1 Introduction

Although the European Alps are investigated intensively by more than 200 years, there are still areas where modern data or even detailed geological maps are rare. One of these areas is situated in the Austroalpine units to the south-east of the Tauern Window, the so-called Kreuzeck Mountains (Figs. 1, 2a). In this area the WNW-trending, south-dipping Main Mylonite Zone (Hoke 1990) forms the contact between two units that differ significantly in their structural and metamorphic history (Figs. 2b, 3) (e.g. Schuster et al., 2004, 2013). Hoke (1990) already pointed out the importance of this shear zone that has been interpreted as a normal fault that was active from the Late Cretaceous to the Early Paleogene. In places the Main Mylonite Zone is affected by brittle faults, which rework the mylonites along their strike (Figs. 2b, 3).

Fig. 1
figure 1

Tectonic map of the Eastern Alps following the nomenclature of Schmid et al. (2004) (modified after Froitzheim et al. 2008). BF Brenner normal fault, KF Katschberg normal fault, DAV Defereggen-Antholz-Vals fault, SEMP Salzach-Ennstal-Mariazell-Puchberg fault, PF Pustertal fault, MV Möll valley fault

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Fig. 2
figure 2

a Tectonic map of the Kreuzeck Mountains and neighbouring areas (modified after Schuster et al. 2013). b Digital elevation model of the study area with sample localities of fission track samples (coordinates are given in Tables 1 and 2)

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Fig. 3
figure 3

Simlified geological map of the study area (modified after Hoke 1990) with localities of CPO samples. Coordinates (WGS 1984) and elevation: KR 11: N 46°53′27.6″ E 13°08′20.4″ 1924 m; KR 19: N 46°53′13.2″E 13°08″9.6″ 2080 m; KR 20: N 46°53′06″ E 13°53′06.12″ 2230 m; KR 22: N 46°53′02.4″ E 13°08′49.2″ 2220 m; KR 24: N 46°53′34.8″ E 13°08′16.8″ 1872 m

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The aim of this study is to shed more light into the kinematic and temporal evolution of the Main Mylonitic Zone and adjacent brittle faults. For this purpose we provide microstructural analysis of quartz-rich rocks including quartz texture analyses. Since it is well documented that both intracrystalline- and recovery processes are strongly T-dependent and form diagnostic microstructures and textures (e.g. Hirth and Tullis 1992; Stipp et al. 2002a, b, 2006) we will link our results with thermochronological data to evaluate the timing of deformation. To unravel the timing of brittle faulting we attempt to date thermal anomalies within fault zones by comparison of zircon- and apatite fission track data (ZFT, AFT) at the transition from fault-related rocks to the undeformed host rock. For this we choose the Ragga–Teuchl fault, a cataclastic fault zone that borders the northern part of the Main Mylonite Zone in the east and strikes away from the mylonites in the western part of the study area (Fig. 2b, 3). Additionally we sampled a well exposed brittle fault to the north of the Ragga Teuchl fault (sample KR 5 in Fig. 2b). Our results show that multidisciplinary methods may provide information about the evolution of a rather small study area from the Late Cretaceous to Late Miocene times.

2 Geological setting and geochronology of the study area

The Eastern Alps are composed of units derived from the European continent, the Penninic oceanic realm and units derived from the Adriatic microplate (Figs. 1, 2a). The Southalpine and Austroalpine units represent the Adriatic microplate and are widely exposed in the Eastern Alps while the units derived from the Penninic oceanic realm and the European margin are mainly exposed in tectonic windows like the Tauern Window (Fig. 1).

The study area is located to the southeast of the Tauern Window (Figs. 1, 2) which consist of polyetamorphic rocks which were overprinted from the Devonian to the Cretaceous (e.g. Hoinkes et al. 1999; Neubauer et al. 1999). The WNW-trending, south-dipping Main Mylonite Zone is situated at the contact of the Prijakt–Polinik and Strieden Complex to the north and south, respectively (Fig. 2) (Schuster et al. 2004, 2013). The mylonitic foliation and stretching lineation generally strikes E–W and/or WNW–ESE (Fig. 3) and kinematic indicators suggest that the Main Mylonite Zone acted as a normal fault where the Strieden Complex moved over the Prijakt–Polinik Complex (Hoke 1990).

The Prijakt–Polinik Complex experienced a metamorphic imprint under amphibolite to eclogite facies conditions during the Eo-Alpine metamorphism (Schmid et al. 2004; Schuster et al. 2001, 2004). Published geochronological data from the Prijakt-Polinik Complex include Cretaceous K/Ar- and Ar/Ar ages on white mica and biotite (Oxburgh et al. 1966; Lambert 1970; Waters 1976; Hoke 1990; Dekant 2009; Wölfler et al. 2015). The Strieden Complex experienced only an anchizonal to lowermost greenschist facies Eo-Alpine imprint (Schuster et al. 2001, 2004). K/Ar and Ar/Ar ages on white mica and biotite reported from the Strieden Complex are between 337 and 141 Ma (Brewer and Jenkins 1969; Brewer 1970; Waters 1976; Hoke 1990; Dekant 2009; Wölfler et al. 2015).

During the Miocene lateral extrusion the whole area was affected by steeply dipping brittle faults (Figs. 2b, 3). According to the distribution of ZFT and AFT data, the Ragga–Teuchl fault separates the study area into two domains with different ages (Wölfler et al. 2008). The Polinik Block to the north of the Ragga–Teuchl (Fig. 2b) fault displays ZFT and AFT data from 45 to 30 Ma and 23 to 7 Ma, respectively (Staufenberg 1987; Dunkl et al. 2003; Wölfler et al. 2008, 2015). The southern block, referred to as Kreuzeck Block (Fig. 2b), is characterised by ZFT and AFT ages from 160 to 54 Ma (Dunkl et al. 2003; Wölfler et al. 2008, 2015) and 33 to 20 Ma (Staufenberg 1987; Wölfler et al. 2008, 2015), respectively. Since the Main Mylonite Zone and the Ragga–Teuchl fault were active at different times we refer the terms Prijakt-Polinik and Strieden Complex to the Cretaceous to Paleogene activity of the Main Mylonite Zone and the terms Polinik and Kreuzeck Blocks to the Oligocene to Miocene activity of the Ragga-Teuchl fault.

3 Methods

The study of microstructures and textures of quartz is aimed to document possible changes in deformation mechanisms that are known to be sensitive to temperature, strain rate, stress and water content (e.g. Hirth and Tullis 1992; Stipp et al. 2002a, b, 2006). For temperature estimates of different dynamic recrystallization mechanisms of quartz we refer to Stipp et al. (2002a). Therefore, below ~300 °C pressure solution and cataclasis are the main deformation mechanisms. Bulging mechanisms (BLG) are active between ~300 and 400 °C and subgrain rotation mechanisms (SGR) are dominant between ~400 and 500 °C. At temperatures above ~500 °C grain boundary migration recrystallization (GBM) is dominant.

We used the X-ray texture goniometer facility of the Institute of Earth Sciences, University Graz in Austria to evaluate crystallographic preferred orientation of quartz. Polished rock chips were placed in the X-ray beam of a texture goniometer (wavelength CuKα = 1.5418, beam current = 40 kV and 40 mA) used in reflection mode. The Brucker Analytical Systems X-ray texture goniometer (D8 Discover) is equipped with an area detector (Gadds HTS). Eight lattice directions (<100>, <110>, <102>, <200>, <201>, <112>, <211>, <113>) have been measured at angle between 0° (center) and 80° (periphery). Fourier analysis were applied for correction of defocusing effects. Lattice planes <001>, <101> and <011> were calculated using the orientation density function (ODF) based on the harmonic method of Roe (1965) and Bunge (1981). For detailed description of the technical procedure see Wenk (1985). Representative <c> -axes (<001>) and a-axes (<110>) orientation distributions are shown as pole figures. In all diagrams the foliation is vertical E–W and the stretching lineation X is oriented horizontal E–W, Y is the centre and Z, the direction of minimum extension is N–S. From the asymmetry of <c>-axes and a-axes with respect to the foliation, the sense of shear was determined.

For fission track thermochronology we used the zircon- and apatite fission track (ZFT, AFT) methods, whose sensitivity intervals are referred to as zircon- and apatite fission track partial annealing zones (ZPAZ, APAZ), ranging from 300 to 200 °C and 120 to 60 °C, respectively (Wagner and Van den haute 1992; Green et al. 1986). The zeta calibration approach was used to determine the ages (Hurford and Green 1983). For thermal history modelling of ZFT and AFT data we used the HeFTy software (Ketcham 2005) with annealing algorithm of Ketcham et al. (1999). We used the following input parameters: single grain AFT ages, c-axis corrected track lengths with standard deviation, Dpar values as kinetic parameters (Dpar: mean diameter of etch figures on prismatic surfaces of apatites parallel to the crystallographic c-axis; Burtner et al. 1994). The starting conditions of the samples are constrained by the ZFT ages and their one sigma errors within the temperature range of 300–200 °C. Final modelling constraint is the surface temperature of ~10 °C.

For dating thermal anomalies within brittle fault zones we sampled two sites with well exposed fault cores, damage zones and host rocks (Figs. 2b, 4). The first one is situated in the Polinik Block (sample KR 5 in Fig. 2b) and displays a ~1 m wide fault core that is surrounded by a ~5 m wide damage zone (Fig. 4a, d). The fault core consists of a fine grained gouge- and cataclasite matrix with clasts that partly reach ~50 µm in diameter (Fig. 4b) and the damage zone is characterized by an strongly fractured gneiss (Fig. 4c). The second brittle fault zone is situated along the Ragga–Teuchl fault and consist of a ~5 m wide fractured zone with several fault cores that is surrounded by a ~10 m wide damage zone (Fig. 4e). In the area of investigation the brittle fault plane dips steeply to the south (185/80). In contrast to the single fault core of the fault zone in the Polinik Block (Fig. 4a, d), the fault core consists of several branching and anastomosing cores that are separated by a strongly fractured damage zone material (Fig. 4e). The damage zone is composed of a strongly sheard orthogneiss. The fault core related rocks continuously develop from fault breccias and coarse grained cataclasites towards fine-grained cataclasites and fault gouges. Both, fault cores and damage zones display signatures of faulting and/or fluid circulation, such as the occurrence of cataclasites and fault gouges, slickensides and secondary grown minerals.

Fig. 4
figure 4

a Damage zone and fault core (sample KR5) within the Polinik Block. AFT ages and track length distributions differ significantly (orientation of the fault plane: 045/79). b Fine grained gouge material of the brittle fault. c Damage zone structure of the brittle fault. d Sketch of the brittle fault in the Polinik Block. The fault zone comprises on single fault core composed fine-grained, grey-coloured gouges and lensoid dark cataclasites (shown in black). KR5 fc (fault core) and KR5 dz (damage zone) display sample localities for fission track analysis. For comparison see Fig. 4a. e Sketch of the brittle structure along the Ragga–Teuchl fault. The fault zone shows multiple cores that are separated and surrounded by damage zone material. KR6 fc (fault core) and KR6 dz (damage zone) display sample localities for fission track analysis

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4 Results

4.1 Quartz microstructures and crystallographic preferred orientations (CPO)

The quartz microstructures from the Polinik Block (sample KR24 of Fig. 3) are characterized by polygonal quartz grains with mainly straight boundaries partly showing 120° triple junctions and a grain size of up to 0.5 mm (Fig. 5a). The CPO pole figures of this sample display c-axes [001] and a-axes [110] with a tendency towards the formation of a single girdle distribution (Fig. 5a). The maximum of the c-axes is located at the Y-axis of the finite strain ellipsoid and the a-axes are symmetrically arranged with respect to the foliation (Fig. 5a).

Fig. 5
figure 5

CPO and Quartz microstructures from the (a) Prijakt–Polinik Complex, the Main Mylonite Zone (b, c and d) and from the Strieden Complex (e).The red arrows in (e) document microcracks. The pole figures are lower hemisphere projections nad logarithmic gradiated. Schistosity (s) and lineation (l) are given in the top right corner of the pole figures

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The quartz microstructures from the Main Mylonite zone (samples KR11, KR19, KR22 of Fig. 3) display sutured grain boundaries and elongated porphyroclasts forming ribbon grains (Figs. 5b, c, d) with a long axis of up to 1 mm. Recrystallized grains are small and do not exceed 0.03 mm. In places the formation of core-mantle structures can be observed (Fig. 5b). The grain boundaries are largely irregular and undulatory extinction and bulges are widespread features.

The CPO pole figures of sample KR11 displays a single girdle distribution with one peripheral maximum oblique to Z (Fig. 5b). The asymmetry of the c-axes indicates a top-to-the-NW shear component. The a-axes are accordingly distributed along a great circle which is 20° oblique to the trace of the foliation, thus confirming a top-to-the-NW displacement (Fig. 5b). The c-axes distribution of sample KR19 shows a main maximum close to Y with a relict or weak single girdle distribution (Fig. 5c). The asymmetry of the c-axes distributions is 15° oblique to the foliation and documents a top-to-the-NW shear component (Fig. 5c). Two a-axes maxima are symmetrically distributed around the lineation with an opening angle of 15°. The unequal maxima indicate a transition from single to type I cross girdle with stronger maximum pointing towards sinistral, i.e. top NW shearing (Fig. 5c). Samples KR22 and KR20 show c- and a-axes indicating a mixed single-cross girdle distribution which indicates a combination of pure and simple shear (Figs. 5d, e). Sample KR20 from the Kreuzeck Block shows large quartz porphyroclasts that appear only slightly elongated (Fig. 5e). Widespread features are undulose and patchy extinction, bulges and microcracks (arrows in Fig. 5e). Bulges are developed along grain boundaries and along fractures. The main deformation mechanism is bulging recrystallization. The c-axes and a-axes distributions are characterized by a single girdle distribution that is 15° oblique to the foliation, documenting top-to-the-NW transport (Fig. 5d).

4.2 Fission track data and thermal history models

ZFT and AFT ages are reported as central ages with 1 sigma errors and are summarized in Tables 1 and 2. Sample locations and age data are indicated in Fig. 2b and Tables 1 and 2. Samples KR5 and KR6 are from brittle faults and each comprise one sample from the fault core (KR5 fc, KR6 fc) one from the damage zone (KR5 dz, KR6 dz) and one from the host rock (KR5 hr, KR6 hr). That means that for these two samples three different rocks have been sampled which have the same capital letters and numbers.

Table 1 New zircon fission track data
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Table 2 New apatite fission track data
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Sample KR9 from the Kreuzeck Block displays ZFT and AFT ages of 67.3 ± 3.9 Ma and 32.8 ± 2.9 Ma, respectively (Figs. 2b, 6 Tables 1, 2). Sample KR8 from the Main Mylonite Zone has a ZFT age of 60.4 ± 4.3 Ma and an AFT age of 33.2 ± 1.9 Ma. The samples KR6 hr and KR6 fc from the Ragga-Teuchl fault display ZFT ages of 55.6 ± 3.3 and 54.2 ± 3.6 Ma, respectively. The AFT ages of the samples KR6 hr and KR6 dz overlap within 1 sigma error and are characterized by similar track length distributions (KR6 hr: 30.4 ± 1.1 Ma and 13.95 ± 0.8 µm; KR6 dz: 28.6 ± 2.7 Ma and 13.51 ± 1.26 µm). However, the fault core sample KR6 fc displays a younger AFT age and shorter track lengths (23.3 ± 0.8 Ma and 11.51 ± 1.95 µm) (Figs. 2b, 6; Table 2).

Fig. 6
figure 6

Zircon- (ZFT), apatite fission track (AFT) ages and mean track length distributions (MTL) against elevation for the Kreuzeck Block, the Polinik fault and the Polinik Block. Circles Kreuzeck Block; squares Polinik fault; polygons Polinik Block; black host rock (hr); green damage zone (dz); red fault core (fc)

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The same applies to the samples from the brittle fault zone in the Polinik Block (sample KR5). The host rock sample yields a ZFT and AFT age of 41.2 ± 2.8 and 15.9 ± 1.0 Ma, respectively. The samples from the damage zone display a ZFT age of 40.5 ± 2.8 and a AFT age of 16.4 ± 0.7. Although the ZFT age from the fault core sample of 40.1 ± 2.2 is similar compared to the ages from the damage zone and host rock (Figs. 2b, 6; Table 1) the AFT data from the fault core display younger AFT ages and shorther MTL (11.5 Ma and 11.75 µm) as observed in the corresponding damage zone and host rock (Figs. 2b, 6; Table 2).

Both fault core samples display not only shorter MTL but also a bimodal distribution of the track lengths and a large standard deviation (Table 2) that are typical for reheated samples (Gleadow et al. 1986).

The thermal history models of host rock samples KR9 hr, and KR6 hr demonstrate that the Kreuzeck Block and the samples from the Ragga-Teuchl fault entered the APAZ in Eocene/Oligocene times (Fig. 7a, b). In contrast, the Polinik Block reached the temperature range of the APAZ in the early Miocene (Sample KR 5 hr and KR5 dz in Fig. 7c, d).

Fig. 7
figure 7

Thermal history inverse models using the HeFTy program (Ketcham 2005). Input parameters: central AFT age with 1 σ error, track length distributions, Dpar values as kinematic parameters. Meas. measured age, Mod. modeled age, GOF goodness of fit, AFT apatite fission track age, MTL/SD mean track length/standard deviation. Black boxes are starting conditions defined by the corresponding ZFT ages; blue boxes define final cooling; green paths acceptable fit; red paths good fit; black line best fit

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5 Interpretation and discussion

5.1 Deformation mechanisms and kinematics related to the regional geological frame

Quartz microstructures from the Main Mylonite Zone are characterized by bulging, sutured grain boundaries, undulatory extinction and a size of recrystallized grains that do not exceed 0.03 mm. These features are indicative for bulging recrystallization (Stipp et al. 2002a, 2010). In places, the formation of core-mantle structures document the transition from bulging recrystallization to subgrain rotation recrystallization (Stipp et al. 2002a). Both recrystallization mechanisms are dominant at temperatures between ~300 and ~450 °C, thus at greenschist facies conditions (Stipp et al. 2002a, 2004).

The temperature range for the muscovite K/Ar and Ar/Ar systems are 430–375 °C and 450–350 °C, respectively (Hames and Bowering 1994; Kirschner et al. 1996; Lips et al. 1998; Harrison et al. 2009), and are in the same range as the temperatures for bulging recrystallization. K/Ar and Ar/Ar muscovite data from the Main Mylonite Zone are between 90 and 78 Ma (Brewer and Jenkins 1969; Brewer 1970; Hoke 1990; Dekant 2009; Wölfler et al. 2015).

As the CPO data indicate top-to-the-NW directed shearing (Figs. 5b–d), we propose that this deformation occurred in the Late Cretaceous contemporaneous to a phase of extension that has been observed in different parts of the Austroalpine nappe stack (e.g. Froitzheim et al. 1997, 2012; Fügenschuh et al. 2000; Liu et al. 2001; Kurz and Fritz 2003). Substantial parts of the Austroalpine nappe pile was overprinted by normal faulting during the Late Cretaceous, associated with formation of the Gosau sedimentary basins (Wagreich 1995; Froitzheim et al. 1994; Neubauer et al. 1995, 2000). In this context the Main Mylonite Zone acted as a normal fault (Hoke 1990) that brought the Strieden Complex on top of the Prijakt–Polinik Complex.

As the transition from ductile to semi-brittle and brittle deformation has been determined between ~300 and ~270 °C (Handy et al. 1999; Stipp et al. 2002a) and the temperature range of the ZFT system ranges between 300 and 200 °C (Wagner and van den Haute 1992), the ZFT data from the Main Mylonite Zone of 60.4 ± 4.3 (Fig. 2b) is considered as the lowermost age limit for ductile to semi-brittle deformation. Since then the Main Mylonite Zone resided in the brittle part of the upper crust (Fig. 8).

Fig. 8
figure 8

Summary of geo- and thermochronological data from the Main Mylonite Zone. K/Ar (muscovite): Waters (1976), Hoke (1990); Ar/Ar (muscovite): Dekant (2009); ZFT: this study; AFT: this study; K/Ar (illite): Kralik et al. (1987)

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Metamorphic conditions in the Polinik Complex reached peak temperatures of 620 °C at ~100 Ma (Hoke 1990). Available Ar/Ar and ZFT ages range from 101 to 67 Ma and 45–30 Ma, respectively (Hoke 1990; Dekant 2009; Wölfler et al. 2008, 2015). The observed quartz microstructures from the Polinik Complex differ from those of the Main Mylonite Zone. They are characterized by polygonal grains with straight grain boundaries, partly forming triple junctions (Fig. 5a). This is indicative for static recrystallization at amphibolites facies conditions at least at ~500° (e.g. Stipp et al. 2002a). We therefore suggest that static recrystallization occurred after metamorphic peak conditions in the Late Cretaceous.

Quartz microstructures from the Strieden Complex are dominated by bulging recrystallization that demonstrate deformation at lower temperatures, roughly between 300 and 400 °C (Stipp et al. 2002a) (Fig. 7e). The CPO data show an asymmetry of the pole figure that indicates top-to-the-NW directed deformation too (Fig. 5e). The Strieden Complex displays Ar/Ar and K/Ar data of white mica that are between 226 and 141 Ma (Hoke 1990; Dekant 2009; Wölfler et al. 2015) and ZFT ages range from 160 to 60 Ma (Dunkl et al. 2003; Wölfler et al. 2008, 2015). Due to this large spread in age data we are not able to estimate the age of the NW-directed deformation in the Strieden Complex. However, we speculate that it is also related to the late Cretaceous NW-directed deformation as observed in the Main Mylonite Zone, just a few meters away (Fig. 3) and as also observed by Hoke (1990).

In summary we conclude that the observed deformation along the Main Mylonite Zone is related to the well documented late Cretaceous extensional phase in the Eastern Alps.

5.2 Fission track data and implications for brittle deformation

The distribution of fission track data and the modelled thermal histories demonstrate that the Kreuzeck and Polinik Block experienced different cooling histories during the Paleogene and Neogene (Fig. 7). Cooling to conditions of the APAZ occurred during Oligocene/early Miocene and middle Miocene times for the Kreuzeck and Polinik Block, respectively. This difference has already been interpreted as a consequence of extension during Miocene lateral extrusion (Wölfler et al. 2008). Therefore the Ragga–Teuchl fault marks the border between footwall and hanging wall units (Polinik- and Kreuzeck Block, respectively) that experienced different cooling histories between the Oligocene and middle Miocene (Wölfler et al. 2015).

The sampled brittle fault zones display different widths and architecture of the corresponding fault core (Fig. 4d, e). Additionally, both fault cores are situated in different host rocks i.e. a paragneis in the the fault zone in the Polinik Block (sample KR 5 in Figs. 2b, 4a, d) and an orthogneiss in the sample of the Ragga-Teuchl fault (sample KR 6 in Figs. 2b, 4e). Therefore, the different style of the fault cores may reflect differences in mechanical strength between host rock and fault zone (e.g. Faulkner et al. 2010).

The ZFT ages of fault related rocks of the Ragga–Teuchl fault and the Polinik Block are similar to those of the host rocks (Figs. 2b, 6). However, fault core related AFT ages are younger and corresponding track lengths are shorter than in the related damage zones and fault cores (Figs. 2b, 6). By applying ZFT, AFT and apatite (U-Th)/He dating, several studies demonstrated significant thermal anomalies due to the infiltration of hot fluids in brittle faults (Tagami et al. 2001; Tagami and Murakami 2007; Yamada et al. 2007; Wölfler et al. 2010, Kurz et al. 2011; Emmel et al. 2012). However, dating of frictional heating was not successful so far (e.g. d’Alessio et al. 2003; Tagami 2012 and references therein). The main reason is possibly related to the short distances over which heat is generated along a fault zone. For a single earthquake, the most significant temperature increase is confined to a ~10-cm-wide zone of the slip surface, and temperature typically returns to a level similar to the pre-earthquake level after a few days (d’Alessio et al. 2003). Although the presence of pseudotachylites has been documented along the Ragga–Teuchl fault (Hoke 1990) it is not clear if frictional heating, fluid flow or possibly a combination of both was responsible to shorten track lengths and to rejuvenate AFT ages. Temperatures during pseudotachylite formation are expected to exceed ~1300 °C d (e.g. Toyoshima 1990; Otsuki et al. 2003). Accordingly we would expect an impact on the ZFT system too. However, the ZFT system of the fault related rocks is not affected by secondary heating. A possible explanation is that fault cores may act as a short-lived, syndeformational fluid flow conduit that rapidly seals to form a barrier to flow (Caine et al. 1996). In that case, fluid flow occurred during, or shortly after brittle deformation. Therefore the AFT ages of the fault cores provide indirect information on the timing of brittle faulting, thus at ~23 ± 0.8 Ma, along the Ragga–Teuchl fault and ~11.5 ± 1.0 Ma along the brittle fault in the Polinik Block (Fig. 2b). The inferred timing of brittle faulting and accompanied fluid infiltration at ~23 Ma fits with K/Ar data of fault gouges from the Ragga–Teuchl fault (~23 Ma, Kralik et al. 1987) and faulting at ~11 Ma may correspond to brittle faulting in the Penninic units immediately to the north of the study area (Wölfler et al. 2008, 2012). Additionally the data correspond to the main phase of lateral extrusion between ~23 and 12 Ma (e.g. Frisch et al. 1998, 2000, Wölfler et al. 2011).

In summary, we present two arguments in favour of brittle deformation along the sampled fault zones in early and late Miocene times. (1) The fault core samples display significantly reduced mean track lengths with a bimodal distribution and younger AFT ages as compared to those of the host rocks or damage zones. (2) The inferred timing of the assumed brittle faulting corresponds to already published data of brittle fault movement along the Ragga–Teuchl fault or in its immediate neighborhood (Kralik et al. 1987; Wölfler et al. 2008, 2012).

6 Conclusions

Structural and thermochronological investigations from the ductile Main Mylonite Zone and the brittle Ragga-Teuchl fault to the southeast of the Tauern Window document the evolution from Late Cretaceous to late Miocene times. Ductile deformation along the Main Mylonite Zone occurred under greenschist facies conditions in the Late Cretaceous. The structural analysis document top-to-the-NW directed deformation that goes along with the general extensional phase during the Late Cretaceous. Thermochronological analysis of fault related rocks suggest a thermal imprint in the early- and late Miocene that is possibly related to fluid circulation during or shortly after faulting.