Landform Analysis, Vol. 10: 50–57 (2009)

Glacial and periglacial relief on the southern slopesof the Western Tatra Mts. (Slovakia) – the results

of the first detailed geomorphological mapping of the Žiarska,Jamnicka, Raèkova and Bystra Valleys

Piotr K³apyta*

Jagiellonian University, Institute of Geography and Spatial Management, Gronostajowa 7, 30-387 Kraków, Poland

Abstract: The article presents the results of the first detailed geomorphological mapping of the Žiarska, Jamnicka,Raèkova, and Bystra Valleys, situated on the southern slope of the Western Tatra Mountains. The field work was supple-mented by digital topographic as well as statistical analysis of rock glaciers distribution. The author focused on the distribu-tion and morphological features of moraines and rock glaciers. Variability of both sets of deposits strongly reflects topo-graphic influences on debris and snow accumulation. The main factor controlling the geometry of landforms was solarirradiance modified by the influence of the local cirque topography. Two generations of the rock glaciers indicate distinctphases of periglacial conditions during the Late Glacial period.

Key words: deglaciation, moraine systems, relict rock glaciers, morphostratigraphy, Western Tatra Mts.

Introduction

The morphology of many currently deglaciatedalpine massifs was strongly transformed during theLate Glacial period by the activity of both glacial andperiglacial conditions. The Late Glacial evolution ofthe alpine type mountains is currently an importantissue in many palaeogeographical and palaeoenvi-ronmental studies (Ivy-Ochs et al., 2006; Lotter et al.,2006; Reutcher et al., 2007). They provide informa-tion about the conditions and type of deglaciation,the activity of periglacial processes and are an indi-rect source of information about both regional andlocal climate fluctuations. The Tatra glacial andperiglacial landforms are still major features of val-ley and cirque floors relief in spite of partial fossiliza-tion by Holocene slope activity. Despite the long pe-riod of investigations, most geomorphological andpalaeogeographical studies were carried out in theHigh Tatra Mts. (Lukniš, 1973; Klimaszewski, 1988;Baumgart-Kotarba & Kotarba, 1997, 2001). Hence,there is much better understanding of local land-forms and their geochronology in this area when

compared to the Western Tatra Mts. The earliestcomments on glacial morphology of the southernslopes of the Western Tatras date back to the worksof Lucerna (1908), who described the moraines ofthe maximal extent and the system of the glacialtroughs in the area between Jalovecka and Kame-nista valleys. He distinguished traces of four glacia-tions and the recessional moraines of the last glaci-ation, denominated them according to the Alpineterminology of Penck and Brückner (1901–1909). Inthe study of Szaflarski (1937), on the southern slope,the author distinguished three sets of recessionalmoraines. In his opinion, the longest ice preservationon the southern slope of the Western Tatra Mts. wasin the highest parts of Bystra (Suchy Zadok cirque)and Žiarska valleys. Unfortunately, these two worksare lacking in comparative cartographical materials,which make field identification of selected land-forms impossible. Apart from the limnological stud-ies of Jamnicke and Bystre Plesa lakes, Młodzie-jowski (1937) as the first provided a simplified sketchmap of the Bystra Valley cirques relief. The most dis-tinctive moraine ridges were marked by the

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* e-mail: woytastry@gmail.com

above-mentioned researcher in front of the SuchyZadok and Bystre Plesa lakes cirques.

Lukniš (1964), based on the previous moraineclassifications, compared the moraine sequence tohis glacial scheme of the High Tatra Mts. The outerand inner moraines of maximal extent were com-pared with C and D stadial oscillations. Relict rockglaciers were first identified by Nemèok & Mahr(1974); however, in the study area they marked only3 rock glaciers: one in the Rohacki cirque and two inthe cirques of the Bystra Valley. According to theiropinion, the formation of rock glaciers in the Tatrasstarted after the complete deglaciation in theperiglacial conditions during transitional period be-tween full glacial-Holocene climates.

In 1987, Halouzka mapped Quaternary sedi-ments of the whole Slovak part of the WesternTatras. Unfortunately, these materials are mostlyunpublished, preventing spatial comparison. In hissubsequent morphostratigraphic scheme, Halouzka(1989) divided moraines which postdate the maximalextent into 3 retreat phases (valley phases) and 3 or 4final (cirque) phases, the last two of which wereformed by the nèvè glaciers (rock glaciers?). Thisscheme strictly corresponds to the morpho-climaticdivision of Lukniš (1973). All geological materials ofHalouzka (1987) were compiled on the GeologicalMap of the Tatra Mountains 1:50,000 (Nemèok et al.,1993), but moraine locations are marked in a veryschematic and imprecise way, hindering their spatialinterpretation.

Till the present study, neither a detailed geomor-phological map, nor an authoritative morphostrati-graphic scheme of deglaciation for particular valleysystems has existed for the southern slope of theWestern Tatras. Especially the last period of gla-cial-periglacial activity is poorly recognized, despiteits clear imprint on the morphology of the cirques.

Study area

The study area comprises three valley systems:Jamnicka, Raèkova, Bystra and the uppermost sec-tion of Žiarska, which are situated in the SlovakWestern Tatra Mountains in their highest, centralpart (Fig. 1). The area is bordered from the north bythe main Tatra ridge ranging from Mt. Banikov(2,178 m a.s.l.) to Mt. Blyšt (2,155 m a.s.l.). From thesouth, it is bordered by the young, Neogene Subtatricfault, along which the Tatra massif had been highlyrotationally uplifted above the Palaeogene flysch ofthe Liptov intermountain basin (Janak, 1994). Thestudy area is built of crystalline and metamorphicrocks, mainly by granites, mica-schists, para- andorthogneisses and migmatites, which belong to theTatricum-type crystalline basement (Janak, 1994).The highest summits rise above 2,150 m a.s.l. (Bystra

2,250 m a.s.l., Jakubina 2,194 m a.s.l.), and are ca. 400m lower than in the High Tatras (Lukniš, 1964). Theglacial cirques lay at an altitude of about 1,700–1,850m a.s.l. (Halouzka, 1987) and comprise well devel-oped glacial and periglacial landforms. Asymmetri-cal uplift of the southern part of the Tatra massifcaused an intensive linear and backward erosionalong with the partial rejuvenation, which led to theformation of deep and steep valley profiles in themiddle and lower valley sections. The valleys of thisrange are more deeply incised than those in the HighTatras, whereas relatively large non rejuvenated sur-faces were preserved in the uppermost sections ofthe valleys (especially in the Bystra, Gaborova,Žiarska and Kamienista valleys ).

Materials and methods

Detailed geomorphological mapping at the scaleof 1:10,000 was performed to obtain informationabout glacial and periglacial landform distribution.Additionally, 1:5,000 mapping was applied to distin-guish complicated sets of moraines and rock glaciersin the glacial cirques, which point to complex pat-terns of deglaciation. Rock glaciers were identifiedon the basis of the occurrence of typical morphologi-cal indicators (frontal slope, ridge-and-furrow relief,orientation of longitudinal axis of boulders). Withinthe rock glaciers’ frontal slopes, core zones altitudes,longitudinal axis orientations and aspects were mea-sured. The fieldwork was supplemented by opticalremote sensing, including 1-m Ikonos images and0.75-m colour orthophotomap of the Tatra Mts.

Statistical analysis of K-means clustering was ap-plied to identify the altitude distribution of the relictrock glaciers fronts, with the help of the R Project forstatistical computing software. A total number of 39measurements of rock glacier fronts elevation werearranged increasingly and tested for possible aggre-gations, which would suggest occurrence of differentrock glacier generations.

Glacial morphology of the Žiarska, Jamnicka,Raèkova and Bystra valleys

Glaciers of the Last Glaciation in the WesternTatra Mountains had a considerable extent (Fig. 1).The largest glacial system was formed in the Jam-nicka Valley. The highly asymmetrical glacier systemwas nourished mostly from the western slopes by theice from seven firn-basins: Jamnicke Plesa Lakes,Jakubina, Rohacki, Smrek, Puste, Maselne and Re-pa cirques. The glaciers terminated at an altitude ofca. 1,000 m a.s.l., but frontal moraines have not beenpreserved and granite-derived accumulation coverdeposited on bedrock built by mica-schists marks themaximal glacial position. Terminal moraines have

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Glacial and periglacial relief on the southern slopes of the Western Tatra Mts. (Slovakia)...

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Piotr K³apyta

Fig. 1. Map of the Western Tatra Mts. landforms within the Jamnicka, Rackova and Bystra valleys, according to the author.Morphosystems mentioned in the text: J-max – maximal moraines in the Jamnicka Valley, R-max - maximal moraines inthe Raèkova Valley, B-max – maximal moraines in the Bystra Valley, J-1 - first morphosystem in the Jamnicka Valley, J-2 –second morphosystem in the Jamnicka Valley, R-1 – first morphosystem in the Raèkova Valley, R-2 – secondmorphosystem in the Raèkova Valley, R-3 – third morphosystem in the Raèkova Valley, B-1 – first morphosystem in theBystra Valley, B-2 – second morphosystem in the Bystra Valley, R-3 – third morphosystem in the Bystra Valley.

1 – sharp rocky ridge crest, 2 – rounded ridge crest covered with debris and vegetation, 3 – asymmetrical ridge crest (steep rocky slopefrom one side and debris-vegetation one from the other), 4 – rounded summits covered with debris and vegetation, 5 – sharp rocky sum-mit, 6 – passes, 7 – rocky slopes and rockwalls, 8 – block slopes with debris covers, 9 – chutes cut in solid rock, 10 – debris flow gullies,levees cut in debris covers, 11 – stream channels, 12 – lakes, 13 – fluvioglacial cones, 14 – landslide niche, 15 – system of fissures, 16 –landslide packets, 17 – colluvia, 18 – rock-slide niche, 19 – rockfall talus slope-rock slide tongue, 20 – glacial cirques, 21 – glacial troughs,22 – moraine ridges; a – moraines of maximal glacial extent, b – moraines of recessional stages, 23 – poorly exposed moraine ridges 24 –massive fronts of moraines of distinct glacial readvance, 25 – ablation moraine covers, 26 – ground moraine covers, 27 – relict rock gla-ciers, 28 – south Tatra boundary, 29 – rock steps, 30 – dips of metamorphic schist complexThe codes of rock glaciers listed in Table 1 are marked on the map.

been deposited within narrow, steep valley sectionand thus were rewashed by postglacial fluvial erosionand covered by slope deposits. In the Raèkova Val-ley, glacier snout terminated at 1,050 m a.s.l. Thisterminal position is marked as the lower edge of thelarge granite boulder accumulation. Massive lateralmoraines mark the maximal glacier tongue extent upto the Ostrica meadow. Ice from the two maincirques: Zadna Raèkova and Gaborova Valley aswell as from two tributaries from the west cirques:Wyżna Kotlina and Jakubina fed the valley glacier ofRaèkova Valley.

In the Bystra Valley (Fig. 1), the glacier had its ac-cumulation area in three highly-elevated firn basinsof Suchy Zadok, Bytre Plesa Lakes, and a smaller ba-sin located under the Jezova. High elevation ofcirque bottoms resulted in large alimentation sur-face and considerable extent of the Bystra glacier.

In the Jamnicka and Raèkova valleys, morainesof the maximal glacial extent were deposited withinthe Tatra massif and did not extend into the fore-land. There is no geomorphological evidence forconfluence during the last glaciation either, as sug-gested in the literature (Lucerna, 1907; Szaflarski,1937; Lukniš, 1964; Nemèok, 1993; Halouzka, 1987).Only in the Bystra Valley the glacier tongue in itsmaximal extent did reach the neighborhood of theTatra foreland, what is marked by the prominent (1km long) right lateral moraine ridge in the mouth ofthe valley (Fig. 1).

The first system of recessional moraines wasformed in the upper valley position in the Bystra(B-1, 1,350 m a.s.l.) and Rackova Valley (R-1, e.g.Polana Pod Klinom 1,430–1,450 m a.s.l.), whereas inthe Jamnicka Valley they were preserved under themouth of the cirques (J-1, Fig. 1). They representmassive, subdued ridges and locally (Puste cirque,Rohacki cirque) ablation moraine covers indicatethat some glacier termini were debris-covered.

The next morphosystem (J-2, R-2, B-2, Fig. 2), in-dicates an outstanding readvance, marked by thesimilar pattern of massive, debris morainic ridgeswith numerous dead ice depressions in the terminalpart of former glacier tongues. The 20–30 m high,steep moraine ridges mark the onset of thedeglaciation dominated by heavy debris input, wellimprinted in the cirque relief. This morphologicalsystem was formed as a continuum of landforms,from debris-covered terminus, through debris cov-ered glaciers, to valley floor rock glaciers (ice-coredrock glaciers). Such relief is particularly well devel-oped in the cirques of Žiarska Valley (WelkeZawraty, Fig. 2; Zr-1 rock glacier) and suggests thatglacier-derived rock glaciers have also developedduring this period. The best-developed regular pat-tern of glacial-periglacial landforms is recorded inthe Bystra Valley cirques (B-2, Fig. 1). The morphol-ogy of this valley consists of highly elevated, non-re-

juvenated valley bottom, and twin cirques of similaraspect and altitudes, with cirque head-wall relief. Al-together, they provide a unique opportunity for dis-tinguishing landform arrangement connected withice decay. Topographical and structural factors ledto the long preservation of the glacial ice. In addi-tion, thick debris cover protected the ice core frommelting, which was intensified by heavy solarirradiance at the southern cirque aspect. Climate-in-duced individual glacial fluctuations are clearly im-printed in the morainic arrangement. On the proxi-mal side of the readvance moraine ridges, tworecessional moraines of minor sub-oscillations oc-cur. They constitute distinct morainic ridges in theinner part of debris-covered zone, which could haveoriginated as a result of the successive remobili-zation of ice cores in the following stadials. Their ge-ometry has been characterised by the decreasingwidth against similar length and topographical clus-tering under the shaded rock walls and rocky slopes.The pattern described above is very well imprinted inthe Suchy Zadok and Bystre Plesa lakes cirques (Fig.1). On the proximal side of these moraines, largedead ice depressions have been formed. In theBystra Valley they are filled with waters of VelkeBystre Pleso and Anitine Oèko Lakes (Fig. 1).

Within the Jamnicka and Raèkova drainage bas-ins, a deeply incised, narrow valley system with rela-tively small cirques prevails. Such topography causedan earlier rise of local glaciers equilibrium linesabove the cirque bottoms; thus, the sequence of gla-cial landforms is incomplete, lacking in the youngestdebris landforms in comparison with the spaciouscorries of the Bystra or Žiarska valleys.

The third morphosystem consists of relict rockglaciers, which appear in the highest part of BanikovRaèkova and Bystra valley cirques (R-3, B-3; Fig. 1).They are in considerable spatial separation from thepreviously described landforms. They are very prom-inent, massive and relatively freshly shaped struc-tures, located below rock walls in the shaded parts ofthe cirques (Figs. 1–2).

Glacial and periglacial landform assemblage onthe southern slopes of the Western Tatras stands outclearly from the moraine sequences on the northernslopes (Klimaszewski, 1988; Kaszowski et al., 1988).Variability of both sets of deposits reflects strongtopographic influences on debris and snow accumu-lation, which is apparent from their geometry. Thecirque moraine sequences occupied the most favour-able zones for ice preservation; thus they are concen-trated in the lateral zones of the corries, near therock walls (Žiarska Valley cirques, Rohacki cirque).The central parts of the glaciers were dominated byice and mostly unprotected from ablation by insulat-ing debris cover. The central sun-drenched part ofthe cirques was ice-free and the moraines were de-posited much higher, in the inner corrie zone. The

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Glacial and periglacial relief on the southern slopes of the Western Tatra Mts. (Slovakia)...

spatial variability of debris accumulation zone of theformer glacier surface was preserved in the relief ofBanikov cirque, where thick zone of ablation mo-raine cover concentrates on the cirque sides,whereas its central part is debris-free.

The main factor controlling the geometry of gla-cial and periglacial landforms was solar irradiancemodified by the influence of the local topoclimatevariables (shading, snow and debris production). Acommon situation in the studied cirques was that gla-cial body split into the two lateral minor debris-cov-ered tongues, which were protected from insolationby the shade and debris may have reached a consid-erable distance down the cirques. Such a specific ge-ometry of glacial forms was also identified on thesouthern slope of the High Tatras in the valleys ofKrivan massif (Ksandr, 1954; Za�ko, 1961).

Distribution of relict rock glaciers

Rock glaciers are morphological indicators ofperiglacial conditions in the mountains; their occur-rence is controlled primarily by climatic, topographicand geological factors (Barsch, 1996), thereby theirposition could be spatially diversified. Basing on airphotos interpretation, Nemèok & Mahr (1974) iden-tified numerous relict rock glacier-like structures inthe Western Tatra Mts., mostly on the northernslope, in the shaded cirques of Zuberska Valley. Thecurrent field work allows the author to identify sev-eral new relict rock glaciers on the southern slope ofthe Tatras, whose location is numbered on thegeomorphological map (Figs. 1–2) and described inTable 1. Most of the identified landforms are initialand small debris bodies, which in 75% are talus-de-

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Piotr K³apyta

Fig. 2. Geomorphological map of the uppermost section of the Žiarska Valley, Western Tatra Mts., according to the author.1 – sharp rocky ridge crest, 2 – rounded ridge crest covered with debris and vegetation, 3 – asymmetrical ridge crest (steep rocky slopefrom one side and debris-vegetation one from the other), 4 – summits, 5 – passes, 6 – rocky slopes and rockwalls, 7 – Richter denudationslope, stabilized by vegetation, 8 – rock steps, 9 – chutes, debris flow gullies, levees cut in debris covers, 11 – stream channels, 11 – rock-fall gravity sorted talus cone, 12 – rockfall gravity sorted talus slope, 13 – alluvial talus slope, 14 – rockfall talus slope-rock slide tongue,15 – alluvial slope, 16 – glacial cirques, 17 – moraine ridges, 18 – massive fronts of moraines of distinct glacial readvance, 19 – poorlyexposed moraine ridges, 20 – ablation moraine covers 21 – ground moraine covers, 22 – rock valley bottom covered by weathered di-scontinuous moraine covers 23 – relict rock glaciers. The codes of rock glaciers listed in Table 1 are marked on the map.

rived, lobate forms, located under rocky slopes androckwalls. Some rock glacier tongues (e.g. Zr-1,Zr-10, Zr-11, Zr-13 in the Žiarska Valley) developedin the cirques with clear spatial and morphologicalconnection with the moraines, what suggests boththeir glacial and periglacial origin.

They were formed beneath small cirque glaciers,which retreated into cirques and became buried ow-ing to high debris supply resulting from the

frost-shattering of the surrounding rockwalls (seeJohnson, 1980, 1987; Benn & Evans, 1998).

Many relict rock glacier surfaces collapsed, butstill retain much of their microrelief: longitudinal,arcuate and transverse ridges and furrows. Steepfrontal slopes are still well developed and preservedas a distinct parabolic ramp, which resembles mas-sive moraine ridges but retain debris accumulationbody on the proximal side. Rock glacier orientationis strongly diversified, over half of the total rock gla-

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Glacial and periglacial relief on the southern slopes of the Western Tatra Mts. (Slovakia)...

Table 1. Distribution and basic morphological characteristic of relict rock glaciers in the study area (according to author).Rock glaciers location depicted in figures 1 and 2

Rockglaciercode

LocalizationFront

elevation(m a.s.l.)

Debrissource Aspect Morphology, shape Other features

Raèkowa Valley

Rc 1 Gaborova valley 1,690 moraine SW tongue shaped distinct fronal ramp, collapsedsurface

Rc 2 Gaborova valley 1,650 talus W lobe with initialtongue

colapsed internal surface

Rc 3 Zadnia Gaborova 1,860 talus E lobate initial, discordant to themoraine cover

Rc 4 slope of Rackova valley 1,470 talus SE lobe with initialtongue

welll developed ridges andfurrows

Rc 5 Zadnia Rackova cirque 1,815 talus NE lobate initial, partly fossilized bydebris flows

Rc 6 Zadnia Rackova cirque 1,815 talus NE tongue shaped initial, partly fossilized bydebris flows

Jamnicka Valley

Jm 1 Jamnickie Lakes cirque 1,736 talus S lobate welll developed ridges andfurrows

Jm 2 Jamnickie Lakes cirque 1,652 talus SW lobate distinct frontal ridge, very wide

Jm 3 Jamnickie Lakes cirque 1,625 talus NE, E lobate very wide, encircle the talusslope

Jm 4 Rohacki cirque 1,555 talus S lobate complex of 2 lobes generation

Jm 5 Rohacki cirque 1,640 talus NE lobate small, distinct frontal ridge

Jm 6 Rohacki cirque 1,765 moraine E tongue shaped distinct frontal ridge, largeboulders

Jm 6a Rohacki cirque 1,780 moraine/talus E lobate inside the debris mass of Jm 6form

Jm 7 Rohacki cirque 1,780 moraine E lobe with tongue discordant to the moraine

Jm 8 Puste cirque 1,650 talus/moraine NE lobate distinct frontal ridge, partlyfossilized

Jm 9 Repa cirque 1,630 talus NE lobate surface covered by dwarf-pine

Bystra Valley

Bs 1 slopes of Bystra valley 1,485 talus E lobate distinct frontal ridge, very wide

Bs 2 slopes of Bystra valley 1,474 talus SSW lobate surface covered by dwarf-pine

Bs 3 slopes of Bystra valley 1,510 talus SSW tongue shaped surface covered by dwarf-pine

Bs 4 slopes of Bystra valley 1,565 talus SSW lobate with tongue surface covered by dwarf-pine

cier number favouring SW (28%) and NE (23%) as-pects (Table 1). The lowest position of the fronts oftalus rock glaciers could be interpreted as the poten-tial zone of permafrost distribution (Haeberli, 1985).In the study area, relict rock glacier Rc-4 in theRaèkova Valley and the Bs-1, Bs-2, Bs-3 forms in theBystra Valley descended to 1,480–1,470 m a.s.l. (Fig.1, Table 1). Hence, the altitude of 1,470 m a.s.l.marks the potentially lowest boundary conditions forpermafrost creep.

Two morphosystems exist within the set of relictrock glaciers. Statistical methods were applied to de-termine altitude variability and potential clustering,which in connection with morphological relationssuggest several landform generations. Among the to-tal of 39 relict rock glaciers, K-means clusteringshows two aggregations. 15 lowest values of altitude(up to 1,690 m a.s.l.) clusters around the mean valueof 1,582.8 m a.s.l., and 24 highest values (above 1,720m a.s.l.) clusters around the mean value of 1,811.167m a.s.l. (Fig. 3). Two generations of rock glacierswere formed in the cirques of Bystra and Žiarska val-leys. In the remaining valleys, because of small sizeand narrow cirque bottoms, this spatial relation waspoorly developed. The first group of talus rock gla-ciers was formed on the slopes of massive debrismorainic ridges, which mark the prominent re-advance. In the Žiarska Valley, a clear morphologi-cal transition between massive moraine ridges andvalley-floor rock glacier body exists (Male andWelkie Zawraty cirques; Fig. 2). This is a classic ex-ample of glacial-periglacial landform continuum.The second group of rock glaciers marks the laststage of deglaciation (Fig. 1). Their position suggeststhat their formation was controlled by the presenceof rock walls and rocky slopes, which were the sourceof snow avalanches and provided shade. Statistical

analysis and morphological relations confirm thepresence of two generations of rock glaciers and in-dicate two distinct phases of periglacial conditionson the southern slopes of the Tatra Mts. during theLate Glacial.

Conclusions

The glacial and periglacial landforms of theWestern Tatras are indicators of palaeoen-vironmental changes controlled mainly by climate.Geomorphological mapping of the Žiarska, Jam-nicka, Raèkova, and Bystra valleys indicates the sig-nificant and well preserved glacial and periglaciallandform assemblage on the southern slopes of theWestern Tatra massif. Apart from the maximalWürm moraines, three sets of landform systemswere distinguished. The second of them points to theprominent readvance of debris-covered glaciers,marked by the 20–30 m high, steep moraine ridges.The last two stages of the Würm glaciation werefixed in the Western Tatras relief as the continuumof talus and glacial-derived landforms: moraineridges, ablation moraines, and rock glaciers. Clearmorphological coincidence of such features, like mo-raines and rock glaciers suggest also their temporalcoexistence. The variability of both sets of depositsreflects strong topographic control on the debris andsnow accumulation; particularly, landform geometrywas heavily reliant on the topoclimatic conditions,which determined the style of deglaciation. Morpho-logical and statistical relations indicate two distinctphases of periglacial conditions linked with rock gla-ciers formation. The third, rock glacier-dominant,morphosystem suggests pure periglacial conditionsduring the ice decay. Because of clear morphologicalrelations, the study area is particularly suitable forfurther study of the morphology and morpho-chronology of the Last Glaciation in the Tatra Mts.

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Glacial and periglacial relief on the southern slopes of the Western Tatra Mts. (Slovakia)...