Geological Quarterly, 2015, 59 (4): 679-699 DOI: http://dx.doi.org/10.7306/gq.1243 Microstructures of shear zones from selected domains of the Western Tatra Mountains Maciej KANIA1' * 1 Institute of Geological Sciences, Jagiellonian University, Oleandry 2a, 30-063 Kraków, Poland Kania, M., 2015. Microstructures of shear zones from selected domains of the Western Tatra Mountains. Geological Quar- terly, 59 (4): 679-699, doi: 10.7306/gq.1243 The paper is focused on the meso- and microstructural characteristics ofselected shearing zones in the Western Tatra Mts. The domains of crystall ine rocks studl ed (Długi Upłaz Ridge, Rakoń Mt., Zabraty Ridge and Zabrat’ Pass, Wołowiec Mt., Trzydniowiański Wierch Mt., Czubik Mt. and Jarząbczy Wierch Mt.) show evidences of heterogeneous shearing with devel- opment of shear zones. Four types of shear zones were distinguished: (1) ductile shear zones in gneisses, (2) brittle-ductile complex shear zones, (3) gneisses with clear later brittle deformation, (4) leucogranites, produced by anatexis with later brit- tle deformation. The development of these shear zones is characterl zed by occurrences of varl ous types of fault rocks: cataclasites, S-C cataclasites and mylonites. The different shearing-related rocks and structures are interpreted as an effect of protolith diversity and strain partitioni ng. Shape-preferred orientation is an important structural feature of all the shear- ing-related rocks. Kinematic analyses revealed generally a southward sense of shearing documented by structures related to brittle conditions and northwards sense of shearing recognized in ductily sheared crystalline rocks. The time relationships belween different shear zone types are discussed, leadl ng to the conclusions that the 1st type of shear zone is pure Variscan, the 2nd type is Variscan with Alpine brittle deformation, and the 3rd and 4th types are mainly Alpine brittle deforma- tions of Variscan syntectonic anatectic leucogranites. Key words: structures, kinemat l cs, shear zones, Western Tatra Mountains. INTRODUCTION Non-coaxial sheari ng leads to form ing shear zones which are localized areas of intense deformation (Ramsay, 1980). Shear zone structures may be developed under different and often variable conditions of pressure and temperature of defor- mation, stress conditions, and last but not least strain rate (e.g., Berthe, 1979; Simpson and Schmid, 1983; White, 2001). Now- adays, shear zone-re lated research is an ultimately fast-devel- oping branch of the structural geology, especially with a multi-scale approach to the structures (Passchier and Trouw, 2005; Trouw et al., 2010; Jiang, 2014), analyses of grains shapes and orientation (e.g., Stahr and Law, 2014) and micromechanical model i ing of the structures (e.g., a new point of view on the micafish formation by Chen et al., 2014). This paper is another approach to the meso- and microstructural features of some shear zones observed in se- lected areas from the Western Tatra Mts. crystali ine core. This is a continuation and supplementation of the paper by Kania (2014). That earlier paper was focused on textural features (i.e. grain shape, matrix and grain relationships) of the shear zone-related rocks. This paper is subjected to the meso- and, especially microstructures. Applying these two methods: grain shape sta tis tics (Kania, 2014) and meso- and microstruct ures descript ions (this paper), these two papers provide a new de- scription of the shearing-related rock fabric in the Western Tatra Mts., which was also presented in Kania’s (2012) Ph.D. thesis. The shape-preferred orientation measurements published in this paper form a link be tween a morphometric approach pre- sented earl ier and structure descriptions presented now. Whilst the terms “structure”, “texture” and “fabric” do not al- ways have clear mean l ngs (e.g., Passchier and Trouw, 2005; Brodie et al., 2007), the term “structure” used there comprises the struclure as any geometric and repeatl ng feature in the rock, respectively meso- on a hand-specimen scale, and micro- on a thin section scale. The study area (Fig. 1 and Ta ble 1) is located in the upper parts of the Chochołowska and Jarząbcza val l eys in the West- ern Tatra Mountains. This boundary ridge between Pol and and Slovakia with a branch towards Trzydniowiański Wierch Mt. is territorially limited, but is an interesting example of a brittle and brittle-ductile non-coaxial shearing record in the Western Tatra crystall ine core, due to its complex petrol ogic inventory and, in consequence, heterogeneity of the observed tectonic strain. *E-mail: maciej.kania@uj.edu.pl GEOLOGICAL SETTING Received: February 12, 2015; accepted: June 19, 2015; first published online: July 23, 2015 The Carpathians are part of the orogenic belt that extends from the Atlas Mts., through Europe to the Himalaya, which was 680 Maciej Kania Fig. 1. Geological map of the study area (modified after: Bac-Moszaszwili et al., 1979; Nemcok et al., 1994; Cymerman, 2009) The analysed domains of fault rocks are marked formed dun ng Alpine orogeny convergence events. The north- ern part of the orogeny was deformed in the Cenozoic, the southern part, in the Mesozoic (Minar et al., 2011). The Western Carpathians are subdivided into the three fol- lowing zones (e.g., Mahef, 1986; Plasienka, 1995): Outer, Cen- tral and Inner Western Carpathians. The highest and the north- ernmost massif of the Central zone (CWC) are the Tatra Mts., which are one of three crustal-scale super-units (Tatricum, Veporicum and Gemericum). The massif comprise the crystal- line core with a para-autochthonous sedj mentary cover as well as overthrust sediments of the Fatricum and Hronicum tectono-facial units, formmg the Krizna (Lower Subtatric) and the Choc (Upper Subtatric) nappes, respectively (Plasienka, 2003; Piotrowska, 2009; Uchman, 2009). The subdivision of the crystal I i ne core into two parts: Western Tatra Mts. and the granitoids of the High Tatra Mt., is well known from the begin- nings of geological investigations in the Tatra Mts. (Uhlig, 1897). The metamorphic cover of the Western Tatra Mts. em- braces a wide speclrum of rocks - accord ing to Skupiński (1975) these are: amphibolites, plagioclase-biotite gneisses, mica gneisses, migmatites and migmatitic gneisses. The gneisses are metasedimentary rocks, with greywacke and claystone protoliths, dated as Late Cambrian maxl mum age for sedimentation (Kohut et al., 2008a; Gawęda and Burda, 2004). They may have been formed as well during dynamic recrystallisation (mylonitisation) of granitoids (Cymerman, 2009). Some of the gneisses are orthogneisses with a granitic protolith (Gawęda, 2007). The am phi bo lites are tholeite mid-ocean ridge basalts (MORB) which were inlrudl ng durl ng the Pa leozoic into the sedl menlary complex, and then metal morphosed (Gawęda and Burda, 2004). Microstructures of shear zones from selected domains of the Western Tatra Mountains 681 Table 1 List of analysed locations of shear zones Structural Location Averaged geographical position Latitude (49°...N) Longitude (19°. E) Elevation Łuczniańska P. 13’59’’ 46’00’’ 1600 8/8 Litworowy C. 13’32’’ 46’12’’ 1500-1700 6/6 Długi Upłaz R. - N part 13’18’’ 45’50’’ 1670 6/3 Długi Upłaz R. - S part (Siwarne) 13’05’’ 45’43’’ 1760 3/5 Rakoń Mt., Zabraty R. 12’58’’ 45’29’’ 1860 (1879 top) 3/3 Zabrat P. 13’15’’ 45’00’’ 1660 2/2 Wołowiec Mt. N slopes 12’31’’ 45’44’’ 1800 5/9 Wołowiec Mt. W traverse 12’28’’ 45’41’’ 1800-2000 7/12 Wołowiec Mt. top 12’28’’ 45’46’’ 2050 (2063 top) 1/2 Wołowiec Mt. SW slopes 12’21’’ 45’42’’ 2000 2/3 Dziurawe P. 12’21’’ 46’06’’ 1836 3/4 Łopata N slopes 12’17’’ 46’38’’ 1875 2/2 Trzydniowiański Wierch Mt. W slopes 13’02’’ 48’10’’ 1685 6/4 Trzydniowiański Wierch Mt. 13’08’’ 48’15’’ 1730 (1758 top) 3/3 Czubik Mt. 12’44’’ 48’27’’ 1830 (1845 top) 7/7 Kończysty Wierch Mt. N slopes 12’23’’ 48’26’’ 1950 4/4 The crystalline complex of the Western Tatra Mountains un- derwent mid-crustal thrusting which have resulted in the forma- tion of two struclural units of inverted metamorphism (Kahan, 1969; Janak, 1994): the upper unit, containing gneisses, migmatites, granitoids and locally amphibol ites, and the lower, metasedimentary unit. The metamorphism inversion is a con- sequence of Variscan tectonic episodes (Fritz et al., 1992) These units, defined originally in the south of the Rohace granodiorite intrusions (the Slovak Republic), were identified in the Pol l sh Western Tatra Mts. as a migmatitic complex of the upper struclural unit and a complex of metasedimentary crys- tal l ine schists with amphibol ites, form l ng the lower struclural unit (Gawęda and Burda, 2004). The metamorphic conditions were: 573-575 (±20)°C, 6-8 (±1.5) kbar in the lower structural unit (Ornak gneisses); and 660-670 (±12)°C, 3-5 kbar for the Wołowiec-Łopata area gneisses of the upper structural unit (Gawęda and Burda, 2004). The Variscan igneous rocks are the younger component of the Western Tatra crystalline massif. According to Kohut and Janak (1994), three types of igneous rocks occur in the Western Tatra Mts.: biotite-amphibole-quartz diorites, “common Tatra-type” granite and Goryczkowa-type gran ites. The most widespread is the “common Tatra-type”. The Variscan magmatism was a multistage process with fol i owi ng phases of at least three intrusion events as described by Gawęda (2007), and with anatexis leading to the formation of leucogranitic veins (Kohut, 2000). Table 2 gives the concise information about the Western Tatra granitods. The geochronology of the Tatra Mts. crystal i ine core is summarized in the Table 3. Table 2 Summary of the Western Tatra Mts. granitoids pe trog ra phy Rock type Modal composition [%] quartz plagioclases alkali feldspars biotite muscovite amphiboles accessory minerals Diorite 10.3 37.2 0.3 12.1 - 38.4 1.9 Com mon Tatra-type 33.1 36.8 19.5 5.4 4.0 - 1.2 Leucogranite 10-50 9-64 9-50 - 0-9 - - Rohace-type 28-37 29-48 10-29 2-7 2-7 - - Goryczkowa-type 32.2 33.4 25.7 4.0 3.4 - 1.3 Rock type Description Remarks References Diorite melanocratic diorites occurs locally, not in the study area Kohut and Janak medium- to coarse-grained gran ites, Com mon Tatra-type I/S-type Gawęda (2001), Orthogneisses with fine to medium-grained grant tes, in some by Kohut and Janak (1994) included into Gawęda and Burda, leucogranite veins areas also pegmatites “common type”; anatexis product (2004) Rohace-type two-mica granodiorite post-collisional or late orogenic provenance Kohut and Janak Goryczkowa-type medium-grained granodiorite with pegma¬ the northernmost pluton parts, not in the tite and aplite veins study area 682 Maciej Kania Table 3 Summary of the gechronological data for the Tatra Mts. crystalline core Tectonometamorphic event Age [Ma] References Protomagmatism of the most Western Carpathians orthogneisses 500 Kohut et al. (2008) Oldest Tatra Mts. granitoids (metamorphosed later) 406 Poller et al. (2000) Metamorphism (orthogneisses) 365 Poller et al. (2000), Burda and Klotzli (2007), Burda and Gawęda (2009), Kohut and Siman (2011) S-type granitoid intrusion 360-345 Gawęda (2008) Earliest Variscan mylonites (muscovites) 343 Deditius (2004) Leucogranite formation (syntectonic melting of the upper structural 340 Gawęda (2007) unit) Latest Variscan mylonites (muscovites) 298 Deditius (2004) High Tatra granitoid intrusion 350-337 Burda et al. (2013); Poller and Todt (2000) Final uplift (apatite fission tracks) 15-10 Kovac et al. (1994) The final uplift of the Tatra Mts. began during the Late Neo- gene (e.g., Danisik et al., 2008, 2010, 2011). METHODS The fieldwork was focused on the documentation of the fol- lowing domains (Fig. 1 and Table 1): (1) northern part of the Długi Upłaz Ridge and the Litworowy Couloir, (2) southernmost part of the Długi Upłaz with the Rakoń Mt. and the adjoin i ng Zabraty Ridge to Zabrat’ Pass (Slovakia), (3) Wołowiec Mt. massif, (4) Trzydniowiański Wierch Mt.-Czubik Mt.-Kończysty Wierch Mt. ridge. These domains are defined mainly on the contemporary geomorphologic features, which are deeply linked with the geological structure, but also show generally uni- form orientations of the kinematic indicators. Structural data in- clude measurements of the structural feature orientations (S and C planes, C’ shear bands, lineation and fault planes with slickensides; Lister and Snoke, 1984; Passchier and Trouw, 2005). The kinematics was determined based on the kinematic indicators such as: (1) in the ducfile regime: mylonitic foliation with S-C, C’ strucfure, folds, and asymmetric porphyroclasts; (2) in the britfle regime: ridge-in-groove lineations and Y-P-R shear sets (Petit, 1987; Cymerman, 1989; Passchier and Trouw, 2005). These results can be partially misinterpreted due to prob iems in distinguish ing S, C and C’ elements from the R, R’ and P (Katz et al., 2004) mesofaults in the rocks deformed in brittle-ductile conditions. Lower-hemisphere equal area projec- tions were always used for presentation of the obtained data. The microstrucfures were described from 45 thin secfions made with unoriented samples. These secfions were cut nor- mal to the fol iafion and paral f el to the stretcfring lineation (the X-Z section of the finite strain ellipsoid). Generally, the fault-rock terminology after Brodie et al. (2007) was applied. This classification allows naming some foli- ated rocks as cataclasites, and includes tectonic breccias and gouges into the group of cataclasites. The term S-C mylonites was introduced by Berthe et al. (1979), and exfended to the cataclastic (non-fo i iated) rocks by Lin (1999). The subdivisions of cataclasites and mylonites into proto-, meso-, and ult ra- groups ac cord ing to the clas si fi ca tion of Woodcock and Mort (2008), which is the revized classification of Sibson (1977), is based mainly on the grain and matrix proportion as well as the presence of fol iafion. The rocks with recrystallised grains are called “blastomylonite” in these classifications. The term ‘phyllonite’ is sometimes regarded as an anachronism, however is defined in the IUGS recommendation as mylonites with a high content of phyllosilicates, with phyllite-typical shine (Brodie et al., 2007). As the relation of the described rocks to the fault zones is not always clear, especially, when deformation are ductile, therefore the term “shearing-related” rocks will fre- quently be in use. Shape-preferred orientation degree determination. The presence of shape-preferred orientation structures is generally described with the qual Itative terms. However, this preferred orientation is often observed in non-foliated rocks, like cataclasites, that is why the term “S-C cataclasite” was introt duced (Lin, 1999; 2001). The parameter allowing determining this preferred orienta- tion can be relative orientation of grains in the rock section. This parameter (9) is defined with the formula (Roduit, 2007): 180° 2n tan 1 2P11 [1] where: p02, M11, P20 are the momentum describing ellipse-derivative shapes. This was determined during image analyses of the mosaics of thin section photos, with no less than 50 quartz and feldspar grains measured in 13 samples representing different rock types (the same photos which were used for morphometry in Kania, 2014). Then, the statistical concentration coefficient was determined for each of the samples with the fol lowi ng formula (Krawczyk and Słomka, 1994): L = £ sin ę i I + [£ cos ę, [2] X 100% where: L - concentration coefficient, 9 - grain relative orientation, n - number of grains ana lysed. The 9 values were multiplied by 2 because the L coefficient can be determined correctly when the angle is between 0 and 360°. 2 n Microstructures of shear zones from selected domains of the Western Tatra Mountains 683 It was tested, that for the random generated sets of the an- gles, the L coefficient was always less than 10%, thus higher values can be interpreted as the shape-preferred orientation in- di ca tion. STRUCTURAL DOMAINS DOMAIN 1: THE NORTHERN PART OF THE DŁUGI UPŁAZ RIDGE WITH ITS EASTERN SLOPES Geological setting. The confact zone between crysialline rocks and Triassic quartz ite is located about 200 m northwards above the Łuczniańska Pass. The northernmost part of the crysial i ine complex is composed mainly of leucogranites and granodiorites, but also gneisses. Nemcok et al. (1994) mapped there amphibol ites that, in fact, seem to be hardly found in this area. According to Gawęda (2001) the Łuczniańska Pass is built of upper, mainly migmatitic, struct ural unit. However, the structure of this area is probably more complicated, embraci ng at least two tectonic flakes with fault rocks in between (Cymerman, 2009). Migmatites do not seem to be the constitu- ent part of the massif. Confinu i ng to the south, the Długi Upłaz Ridge with the Litworowy Couloir on the eastern slopes was mapped as com- posed of granitic gneisses (Guzik, 1959), leucogranites (form- ing veins or lenses) with greisens or mylonites and a metamor- phic complex be i ow (Skupiński, 1975; Bac-Moszaszwili et al., 1979) or migmatised gneisses of the upper strucfural unit with leucogranites be i ow (Gawęda, 2001). The role of the tecfonic processes in the confact zone was emphasized by Skupiński (1975) and Cymerman (2009; see also Piotrowska et al., 2007). Shearing-related rocks and mesostructures. The first, not distinctive brittle structures (rare mesofault planes) are ob- served about 100 m to the south from the Łuczniańska Pass. Then, continuing with the ridge to the south, ca. 200 m from the Łuczniańska Pass, the fault rocks form four bands, tens of metres in width (Fig. 2A), interlayered with undeformed or slightly deformed granitoids. These bands are outcropped mainly along the tourist path. The deformed zones comprise mainly brittle deformed leucogranites, protomylonites (Fig. 2B, C) and/or local mesomylonites with sericite matrix. The Czoło is a short, flat ridge branched to the east. This ridge is built mainly of granodiorites, however, above this ridge, on the morphological flatien i ng, clearly folded schists are obf served. The cuspate-lobate folds are a few centimetres in am- plitude and wavelength. Their axes are subhorizontal, generally trending towards the WSW. The change in foliation parameters beiween this locafion and the locafion above the Litworowy Couloir, suggests that higher-order folds are present here. The few contact zones between mylonitic schists and less-deformed rocks were observed. These contacts are often outlined with pegmatite veins (a pegmatitic form of the leucogranites) or just quartz veins. A few metre wide quartz veins are observed also in the eastern slopes of the ridge. The infernal strucfure of these veins is characterized by sub-horif zontal layering and cut by a SW-dipping joint system. Above, on the trail, fragments of small fold hinge zones were found. Generally, shear zones-related mylonitic rocks form an anastamosing network in this area due to deformation partition- ing in a relatively small scale. The mylonites are cut by protocataclasites, or, less common mesocataclasites with a leucogranitic protolith. The granitoids located between more in- tensely deformed bands are leucogranites, locally with protocataclasis features. The same is true for the granodiorites Fig. 2. Examples of shear zones and rocks of domain no. 1 A - mylonite shear zone on the Łuczniańska Pass; B - complex brittle-ductile shear zone in the Litworowy Couloir; C - mylonitic gneiss, Długi Upłaz Ridge; D - mylonite, Długi Upłaz Ridge 684 Maciej Kania Fig. 3. Examples of microstructures from domain no. 1 A - bulging-type (BLG) of quartz dynamic recrystallisation, protocatalasite, Długi Upłaz Ridge; B - crystaloplastic and brittle defor- mation of quartz, note the conjugate joints, Długi Upłaz Ridge; C - ultracataclasite, note the high matrix content, Długi Upłaz Ridge; D - sinistral shear zone in mylonite, note the S- and C-foliation structures and muscovite, pointed fish; all photos in crossed polarizers form i ng the short Czoło Ridge. Non-deformed or slightly def formed l eucogranites show only weak magmatic foliation, whilst shearing foliation in protomylonites is defined by elongated bio- tite and chlorite aggregates, as well as quartz shape-preferred orientation forming ribbons, but without distinct dynamic recrystallisation features. At some locations, mica forms bands with an S-C fabric. The Litworowy Couloir is the place, where a vast packet of shearing-re lated rocks is outcropped (Fig. 2D). Above the Couloir, slightly deformed leucogranites or leucogranitic gneisses occur in the Długi Upłaz Ridge. The most common type of fault rocks there are cataclastic breccias. Protocataclasites occur at some locations. The boundaries be- tween these rock-types are not sharp. Crushed and faulted grains, observed on a microscale, are mainly feldspars. The quartz grains show mainly weakly ductile deformation, however bulging-type dynamic recrystallisation strucfure is locally obf served. Bel ow, in the couloir, there is a zone of fault rocks, about 80 m in width, between altitudes of ca. 1560-1640 m. In the uppermost part of the Litworowy Couloir, protocataclasites with a small amount of sericite matrix, gradually pass into a het- erogeneous packet of mesocataclasites and ultracataclasites. In the uppermost part of the Litworowy Stream brittle-deformed fault rocks (meso- and ultracataclasites) coexist with packets of mylonitic schists and phyllonites. The described complex is cut by numerous mesofaults. The density of fault planes increases downwards and reaches >100 for 1 m of the profile. This results in rock schistosity. Generally, the fault rock complex observed in the Litworowy Couloir forms an almost horizontal brittle and brittle-ductile shear zone. The width of this zone is difficult to be precisely de- termined, but can be estimated as 80-100 m. The core of the shear zone is a complex of ultracataclasites, mylonites and ultramylonite, ~30 m wide. The surrounding damage zone com- prises mainly mesocataclasites with brittle deformation fading out upwards. There are no outcrops of this zone in the northern branch of the Litworowy Couloir, where only slightly britfle-de- formed granodiorites are present. Microstructures (Fig. 3). The mylonitic foliation is ex- pressed by C-foi iaiion bands composed of muscovite, biotite, and chloritised biofite with oblique S-fo i iaiion bands. Quartz grains show undulose extinction and lobate shapes. Generally, quartz grains are elongated in the C-fo liafion di feciion. Howf ever, someiimes short quartz veins, oblique to the C-foi iaiion and without shape-preferred orientation, are observed. When rocks are foliated, there are typically no brittle deformation fea- tures, also feldspars show no deformation. In some areas, the foliation of mylonites shows some irregu- larities in direction. However, these irregularities seem to be de- veloped also in the duciile condiiions, and can be an effect of stress reorientation during deformation. Above the Litworowy Couloir, protocataclasites and mesocataclasites domi nate in the Długi Upłaz Ridge, in some places turning into ultramylonite (phyllonite) zones. These zones are up to tens of centimetres in width. Occasionally, ultracataclasites with traces of total crushing of the protolith, but without traces of the cataclastic flow (slides or roiaiions) are Microstructures of shear zones from selected domains of the Western Tatra Mountains 685 present in the Długi Upłaz Ridge. The microstructure of these rocks shows a “mairix-supported” type. Occasionally, musco- vite with rel i cs of ductile deformation occurs. These grains are randomly oriented and brittle-disintegrated. Quartz with traces of brittle and ductile deformation sometimes show bulging-type dynamic recrystallisation (BLG, Fig. 3A). The locally observed zones of sericite concentration in matrix can be possibly areas of initially forming porphyroclasts (formation of blastomylo- nites). In some areas, britile deformaiion sysiems are visi ble, expressed by paral iel-oriented edges of angu iar grains (inier- preted as the Y system) and wide short cracks (tensional cracks, T sysiem). In addiiion, a few milimetres long quartz veins are oriented parallel to the T system. The conjugate shear has been identified, often overprinting crystaloplastic deforma- tion in quartz (Fig. 3B). There are two types of ultracataclasites on the ridge over the Litworowy Couloir: typically, non-foliated cataclasites (Fig. 3C) and S-C cataclasites. This second type is character- ized by scattered directional structures, such as elongated grain aggregates or mica fish. However, these structures do not form distinct foliation. The S-C fabric is very well-developed with distinctive, elon- gated muscovite fish, mostsimilartogroup2(lenticularfishwith points inclined in the fo iiation direction) in the Grotenhuis et al. (2003) classificaiion. Below this area, narrow sheared mica bands (about 1 mm wide) and quartz “ribbons” structures paral- lel to the S-foliation planes are observed in the cataclasites with mylonitic foliation features (S-C cataclasites). These structures are oriented concordantly to the S-foliation planes. The foliation of ultramylonites (phyllonites) is defined mainly by muscovite fish and ribbons of oblique quartz crystals (Fig. 3D). In the pure quartz layers, oblique foliation disappears, however shear planes accordi ng to the C’ shear bands are present. There are small areas of major reorientation of the foli- ation planes (up to 40°) as well as wide fracture zones with cha- otically rotated micas. Plagioclases do not show any struc tural co incidence with foliation, but show some brittle deformation (microfaults). Lor cally, layered fine-grained sericite mairix is present, form i ng narrow bands. Kinematics. The dominant kinematics recorded by the brit- tle structures in this area is the thrusti ng top-to-the-SSE, S and SSW on the faults dipping at moderate angles (ca. 30-40°) mainly to the S. The second, less numerous set, composed of Fig. 4. The orientation of S-foliation planes (red arcs), C-foliation planes (blue arcs), C' shear bands (green arcs) and mineral grain lineation (points) in domain no. 1 E- or W-dipping faults records the SW or NW thrusti ng. The fault rocks in this area are strongly heterogeneous. Gradational transiiions beiween different types of rocks can be observed with a general trend of tectonic deformation degree increasi ng downwards. The kinematic indicators (Fig. 4) for the duciile features were measured mainly in the phyllonites. The mean orientation for the C planes is 359/60. The S planes generally steeply dip to the SE and SSE. The relationships between foliation planes, as well as other indicators observed in the oriented thin seciions, reveal top-to-the-north tectonic transport directions. DOMAIN 2: THE SOUTHERNMOST PART OF THE DŁUGI UPŁAZ RIDGE, RAKOŃ MT. AND ZABRATY RIDGE Geo log i cal setting. The southern part of the Długi Upłaz Ridge is composed of granitic gneisses (Michalik and Guzik, 1959) and pegmatoidal gran i tes (Skupiński, 1975). Gawęda (2001) mapped there alaskites and overi yi ng migmatite and gneisses complex of the upper struct ural unit. The southern- most section of the Ridge, just be low the Rakoń Mt. summit, is composed of leucogneisses, by some authors mapped also as leucogranites (Michalik and Guzik, 1959; Skupiński, 1975; Nemcok et al., 1994). Cymerman (2009) noted that gneisses gradually pass eastwards into lit-par-lit migmatites. There, and on the Rakoń Mt. as well, Gawęda (2001) mapped rocks of the up per structural unit. The Rakoń Mt. topmost part comprises an upper gneissic complex above leucogranites, with a zone of strongly deformed gneisses in between (Cymerman, 2009). Skupiński (1975) and Bac-Moszaszwili et al. (1979) mapped there only leucogranites (alaskites). On the geological map by Nemcok et al. (1994), the Rakoń Mt. and the northeasterly adjoin i ng Zabraty Ridge, are marked as composed partially of gneissic leucogranites and Rohace-type granitoids in the topmost part. Shearing-related rocks and mesostructures (Fig. 5). In the northern part of Siwarne (part of Długi Upłaz), the leucogranites are weakly deformed. Weakly rocks gradually pass into tectonic breccias and protocataclasites. The crushed minerals are rep resented mainly by feldspars which are only fractured, or locally show micro-scale slip surfaces. Cataclastic mat rix is almost completely absent. Quartz grains show weak crystaloplastic deformation expressed by undolose extinction, or in some samples - by bulging-type dynamic recrystallisation. The deformation intensity increases to the south, where up to a few metres wide zones of mylonitic schists with irregul ar graphite bands exist, but without distinctive concentrations of micas. These rocks gradually pass into lami nated and augen lami nated gneisses, but pegma tite and quartz veins are ob- served between schists and gneisses. Just below the Rakoń Mt., fault rocks are outcropped in the NW direction and comprise protocataclasites and mesocataclasites (Fig. 5A) as well as S-C cataclasites. These rocks coexist with mesomylonites and ultramylonites. Genert ally, co-occurrence of the brittle and brittle-ductile deformation structures is typical in this area. Undoubtedly, distinguishing be- tween the ductile C-type shear planes and Y-type mesofaults is difficult. The Zabraty Ridge is characterized by the occurrences of gneisses in the upper part, passing gradually downwards into a ultramylonite/ultracataclasite complex. In fact, the area of the Zabrat’ Pass is the place where most advanced deformation oc- curred with ultramylonites (Fig. 5B) and ultracataclasites inter- changi ng in the relatively small area. 686 Maciej Kania Fig. 5. Examples of hand-specimens from domain no. 2 A - Rakon Mt. cataclasite with graphite bands; B - Zabrat’ Pass ultramylonite Microstructures (Fig. 6). The proportion ofthe moderately and strongly deformed rocks (meso- and ultracataclasites) on the weakly deformed rocks (protocataclasites) increases west- wards. The ultracataclasites form layers with the maxi mum width of ~10 cm, and are cut with numerous conj ugate shears. Graph ite bands also occur in the form of up to 1 mm veins (Fig. 6A). In the mylonites, S-C-foliation structures are clearly recognizable. Below the Rakoń Mt. on the Zabrat’ Pass, very well-devel- oped mylonites with rotational core - mantle structure porphyroclasts were found (Fig. 6C). Fine-grained quartz ag- gregates on the sericite-dominated background emphasize the C-fo li a tion planes, to gether with micas, which show no sigmoid shapes. One-sided syntaxial pressure fringes (Bons et al., 2012) are well-developed on opaque minerals (Fig. 6B). As noted above, the deformation style locally changes dramatically in the small scale (Fig. 6D), with sharp boundaries between. Kinematics. The main set of thrusting faults has the top-to-the-S kinematics. These faults dip mainly to the N, NNE and S at moderate angles. The second set of faults is com- posed of moderate to steep faults dipping to the S with top-to-the NE sense of sheari ng recorded. In the predominant ductile deformed zones, S-C-foliation is not homogeneous (Fig. 7). The C planes dip at low and moder- ate angles to the eNe, or at steep angles to the NW and NNW. The S planes dip to the E, ESE, and SE at moderate angles. The spatial re i ationships of the C and S planes record a dom i - nant tectonic transport di reciion top-to-the-NNE and NE. The same is proved by the C’ synthetic shears dipping to the NE, as well as by orientation of porphyroclasts and mica fish in oriented thin sections. DOMAIN 3: THE WOŁOWIEC MT. MASSIF Geo log i cal setting. The Wołowiec Mt. massif (Fig. 8) is composed of granitic gneisses and gneisses (Michalik and Guzik, 1959). Be l ow the metamorphic complex, leucogranites with amphibolite inclusions occur. Skupiński (1975) mapped there a single horizon, tens of metres wide, of “tectonic greisenisation”. This zone is marked also by Bac-Moszaszwili et al. (1979) as mylonites. However, Żelaźniewicz (1996) stated that these mylonites (as well as mylonites mapped by those au- thors in other areas) form numerous en-echelon low-angle zones instead of continuous horizontal outcrops. Cymerman (see Piotrowska et al., 2007) mapped a band of cataclastic rocks on the NW Wołowiec Mt. slopes, and interpreted it as a basement of one of thrust-sheets buildi ng the Wołowiec Mt. massif. Lower parts of the SW and SE slopes of the Wołowiec Mt. and the area of the Jamnicka Pass are composed of Rohace-type granodiorites (Nemcok et al., 1994). Gawęda (2001) included the Wołowiec Mt. into the upper structural unit but marks a few SW-NE narrow mylonitic zones cutting the up- per struct ural unit, alaskites and the lower struct ural unit. The shear zone-rel ated micas were dated by Deditius (2004), re- vealing 343 ± 13 to 298 ± 11.3 Ma (40Ar/3 Ar method on musco- vites), and in terpreted as a product of two ductile deformation events: older, related to overthrusting of the metamorphic com- plex, and younger, related to the Rohace-type granodiorite in- tru sion. The contrasts in the Wołowiec Mt. massif lithology are strongly linked with geomorphological features, which is marked i.e. by steep rocky slopes in the southern part of the mas sif. Shearing-related rocks and mesostructures (Fig. 9). The occurrences of fault rocks on the N and NW slopes of the Wołowiec Mt. begin in the vicini ty of the border pole no. 249/5 and continue southwards to the top of the massif. Along the touristic pathway, zones of cataclasis can be de tected basi ng on the fragments found on the ground. These fragments are weakly deformed leucogranites and granodiorites, alternating with granitic gneisses, locally folded (Fig. 9A). Bi o tite-rich S-C cataclasites were also found. Pegmatites are also observed in this area. The eastern slopes of Wołowiec Mt. are very steep, often vertical, and therefore difficult to access. However, in the rock fragments found below these walls (Skrzynia, Skrajniak), granodiorites and granodiorite or leucogranite-based cata- clasites can be often found (Fig. 9B). In trenches cutting the top of the Wołowiec Mt., mesocataclasites with a leucogranitic protolith occur. Numert ous brittle shear planes, formi ng a typical Y-P-R sheari ng sys- tem, cut these rocks. Numerous, good quali ty outcrops of the fault rocks are lo- cated on the NW and W slopes of the Wołowiec Mt., in the terri- tory of the Slovak Repub i ic. Along the patch travers i ng the top- most parts and branching from the touristic pathway at an alti- tude of ca. 1835 m, there are four zones of weak to moderate cataclasis of the leucogranites and granodiorites. A well-outcropped complex of the fault rocks can be obf served on the W slopes of the Wołowiec Mt. along an unofficial touristic path at altitudes of ca. 1900-1950 m. At least four nar- row zones of mylonites and phyllonites, up to tens of cm in width, occur there. Up to 20 m wide bands of cataclasites are present in between. The protolith of the cataclasites was mainly granodiorite what is proved by their mineral composition. At some places, mesocataclasites pass into ultracataclasites. On the SW slopes of the Wołowiec Mt. (south of the Wołowiec-Jamnicka Pass touristic pathway) a few niches with meso- and ultracataclasite outcrops are present. Locally, bands of quartz and mica mylonites or mylonitic schists and phyllonites Microstructures of shear zones from selected domains of the Western Tatra Mountains 687 Fig. 6. Examples of microstructures from domain no. 1 A - catalasite from the Rakon Mt. with a system of joints filled with sericite and a graphite band (lower right corner); B - fringe structure in the pressure shadow of an opaque mineral grain (probably hematite); C - quartz pophyroclasts in ultramylonite from the Zabrat’ Pass; D - sharp border between textural types observed in the shear zone on the Zabrat’ Pass: lower part - ultramylonite, upper part - protomylonite; all pho- tos in crossed polarizers Fig. 7. The orientation of S-foliation planes (red arcs), C-foliation planes (blue arcs), C' shear bands (green arcs) and mineral grain lineation (points) in domain no. 2 688 Maciej Kania Fig. 8. The general view of domain no. 3, northern part A - shear zones on the almost vertical Wołowiec Mt. wall; B - leucogranite/cataclased leucogranite-dominated zones; C - the Wołowiec Mt. top, with cataclased granodiorites; D, E - complex shear zones on the western slopes with graphite are also observed. The protolith of the cataclasites was Rohace-type granodiorite. The rocky part of the main Western Tatra Mts. Ridge, east of the top of the Wołowiec Mt., is an area of shear zone with complex lithologies. Below an altitude ofca. 1900 m, packets of crystalline (sericite, biotite, sillimanite chlorite, epidote-quartz; Fig. 9C, D) schists are present. These rocks can be classified as phyllonites and mylonites with well-de vel oped fo li a tion planes form i ng schistosity with distinctive asymmetric features like mica fish occasionally with later deformation. Microstructures (Fig. 10). In the samples from the NW slopes of the Wołowiec Mt., feldspars show features of brittle and brittle-ductile deformation (Wiliiams et al., 2000; Passchier and Trouw, 2005), as well as quartz with traces of dynamic recrystallisation in the subgrain rotation process (Halfpenny et al., 2006), forming aggregates of elongated grains. Sericite ma- trix is present on the feldspar/feldspar contacts. The W slopes of Wołowiec Mt. show a complicated pattern of rocks and their microstructures. Mylonites are interchanged with cataclasites, these two fault rock types are difficult to distin- guish macroscopically. In addition, a few cm wide zones of phyllonites occur, especially southwards. In these rocks, S-C mylonitic fo liation is well developed in mica: mainly biotite or chloritised biotite—chlorite. Mica fish structures are abundant and show traces of multistage deformation (Fig. 10A, D, E). In addition, sillimanite fibrolite nests are present. They are elon- gated paral t el to the mineral grain lineation on the S planes. Recrystallised quartz forms core-mantle porphyroclasts (Fig. 10B). Locally, the fault rocks form a kind of tectonic microscale mélange composed mainly of mylonitic sericite matrix, quartz grains with pressure shadows, sheared with numerous shear bands or microfaults. On the W slopes of the Wołowiec Mt., ultracataclasites are characterized by a high grain to reduced grain matrix content ratio - up to 1:1. Some of the ultracataclasites show weak folia- tion or matrix layeri ng. Cataclastic breccias or fault gauges lo- cally occur. The main deformation mechanisms observed in the microscale are brittle deformation of plagioclases with intracrystalline slip systems. Further to the south in cataclasites, shear folds and microfolds are also observed (Fig. 10C, D). On the Łopata Mt., deformations are local i zed in the narrow zones of folded micas and chaotic aggregates of quartz with bulgi ng recrystallisation features and with microscale folds of the recrystallised matrix. Kinematics. The sense of shearing recorded in the brittle structures is variable, however top-to-the-S thrusting dominates on the relatively low-angle, mostly N-dipping faults. The second set of faults is also characterized by south-dipping shears with top-to-the-N kinematics. The C planes in the mylonitic foliation dip to the WSW at low to moderate angles. The S planes dip to the SE and SW at low angles. This records (Fig. 11) the tectonic transport di reciion top-to-the-WNW-NNW. The same direction is recorded by the C’ shear band dipping to the NW at low angles. DOMAIN 4: TRZYDNIOWIAŃSKI WIERCH MT., CZUBIK MT. AND KOŃCZYSTY WIERCH MT. Geological setting. The Trzydniowiański Wierch Mt. (Fig. 12) in its upper part is composed of two leucogranitic pack- ets with gneissic bands in between (Michalik and Guzik, 1959). Microstructures of shear zones from selected domains of the Western Tatra Mountains 689 Fig. 9. Examples of hand-specimens from domain no. 3 A - fold developed in the Wołowiec Mt. gneiss; B - cataclasite from the Skrajniak; C - gneiss with well-visible S-C-foliation and C’ shear bands, inducing dextral sense of shearing, from the Dziurawe Pass area; D - blastomylonite from the Łopata Mt. A mylonitic zone cuts the massif horizontally and is outcropped on the northern slopes (Skupiński, 1975; Bac-Moszaszwili et al., 1979; Gawęda 2001). To the south, the Czubik Mt. topmost parts are composed of granodiorites with granitic gneisses be- low (Michalik and Guzik, 1959). The contemporary morphology of the slope, with three zones of flatten i ng, can be linked with zones of intensive cataclasis, developed within leucocratic gra- nitic gneisses or leucogranites. On the eastern slopes, quartz veins are outcropped, sim i lar to these described on the western slope of the Chochołowska val ley. Shearing-related rocks and mesostructures (Fig. 13). The fault rocks occur on the western slopes of the Trzydniowiański Wierch Mt. along the touri st pathway. This area lacks of outcrops, however, some observations are possi- ble. The deformed rocks in this area are mainly leucogranites (Fig. 13A) or leucocratic granitic gneisses whose gneissic struc- ture is a relic of an older deformation stage (Fig. 13B). The general trend is an upward increase of non-coaxi al shearing intensity. The cataclastic, locally chaotic breccias grad u ally change to protocataclasites, which is marked by the development of intragranular slip surfaces and results in a block-controlled cataclastic flow regime according to Ismat and Mitra (2005). To the north, some occurrences of weakly to moderately deformed leucogranites were observed. The lush mountain pine cover does not al low a detailed analysis of these rocks, however, it seems that there are a few up to tens of centimetres wide deformed zones, with non-deformed gran i te in between. The area of the Czubik Mt. is characterized by occurrences of the packet of cataclased leucogranites and granodiorites. The products of deformation of granodiorites are cataclastic (Fig. 13C) and chaotic breccias gradually passing into protocataclasites. On the western slopes of the Czubik Mt. oc- cur up to 20 cm wide zones of mylonites (mylonitic schists, phyllonites) with millimetre-scale graph i te bands. The intensity of deformation decreases southwards. On the Konczysty Wierch Mt. northern slopes, a number of zones of granodiorite breccias were observed. These are fracture brec- cias, locally chaotic breccias, without cataclastic matrix. Microstructures (Fig. 14). In the Trzydniowianski Wierch Mt. area, the characteristic feature is brittle microstructures overprinti ng ductile ones. These are mainly S-C mylonitic folia- tion relics; some white micas show traces of brittle deformation. Older, mainly ductile structures, especially mica bands, were later reworked duri ng cataclasis. In the Czubik Mt., there are cataclasites with the block-con- trolled cataclastic flow type and small amounts of cataclastic sericite matrix (Fig. 14A). However, the amountof matrix is vari- able, lo cally pro mot ing protocataclasites to meso- or even ultracataclasites (Fig. 14B). Quartz is dynamically recrystallised in the bulgi ng recrystallisation process. The granitic gneiss de- formation is focused mainly in the mica bands which were sheared and broken, and locally their fragments were rotated. Therefore, the rock has features of tectonic microbreccia. At places, core-man tle ro tat ing porphyroclasts are also present. In the areas of typical gneisses or mylonites (Trzydniowianski Wierch Mt., Czubik Mt. western slopes), well-developed C’ sheari ng bands are observed (Fig. 14C). In the Konczysty Wierch Mt. cataclasites intracrystalline fractures in feldspars and undulose exti nction in quartz are deformational microstructures observed. 690 Maciej Kania Fig. 10. Examples of microstructures from domain no. 3 A - brittle dextral shearing of muscovite fish-an example ofthe structures overprinting in cataclasite from the Wołowiec Mt.; B - de- tailed view of the quartz core-mantle structure: one wing (in the centre) and part of 8-type porphyroclast (on the right), Wołowiec Mt.; C - intrafoliation microfolds in mylonite from the complex brittle-ductile shear zone, Wołowiec Mt.; D - muscovite fish structure indi- cating sinistral sense of shearing, Dziurawe Pass; E - muscovite fish sheared in brittle conditions, forming domino-type structure; F - asymmetric microfolds developed in dextral shearing in the Dziurawe Pass mylonite ■4 Fig. 11. The orientation of S-foliation planes (red arcs), C-foliation planes (blue arcs), C' shear bands (green arcs) and mineral grain lineation (points) in domain no. 3 Microstructures of shear zones from selected domains of the Western Tatra Mountains 691 Fig. 12. The general view of domain no. 4 from the Konczysty Wierch Mt. to the north A - gneisses with brittle shearing overprint; B - leucogranites with protocataclasis and cataclasites with remnants of ductile structures; C - outcrops of massive quartz veins Fig. 13. Examples of hand-specimens from domain no. 4 A - leucogranite from the Czubik Mt. area with brittle deformation; B - mylonite from the Trzydniowański Wierch Mt. with clear S-C-foliation (dextral sense of shearing); C - protomylonite from the Trzydniowański Wierch Mt. 692 Maciej Kania Fig. 14. Examples of microstructures from domain no. 4 A - cracked and partially bended plagioclases in leucogranite from the Czubik Mt.; B - more advanced cataclasis than in photo A, with abundance of the cataclastic matrix; C - C’-type shear band cutting mylonitic fo I i at ion in gneiss from the Trzydniowianski Wierch Mt. (sinistral sense of shearing) Kinematics. There are two distinctive sets of brittle shear- ing. The first one is characterized by thrust faults dipping at moderate angles mainly to the N, with top-to-the-SE sense of sheari ng. The second set embraces mostly S-dipping faults with the N-NW direction of tectonic transport. The C planes in the mylonitic foliation have different dip azi- muths in the range NNE-E-SSE with moderate to steep ant gles. The S planes dip to the SE at moderate angles. The inter- pretation of these relationships is difficult, but top-to-the-SW tectonic transport direction seems to be dom I nant among duc- tile structures in this domain (Fig. 15). Fig. 15. The orientation of S-foliation planes (red arcs), C-foliation planes (blue arcs), C' shear bands (green arcs) and mineral grain lineation (points) in domain no. 4 QUANTITIVE DETERMINATION OF THE STRUCTURE SHAPE-PREFFERED ORIENTATION Table 4 shows the concentration coefficient of samples in which morphometrical analysis was done. The coefficient val- ues vary befween 13 and 82%. The min i mal value was obf served in the ultracataclasite from the Długi Upłaz. Higher val- ues are observed in some leucogranites: 40% (Łuczniańska Pass sample). This is re iated to the magmatic foi iafion devel- oped duri ng anatexis, as well as to the inheri ted older fo i iation. Similar coefficients are observed in most of cataclasites, how- ever, the presence of monoclinic struciures (S-C cataclasites) makes the coefficient higher (L > 50%). The highest values are Table 4 Concentration coefficents (L) of the relative grain orientations in selected samples Texture Location Rock name type (structural domain) L [%] leucogranite A1 Łuczniańska Pass (1) 37 cataclastic breccia A2 Wołowiec Mt.(3) 46 protocataclasite A2 Kończysty Wierch Mt. (4) 29 protocataclasite A2 Wołowiec Mt. (3) 37 C2 Trzydniowiański Wierch 48 protocataclasite Mt. (4) mesocataclasite A2 Długi Upłaz (1) 71 mescocataclasite C3 Dziurawa Pass (3) 35 ultracataclasite A3 Długi Upłaz (1) 13 ultracataclasite B4 Zabrat’ Pass (2) 33 protomylonite C2 Wołowiec Mt. (3) 50 mesomylonite D3 Zabrat Pass (2) 61 ultramylonite C4 Długi Upłaz (1) 71 ultramylonite D4 Zabrat Pass (2) 82 The textural types are defined in Kania (2014) Microstructures of shear zones from selected domains of the Western Tatra Mountains 693 ob served in mylonites, up to 82% in the Zabrat Pass ultramylonite, where porphyroclasts are elongated and oriented along the foliation. DISCUSSION Taki ng into account the type of structures corre i ated with the protolith rock, the fol lowi ng four structural types of shear zones can be distinguished in the discussed area (Fig. 16): - The 1st type shear zones with structures developed only in the ducii le conditions. These are mainly meso- to ultramylonites, often with high mica content (the term “phyllonite” (Brodie et al., 2007) seem to be useful for rocks with high mica content and dense foliation planes). The characteristic feature is that the zones are now lo- cated mainly on mountain passes (Łuczniańska, Zabrat’, Dziurawa). - The 2nd type zones that developed in the brittle-ductile conditions. These zones form large packets, formed by various types of shearing-re lated rocks (but mainly proto- to mesomylonites, and cataclasites). The charac- teristic feature is the density of mesofaults, at some places even above 100 planes per a 1 metre profile. Two examples in the investigated area are the Litworowy Couloir and the Wołowiec Mt. massif. - The 3rd type shear zones which are developed in the brittle regime of deformation, but preserve some fear tures of earl ier deformation, like mica fish. These types of shear zones are characteri stic for the marginal areas of thrust sheets, and occur in the vicini ty of non-de- formed leucogranites on the Czubik Mt. - The 4th type shear zones with only weak to moderate brittle deformation (mainly proto-, sometimes mesocataclasites). These zones occur mainly in the northern parts of domains no. 1 and no. 4, i.e. the Długi Upłaz and the Trzydniowiański Wierch Mt. However, even these rocks show moderate, but significant shape-preferred orientation of grains. The list above can be upgraded by addi ng gneisses which, obviously, were sheared, however, these form massifs rather than limi ted local ized shear zones. The interesting problem is the relationships between shear zone types listed above and the lithology of rocks which under- went shearing-related dynamic metamorphism. Such correla- tion is problematic due to the fact that numerous protolith lithologies occurred in this area. The variabil i ty of structures of- ten observed on the thin sec tion scale makes modal mineral analyses mostly unusable for determination of the protolith. However, location of the shear zones, and their spatial relation- ships, all ows to formulate the following observations: - the 1st type shear zones are metamorphic schists, which probably have not undergone advanced later de- formation; - the 2nd type shear zones seems to be developed mainly from granodiorites, probably as an effect of their shear- ing; - the 3rd type shear zones are gneisses or granitic gneiss- es which underwent later deformation in the brittle condi- tions; - the 4th type shear zones are leucogranites which have not been deformed under ductile conditions, however brittle deformation is clearly visible, and observed shape-preferred orientation marks a non-coaxial defor- ma tion re gime. This overview indicates advanced deformation partitioning - which means a subdivision of deformation into domains with different deformation patterns (Passchier and Trouw, 2005) - of the Western Tatra crystal i ine core, correspond i ng with the de- formed rock type. The ductile shear zones were later reactF vated, however, new brittle and brittle-ductile shear zones were also created form i ng a complex lithological structure. The rate of deformation was different in different parts of the complex (Kania, 2014). Brittle reworki ng of the older ductile structures could lead to the formation of tectonic melange zones, however, in most cases it seems that the older discon tinu ities were the basis for sim i iarly (but not exactly the same) oriented brittle shear zones. This disorientation is typical when taking into ac- count reactivation of the shear zones (Bons et al, 2012). The idea of two inverted metamorphic structural units (Janak, 1994; Gawęda, 2001; Gawęda and Burda, 2004) seems to be too much simplified. Especially, the interpretation of the upper parts of the Długi Upłaz Ridge and of the Wołowiec Mt. as a migmatite upper structural unit, as it was shown on the map by Gawęda (2001), might need some re con sid era tion. Migmatites are not very common in this area and are not marked on the older maps (e.g., Bac-Moszaszwili et al., 1979) where leucogranites (called “alaskites” there) and mylonites domi nate, whilst other metamorphic rocks (gneisses, schists, probably also amphibolites) occur sporadically. The compli- cated struc ture is not only due to the diversity of protoliths (leucogranites, which are a product of anatexis of earl ier de- formed rocks (orthogneisses), Rohace-type granodiorites, and metamorphic rocks, but also due to the diversity of multi-stage deformation products. The most prominent shear zones are those of the 2nd type. In the study area they form two packets of sheari ng-re lated rocks, up to hundreds of metres wide. The first one cuts the Długi Upłaz Ridge, and forms deformational complexes in the Litworowy Couloir, outcropped at altitudes of ca. 1400-1500 m. The second one is the upper part of the Wołowiec Mt. massif, above an altitude of ca. 1800 m. From the structural point of view, this is the upper wall of the Wołowiec Mt. overthrust (Cymerman, 2011). This wall has a form of a strongly heteroge- neous complex of fault rocks, formed in a brittle and brittle-duc- tile compressional regime. The compression resulted in the for- mation of numerous hierarchical tectonic flakes. Within the massif, the fault rock lithology varies vertically (protocataclasites near the Wołowiec Mt. summit, meso- and ultracataclasites below), as well as laterally (increasing grade of deformation intensity southwards). The vertical gradient, per- pendicu iar to the thrust plane is interpreted as an effect of the decreasing deformation intensity in the damage zone of the Wołowiec Mt. overthrust (Childs et al., 2009). The horizontal (subhorizontal) gradient can be linked with the proxi mi ty of the Wołowiec Mt. overthrust margin. The structures and the interpreted process described above are correct also for the Długi Upłaz with the Litworowy Couloir. The sequence of fault rocks in the Litworowy Couloir (cataclasites, S-C cataclasites, mylonites) resembles the se- quence observed on the western slopes of the Wołowiec Mt. The observed fault rock complexes should be considered as shear zones paral iel to the thrust i ng planes of tectonic flakes in the crystal I ine core. The complex internal structure of such zones was underlined by Żelaźniewicz (1996); however, he had not discussed the diversity of the fault rock present in these zones. The characteristic feature observed is the presence of quartz and pegmatite veins near the mylonitic schist zones. At least four such zones were found between the Łuczniańska Pass and the Rakoń Mt. Cymerman (2009) linked the presence 694 Maciej Kania Fig. 16. Sketch-map of the dominant types of shearing zones and orientation of mesofaults in the selected areas (Angelier's diagrams, lower hemisphere, equal-area projection; red arrows marks mean tectonic transport direction) For further explanations see text of the white quartz veins (so-called “gooses”) with shearing and thrust i ng zones. On the other hand, Gawęda (2001) stated that pegmatites occur in the core parts of folds. This is obviously normal situation in shear zones (Hudleston, 1989), however, lam inated veins seem to be rather a product of sili ca transport and deposition along shear zones, especially at the contact be- tween hardened and softened zones, as it was described ear- lier. The fault rock complex of the Trzydniowiański Wierch Mt. with two types of shear zones (3rd and 4th) can be interpreted as a product of low-angle overthrusting of the leucogranitic flake over the granitic gneisses. Such a structure can be inter- preted also as developed during syntectonic anatexis when the melt forms leucogranitic veins, and gneisses form the restite. The stress was mainly accommodated by deformation of the older ductile deformation zones in the granitic gneisses. The upper, leucogranitic, packet shows signs of magmatic syntectonic foliation. Subsequently, leucogranites underwent only weak to moderate brittle deformation, resulting mainly in the formation of some breccias and protocataclasites. The analysis of the kinematics of non-coaxial brittle shear- ing structures - Y-P-R fault systems (Katz et al., 2004), docu- mented sense of sheari ng top-to-the-SE, S and SW (Fig. 16). The most common sense of shearing recorded by the ductile or brittle-ductile kinematic indicators is top-to-the-NW and W. Sim- ilar senses of shearing were observed also in the other areas of the Western Tatra Mts., e.g. on the Łopata Mt., the Niska Pass and on the Jarząbczy Wierch Mt. (Cymerman, 2011). It indk cates that the movement field during brittle deformation pn> cesses was relatively homogenous in the whole Western Tatra Mts. crystalline core. The deformation processes were intense, as proved by thick complexes of fault rocks on the Wołowiec Mt. Microstructures of shear zones from selected domains of the Western Tatra Mountains 695 or in the Litworowy Couloir. The grain shape indicators analysis of the fault rocks in the Western Tatra Mts. (Kania, 2014) sug- gests this was a long process, below the feldspar plasticity limit, but with dynamic recrystallisation of quartz and intense sericitisation of feldspars. The domi nant products of britt le de format ion in the de- scribed area are complexes of protocataclasites and some mesocataclasites formed duri ng a block-controlled cataclastic flow (Ismat and Mitra, 2005; Kania, 2014). The presence of brit- tle re gime-re lated ki ne matic in di ca tors, as well as mea sured shape-preferred orientation, marks a non-coaxial character of these processes. The mylonites observed in the study area are mainly low-grade mylonites, as they are defined by T rouw et al. (2010), with the following distinctive features: crystal-plastic deforma- tion of quartz, elongated shapes, undulose ex tinc tion, and sometimes bulging recrystallisation (BLG). At some places, subgrain recrystallisation aggregates are present, but more likely is that there are effects of a decreasing strain rate instead of increasing temperature (Hirth and Tullis, 1992). Feldspars underwent mainly brittle deformation, with some crystal-plastic structures. Common occurrences of asymmetric kinematic indi- ca tors (like mus co vite fish), as well as sharp transi tions be- tween textural types (Fig. 6D) also mark the low-grade mylonites that formed in the temperature range between 250 and 500°C (Trouw et al., 2010). The most intrigu i ng problem is time re lationships between the described shear zones. In lack ing good geochronological data, it is still possible to make some conclusions. According to the four shear zone types listed at the beginning of this discussion: - The 1st type shear zones represent only ductile defor- mation, which can be interpreted as a Variscan metat morphism product. The reactivation of these zones can- not be excluded, however, there are no clear evi dences for this. - The 2nd type shear zones reptesent ductile and britf tle-ductile shearing, mainly in granodiorites. The Alpine age of the older structures seems possible. - The 3rd type shear zones are Variscan gneissic rocks which underwent later (Alpine) brittle deformation. - The 4th type shear zones are leucogranites, and their brittle deformation can be of the same age as in the 3rd type. However, these rocks show no ductile deformation due to later leucogranite emplacement, other than meta- morphism of gneisses. In fact, these leucogranites are a product of Variscan anatexis with Alpine brittle deforma- tion. The question arises if ductile-brittle deformation can be not only Variscan but also Alpine in age. Analysis of the available data shows that duri ng the Alpine orogeny there were the fol- lowing stages with conditions favourable for brittle and duct tile-brittle deformation, as well as for hydrothermal processes (Fig. 17): 1. Upper Cretaceous eo-Alpine metamorphism with conditions for mylonitisation at 140-120 Ma (Maluski et al., 1993) and intense compressional tectonics (Jurewicz, 2005). 2. Cretaceous and Cretaceous/Paleogene boundary with probable mylonitisation (or phyllonitisation) epi- sodes at 89-85 Ma and 66 Ma (Maluski et al., 1993). 3. Eocene-Oligocene compressional stage (Lefeld, 2009), with the beginning of uplift marked with pseudotachylyte generation (Kohut and Sherlock, 2003). 4. Rotational uplifting of the Tatra blockduring the Mio- cene (Jurewicz, 2005). The temperature of the Tatra massifexceeded 100°C in the Palaeogene and even in the Miocene (Kovac et al., 1994; Anczkiewicz, 2005; Anczkiewicz et al., 2013), which means conditions favourable for hydrothermal activity. The young hy- drothermal activity is proved also by dating of clay minerals from the so-called “clay pockets”, containing fault gauges in the High Tatra Mts. (Kuligiewicz, 2011). The Tatra massif may have been additionally warmed up during Miocene magmatism in the Central Western Carpathians (e.g., Danisfk et al., 2008, 2010, 2012). Moreover, the cool i ng of the Tatra Mts. was slower in their western part, due to the westward plunging of the Miocene rotation axis (Jurewicz, 2005). These data support the thesis of the role of the hydrothermal process in the formation of different deformation complexes (strain softening and strain hardening subzones of the parent shear zones; Kania, 2014). The role of the greisenisation process, earlier postulated by Skupiński (1975), was not so important, however, it was observed. The question is if it was really “tectonic greisenisation”, as Skupiński wrote, or just small-scale greisenisation along some of the shear zones, which seems to be more likely due to lack of struc- ture-connected greisenisation evidences. On the other hand, there are opin ions (Żelaźniewicz, 1996) that mylonites are of a Variscan age and could be overprinted by Alpine processes. This is not probable, especially when re- gard i ng a general southward sense of shear marked by ductile kinematic indicators. Nonetheless, the shear zones dominated by brittle-ductile deformation may have been formed mainly duri ng the Alpine orogeny and inheri ted some of the Variscan features at that time. The applied method of statistical determination of the shape-preferred orientation allows the recognition of directional features even in non-foliated rocks. However, the shape-preffered orientation of an aggregate reflects long-time and multistage history of the deformation, so it is not an indica- tor of the mean or late stage kinematics (Stahr and Law, 2014). In fact, if 37% value was achieved in the syntectonic anataxesis of the leucogranite, lower values (observed in one of the cataclasites) could be interpreted as an effect of disi ntegration and then chaotic disorientation of grains duri ng cataclasis. On the other hand, the higher values were achieved during non-co- axial shearing processes in the cataclasites, as well as mylonites. The interesting question should be a comparison of the brit- tle structures developed in the crystalline rocks and those in T ri- assic quartzites (Seisian) of Tatricum. Some preliminary data shows that the orientation of the dominant fault set on the Długi Upłaz Ridge (Fig. 16) is similar to the one set of joints observed in quartzite at the Upalone site. This problem needs further in-depth investigation. The fault plane orientations and shear sense recorded in the brittle structures (Fig. 16) are characieri stic for the Alpine orogeny processes, bei ng an effect of the ALCAPA terrain mi- grafion to the north (Csontos and Voros, 2004). However, the complicated and non-unambiguous pattern of brittle kinematics is an effect of the location on the NW corner of the Al- pine-Carpathian mountain belt as well as of thrusting processes in the autochthonous basement of the Western Carpathians (Jarosiński, 2011). Yet, this interpretation applies only to sets of mesofaults, and is just a part of the complicated kinematic and structural overview of the Western Tatra crystalline massif. 696 Maciej Kania Fig. 1l. Compiled scheme of the Tatricum tectono-metamorphic evolution Temperatures: 1 - maximum of the Variscan metamorphism (Polleret al., 2GGG; Gawęda and Burda, 2GG4); 2- eo-Alpine metamor- phism (Daniśik et al., 2G11, 2G12); 3a, b - Ar/Ar dating (Maluski et al., 1993); 4 - Tatricum cooling (Kovac et al., 1994); 5 - apatite fis- sion track dat i ng (Burchart, 1972); 6 - cooli ng field of the Tatra massif, FT dat i ng (Anczkiewicz, 2GG5), 7 - Miocene temperature rising (Daniśik et al., 2G12). Geoiogical events: G1 - granitoid intrusion, protolith for gneisses (Poller et al., 2GGG); G2 - Rohace granodiorite intrusion (Poller etal., 2GGG); G3- leucogranite syntectonic formation (Gawęda, 2GG1); VM - main stage of the Variscan metamorphism (Polleretal., 2GGG; Gawęda and Burda, 2GG4); EAM - eo-Alpine metamorphism (Daniśiket al., 2G11, 2G12); N1 - Choc unit overthrusting, N2 - Krizna unit overthrusting (Jurewicz, 2GG5); N3 - eo-Alpine overthrusting (Daniśik et al., 2G12); N4 - Eocene/Oligocene overthrusting (Lefeld, 2GG9); MYL - Alpine mylonites generation (Maluski et al., 1993). Tectonic phases accord- ing to Jurewicz (2GG5). Deformation conditions: BR - brittle, BR/DU - brittle-ductile, DU - ductile, orange bars - pre-Alpine stage of brittle-ductile deformation and Alpine stage of brittle deformation according to Jurewicz and Bagiński (2GG5); blue line - interpreted conditions of deformation in the Western Tatra Mts.: a - Variscan ductile deformation, b - more ductile conditions during the eo-Al- pine metamorphism, c - formation of Alpine mylonites, d - more ductile conditions duri ng the Miocene thermal event Microstructures of shear zones from selected domains of the Western Tatra Mountains 697 CONCLUSIONS 1. The shear zones take a key role in the Western Tatra crystalline massif structure. Numerous heterogeneous, gener- ally sub-horizontally oriented shear zones were developed dur- ing mainly non-coax ial sheari ng of different protholitic rocks. 2. Four types of shear zones have been distinguished: (1) ductile shear zones in gneisses, (2) brittle-ductile complex shear zones, (3) ductile mylonitic shear zones in gneisses with clear later brittle deformation overprinted, (4) brittle shear zones developed in leucogranites after their anatectic formation. 3. These shearing deformation processes were long-lasting with the development of different asymmetric structures at dif- ferent levels and probably at different times. The brittle struc- tures are in general younger than the ductile ones, the strain partition i ng was crucial in the formation of the shear zones. 4. The shear sense recorded by the structures formed in the ductile conditions is different from the main ductile-brittle and brittle regime of deformation. Acknowledgements. I am especially gratetul to M. Kohut and Z. Cymerman, the reviewers of this paper, for their remarks and advices. I thank the Directorate of the Tatra National Park for the permission to conduct fieldwork. The study was financed by the Jagiellonian University funds for young scientists, and was part of my Ph.D. thesis. REFERENCES Anczkiewicz, A., 2005. Cenozoic uplift of the Tatra and Podhale Ba- sin from the perspective of the apatite fission track analyses. Polskie Towarzystwo Mineralogiczne. Prace Specjalne, 25: 261-264. Anczkiewicz, A., Środoń, J., Zattin, M., 2013. Thermal history of the Podhale Basin in the internal Western Carpathians from the perspective of apatite fission track analyses. Geologica Carpathica, 64: 141-151. Bac-Moszaszwili, M., Burchart, J., Głazek, A., Iwanow, A., Jaroszewski, W., Kotański, Z., Lefeld, J., Mastella, L., Ozimkowski, P., Roniewicz, P., Skupiński, A., Westwalewicz-Mogilska, E., 1979. Geological map of the Pol- ish Tatra Mountains (in Poli sh with Engl ish descriptions). Wyd. Geol., Warszawa. Berthe, D., Choukroune, P., Jegouzo, P., 1979. Orthogneiss, my- lonite and non-coaxial deformation of granites: the example of the South Armorican Shear Zone. Journal of Structural Geology, 1: 31-42. Bons, P., Elburg, M., Gomez-Rivas, E., 2012. A review of the for- mation of tectonic veins and their microstructures. Journal of Structural Geology, 43: 33-62. Brodie, K., Fettes, D. Harte, B., Schmid, R., 2007. Structural terms in cluding fault rock terms. Recommendations by the IUGS Subcomission on the Systematics of Metamorphic Rocks. Web version of 01.02.07. http://www.bgs.ac.uk/scmr/docs/pa- pers/paper_3.pdf [15.07.2013] Burchart, J., 1972. Fission-track age determinations of accessory ap a tite from the Tatra Mountains, Po land. Earth and Planetary Science Letters, 15: 418-422. Burda, J., Gawęda, A., 2009. Shear-influenced partial melting in the Western Tatra metamorphic complex: geochemistry and geochronology. Lithos, 110: 373-385. Burda, J., Klotzli, U., 2007. LA-MC-ICP-MS U-Pb zircon geochron- ology of the Goryczkowa type grani te - Tatra Mts., Po I and. Prace Specjalne PTMin, 31: 89-92. Burda, J., Gawęda, A., Klotzli, U., 2013. U-Pb zircon age of the youngest magmatic activ ity in the High Tatra grani tes (Central Western Carpathians). Geochronometria, 40: 134-144. Chen, Y., Jiang, D., Zhu, G., Xiang, B., 2014. The formation of mica fish: A modeling investigation based on micromechanics. Jour- nal of Structural Geology, 68: 300-315. Childs, C., Manzocchi, T., Walsh, J., Bonson, C., Nicol, A., Schapfer, M., 2009. A geometric model of fault zone and fault rock thickness variations. Journal of Structural Geology, 31: 117-127. Csontos, L., Voros, A., 2004. Mesozoic plate tectonic reconstruc- tion of the Carpathian region. Palaeogeography, Palaeoclimatology, Palaeoecology, 210: 1-56. Cymerman, Z., 1989. Determination of the sense shear (in Poli sh with English summary). Przegląd Geologiczny, 37: 605-613. Cymerman, Z., 2009. Tektonika alpejska waryscyjskiego krystaliniku Tatr Zachodnich - przykłady od Łuczniańskiej Przełęczy po NW zbocza Wołowca - Wycieczka terenowa A5 (in Polish). In: LXXIX Zjazd Polskiego Towarzystwa Geologicznego “Budowa geologiczna Tatr i Podhala ze szczególnym uwzględnieniem zjawisk geotermalnych na Podhalu” , Bukowina Tatrzańska, 26-29 września 2009, materiały konferencyjne: 121-133. Cymerman, Z., 2011. Zlokalizowane strefy ścinania w skałach krystalicznych na obszarze polskiej części Tatr Zachodnich (in Pol ish). In: Tatrzańskie Warsztaty Geologiczne (eds. T. Rychliński and P. Jaglarz): 20-49, Zakopane, 13-16 października 2011. Danisik, M., Kohut, M., Dunkl, I., Frisch, W., 2008. Thermal evolu- tion of the Żiar Mts. basement (Inner Western Carpathians, Slovakia) constrained by fission track data. Geologica Carpathica, 59: 9-30. Danisik, M., Kohut, M., Broska, I., Frisch, W., 2010. Thermal evo- lution of the Mala Fatra Mountains (Central Western Carpathians): insights from zircon and apatite fission track thermochronology. Geologica Carpathica, 61: 19-27. Danisik, M., Kadlec, J., Glotzbach, C., Weisheit, A., Dunkl, I., Kohut, M., Evans, N., Orvosova, M., McDonald, B., 2011. Tracing metamorphism, exhumation and topographic evolution in orogenic belts by mult iple thermochronology: a case study from the Nizke Tatry Mts., Western Carpathians. Swiss Journal of Geosciences, 104: 285-298. Danisik, M., Kohut, M., Evans, N., McDonald, B., 2012. Eo-Alpine metamorphism and the “mid-Miocene thermal event” in the Western Carpathians (Slovakia): New evi dence from mul tiple thermochronology. Geological Magazine, 149: 158-171. Deditius, A., 2004. Characteristics and isotopic age of the musco- vite blastesis from the mylonitic zones in the crystalline rocks of the Western Tatra Mountains (in Polish with Engl ish summary). Prace Naukowe Uniwersytetu Śląskiego, 16: 121-150. Fritz, H., Neubauer, F., Janak, M., Putis, M., 1992. Variscan mid-crustal thrusting in the Carpathians II: kinematics and fabric evol ution of the Western Tatra basement. Terra Abstract, Sup- plement 2 to Terra Nova, 4: 24. Gawęda, A., 2001. Alaskites of the Western Tatra Mountains. A re- cord of Early-Variscan collision stage in the Carpatians pre-con- tinent (in Polish with English summary). Wydawnictwo Naukowe Uniwersytetu Śląskiego, Katowice. Gawęda, A., 2007. Variscan granitoid magmatism in Tatra Moun- tains - the history of subduction and continental collision. AM Monograph, 1: 319-332. 698 Maciej Kania Gawęda, A., 2008. An apatite-rich enclave in the High Tatra granite (Western Carpathians): petrological and geochronological study. Geologica Carpathica, 59: 295-306. Gawęda, A., Burda, J., 2004. Evo I ution of the metamorphism and deformations in the crystall ine complex of the Western Tatra Mountains (in Poll sh with Engl ish summary). Prace Naukowe Uniwersytetu Śląskiego, 16: 53-184. Gawęda, A., Doniecki, T., Burda, J., Kohut, M., 2005. The petro- genesis of quartz-diorites from the Tatra Mountains (Central Western Carpathians): an example of magma hybridi zati on. Journal of Mineralogy and Geochemistry, 181: 95-109. Grotenhuis, S.M., Trouw, R.A.J., Passchier, C.W., 2003. Evo i u- tion of mica fish in mylonitic rocks. Tectonophysics, 372: 1-21. Guzik, K., 1959. Szczegółowa Mapa Geologiczna Tatr, 1:10 000, arkusz B1, Bobrowiec (in Polish). Wyd. Geol., Warszawa. Halfpenny A., Prior, D.J., Wheeler, J., 2006. Analysis of dynamic recrystallization and nucleation in a quartzite mylonite. Tectonophysics, 427: 3-14. Hirth, G., Tullis, J., 1992. Dis I ocation creep regimes in quartz ag- gregates. Journal of Structural Geology, 14: 145-160. Hudleston, P., 1989. The association of folds and veins in shear zones. Journal of Structural Geology, 11: 949-957. Ismat, Z., Mitra, G., 2005. Foldl ng by cataclastic flow: evo I ution of controlling factors during deformation. Journal of Structural Ge- ol ogy, 27: 2181-2203. Janak, M., 1994. Variscan up I ift of the crystal l ine basement, Tatra Mts., central western Carpathians: evidence from 40Ar/39Ar laser probe dati ng of biot ite and P-T-t paths. Geologica Carpathica, 45: 293-300. Jarosiński, M., 2011. Współczesne naprężenia tektoniczne w polskich Karpatach i na ich przedpolu: czy strefa szwu kolizyjnego jest mechanicznie spójna (in Polish)? In: IX Ogólnopolska konferenecja z cyklu “Neotektonika Polski” - Neotektonika Karpat i Polski pozakarpackiej: podobieństwa i różnice (ed. W. Zuchiewicz): 25-26, Kraków, 24-25 czerwca 2011. Jiang, D., 2014. Structural geology meets micromechanics: A self-consistent model for the multiscale deformation and fabric development in Earth's ductile lithosphere. Journal of Structural Ge ol ogy, 68: 247-272. Jurewicz, E., 2005. Geodynamic evolution of the Tatra Mts. and the Pieniny Klippen Belt (Western Carpathians): problems and comments. Acta Geologica Polonica, 55: 295-338. Jurewicz, E., Bagiński, B., 2005. Deformation phases in the se- lected shear zones within the Tatra Mountains granitoid core. Geologica Carpathica, 56: 17-28. Kahan, S., 1962. Eine neue Ansicht über den geologischen Aufbau des Kristallinikums der West Tatra (in German). Acta Geologica et Geographica Universitatis Comenianae, 12: 115-122. Kania, M., 2012. The structure and the evo I ution of the Alpine age shear zones in the crystalline core of the Polish part of the West- ern Tatra Mts. (in Poll sh with Engl ish summary). Unpub I ished Ph.D. thesis, Jagiellonian University, Kraków. Kania, M., 2014. Microfabric diversity and grain shape analysis of fault rocks from the selected areas of the Western Tatra Moun- tains. Geological Quarterly, 58 (1): 3-18. Katz, Y., Weinberger, R., Aydin, A., 2004. Geometry and kinematic evolution of Riedel shear structures, Capitol Reef National Park, Utah. Journal of Structural Geology, 26: 491-501. Kohut, M., 2000. Why are alaskites not present in the Slovak part of the Tatra Mountains? Prace Specjalne PTMin, 17: 187-189. Kohut, M., Janak, M., 1994. Granitoids of the Tatra Mts., Western Carpathians: field relations and petrogenetic implications. Geologica Carpathica, 45: 301-311. Kohut, M., Sherlock, S., 2003. Laser microprobe 40Ar-39Ar analysis of pseudotachylyte and host-rocks from the Tatra Mountains, Slovakia: evi dence for late Palaeogene seis mic/tec tonic ac tiv- ity. Terra Nova, 15: 417-424. Kohut, M., Siman, P., 2011. The Goryczkowa granitic type - SHRIMP dating of an original granodiorite-tonalite va ri ety. Mineralogia, 38: 113-114. Kohut, M., Poller, U., Gurk, C., Todt, W., 2008a. Geochemistry and U-Pb detrital zircon ages of metasedimentary rocks of the Lower Unit, Western Tatra Mountains (Slovakia). Acta Geologica Polonica, 58: 371-384. Kohut, M., Uher, P., Putiś, M., Sergeev, S., Antonov A., 2008b. Dating of the Lower Carboniferous granitic rocks from the West- ern Carpathians in the light of new SHRIMP U-Pb zircon data. 7th annual Christmas meetl ng of SGS (in Slovak). Mineralia Slovaca, 40: 3-4. Kovac, M., Kral, J., Marton, E., Plaśienka, D., Uher, P., 1994. Al- pine uplift history of the central western Carpathians: geochron- ol ogi cal, paleomagnetic, sed i men tary and struc tural data. Geologica Carpathica, 45: 83-96. Krawczyk, A., Słomka, T., 1994. Podstawowe metody matema- tyczne w geologii (in Poli sh). Wydawnictwo AGH. Kuligiewicz, A., 2011. Mineralogy of the clay gouges developed in shear zones of the High Tatra Mountains (in Polish with English summary). Unpublished MSc. thesis, Jagiellonian University, Kraków. Lefeld, J., 2009. Alpine orogenic phases in the Tatra Mts (in Polish with English summary). Przegląd Geologiczny, 57: 669-673. Lin, A., 1999. S-C cataclasite in granitic rock. Tectonophysics, 304: 257-273. Lin, A., 2001. S-C fabrics developed in cataclastic rocks from the Nojima fault zone, Japan and their implications for tectonic his- tory. Journal of Structural Geology, 23: 1167-1178. Lister, G., Snoke, A., 1984. S-CMylonites. Journal of Structural Ge- ology, 6: 617-638. Mahel’, M., 1986. Geologickä stavba ceskoslovenskych Karpät/Paleoalpinske jednotky 1 (in Czech). VEDA, Bratislava. Maluski, H., Rajlich, P., Matte, P., 1993. 40Ar-39Ar dating of the Inner Carpathians Variscan basement and Alpine mylonitic overprint- ing. Tectonophysics, 22: 313-337. Michalik, A., Guzik, K.,1959. Szczegółowa Mapa Geologiczna Tatr, 1:10 000, arkusz C1, Wołowiec (in Polish). Wyd. Geol., Warszawa. Minaer, J., Bielik, M., Kovaec, M., Plasienka, D., Barka, I., Stankoviansky, M., Zeyen, H., 2011. New morphostructural subdivision of the Western Carpathians: an approach integrat- ing geodynamics into targeted morphometric analysis. Tectonophysics, 502: 158-174. Nemcok, J., Bezak, V., Biely, A., Gorek, A., Halouzka, R., Janak, M., Kahan, S., Kotański, Z., Lefeld, J., Mello, J., Reichwalder, P., Rączkowski, W., Roniewicz, P., Ryka, W., Wieczorek, J., Zelman, J., 1994. The geo I ogl cal map of the Tatra Mountains 1:50 000. Stätny geologicky ustav Dionyza Stura, Bratislava. Passchier, C., Trouw, R., 2005. Microtectonics. Springer 2nd, re- vised and en larged edition. Petit, J., 1987. Criteria on the sense of movement on fault surfaces in brittle rocks. Journal of Structural Geology, 9: 597-608. Piotrowska, K., 2009. Wykaz jednostek strukturalnych Tatr. In: LXXIX Zjazd Polskiego Towarzystwa Geologicznego “Budowa geologiczna Tatr i Podhala ze szczególnym uwzględnieniem zjawisk geotermalnych na Podhalu”, Bukowina Tatrzańska, 26-29 września 2009, materiały konferencyjne: 27-28. Piotrowska, K., Cymerman, Z., Rączkowski, W., Bac-Moszaszwili, M., 2007. Szczegółowa Mapa Geologiczna Tatr 1:10 000, arkusz Góra Rakoń (in Polish). CAG PIG, Warszawa. Plasienka, D., 1995. Passive and active margin history of the north- ern Tatricum (Western Carpathians, Slovakia). Geologische Rundschau, 84: 748-760. Plasienka, D., 2003. Development of basement-involved fold thrust structures exemplified by the Tatric-Fatric-Veporic nappe syst tem of the Western Carpathians (Slovakia). Geodinamica Acta, 16: 21-38. Poller, U., Todt, W., 2000. U-Pb single zircon data of granitoids from the High Tatra Mountains (Slovakia): implications for the geodynamic evolution. Transactions of the Royal Society of Ed- inburgh Earth Sciences, 91: 235-243. Poller, U., Janak, M., Kohut, M., Todt, W., 2000. Early Variscan magmatism in the Western Carpathians: U-Pb zircon data from Microstructures of shear zones from selected domains of the Western Tatra Mountains 699 granitoids and orthogneisses of the Tatra Mountains (Slovakia). International Journal of Earth Sciences, 89: 336-349. Ramsay, J.G., 1980. Shear zone geometry: A review. Journal of Structural Geology, 2: 83-99. Roduit, N., 2001. JMicroVision: un logiciel d'analyse d'images pétrographiques polyvalent (in French with Engl ish summary). Unpublished Ph.D. thesis, Université de Geneve. Sibson, R., 1911. Fault rocks and fault mechanisms. Journal of the Geological Society, 133: 191-213. Simpson, C,. Schmid, S., 1983. An evaluation of criteria to deduce the sense of movement in sheared rocks. GSA Buli etin, 94: 1281-1288. Skupiński, A., 1915. Petrogenezis and structure of the crystali ine core between Ornak and Rohacze, Western Tatra Mts. (in Polish with English summary). Studia Geologica Polonica, 49: 1-1G5. Stahr, D., Law, R., 2014. Strain memory of 2D and 3D rigid inclusion popul at ions in viscous flows — What is clast SPO telli ng us?. Journal of Structural Geology, 68: 347-363. Trouw, R., Passchier, C., Wiersma, D., 2010. Atlas of Mylonites and Related Microstructures. Springer-Verlag, Berlin. Uchman, A., 2009. Stratygrafia i sedymentologia utworów mezozoiku Tatr i Podhala (in Polish). In: LXXIX Zjazd Polskiego Towarzystwa Geologicznego “Budowa geologiczna Tatr i Podhala ze szczególnym uwzględnieniem zjawisk geotermalnych na Podhalu”, Bukowina Tatrzańska, 26-29 września 2009, materiały konferencyjne: 9-26. Uhlig, V., 1897. Die Geologie des Tatragebirges. I: Einleitung und stratigraphischer Teil. Denkschrifte der Akademie derf Wissenschaften in Wien, Matematisch-Naturwissenschaftliche Klasse, 64: 643-684. White, S., 2001. Textural and microstructural evidence for semi-brit- tle flow in natural flow rocks with varied mica contents. Interna- tional Journal of Earth Sciences, 90:14-27. Williams, M., Melis, E., Kopf, C., Hanmer, S., 2000. Microstructural tectonometamorphic processes and the development of gneissic layering: a mechanism for metamorphic segregation. Journal of Metamorphic Geology,18: 41-57. Woodcock, N., Mort, K, 2008. Classification of fault breccias and related fault rocks. Geological Magazine, 145: 435-440. Żelaźniewicz, A., 1996. Mylonites in crystali ine basement of the Polish Western Tatra Mts. Polskie Towarzystwo Mineralogiczne. Prace Specjalne, 7: 23-26.