) granite gneiss MM27 from the Hochreichart Plutonic Suite, (c, d) hornblendebiotite quartz monzodiorite gneiss MM12 and (e, f) biotite granite MM18, both representative of the Pletzen Pluton (Hintertal Plutonic Suite) and (g, h) granite gneiss MM20 of the Griessstein Pluton (Hintertal Plutonic Suite). Photomicrographs on the left-hand side are shown with crossed polarizers and those on the right-hand side under parallel polarizers. All scale bars are 400 µm. Abbreviations: Bt: biotite, Hbl: hornblende, Kfs: K-feldspar, Ms: muscovite, Pl:plagioclase, Qz: quartz, Spn: sphene (titanite). Abbreviations for names of rockforming minerals follows Whitney and Evans (2010) plagioclase and around 10 vol% muscovite. Pegmatitic dikes (MM5, MM51 and SP61) crosscut paragneisses mainly discordantly. These dikes show a larger average grain size compared to the granitic dikes; the mineral assemblage is characterized by albitic plagioclase, K-feldspar, quartz and muscovite (approximately 30-25 vol% plagioclase, 20-15 vol% K-feldspar, 40-35 vol% quartz, 10-5 vol% muscovite) as well as titanite and tourmaline as accessory phases.

Whole-rock major, trace and rare earth elements
Major, trace and rare earth element (REE) compositions of forty-eight metagranitoids (including granitic, leucogranitic and pegmatitic dikes) are listed in supplementary Tables S2a-c and plotted in Figs. 5,6,7,8,9 and 10. Selected typical analytical data on major, trace and rare earth element (REE) compositions for the distinct plutonic suites are provided in Table 1 Table S2) were also included, as these are part of the complete data set discussed in this study. All metagranitoids of the Seckau Complex follow the calc-alkaline fractionation trend (Irvine and Baragar 1971) and in the Peccerillo and Taylor (1976) diagram the calc-alkaline to high K calc-alkaline series. Metagranitoid rocks of the Hochreichart Plutonic Suite (HrPS) predominantly fall in the granite field, whereas metagranitoids of the Hintertal Plutonic Suite (HtPS), subdivided into the Pletzen Pluton (PltzP) and the Griessstein Pluton (GrstP), range in their composition from quartz monzodiorite to granodiorite to granite (Fig. 5a).
Granites of the Hochreichart Plutonic Suite show a consistently peraluminous character (Shand 1943) and reflect S-type to minor I-type affinity (Chappell and White 2001) with A/CNK values (molar proportions of Al 2 O 3 / (CaO + Na 2 O + K 2 O)) in the range between 1.08 and 1.51 and A/NK values (molar proportions of Al 2 O 3 / (Na 2 O + K 2 O)) ranging from 1.15 to 1.73.
Metagranitoids of the Hintertal Plutonic Suite show a meta-to peraluminous trend for the Pletzen Pluton and peraluminous character for the Griessstein Pluton, with A/ CNK values ranging from 0.88 to 1.10 and 1.10 to 1.23 for the Pletzen and Griesstein Pluton, respectively. The A/NK values for the Pletzen Pluton range from 1.43 to 2.31, and from 1.34 to 1.58 for the Griessstein Pluton (Fig. 5b).
On the (Y + Nb) vs. Rb tectonic discrimination diagram for granites (Pearce et al. 1984) the metagranitoids of the Hochreichart Plutonic Suite and the Hintertal Plutonic Suite plot predominantly in the volcanic-arc granite field (VAG), reflecting geochemical signatures of an active continental margin. Only few samples are marginally located in the syncollisional granites field (syn-COLG; MM63, MM36) and in the within-plate granite field (WPG; MM33, SP79, MM32, SP59), respectively (Fig. 6). However, most likely, these samples also reflect a VAG setting.

Hochreichart plutonic suite
Binary major oxide vs. SiO 2 variation diagrams for peraluminous metagranitoids of the Hochreichart Plutonic Suite show typical fractionation trends for most of the major oxides. There is a general decrease in TiO 2 , Al 2 O 3 , MgO, CaO ( Fig. 7a- contents range from 0.21 to 2.05 wt% and from 0.04 to 0.17 wt%, respectively. Large ion lithophile elements (LIL), e.g., Rb, Ba (Fig. 8a, c) and transition metals such as Sc, V and Cr ( Fig. 8d-f), predominantly display a negative correlation with SiO 2 , whereas high field strength elements (HFSE e.g., Y, Zr, Nb) ( Fig. 8g-i) show no significant fractionation trend or display only a slight decrease against SiO 2 . Rb values are usually high and range between 91 and 229 µg/g, with the exception for samples MM13 (32 µg/g) and MM27 (64 µg/g), Sr contents are low with an average of about 100 µg/g, and Ba values vary from 186 to 956 µg/g. Sc contents are between 2 and 12 µg/g, V values ranges from 2 to 66 µg/g, and Cr contents vary between 1 and 35 µg/g. Y and Zr values range from 5 to 58 µg/g and 40 to 262 µg/g, respectively; Nb contents range from 4 to 17 µg/g (Table 1; supplementary Table S2a).
On the mantle-normalized (McDonough and Sun 1995) multi-element variation diagram, the metagranitoids of the Hochreichart Plutonic Suite show consistent trace element patterns, with enrichment in Rb, U, K, Pb, Nd, Sm and strong depletion in Ba, Nb, Ta, Sr, P and Ti as well as relatively flat distribution patterns in HREE (Fig. 9a) Table 1 Selected whole-rock major (wt%), trace element and REE compositions (μg/g) for metagranitoids of the Hochreichart and Hintertal Plutonic Suites; *major elements, Rb and Sr analytical data published in Mandl et al. (2018); published data are displayed in italic notation. Sample MM16 is a reference sample for the chemical composition of paragneisses that were used for rhyolite-MELTS calculations (Gualda et al. 2012) Hochreichart Plutonic Suite

Hintertal plutonic suite
Meta-to peraluminous metagranitoids of the Hintertal Plutonic Suite show similar fractionation trends compared to the Hochreichart Plutonic Suite for most major oxides (Fig. 7), but display a larger variation in SiO 2 and have a positive correlation of K 2 O with SiO 2 (Fig. 7f). However, trace element variation diagrams (Fig. 8) show clear differences in their distribution pattern of predominantly LIL elements. Rb indicates a positive correlation with SiO 2 (Fig. 8a), Sr a negative one (Fig. 8b), and Ba content is more or less constant with an average of about 1060 µg/g (Fig. 8c). Sc, V, Cr, Y and Zr indicate negative trends (Fig. 8d-h). Nb is more or less constant with an average of about 12 µg/g at SiO 2 values < 70 wt% and decreases then with increasing SiO 2 (Fig. 8i). Based on field observations, petrographic, geochemical and geochronological criteria, the metagranitoids of the Hintertal Plutonic Suite can be subdivided into (a) the Pletzen Pluton and (b) the Griessstein Pluton (Mandl et al. 2018). Consequently, metagranitoids of the Hintertal Plutonic Suite are discussed separately with regard to the aforementioned plutons.

Dikes
Granitic, leucogranitic and pegmatitic dikes vary widely in their major and trace element composition (Table 1; supplementary Table S2c). Partly they define a separate trend as seen in the SiO 2 vs K 2 O and SiO 2 vs Rb bivariate diagrams (Figs. 7 and 8). On mantle-normalized and chondritenormalized multi-element variation diagrams (McDonough and Sun 1995) the dikes fall into two distinct groups.
The first group contains pegmatitic dikes intruding the paragneisses (Glaneck Metamorphic Suite) (MM5, MM51, SP61). Further, one leucogranitic dike (MM3) and one granitic dike (MM69) intruded into the metagranitoids of the Hochreichart Plutonic Suite. The samples are dominated by positive Rb, U, K and Pb anomalies as well as negative Nb and Ti anomalies (Fig. 9g). On the chondrite-normalized (McDonough and Sun 1995) REE diagram (Fig. 9h), LREE and HREE patterns are relative constant with (La/Yb) N ranging from 1.51 to 3.52. A negative Eu anomaly with (Eu/ Eu*) N values vary from and 0.57 to 0.92, with the exception of sample MM3, which has a positive Eu anomaly.

Geochemical evolution of the magmatic suites of the Seckau Complex
The granitoids of the Seckau Complex were previously considered to be part of the intra-Alpine Variscan intrusive complexes (e.g., Schermaier et al. 1997). New geochronological data, however, revealed that the metagranitoids of the Seckau Complex are part of both Late Cambrian to Early Ordovician, and Late Devonian to Mississippian (i.e. early Variscan) plutons (Mandl et al. 2018). This requires, therefore, a re-evaluation of the pre-Alpine evolution of this part of the Eastern Alps, and its magmatic and geochemical development in particular, as the distinct plutonic suites need to be treated separately in terms of crystallization and fractionation trends. Both intrusive complexes, however, display geochemical characteristics of volcanic-arc granites and are therefore related to distinct active continental margins.

Hochreichart plutonic suite
Metagranitoids of the Hochreichart Plutonic Suite are chemically evolved and, calculated back to the time of emplacement (~ 496 Ma), display relatively low initial 87 Sr/ 86 Sr values between 0.7056 and 0.7061 (Table 2) displaying I-and S-type geochemical characteristics. These metagranitoids show generally high Rb values and a low Sr content resulting in a high Rb/Sr ratio, being typical for an evolved granitic magma. Negative fractionation trends of several major and trace elements indicate the crystallization of zircon, apatite, Fe-Ti-oxide, feldspar and subordinately of biotite with cooling. The presence of a negative Eu anomaly, seen in chondrite-normalized multi-element variation diagrams (Fig. 9b), indicates the crystallization and fractionation of plagioclase from the granitic source. Table 2 Calculated initial 87 Sr/ 86 Sr for metagranitoids of the Hochreichart Plutonic Suite (HrPS) and the Hintertal Plutonic Suite (Pletzen Pluton (HtPS, PltzP) and Griessstein Pluton (HtPS, GrstP)). Rb and Sr data (µg/g) were taken from Pfingstl et al. (2015) and the average age of the respective granitoids were calculated from U-Pb zircon ages represented in Mandl et al. (2018)  The similar geochemical behavior of K and Rb is also a good indicator to demonstrate fractionation effects on granitic melts (Cerńy et al. 1982;Quemeneur and Lagache 1999;London 2008). The correlation of e.g., K/Rb ratio vs. Sr (Fig. 10i) suggests that the studied granitoids of the Griesssstein Pluton are generally more evolved than the Pletzen Pluton granitoids and thus most likely have been derived from the same source. Interestingly, sample (a-h) SiO 2 (wt%) vs major oxides (wt%) and trace elements (µg/g). (i) K/Rb ratio vs trace elements (µg/g) for metagranitoids of the Pletzen Pluton and the Griessstein Pluton as well as for pegmatitic and granitic dikes MM22 deviates in this variation diagrams from the trend and might indicate slight wall rock contamination. The spatial relationship of the different plutonic bodies, with small volumes of the Late Devonian/Early Carboniferous Griessstein Pluton occurring between the Late Devonian/Early Carboniferous Pletzen Pluton and the Late Cambrian/Early Ordovician Hochreichart Suite, points to two explanation models: (1) the Griessstein Pluton is the result of contamination of the Pletzen Pluton by the Hochreichart Suite wall rock or (2) the Griessstein Pluton represents a more evolved Pletzen Pluton composition. We therefore discuss the chemical characteristics of the different plutonic suites and use rhyolite-MELTS (Gualda et al. 2012) to compare observed compositions with calculated ones.
A possible assimilation of Hochreichart granitic rocks into the marginal portions of the Pletzen intrusives was tested in order to explain the differences between the two plutons of the Hintertal Suite. By using average major and trace element compositions of Hochreichart and Pletzen plutonic rocks it was not possible to obtain the measured composition of the Griessstein Pluton. Assuming an assimilation of 10% of the Hochreichart Pluton, lower SiO 2 and Rb values as well as higher Sr, V, Cr and Nd values would be required to reproduce the chemical composition of the Griessstein Pluton. Alternatively, we have also tested the Glaneck Metamorphic Suite paragneisses as contaminant for the Pletzen intrusives (representative chemical composition data of paragneisses are provided in Table 1; sample MM16, Fig. 3). Again, the observed chemical composition of the Griessstein Pluton could not be reproduced: by mixing 10% of paragneiss to the Pletzen Pluton; SiO 2 , TiO 2 , and Al 2 O 3 remain constant, K 2 O and Rb decrease and MgO increases. Therefore, we consider the Griessstein Pluton to be the product of a fractionation process from the Pletzen Pluton where probably only small amounts of wall rock or a SiO 2 -rich melt were assimilated. Major element calculations derived from rhyolite-MELTS demonstrate that, at isobaric crystallization conditions of 0.3 GPa, 20 to 30% of the Pletzen melt (calculated with an average composition of the samples MM17, MM18, MM19, MM23, MM55, MM56, MM65) needs to crystallize in order to produce a composition close to the Griessstein Pluton (calculated with an average composition of the samples MM20, MM21, MM22, MM52, MM53, SP53) ( Table 3). The more evolved nature of the Griessstein pluton is responsible for the peraluminous nature and stability of muscovite. The Sr isotopes are similar to the Pletzen Pluton. When considering the geochemistry of the Griessstein Pluton, then a I-to S-type character can be inferred, as the Sr isotopes display I-type, and the peralkaline affinity S-type characteristics. We conclude that the Griessstein Pluton is the result of 20 to 30% fractionation of mainly plagioclase and amphibole, among other minerals (e.g., Chappel et al. 2012). The K/Rb ratio does not significantly increase (approx. 10 to 20% relative) by fractionation of 20 to 30%, as the Rb values only change slightly (10 to 15%), and the K values remain high. However, in Harker diagrams the Griessstein Pluton Rb values are always higher and the Sr values are lower-as expected-compared to the Pletzen Pluton. A slight Eu anomaly is obselvable indicating the proposed plagioclase fractionation. Considering the arguments regarding rhyolite-MELTS calculations described above, as well as the quite similar ages of the Pletzen and Griessstein Pluton (Mandl et al. 2018), we infer that although the Griessstein Pluton geochemically shows, for some portions, S-type character, it genetically evolved from metaluminous I-type melt. Based on the equation of Watson and Harrison (1983), whole-rock zircon saturation temperatures (T Zr ) were calculated for both plutons of the Hintertal Plutonic Suite. Calculated T Zr of the parental Pletzen Pluton range from 765 to 833 °C with an average of 793 °C. The Griessstein Pluton indicates insignificant lower temperatures ranging from 764 to 814 °C with an average of 788 °C.
The Griessstein Pluton as currently exposed, however, only accounts for approximately 10% of the total Hintertal Plutonic Suite. Either it is just the result of fractionation of small volumes of the original plutonic source, or the Griessstein Pluton intruded at shallower crustal levels and large parts of it were eroded during subsequent uplift of the Variscan Orogen and / or post-Variscan continental rifting. Granitoid components recovered in the Permian clastic meta-sediments of the Rannach Formation have a similar appearance to the Griessstein rocks. Thus, erosion of essential parts of the Griessstein Pluton is rather likely.  (Mandl et al. 2018) and are interpreted as late fractionation products from the same source region of the Pletzen Pluton, as can be seen by various variation plots e.g., Al 2 O 3 , MgO, P 2 O 5 vs. SiO 2 (Fig. 7a, b, g) as well as e.g., Sr vs. SiO 2 and V vs. SiO 2 (Fig. 8b, e).

Pre-Variscan evolution
In late Neoproterozoic to Early Cambrian times northern Gondwana destabilized through activity and retreat of the Cadomian Arc. However, the late Cambrian / Ordovician evolution was diachronous in several Peri-Gondwana fragments. Its eastern segments, hosting the future Alpine basement units, experienced short periods of ocean floor formation and re-amalgamated to Gondwana-derived continental blocks in Early Ordovician times (e.g., Frisch et al. 1987;Stampfli et al. 2013;von Raumer et al. 2013von Raumer et al. , 2015Cocks and Torsvik 2021). Thus, in this part of the former eastern Gondwana margin, two sutures are thought to exist, an older (Cadomian) suture and a younger suture that formed in Ordovician times. The latter is sometimes referred to as Ceneric suture or Ceneric Orogen (e.g., Zurbriggen 2017; Burda et al. 2021). Remnants of Cambrian / Lower Ordovician short-lived oceanic and riftrelated fragments scatter along the Western Alps, Eastern Alps and Carpathians including the Chamrousse ophiolite (Western Alps: ca 500 Ma), the Ötztal and Silvretta gabbros and the Seckau-Schladming metabasites (520-510 Ma), eclogite protolith and arc basalts (ca. 530-490 Ma) south of the Tauern Window and ca. 498 Ma old island-arc related igneous rocks from the Carpathians (for summary see Faryad and Hoinkes 1998;Faryad et al. 2002;Haas et al. 2020;Burda et al. 2021;Huang et al. 2021). Our data from the Hochreichart Suite with 508 ± 9 Ma to 486 ± 9 Ma old arc-related granitoids suggest the existence of a Ceneric active margin with its remnants now exposed in the Seckau Complex. The exact position of this arc segment along a probably Ceneric or Proto-Rheic subduction zone (Burda et al. 2021) expanding from today's North Africa to south China cannot be resolved from our data (Fig. 11a). Considering the age of eclogite facies metamorphism of the Ceneri Complex (Franz and Romer 2007), indicating peak metamorphic conditions of 710 ± 30 °C at 2.1 ± 0.25 GPa, dated by U-Pb zircon and rutile at 457 ± 5 Ma and 443 ± 19 Ma indicating a Late Ordovician age of subduction metamorphism, the Hochreichart Pluton may represent a magmatic arc along the Ceneric active margin (Fig. 11) that predates the closure of the Proto-Rheic ocean.

Variscan evolution
For the Variscan evolution, two in part contrasting models exist. Kroner and Romer (2013) argue for the existence of a single ocean, the Rheic Ocean (Zulauf 2007), that closed shortly before the Variscan orogeny. In their model many subduction zones evolved within former northern Gondwana, the "Armorican Spur", but most of them are considered as intracontinental subduction zones. Another group of authors (Stampfli et al. 2002(Stampfli et al. , 2013von Raumer et al. 2013von Raumer et al. , 2015Franke et al. 2017) favor the existence of microcontinents (Hun or Galatia Terranes) that amalgamated by closure of multiple, probably small oceanic basins. Since remnants of related ophiolites are not preserved within the Seckau Complex we hardly can support one of those assumptions. However, we can confirm the existence of related early to mid-Variscan (365 ± 8 Ma to 343 ± 12 Ma) plutons with calc-alkaline meta-to peraluminous (Pletzen Pluton) and peraluminous character (Griessstein Pluton) (the term "mid Variscan" in this context refers to von Raumer and Stampfli 2008). These are interpreted to represent arc granitoids corresponding to the early Variscan "Cordillerian" I-type suite. Those granitoids scatter all over the Variscan belt and occur within the northern Saxothuringian (Odenwald), in Central Bohemia (Central Bohemian Batholith; Košler and Farrow 1994;Zák et al. 2011) and the intra-Alpine realm (e.g., eastern part of the Hohe Tauern Batholith, Schladming Batholith) (e.g., Finger et al. 1997). Granitoids with similar geochemical characteristics ("Cetic granitoids") also occur, as exotic fragments, along the southern margin of the Bohemian Massif, close to the northern front of the Eastern Alps. The so-called "Cetic granitoids" are embedded in sediments of the Ultrahelvetic and the Rheno-Danubian Flysch Belt and are considered to be part of the Cetic Massif, a hypothetical crystalline basement block which adjoins the Moldanubian Unit to the south and underneath the Eastern Alps . Considering the fact that the intra-Alpine, early Variscan arc granitoids occur far to the south of the classic ophiolite-decorated Rheic suture, expanding from the British Lizard Complex to the Mid-German Phyllite Zone, we argue for the existence of multiple arcs and closure of multiple oceanic basins. This is supported by findings of early Variscan ca. 370 Ma old meta-ophiolites in the Alpine Carpathian realm (Putis et al. 2009;Burda et al. 2021). Subsequently, in Tournaisian to Visean (Mississippian) times, flysch type sediments were deposited within low-grade metamorphosed fossiliferous units, presently exposed in the Eastern Alps (Hubmann et al. 2013). Flysch sediments overlie passive continental margin sedimentary sequences that were deposited either on the northern Gondwana margin (e.g., Neubauer and Handler 2000) or on the southern rim of Galatia (e.g., Haas et al. 2020). These data suggest a model with double-sided subduction, the southern of which has northward polarity and dips below the Galatia fragment (von Raumer et al. 2013). The general paleogeographic position of the Seckau Complex during the Variscan orogenic phase is considered to be south to southeast of the Bohemian Massif, proximal to the eastern Hohe Tauern, the Schladming Tauern, and the Western Carpathians . Granitoid emplacement Fig. 11 a) Late Cambrian -Early Ordovician plate tectonic situation. Future Alpine Basement hosting Seckau magmatic suites are located along the Ceneric active margin (modified after Burda et al. 2021). b) Late Devonian -Tournaisian plate tectonic situation and cross section across Galatia microcontinent with bipolar subduction of Paleotethys and Rheic-Rheno-Hercynian (R) oceans (modified after Haas et al. 2020) can be related to the closure of differently termed oceanic domains (Galicia-Moldanubian Ocean or Paleotethys: Paleotethys in Fig. 11b).

Conclusions
There is wide consensus that pre-Alpine crustal blocks now distributed within the Eastern Alps derived from the former northern Gondwana margin. However, magmatic and tectonic phases that cover a time range from Cambrian Gondwana destabilization to Pangea formation remained unresolved so far. As the metagranitoids of the Seckau Complex are part of both late Cambrian to Early Ordovician and Late Devonian to Mississipian (early Variscan) intrusive complexes, a re-evaluation of the magmatic and geochemical pre-Alpine evolution of this part of the Eastern Alps is required. Our geochemical data, together with previously published age data, allow the reconstruction of these phases.
The Late Cambrian to Early Ordovician metagranitoids of the Hochreichart Plutonic Suite can be classified as part of a magmatic arc system along the northern Gondwana margin. Calcalkaline suites developed above the southward subducting Prototethys ocean. Retreat of this arc opened short -living oceanic basins (now preserved, e.g., in the Speik Complex ;Neubauer 1988;Neubauer et al. 1989;Neubauer and Frisch 1993) that may have been closed shortly after their formation.
In the Middle Ordovician continental slivers succeeded to rift off the northern Gondwana margin through opening of the Paleotethys. This ocean closed during Devonian -Early Carboniferous times including the formation of a second magmatic arc system at c. 350 Ma, represented by the metato peraluminous Hintertal Plutonic Suite. The early Variscan granitoids of the Seckau Complex are interpreted as part of an active margin that evolved to the south of today's Bohemia and the Hohe Tauern. Final collision between Gondwana and Laurussia formed late Variscan granitoids now exposed in the western Tauern Window, the European basement of the Swiss Alps (e.g. Aar Massif) and the Bohemian Massif.