Geologic evolution of the Tatra Mountains

Granitoids of the Tatra Mountains are polygenetic, with several batches of granitoid magma having intruded between ~370 and 340 Ma (Burda et al., Reference Burda, Gawęda and Klötzli2011, Reference Burda, Gawęda and Klötzli2013; Gawęda et al., Reference Gawęda, Doniecki, Burda and Kohút2005, Reference Gawęda, Szopa and Chew2014). U-Pb dating of apatite returned the most-recent dates at ~340 Ma, which means that the granitoids have not experienced temperatures above the closure temperature of the U-Pb system in apatite, i.e. above 350–550°C, since 340 Ma (Gawęda et al., Reference Gawęda, Szopa and Chew2014). The earliest dates recorded by ⁴⁰Ar-³⁹Ar dating of white micas from mylonitization zones within the crystalline core are Variscan (~333 Ma; Maluski et al., Reference Maluski, Rajlich and Matte1993). These dates, however, could reflect post-magmatic extension (Gawęda et al., Reference Gawęda, Szopa and Chew2014). The core was uplifted and eroded during the Permian and the Early Triassic (Jurewicz, Reference Jurewicz2005). Subsequent transgression resulted in sedimentation of various siliciclastic sediments and carbonates that prevailed during the Mesozoic. Tectonic activity during this Era comprised Middle to Late Triassic rifting and extension, and a major thrusting and nappe-forming Alpine event in the Late Cretaceous (Jurewicz, Reference Jurewicz2005; Králiková et al., Reference Králiková, Vojtko, Sliva, Minár, Fügenschuh, Kovác and Hók2014; Plašienka et al., Reference Plašienka, Grecula, Putiš, Kovác, Hovorka, Grecula, Hovorka and Putiš1997). Mylonites from the Tatra Mountains and adjacent areas returned ⁴⁰Ar-³⁹Ar ages of the latter tectonic phase in the 75–89 Ma range (Maluski et al., Reference Maluski, Rajlich and Matte1993). Evidence of an earlier, Early Cretaceous thermotectonic event in the 140–120 Ma range was also found (Maluski et al., Reference Maluski, Rajlich and Matte1993). As inferred from a fluid inclusion study, temperatures of Alpine deformation for selected shear zones within the Tatra granitoid core did not exceed 250°C (Jurewicz & Kozłowski, Reference Jurewicz and Kozłowski2003). The early Cenozoic evolution of the Tatra Mountains is difficult to determine because no sediments from that period lay directly on the crystalline core (Anczkiewicz et al., Reference Anczkiewicz, Danišik and Środoń2015), but zircon fission track (ZFT) ages of 77±11 to 63±6 Ma (Králiková et al., Reference Králiková, Vojtko, Sliva, Minár, Fügenschuh, Kovác and Hók2014) suggest a period of cooling and probable erosion. The final uplift took place in the Miocene (~20 Ma) and was preceded by late Eocene–Oligocene burial that started at about 45 Ma (Králiková et al., Reference Králiková, Vojtko, Sliva, Minár, Fügenschuh, Kovác and Hók2014). Anczkiewicz et al. (Reference Anczkiewicz, Danišik and Środoń2015) and Śmigielski et al. (Reference Śmigielski, Sinclair, Stuart, Persano and Krzywiec2016) demonstrated, by thermal history modeling based on ZFT and apatite fission track (AFT) ages, that temperatures during Paleogene burial were >150°C. AFT ages of crystalline-core samples are scattered from 15 to 30 Ma, which may indicate that the final uplift of the core involved block tectonics (Anczkiewicz et al., Reference Anczkiewicz, Danišik and Środoń2015). AFT dates record uplift from the 100°C isotherm, i.e. a depth of 5 km assuming a 20°C/km geothermal gradient.

Clay gouges

Clay gouges in the Tatra Mountains occur mainly along steeply dipping shear zones that were formed during pre-Alpine times (Jurewicz, Reference Jurewicz2006) and are accompanied by mylonites and cataclasites. Shear zones in the Tatra Mountains and surrounding areas have probably undergone multiple episodes of re-activation, as can be inferred from ⁴⁰Ar-³⁹Ar dating of fault-associated rocks that revealed Late Cretaceous and Paleogene ages (Kohút & Sherlock, Reference Kohút and Sherlock2003; Maluski et al., Reference Maluski, Rajlich and Matte1993) and from tectonic reconstruction models that imply final uplift of the High Tatras in the Neogene (Anczkiewicz, Reference Anczkiewicz, Danišik and Środoń2015; Jurewicz, Reference Jurewicz2005; Králiková, Reference Králiková, Vojtko, Sliva, Minár, Fügenschuh, Kovác and Hók2014).

Bulk composition of the gouges

The most abundant components of the gouge samples were quartz, with contents varying between 33 and 52%, and dioctahedral mica (Table 2). The sum of the amounts of the dioctahedral 2:1 layer silicates in bulk gouge varied widely between 56% for sample TM4d and 24% for sample ZG, with the average about 44% (Table 2). Chlorite was a minor constituent (≤4%) of all samples. Plagioclase was abundant in some samples, a little K-feldspar was present in a few samples, and one sample contained discrete dioctahedral smectite (14%). Small amounts of calcite in some samples and a very small amount of anatase in one sample were also observed.

Table 2 Results of qXRD analysis (mass %) of bulk samples with the goodness of fit parameter R_wp

Composition of the <0.2 μm fractions

All fine-clay fractions separated from studied samples contained discrete illite, expandable dioctahedral phyllosilicates (I-S and discrete dioctahedral smectite), and chlorite, as evidenced by XRD patterns of oriented mounts (Fig. 3 and associated Research Data). In addition, the presence of a band at 3696 cm^–1 in the FTIR spectra of samples TM4b, TM4d, TM5, and TM6 indicated the presence of small admixtures of kaolinite, which were below the XRD detection limit (Fig. 4). Modeling of the XRD patterns of a few of the fine-clay fractions with the Sybilla (Chevron proprietary) software indicated the presence of at least two illite and/or I-S populations (Table 3). The <0.2 μm fractions were dominated by 2:1 phyllosilicates, with prevailing mixed-layered I-S and discrete illite and minor amounts of chlorite. Kaolinite was not included in the modeling because it was present as a small admixture, detectable only by FTIR (Figs 3 and 4). In the case of the KP sample, the model that produced the best fit was relatively simple and contained only chlorite, illite, and highly illitic R1 I-S (8% smectite; Table 3). In the TM4 set of samples, two groups were distinguished. For samples TM4a and TM4b, models included highly illitic I-S and either highly smectitic (88%) I-S or discrete smectite. Models proposed for samples TM4c and TM4d contained two populations of ordered (R1), highly illitic I-S with different percentages of smectite. The remaining phases in both groups were discrete illite and chlorite (Table 3).

Fig. 3 XRD patterns of oriented mounts for <0.2 μm fractions of the KP (top) and TM4d (bottom) samples with theoretical models calculated with Sybilla (Chevron proprietary) software. EG denotes patterns of ethylene glycol-solvated clay

Fig. 4 FTIR spectra of fine-clay fractions of the investigated samples. The band at 3696 cm^–1, at the side of the main OH-stretching envelope of dioctahedral 2:1 phyllosilicates at ~3625 cm^–1, indicates the presence of kaolinite

Table 3 Parameters of Sybilla (Chevron proprietary) models for <0.2 μm Ca²⁺-exchanged and ethylene glycol-saturated fractions of selected samples

Quantitative analysis of size fractions of the KP sample

1M _d, 1M, and 2M ₁ polytypes (of dioctahedral mica and/or illite) were identified in <0.2, 0.2–2, 2–10, and 10–20 μm size fractions separated from the KP sample, based on the presence of diagnostic reflections in the 20–30°2θ range in the XRD patterns of random powder mounts (Fig. 5). Because these size fractions were selected for ⁴⁰Ar-³⁹Ar dating, a detailed quantification of the relative proportions of these polytypes was performed. While 1M and 2M ₁ structures are described adequately by default structure files available in the Profex-BGMN database, the 1M _d structure is simplified, which may cause imprecise quantification. Therefore, the 1M _d structure description provided by Ufer et al. (Reference Ufer, Kleeberg, Bergmann and Dohrmann2012) was used instead. This structure allowed simulation of peak broadening resulting from the presence of 60° and/or 120° rotations along the c* crystallographic direction and cis and trans vacancies in the octahedral sheet. Tests performed for 1M _d structures containing 120° rotations and both 120° and 60° rotations, both with and without preferred orientation (Table S1), revealed that the differences in relative proportions of different polytypes among quantifications based on different 1M _d structural models were smaller than the qXRD error assumed to be 5% (absolute). The exception was the quantification using the 1M _d structure with 120° rotations without preferred orientation for the <0.2 μm size fraction. This model was considered as oversimplified, because it was the one that returned results inconsistent with the three other quantifications for this size fraction (Table S1). Generally, the amount of the 1M _d polytype decreased systematically from the finest to the coarsest size fraction. The 2M ₁ polytype displayed the opposite trend, and the 1M content remained relatively constant among size fractions.

Fig. 5 XRD patterns of random powder mounts of different size fractions of the KP sample with theoretical patterns calculated with BGMN-Profex software

Given the similarity of the results obtained with the three models considered as reliable, quantification involving the 1M _d illite model with 120° rotations and preferred orientation was used in further considerations (Table 4). This model was chosen over the two models that include 60° rotations because, in XRD patterns of examined samples, separate reflections in the 37–39°2θ range were observed, which is characteristic for structures that do not contain 60° rotations (Fig. 5). If such rotations were present, only one broad reflection should be observed in the 37–39°2θ range instead.

Table 4 qXRD analysis results and K₂O contents (all as percent by mass) of size fractions of the KP sample. See text for estimates of the analytical errors

Problems associated with polytype quantification

Precise quantification of polytypes can be affected by several problems. Relative amounts of 1M and 1M _d polytypes can depend on definition of these structures. Theoretically, if a structure of 1M _d polytype with reflections similar to those of 1M is used, part of the XRD intensity in the regions of overlap is assigned to the 1M _d polytype, which leads to reduction in the amount of 1M polytype in quantification. For example, Grathoff and Moore (Reference Grathoff and Moore1996) assumed that the 1M _d polytype contains 60% trans- and 40% cis-vacant layers; the fraction of 0° rotations is 0.6; and the fraction of 60°, 180°, and 300° rotations is 0.6. This model results in reflections at 3.61 and 3.10 Å, similar to those of the 1M phase (Fig. 2 of Grathoff & Moore, Reference Grathoff and Moore1996). In the case of the 1M _d polytype of the KP sample in the present study, no 60°, 180°, and 300° rotations were assumed, and BGMN was allowed to optimize trans- vs. cis-vacant layer contents and fraction of 0° rotations for each size fraction separately. This led also to some overlap of reflections of 1M and 1M _d phases at ~24 and 27°2θ (Fig. 5). Refined structures for the 1M _d polytype (Table 5) were somewhat different from those assumed by Grathoff and Moore (Reference Grathoff and Moore1996). Generally, there were fewer 0° rotations, which means that XRD patterns of the 1M _d polytype had more diffuse reflections. The 1M _d structures were also more dominated by trans-vacant layers.

Table 5 Detailed structural parameters of dioctahedral mica and/or illite polytypes obtained by Profex-BGMN optimization. B1 – crystallite size parameter, p0 – fraction of 0° rotations, pcv – fraction of cis-vacant layers. Parameters p0 and pcv were refined only for the 1M _d polytype

The crystallinity of all phases is another important factor, because samples with larger crystallites produce more intense reflections than compositionally equivalent samples with smaller crystallites. In the case of polytype quantification, the larger the crystallites of a polytype, the smaller the amount of that polytype required to fit the experimental XRD pattern of a sample.

⁴⁰Ar-³⁹Ar dating

The smaller age values of finer size fractions (Fig. 6) pointed toward tentative acceptance that a basic assumption of ⁴⁰Ar-³⁹Ar radiometric dating of clay mixtures was fulfilled, i.e. that the younger, authigenic component has smaller crystallites and is relatively concentrated in finer size fractions (Kelley, Reference Kelley2002). None of the Ar-release patterns exhibited a plateau (Fig. 6). This behavior is typical of very fine material and does not invalidate the dates obtained (Haines & van der Pluijm, Reference Haines and van der Pluijm2008). Total-gas age values instead of retention age values were used because samples were Ca-exchanged before radiometric dating, which makes valid the assumption that no weakly bonded potassium is present in the non-retentive sites. Using total-gas age values is appropriate under this assumption (van der Pluijm & Hall, Reference van der Pluijm, Hall, Rink and Thompson2015). In addition, total-gas age values are equivalent to conventional K-Ar age values. The age values of authigenic and inherited material were calculated under the assumption that the 1M _d polytype is authigenic and that the 1M and 2M ₁ polytypes were inherited. That the 1M polytype was inherited from the wall rocks seemed likely, because formation of this polytype as an authigenic clay gouge component is not widely documented (Haines & van der Pluijm, Reference Haines and van der Pluijm2012).

Fig. 6 Ar-release patterns of dated size fractions

The results obtained for authigenic and inherited components using the IAA concept were −14±31 and 180±91 Ma for authigenic and inherited components, respectively. The average age values obtained by Monte Carlo calculations in the MODELAGE-based approach (hereinafter MODELAGE approach) were −4±40 and 165±62 Ma for authigenic and inherited components, respectively. The ratio of potassium content in authigenic and non-authigenic components (⁴⁰K_authigenic/⁴⁰K_{non-authigenic}) was 1.1±0.2. Results for particular Monte Carlo runs are presented in Table S2.

Calculation of K contents and age values in a three-component system

Potassium contents of size fractions separated from the KP sample varied from 6.89 to 8.52% (as K₂O) and were inversely correlated with the particle size (Table 4). The examined material contained three dioctahedral mica and/or illite polytypes (1M _d, 1M, and 2M ₁) which might differ from one another in age and K₂O content. Following the reasoning of Szczerba & Środoń (Reference Szczerba and Środoń2009), determination of the K₂O content of each polytype is an important prerequisite for age determination. Assuming that each polytype has the same K₂O content in each size fraction, the following set of linear equations is obtained:

(1a) $w_1{f}_{1a}+w_2{f}_{2a}+w_3{f}_{3a}=w_a$

(1b) $w_1{f}_{1b}+w_2{f}_{2b}+w_3{f}_{3b}=w_b$

(1c) $w_1{f}_{1c}+w_2{f}_{2c}+w_3{f}_{3c}=w_c$

(1d) $w_1{f}_{1d}+w_2{f}_{2d}+w_3{f}_{3d}=w_d$

where f stands for the mass fraction of a given polytype in a size fraction as determined with qXRD (Table 4), w stands for the mass fraction of K₂O in a polytype or in a size fraction, subscripts 1, 2, and 3 denote the 1M _d, 1M, and 2M ₁ polytypes, respectively, and subscripted letters indicate the size fraction: a – <0.2 μm; b – 0.2−2 μm; c – 2−10 μm; d – 10−20 μm; e.g. f _1a stands for the mass fraction of the 1M _d polytype in the <0.2 μm size fraction. The symbols w _a – w _d denote the mass fractions of K₂O in size fractions a to d, respectively (Table 4).

The matrix inversion technique was applied in order to facilitate handling of the set of linear equations with three unknowns (Collins, Reference Collins1990). This method is applicable to sets of equations with an equal number of equations and unknowns. Three subsets of Eq. 1 having three equations each were selected for matrix inversion. These were Eqs 1a, 1b, and 1c; 1a, 1b, and 1d; 1a, 1c, and 1d. The subset of Eqs 1b, 1c, and 1d was not used, because it had very small differences in polytype contents. The set of Eq. 1a, 1b, and 1c can be written in matrix form as:

(2) $\left(\begin{array}{ccc}{f}_{1a}& f_{2a}& f_{3a}\\ f_{1b}& f_{2b}& f_{3b}\\ f_{1c}& f_{2c}& f_{3c}\end{array}\right)\left(\begin{array}{c}{w}_1\\ w_2\\ w_3\end{array}\right)=\left(\begin{array}{c}{w}_a\\ w_b\\ w_c\end{array}\right)$

Analogous equations can be written for the remaining subsets. The first matrix on the left in Eq. 2 contains mass fractions of polytypes in size fractions <0.2, 0.2−2, and 2−10 μm. If the determinant of this matrix is other than 0, both sides of Eq. 2 can be multiplied by the inverse fraction matrix. This was the case for all subsets. The inverse matrix equation for the subset 1a-1b-1c is, therefore,

(3) $\left(\begin{array}{c}{w}_1\\ w_2\\ w_3\end{array}\right)={\left(\begin{array}{ccc}{f}_{1a}& f_{2a}& f_{3a}\\ f_{1b}& f_{2b}& f_{3b}\\ f_{1c}& f_{2c}& f_{3c}\end{array}\right)}^{-1}\left(\begin{array}{c}{w}_a\\ w_b\\ w_c\end{array}\right)$

An analogous transformation was made for the two remaining subsets.

Once a value for the K₂O content of each polytype is known, calculation of a K-Ar age value for each polytype is possible. The ⁴⁰K content of a size fraction is given by

(4) ${}_{}{}^{40}K=f_1{{}_{}{}^{40}K}_1+f_2{{}_{}{}^{40}K}_2+f_3{{}_{}{}^{40}K}_3,$

where ⁴⁰K denotes a specific amount (amount of substance per unit mass) of ⁴⁰K and f denotes mass fraction of a polytype as in Eq. 1. Similarly, for the radiogenic Ar content of a size fraction

(5) ${}_{}{}^{40}{\mathrm{Ar}}^{\ast }=f_1{}_{}{}^{40}{\mathrm{Ar}}_1^{\ast }+f_2{}_{}{}^{40}{\mathrm{Ar}}_2^{\ast }+f_3{}_{}{}^{40}{\mathrm{Ar}}_3^{\ast },$

where ⁴⁰Ar^* denotes a specific amount of radiogenic argon. The K-Ar method age equation yields

(6) $e^{\lambda t}-1=\frac{\lambda }{{\lambda }_{\mathrm{Ar}}}\left(\frac{{}_{}{}^{40}{\mathrm{Ar}}^{\ast }}{{}_{}{}^{40}K}\right).$

Substitution of Eq. 5 into Eq. 6 gives a relationship that may be expressed as

(7) $e^{\lambda t}-1=\frac{\lambda }{{\lambda }_{\mathrm{Ar}}}\left(\frac{f_1{{}^{40}K}_1}{{}^{40}K}\frac{{}^{40}A{r}_1^{\ast }}{{{}^{40}K}_1}+\frac{f_2{{}^{40}K}_2}{{}^{40}K}\frac{{}^{40}A{r}_2^{\ast }}{{{}^{40}K}_2}+\frac{f_3{{}^{40}K}_3}{{}^{40}K}\frac{{}^{40}A{r}_3^{\ast }}{{{}^{40}K}_3}\right)],$

which leads to

(8) $e^{\lambda t}-1=\frac{f_1{{}^{40}K}_1}{{}^{40}K}\left(e^{\lambda t_1}-1\right)+\frac{f_2{{}^{40}K}_2}{{}^{40}K}\left(e^{\lambda t_2}-1\right)+\frac{f_3{{}^{40}K}_3}{{}^{40}K}\left(e^{\lambda t_3}-1\right).$

Despite the fact that atomic proportions of ⁴⁰K in the polytypes and in the size fractions are used in Eq. 8, potassium contents can be used instead, because the relative abundance of ⁴⁰K in common terrestrial materials is virtually constant, i.e. one may assume that ⁴⁰K/K₂O in each polytype and in each size fraction is the same. Assuming that the age value of each polytype is constant among size fractions, following from Eq. 8 is that (for subsystem 1a-1b-1c; notation as in Eq. 1):

(9) $\left(\begin{array}{c}{e}^{{\lambda t}_1}-1\\ e^{{\lambda t}_2}-1\\ e^{{\lambda t}_3}-1\end{array}\right)={\left(\begin{array}{ccc}\frac{f_{1a}{w}_1}{w_a}& \frac{f_{2a}{w}_2}{w_a}& \frac{f_{3a}{w}_3}{w_a}\\ \frac{f_{2a}{w}_1}{w_b}& \frac{f_{2b}{w}_2}{w_b}& \frac{f_{3b}{w}_3}{w_b}\\ \frac{f_{3a}{w}_1}{w_c}& \frac{f_{2c}{w}_2}{w_c}& \frac{f_{3c}{w}_3}{w_c}\end{array}\right)}^{-1}\left(\begin{array}{c}{e}^{{\lambda t}_a}-1\\ e^{{\lambda t}_b}-1\\ e^{{\lambda t}_c}-1\end{array}\right)$

Analogous equations can be written for the two remaining subsets of Eq 1.

An attempt was made to calculate K₂O contents and age values of the three mica and/or illite polytypes identified in sample KP using the logic described above. The set of four equations with three unknowns (w ₁, w ₂, and w ₃; Eq 1) is inconsistent after substitution of mineralogical and chemical data for the KP sample, i.e. no set of w ₁, w ₂, and w ₃ values exists that simultaneously satisfies all equations. Furthermore, different K₂O contents and age values are obtained for corresponding polytypes when data are substituted into Eqs 3 and 9 written for different subsets of Eq. 1. This is interpreted as a result of analytical errors, mainly the error of qXRD, which is two orders of magnitude greater than the error of K determination. An attempt was made to remove the inconsistency by optimization of the analytical results, allowing measured values to vary within ranges defined by their 1σ measurement uncertainty. An Excel spreadsheet with Solver™ add-in was used to simultaneously minimize (1) the sum of squared differences in K₂O contents obtained for each polytype with different subsets of Eqs 1 and (2) the sum of squared differences in age values obtained for each polytype with different subsets of Eq. 1. The mass fraction of each polytype and the sum of mass fractions of K-free phases in size fractions were allowed to vary in the ±5% range. Optimized size fraction compositions had to sum to 100%. The K₂O content of each size fraction was allowed to vary within the ±0.05% range, corresponding to the 1σ measurement error of K₂O determination. Similarly, age values of size fractions were optimized in the range defined by the 1σ analytical uncertainty of the ⁴⁰Ar-³⁹Ar analysis. The optimization allowed to obtain a set of data (Table 6), which returned consistent values for the K₂O contents and age values of the polytypes: w ₁ = 8.77%, w ₂ = 11.28%, and w ₃ = 10.35%, t ₁ = −6 Ma, t ₂ = 205 Ma, and t ₃ = 101 Ma for 1M _d, 1M, and 2M ₁ illite, respectively.

Table 6 Optimized mineralogical composition (mass %), K₂O content, and age value for various size fractions of the KP sample

The above-mentioned K contents and age values for the polytypes are not associated with any estimate of uncertainty. In order to rectify this issue, a Monte Carlo approach was used. Calculations of K₂O contents and age values of polytypes were repeated 1000 times using randomly changed optimized input data (Table S3). For each repetition, values of polytype contents, K₂O content, and ⁴⁰Ar-³⁹Ar age for each size fraction were randomly drawn, each from a population having a normal distribution about the optimized value of that variable (Table 6) and a standard deviation equal to the 1σ measurement uncertainty, and substituted into Eqs 3 and 9. For each subset of Eq. 1, a small number of repetitions (between 2.7 and 3.3%) returned e^λt − 1 values that were smaller than −1 and consequently could not be converted to Ma. These repetitions were discarded when analyzing age values of the polytypes.

Interestingly, the results obtained showed that w ₁, w ₂, and w ₃, as well as age values of the1M _d, 1M, and 2M ₁ polytypes do not have normal distributions (Table S4 and Fig. S1). This is confirmed by the results of the Shapiro-Wilk test, which returned p-values of <0.05 for K₂O contents and age values of the polytypes generated by the Monte Carlo calculations (Table S4). Visual inspection of histograms of K₂O contents and age values of the polytypes points toward a Cauchy (Lorentz) distribution, i.e. symmetric distribution with very long tails on both sides of the maximum (Fig. S1). In such a situation, statistical measures other than the mean and the standard deviation are needed to provide an accurate description of data. For this reason, the median and the interquartile range (IQR) were used for the central value and the uncertainty range, respectively, of calculated age values in the three-component system. The results (median values) of the Monte Carlo approach differed from results of initial optimization; however, the former are considered as more reliable because results of the Monte Carlo approach can be associated with uncertainties based on their IQR ranges. The three-component age values used in further considerations are median values averaged across all subsets (Table 7). The associated uncertainties are based on correspondingly averaged IQR values and are presented as plus or minus one-half of the IQR.

Table 7 Age values (Ma) calculated with the different approaches used in the present study

No large differences were found in the median of calculated K₂O values among the polytypes. This result agreed with a ⁴⁰K_authigenic/⁴⁰K_{non-authigenic} ratio not differing significantly from 1, as calculated with the MODELAGE approach.

Comparison of age values calculated with various approaches

Both IAA and MODELAGE approaches returned negative age values of the authigenic component of the gouge. The time ranges of formation of the authigenic component, as defined by 1σ uncertainties, were −45 to 17 Ma and −44 to 36 Ma, for IAA and MODELAGE approaches, respectively. The earlier boundary of the range for the MODELAGE approach is close to the total gas age of the finest size fraction (38.44±0.17 Ma). In the three-component system, the age value for the 1M _d polytype was 15±37 Ma. All age values obtained for the youngest component of the gouge point towards post-Paleogene formation of this component, most probably during final Miocene uplift of the core, as indicated by the median values of 1M _d age calculated with the three-component approach (Table S4).

IAA and MODELAGE approaches returned age values for the inherited component of 180 and 165 Ma, respectively, with corresponding 1σ time ranges being 89−271 Ma, and 103−227 Ma. The three-component system returned age values of 135 Ma (IQR time range 78−192 Ma) and 121 Ma (IQR time range 65−177 Ma) for the 1M and 2M ₁ polytypes, respectively. Disregarding error, the age values for the inherited component coming from IAA and MODELAGE approaches correspond roughly to late Early Jurassic−Late Jurassic extension. Median age values for the 1M and 2M ₁ polytypes obtained with the three-component approach correspond to a thermotectonic event that was suggested to have affected the area around 140–120 Ma (Maluski et al., Reference Maluski, Rajlich and Matte1993). A definitive link of any component to a particular phase of tectonic activity in the area is, however, not possible because of large uncertainties around the calculated age values. An alternative explanation of such age values in the present work is that they are the result of partial resetting of the K-Ar system of micas formed during intrusion of Tatra granitoids 340–370 Ma by one or more of the subsequent tectonic events.

Interpretation of polytype age values obtained in the present study is highly speculative because of large uncertainties associated with those values. Several factors can possibly contribute to such large uncertainties. First, variability of polytype contents among separated size fractions is relatively small. In addition, the relative amount of the 1M polytype is small, which also amplifies the error in the three-component approach. In two-component approaches, a small variability of 2M ₁ + 1M polytype contents makes the regression upon which the age value calculation is based poorly constrained (Pevear, Reference Pevear1999; Szczerba & Środoń, Reference Szczerba and Środoń2009). In addition, for IAA and MODELAGE approaches, data points are scattered around the best fitting line (Fig. 7), which can be the result of errors in qXRD analysis. The scatter can indicate that the dated materials do not meet the assumptions behind IAA and MODELAGE approaches, e.g. potassium content or age value of a given polytype varies among size fractions.

Fig. 7 Plots of e^λt – 1 vs. the appropriate measure of the non-authigenic component for IAA and MODELAGE interpretative concepts. For MODELAGE, the extrapolation is for averages of 1000 runs using a Monte Carlo approach (light gray crosses). Gray diamonds and dashed extrapolation line – IAA approach.

Origin of the components identified in clay gouges

Compared to the surrounding rocks, the gouges are enriched in quartz and muscovite and depleted in plagioclase and K-feldspar. Unlike the High Tatra granitoids, the gouges are almost completely devoid of biotite. Other phases, which do not occur in fresh granitoids, are chlorite, calcite, 1M _d illite, I-S, smectite, and kaolinite. The observed differences between compositions of wallrocks and gouge follow patterns described for other shear zones developed in igneous and metamorphic rocks of similar mineralogical composition (Abad et al., Reference Abad, Jiménez-Millán, Schleicher and van der Pluijm2017; Boles et al., Reference Boles, Mulch and van der Pluijm2018; Haines & van der Pluijm, Reference Haines and van der Pluijm2012; Hayman, Reference Hayman2006; Surace et al., Reference Surace, Clauer, Thélin and Pfeifer2011).

In the investigated gouges, quartz and feldspars were inherited from the surrounding granitoids and mylonites. These minerals can be macroscopically identified in the wallrocks and as crushed grains in hand specimens of investigated samples. Larger proportions of quartz (relative to the granitoids) can be interpreted as a result of a decrease in rock volume within the shear zone (Goddard & Evans, Reference Goddard and Evans1995; Schleicher et al., Reference Schleicher, Warr and van der Pluijm2009). Smectite and kaolinite are considered as authigenic components of the examined gouges. These phases do not occur in the host rocks of the gouges. A weathering origin of the smectite is considered unlikely, because it coexists with chlorite, which is broken down before precipitation of smectite during weathering (Skiba, Reference Skiba2007). Because the investigated materials have no signs of weathering, the small quantities of kaolinite found are also most likely authigenic. Chlorite present in studied gouges is is probably inherited from the parent rocks. Chlorite in general is commonly found in the Tatra granitoids as a product of biotite alteration (e.g. Gawęda & Włodyka, Reference Gawęda and Włodyka2012; Gawęda et al., Reference Gawęda, Doniecki, Burda and Kohút2005; Turnau-Morawska, Reference Turnau-Morawska1948). Chloritization, which is always complete in the granitoids located next to a fault, is believed to have taken place during Alpine dynamometamorphism (Jurewicz & Bagiński, Reference Jurewicz and Bagihski2005; Leichmann et al., Reference Leichmann, Jacher-Sliwczynska and Broska2009), before the gouges formed.

The majority of the discrete 1M _d illite polytype, as well as the I-S, is authigenic and the majority of the 1M and 2M ₁ polytypes was inherited. During age calculations I-S was included in the 1M _d component and all interpretations derived for 1M _d illite apply also to I-S in this respect. A possible source of non-authigenic 1M _d polytype is wall rock containing feldspars, which often had been hydrothermally altered to sericite or illite of uncertain polytype (Uchman & Michalik, Reference Uchman and Michalik1997). According to the best knowledge of the authors, no detailed information on sericite from the Tatra Mountains is available in the literature.

The parent rock is the most likely source of the 2M ₁ polytype, which has been considered herein as an inherited component of the gouge. Taking into account the geologic history of the area (Kohút & Sherlock, Reference Kohút and Sherlock2003; Maluski et al., Reference Maluski, Rajlich and Matte1993), the 2M ₁ polytype must have formed originally during crystallization of granitoids ~340−370 Ma, with possible recrystallization during the main Alpine event between 70 and 140 Ma.

A relatively large variability in the clay mineralogy of the gouges is exemplified by the TM4 site, where samples were taken 10–15 cm apart. This may be due to polycyclic formation of the gouges, reflecting both temporal and spatial variability of the conditions inside the gouge at the centimeter scale.