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Fig. 1. Location of (A) the Tatra Mts. within the Carpathians and (B) the study area in the Tatra Mts. The Western Tatra Mts. are mainly composed of crystalline rocks of the Paleozoic age (State Geological Institute of Dionyz Stir, 2013). Most of the mountain range consists of igneous rocks (granitoids), but the southern and northern parts are built of metamorphic rocks (mica schists, gneisses). In the outer areas of the mountain range, especially in the north, the crystalline rocks are overlain by Mesozoic sedimentary rocks (limestones, sand- stones) (State Geological Institute of Dionyz Sttir, 2013; Kralikova et al., 2014). The Western Tatra Mts. are bounded in the south by the sub-Tatra fault, along which the southern crests were uplifted to slightly higher elevations than the northern ones. The largest uplift accelerated from the end of the Late Miocene to the Pleisto- cene (Baumgart-Kotarba and Kral, 2002; Kralikova et al., 2014; Jacko et al., 2021; Vitovic et al., 2021) and has continued into the postglacial period as documented by post-LGM fault scarps (Panek et al., 2020). The Western Tatra Mts. are ~300 m lower compared to the High Tatra Mts., which is due to the asymmetrical rise of the However, dating of rock glaciers in some other European re- gions, such as the Tatra Mts., Western Carpathians, has been limited. The age of rock glaciers in the Tatra Mts. was initially deduced based on paleoclimatic considerations and relative dating methods. Kotarba (1992) claimed based on paleoclimatic re- constructions that rock glaciers in the Tatra Mts. formed during the Greenland Stadial 1 (GS-1) (~Younger Dryas). Several authors extended the age span of rock glaciers in the Tatra Mts. using the

Figure 1 Location of (A) the Tatra Mts. within the Carpathians and (B) the study area in the Tatra Mts. The Western Tatra Mts. are mainly composed of crystalline rocks of the Paleozoic age (State Geological Institute of Dionyz Stir, 2013). Most of the mountain range consists of igneous rocks (granitoids), but the southern and northern parts are built of metamorphic rocks (mica schists, gneisses). In the outer areas of the mountain range, especially in the north, the crystalline rocks are overlain by Mesozoic sedimentary rocks (limestones, sand- stones) (State Geological Institute of Dionyz Sttir, 2013; Kralikova et al., 2014). The Western Tatra Mts. are bounded in the south by the sub-Tatra fault, along which the southern crests were uplifted to slightly higher elevations than the northern ones. The largest uplift accelerated from the end of the Late Miocene to the Pleisto- cene (Baumgart-Kotarba and Kral, 2002; Kralikova et al., 2014; Jacko et al., 2021; Vitovic et al., 2021) and has continued into the postglacial period as documented by post-LGM fault scarps (Panek et al., 2020). The Western Tatra Mts. are ~300 m lower compared to the High Tatra Mts., which is due to the asymmetrical rise of the However, dating of rock glaciers in some other European re- gions, such as the Tatra Mts., Western Carpathians, has been limited. The age of rock glaciers in the Tatra Mts. was initially deduced based on paleoclimatic considerations and relative dating methods. Kotarba (1992) claimed based on paleoclimatic re- constructions that rock glaciers in the Tatra Mts. formed during the Greenland Stadial 1 (GS-1) (~Younger Dryas). Several authors extended the age span of rock glaciers in the Tatra Mts. using the

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Fig. 2. Rock glaciers selected for exposure dating in the Spalena (A) upper, (B) middle, and (C) lower valley; (D) Smutna valley; (E) Roha¢ska valley; (F) Ziarska valley; Jamnicka (( north and (H) south valley. The location of the centroids of the rock glaciers is given in Table 1.
Fig. 2. Rock glaciers selected for exposure dating in the Spalena (A) upper, (B) middle, and (C) lower valley; (D) Smutna valley; (E) Roha¢ska valley; (F) Ziarska valley; Jamnicka (( north and (H) south valley. The location of the centroids of the rock glaciers is given in Table 1.
Morphometric and climate characteristics of the dated rock glaciers in the Western Tatra Mts. Table 1
Morphometric and climate characteristics of the dated rock glaciers in the Western Tatra Mts. Table 1
10Be surface exposure ages for the samples collected at the rock glaciers in the Western Tatra Mts. Samples with outlier exposure ages are shown in italic: Table 2
10Be surface exposure ages for the samples collected at the rock glaciers in the Western Tatra Mts. Samples with outlier exposure ages are shown in italic: Table 2
10Be surface exposure ages for the sampled rock glaciers in the Western Tatra Mts. The location of the rock glacier centroids and individual samples is given in Tables 1 and 2 respectively. * The degree of scatter in ages according to the method of Blomdin et al. (2016).
10Be surface exposure ages for the sampled rock glaciers in the Western Tatra Mts. The location of the rock glacier centroids and individual samples is given in Tables 1 and 2 respectively. * The degree of scatter in ages according to the method of Blomdin et al. (2016).
Fig. 3. '°Be exposure ages for the sampled boulders and weighted mean exposure ages (bold) for the dated rock glaciers in the Western Tatra Mts. Italics indicates exposure age removed from the dataset based on the ? test. Asterisks represent dates published by Engel et al. (2017). Geomorphological features follow Ktapyta (2015). The location of th centroids of the dated rock glaciers and individual samples is given in Tables 1 and 2, respectively.
Fig. 3. '°Be exposure ages for the sampled boulders and weighted mean exposure ages (bold) for the dated rock glaciers in the Western Tatra Mts. Italics indicates exposure age removed from the dataset based on the ? test. Asterisks represent dates published by Engel et al. (2017). Geomorphological features follow Ktapyta (2015). The location of th centroids of the dated rock glaciers and individual samples is given in Tables 1 and 2, respectively.
Fig. 5. Timing of rock glaciers and other paleopermafrost features around the Tatra Mts. Exposure ages for rock glaciers after Engel et al. (2017), Zasadni et al. (2020), and this study. Cryogenic cave carbonates (Zak et al., 2012; OrvoSova et al., 2014), rock slope failures (Panek et al., 2016), frost wedges (Kovacs et al., 2007; Fiedorczuk et al., 2007; Fabian et al., 2014; Ewertowski et al., 2017; Farkas et al., 2023), pingo scar (HoSek et al., 2020), and thermokarst features (Blaszkiewicz, 2011; Btaszkiewicz et al., 2015; Hosek et al., 2019) constrain the timing of permafrost occurrence or permafrost degradation. The weighted mean ages and weighted mean standard deviations for individual locations are reported. Vertical bars show the elevation of rock glacier fronts, entrance of caves, and the lowest detachment zone for rock slope failures. The temperature offset (grey dashed line) relative to the present (Kindler et al., 2014), 8'80 data (grey solid line), and INTIMATE event stratigraphy (Rasmussen et al., 2014) are derived from the NGRIP ice core on the GICCO5modelext time scale. Fig. 4. Timing of rock glacier stabilization in the Western Tatra Mts. The probability density plot (purple shading) and Kernel Density Estimation (in cyan) of '°Be exposure age (n = 40) obtained in this study and reported for rock glaciers in the Roha¢ska and Salatinska valleys by Engel et al. (2017). Vertical lines indicate mean ages with proportions for th modelled peaks and open circles show individual exposure ages (Vermeesch, 2012).
Fig. 5. Timing of rock glaciers and other paleopermafrost features around the Tatra Mts. Exposure ages for rock glaciers after Engel et al. (2017), Zasadni et al. (2020), and this study. Cryogenic cave carbonates (Zak et al., 2012; OrvoSova et al., 2014), rock slope failures (Panek et al., 2016), frost wedges (Kovacs et al., 2007; Fiedorczuk et al., 2007; Fabian et al., 2014; Ewertowski et al., 2017; Farkas et al., 2023), pingo scar (HoSek et al., 2020), and thermokarst features (Blaszkiewicz, 2011; Btaszkiewicz et al., 2015; Hosek et al., 2019) constrain the timing of permafrost occurrence or permafrost degradation. The weighted mean ages and weighted mean standard deviations for individual locations are reported. Vertical bars show the elevation of rock glacier fronts, entrance of caves, and the lowest detachment zone for rock slope failures. The temperature offset (grey dashed line) relative to the present (Kindler et al., 2014), 8'80 data (grey solid line), and INTIMATE event stratigraphy (Rasmussen et al., 2014) are derived from the NGRIP ice core on the GICCO5modelext time scale. Fig. 4. Timing of rock glacier stabilization in the Western Tatra Mts. The probability density plot (purple shading) and Kernel Density Estimation (in cyan) of '°Be exposure age (n = 40) obtained in this study and reported for rock glaciers in the Roha¢ska and Salatinska valleys by Engel et al. (2017). Vertical lines indicate mean ages with proportions for th modelled peaks and open circles show individual exposure ages (Vermeesch, 2012).
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Rock GlacierTatra Mountains
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