General Aspects of Denudation Chronology of the West Carpathians

S T U D I A G E O M O R P H O L O G I C A C ^ R P ^ T H O -B A L C A N I C A

VOL. XXxvllI KRAKÓW 2004 PL ISSN 008l-6434

L A N D F O R M E V O L U T I O N I N M O U N T A I N A R E A S

JOZEF MINAR, MARIA BIZUB0VA, MICHAL GALIAY (BRATISLAVA)

GENERAL ASPECTS OF DENUDATION CHRONOLOGY OF THE WEST CARPATHIANS

Abstract. We outline relevant methodical approaches for the revision of the West Carpathian denudation chronology. They are based on ihe exploiiation of a new geoiectonical reconstruction or Neogene evolution of the Carpathians, absolule dating methods, complex geomorphological research, quanŁiri- cation and modelling, which resul(ed in the creation of geomorpho]ogica] informa(ion system. [( is methodologicalv important to distinguish between local and regional denudation chrono]ogy too. The general character of the West Carpathian denudation chronology is determined by tectonic and climatic conditions, which are homogenous in the maiority or the West Carpathians ror a relevant iime period. This homogeneity has, as a rule, a characteristic [rend in space and time. The period of extensional tectonics in Badenian-Pannonian (Kovó ć 2000) is ihe example, wilh which we connect (he creation of lhe polygene(ic initial flat surface of Lhe majority of the ciirrenl relief -the Midmou- ntain level. Tectonic subsidence is generally a key factor ror the explanation of planation in tectonic- albł aciive regions. We consider ihe W-E and S-N shifting of the denudation phases in the West Car- pa(hians Lo be in harmony with ihis geotectonic influence. The existence of three generalions of Neogene planation surfaces is documented at two loca- (ions in the wesi and centra] Slovakia. The contribution (o the iden(irication and dating or recent tectonic movements (site Devfnska Kobyla - Bratislava) and to the dating of lhe youngest West Carpal- hian volcanism (site Putikov Vfśok near town Novó Bańa) are shown in these examples too.

Key words: denudation chronology, geomorphological mapping, planation surface, geomorphological evolution, Wesi Carpathians

INTRODUCTI0N

Decreasing interest is devoted to denudation chronology in geomorphology. Development of methods of absolute dating rightfully focuses the attention of geomorphologists, however methods of relative dating of land surfaces (stratigraphy, denudation chronology) are still relevant (Watchman and Twidale 2002). Denudation chronology is an inherently geomorphological manner of dating. Spatial re]ationships among ]andforms have essentially simi]ar informational 6 power, as do relationships among rock layers. Nobody doubts the value of stratigraphy in geosciences, however denudation chronology does not have such high status. J. Wh i tt ow (1984) wrote: "Unless methods of absolute dating or pollen analysis are adopted, denudation chronology must remain a rather subjective and speculative exercise rather than a scientific study". Certainly, scientific denudation chronology must be linked with methods of rock dating. Knowledge of the ages of base rocks, regoliths or correlated deposits are necessary conditions for the scientific conceptualisation of denudation chronology. However, spatjal re]a- tionships of ]andforms (the basis of denudation chronology) give unique chrono- ]ogical information in connection with stratigraphy and absolute dating. The West Carpathians are an autonomic part of the Carpathian chain with specific geotectonic and morphological evolution. The solution of problems connected with the surfaces of p]anation and denudation chronology has a ]ong and rich tradition in the region (in detail see 8 i zub ovó 1993). In the first half of the 20Łł` century the concept of abrasion represented the first mains[ream of ideas re- lated to the genesis of the West Carpathian's planation surfaces. This concept represented the opinion that levels in mountains and in the intramountain basins of the West Carpathians are the remains of abrasion terraces of the oscillating Neo- gene sea. The main proponent was H. H a s s i n g e r (1914). His ideas were developed primarily by J. D a n e ś (1920), F. Vi t a s e k (1932), V. D ć d i n a (1922), and J. H ro m Ó d k a (1929). M, L u k n i ś (1964) admitted the existence of al)rasion levels on the westem slope of the Malć Karpaty Moun[ains too. Advocates of the second mainstream of ideas - denudation conception - assumed planation in the subaerial conditions as well as a big influence from neotectonics and changes of the base level. The first of them, L. S a w i c k i (1909) expressed the opinion of denudation genesis of levels of the Wes[ Carpathians. These ideas were developed by many authors; J. Smoleński (]9] 1), F. Ma- chatschek and M. Danzer (1924), J. Moschelesovó (1923), L. Dinev (1943), M. Klimaszewski (1934,1965), M. Liikniś (1962,1964), E. Mazur (1963,1965), T. Czudek et al. (1965), and L, Starkel (1965,1969). The scheme of denuda{ion chronology of the West Carpathians, which was for many years been the basis of studies of Slovak georelief, was presented in the 1960's by M. Lukniś and E. Mazńr. Though the authors published their result indi- vjdua]]y, a mutual influence was evident. They assumed simu]taneous evolution in the entire territory of the West Carpathians, but {hey had a different opinion on the age of the planation surfaces. M. L u k n i ś (1962,1964) considered two generation of planation surfaces - the o]der from the Sarmatian-Pannonian age and the younger from the Late P]iocene, as a pediment 70-150 m above present river valley bottom. M. Lukniś later shifts the age of the younger level to the Mindel-Riss integlacja] and considers the existence of older surfaces, exhumed from Pa- leogene sediments or volcanic rocks. E. M a z ń r ( 1963, 1965) considered the existence of a third generation of planation surfaces. The Top level, which was formed by processes of subaeric destruction after Styerian phases, is the oldest 7

(Tortonian and Early Sarmatian). The Midmountain level was placed in the Pa- nnonian. It is a supposed pediplane with large regional extent. The River level originated in the Late Pliocene and was formed by lateral river erosion as well as by parallel retreat of slopes. E. Mazńr's concept employed the correlation between levels, filling of the intramountain basins and phases of tectonic processes and was the basis for regional geomorphological research in Slovakia until of 1990,s. Eleven years ago, we introduced a new point of view on the planation surfaces question, on the basis of new geological and geomorphologic facts (Bi- zu b ovó and M i na r 1992). In comparison with E. M azńr (1963), we assumed longer formation of the Midmountain level and stressed the time-space dynamics of planation surfaces formation (W-E and S-N shift of principal stages in time) as well as an existence of more unfinished geomorphologic cycles, one from which results in the Undermidmountain level (Zat'ko et al. 1990) -likewise as M. Klimaszewski (1965) and L. Starkel (1965) recognised for the Polish Carpathians a long time ago. The mechanism of the formation and age of planation surfaces, their relationship to the geodynamic evolution of the West Carpathians and the question of simultaneity of the West Carpathian evolution has become a subject of discussion recently. W. Z u c h i ewi c z (1987) empha- sized the problems of defining the time and spatial characters of the surface planation in the Polish Carpathians. He mentioned asynchronous evolution of the West and East Carpathians. We have pointed out asynchronous evolution of georelief in the Outer and lnner West Carpathians (Bizubova 1998). J. Ćin- ć ura (1998) prefers the origin of planation surfaces before Neogene. J. Urbó- nek (2002) challenges the existence of a uniform initial surface of the West Carpathians (the Midmountain level). Criticism of the schematic approach to West Carpathians denudation chronology is well founded. Regional denudation chronology expresses the trend, which can be changed in space and time and deformed or fully masked by local factors. Smaller landforms are influenced predominantly by local factors, but within the framework of regiona] influences. Knowledge of the regional framework contributes to the solution of local denudation chronology problems, which are very important for detailed geoecological research, natural hazards and risk evaluation and estimation of ecological stability or carrying capacity. On the other hand the regional conceptions have to be conceived and confirmed on the basis of detailed local studies.

MATERIAL AND METHODS

The speculative character of denudation chronology is generally regarded as its biggest weakness. It is a consequence of limited accessible information and subsequently its main characteristic method - abduction. Abduction (reverse 8

deduction) combines the resulting state of affairs (8) with a law (L) to infer the controlling state of affairs (A) (Rhoads and Thorn 1993). Uncertainty of various inferences increases with the age and area of the study object, and together decreases the possibility of quantification. Corroboration of the inferences is consequently very often problematic. However, if the inferences create a logical system then their credibility rises with the number of system elements and their mutual connections. This is the way to create more credible denudation chronology. Ergo, the regional scheme of denudation chronology should reflect the maximum of the available facts and information and their mutual relations. The traditional scheme of the West Carpathians denudation chronology was created on the basis of a whole spectrum of contemporary methods and information (study of territorial differentiation of planation surfaces, analysis of regolith, truncated rocks, correlated sediments or paleoclimatic and neotectonic recons[ruc[ions). Possibilities of morphological interpreta[ions are at present extended by modern p]ate tectonic reconstructions (K o v ó ć 2000), which are based on modern dating methods (radiocarbon, uranium series and argon dating, fission track da[ing, paleomagne[ism and oxygen isotope ratios, electron spin resonance) and an- other geophysical, geochronologic, volcanologic, paleomagnetic, structural and sedimentological data. Reconstructions involve description and explanation of reasons of movement and rotation of the West Carpathians block as well as cha- racteristics of tectonics in time and space. An inherent potential of geomorphology for the solu[ion of denudation chronology problems lies in the quantification of used methods, in respect of the hierarchical nature of georelief, in system approach and in effective use of models and modelling. All these aspects led to the creation and use of the geomorphological information system, which is the most powerfu] instrument for the formation of denudation chronology. Complex geomorphological mapping on the basis of the elementary landforms concept (Mj nó r 1995) is a suitable basis for creation of such system. The elementary landforms are exactly geometrically defined elementary parts of geore]ief, which are characterised by roughly constant values of altitude, or some from altitude derived morphometric parameters (slope, aspect, curvatures etc.). The geometrical homogeneity is a consequence of their genetic homogeneity and age homogeneity, as well as a condition for the homogeneity of recent geomorphic processes in the e]ementary landforms. Map- ping of the elementary landforms requires the harmonization of various genetic, geometric, dynamic and chronologic information not only for individual elementary landforms, but also for their spatial and hierarchical struc[i]res. A strong basis for the creation and verification of local and regional denudation chronology conceptions is created in this way. We treat as fundamental the separation of regional and local denudation chronologies from the point of view of methodology and interpretation. Local chronologies make elemental constructional components for regional chronology, which is made by their generalisation, whereas regional denudation chronology has to be 9

onv a working hypothesjs in the process of the creation of local denudation chronologies. Some of the methods and information sources have similar importance for both, others are more significant for one, or the o[her (Fig. 1).

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Fig.1. Methods and information sources of regional and local denudation chronology and their relationships

GENERAL OUTLINE OF THE WEST CARPATHIANS DENUDATION CHRONOLOGY

The absence of full area, systema[ic geomorphic mapping and functional geomorphological information system are the main barriers to the creation of modern regional denudation chrono]ogy of the West Carpathians. However, ac- cumulated new geomorphological and geotectonical knowledge has enabled the modification and appendage of traditional conceptions of [he West Car- pathians denudation chronology so that the modified conception can be used as a working hypothesis for the crea[ion of local denudation chronologies and a generally acceptable regional chronology of the West Carpathians. Our ini[ial revision of the WesŁ Carpathians denudation chronology (Bi- zubova and Minór ]992) was based on strictly defined tectonic phases. But 10

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{he latest geotectonic reconstructions (Kovóć 2000) break away from it and stress a continuity of tectonic development. So space for the formation of planation surfaces is seemingly reduced. However, the improved localisation and explanation of the phases of tec{onic compression and extension in space and time enab]es us to look for a dynamic explanation of planation process and explain other significant characteristjcs of the West Carpathians landforms too. Tab]e 1 corre]ates the main geotectonic events (Kovś ć 2000; Davi d s o n 1997), paleogeographical conditions (P 1 a n d e r ovó et al.1992; Va s s 1989) and their probab]e morphological impact in the West Carpathians. The neotectonic uprising of the West Carpathians is possibly connected with the Early Miocene global compressjona] pulse (Davidson 1997). Regionally this resulted in the collision of the Alpaca lithospheric block with the North European platform, which caused the compression of the West Carpathians and their eastward ex- trusion. Consequently the retreat of subduction in the front of the North European platform caused the ro]l back effect and the tectonic stretching and extension of the territory (K o v ó ć 2000). The rise of marine and ]ake basins not only on the periphery but also within the West Carpathians is evidence of subsidence tendencies connected with the extensional regime. The coincidence of the main direc- tions of reconstructed ex[ension (K ovó ć 2000) with the planview of the spurs of the Pannonian basin and intramountain basins confirm this implication. There- fore the depth of the Neogene bases in the basins can generally signalise the in- tensibJ of the subsidence tendencies (Fig. 2).

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Tectonic subsidence plays a crucial role in our explanation of the orjgin of the Pannonian Midmountain level (Mazńr 1963,1965), or the initial Sarmato-Pan- nonian surface (Lukniś 1962,1964), which has a key position in the West Carpathians denudation chronology. It is problematic to explain the origin of this surface by a simple pediplanation process in the framework of mobilistic geotectonic conceptions. We created a hypothesis of planation in tectonically active regions and the final flat surface we named tectoplain (Minór 2003). The tectoplain is a polygenetic (denuda{ion-accumulation), stepped flat surface rapidly formed under conditions of prevailing extension and subsidence tectonics. Its rapid rise is due to the tectonic subsidence of a part of a.block below the base level, rapid retreat of fault slopes, expansive abrasion during a transgressive regime, local sediment deposition that together with tectonic erosion eliminates isostatic compensational uplift (Fig. 3). The majority of the surface probably has the character of a pedip]ain and accumulation planes but it also includes abrasion terraces, older subsided planation surfaces, exhumed surfaces or stripped plains. Dominance of erosion and accumulation over the local tectonic differentiation is the basic condjtion of tectoplain formation (Fig. 4).

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Fig. 3. Teclonically induced plana[ion effec[ (8) in comparison with standard planation (A). A - De- nudation processes have Ło remove not only the mass of the initial mountains, buŁ also the mass of rocks up]ifted above the see level by compensating isostatic rise. The plana[ion effect of abrasion in a regressive regime of the sea is low, 8 -Tec[onic subsidence caused by an extensional 'iectonic regime can exceed lhe effec[ of compensative isostatic rise, which is reduced also by reiention of sediments in the local depressions. Sea transgression markedly enhances the errect of abrasion, and denudation on aciive fault lines is accelerated. Accumulation in depressions subsided under base level and subsidence of part of the initial mountains under ihe base leads to more rapid planaŁion [oo 14 -J-``````-Ł=,-,,,,,

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The Midmountain level could have been formed in the extensional tectonic phase after the final nappe pushing in the Outer West Carpathians. The process was in accordance with the character of tectonics; most jntensive on the south and fading oiit northwards (in the Outer Carpathians) and simultaneously the planation shifted from the west to the east. The plane surface achieved maximum extent in the Late Miocene (Pannonian in the west and Pannonian-Early Pontian in the east) at the time of [ectonic inversion and formation of the new compression regime. The Pliocene - recent global compressional pulse has, according to J. K. Davi dson (1997), increasing intensity in the Late Pliocene and Quaternary. It seems that the rising thrust of the Adriatic plate on the West Carpathians, without compensation by subduction (Kovó ć 2000) is in line with this tendency. There- fore we suppose an existence of times of relative tectonic calm in the Pontian and Late Pliocene (up to Early Quatemary) during which were formed pediments of 15

the Undermidmountain and River levels. Naturally, the question of temporal and spatial differentiation of the origin of the pediments is opened. A system of Qua- ternary cryoplanation surfaces and river terraces creates the last element of the general scheme of the West Carpathians denudation chronology.

EXAMPLES OF LOCAL DENUDATION CHRONOLOGY

The general outline of the West Carpathians denudation chronology has to be (according to our propositions) synchronized with the results of local morphochronological studies. The local denudation chronology moreover brings new specific information. Therefore we notice two small examples of such results, which were obtained on the basis of detailed, complex geomorphological research. The Deu`nska Kobyla is a part of the Malć Karpaty Mountains above of the con- fluence of the Danube and Morava rivers. The result of detailed complex geomorphological research of the territory is published in a map of scale 1 : 10,000 ( M i n ó r and M i ć i a n 2002). On the boundary between the Carpathians and the Vienna basin a system of three Neogene planation surfaces (the Midmountain, Undermidmountain and River level) and a system of Quatemary river teiTaces with the cryoplanation glacis at the same altitude as the oldest Early Pleistocene terraces, has evolved (Fig. 5). The site is in very good condition for dating planation surfaces as they truncate (or are covered by) rocks of various age (Scheme 1). The Midmountain level trLincates Mesozoic, but also Badenian and Sarmatian sediments, in addition the Undermidmountain level is situated on the Pannonian sediments and the River level site directv above the oldest Quaternary terraces. The si- tuation is thus fully in harmony with our general outline of the West Carpathians denudation chronology. A local peculiarity is the occurrence of the exhumed abrasion surfaces (terraces), which can be integrated to any of the planation surfaces. More- over, a local morphochronological study in this case also brings veiy interesting neótectonic conclusions. Two systems of morphotectonic framework were identified. On the basis of the age of the youngest faulted surfaces, the time of the last tectonic movements was specified. Significant horizontal movement (some hundreds of meters) during the Late Pleistocene or Holocene was identified in this way, which is extremely important from the point of view of the seismic hazard estimation of the very rapidly developing periphery of Bratislava. The results of detailed geomorphological research in the middle Hron river region (Z a t'ko et al.1990; M i nór 1995) are our second example (Fig. 6). Three easily datable Neogene surfaces of planation have been identified here too. The age of the Midmountain level generally determines the age of truncated volcanic rocks -the Sarmatian andesites (L u k n i ś 1962 , 1964). The position of the youngest Sarmatian lava flows in the central part of the Pohronsky lnovec Mountains only some dozens of meters above the Midmountain level and a harmony of the 16

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Fig. 6, Situational map or the middle Hron river region

]ava flows' lamination with surface slope suggest, that ]ava flows were flowing to the valley bottoms, which were the base level for the formation of the Mid- mountain level. It is in agreement with the idea of the Sarmato-Pannonian age of the Midmountain level (Lu kn i ś 1962,1964). An existence of two steps (pediments) above the river terraces is visible in the Hron valley, mainly at the edge of the Źiarska kotlina Basin. While the lower step is a direct continuation of the highest river terraces (consequently it is the La[e P]iocene-Early Pleistocene age), the higher step is partly covered by the "Hron gravels formation", which is dated from the Pliocene to Early Pleistocene. Considering the Late Pannonian age of some base basaltic rocks (e.g. the flat top of the Śibenićny vrch near the town Źiar nad Hronom), the higher step can have been created in the Pontian-Pliocene period and therefore can be a fragment of the Undermidmountain level. The dating of the youngest West Carpathians volcanism (volcano "Putikov vfśok" near the town Novó Bańa) is an excellent example of effective uti]ization of the ]ocal denudation chronology in this territoiy. Repeated dating by direct methods 19

did not bring adequate results. The standard Ar-K dating method showed a value below the detectability limit of the method (0.4 Ma), or a va]ue near it (0.53 Ma) ( Ś i m o n and H a 1 o u z ka 1996). The latest dating attempts by Ar-Ar method give ambiguous results too (L. Śimon -personal communication). The set of following geomorphic indicators enabled us (Za t'ko et al.1990) to specift the age of volcanism to the Riss-Wurm interglacial, at most to the Earb Wtlrm (1.31).6 Ma). The main evidence is the position of the lava flow base at the level of the recent floodplain, which is at the same level as the base of the lowest (Wtirm) terrace. Other evidence represents the character of the cross section and longitudinal pro- files of the valleys influenced by volcanism, shallow undeveloped periglacial dells on the lava flows, or the freshness of the cinder cone form.

CONCLUSIONS

We suppose, that despite doubts about the regional West Carpathians denudation chronology, this is the chance to find its modern face today. On the one hand it requires respect of the new geotectonic reconstruction and resiilts of modern methods of geological dating, the creation of the complex geomorphic information systems based on the detailed research and mapping, quantification and modelling. On the other hand, the regional denudation chronology has to be more flexible, not static; jt must respect an existence of the temporal and spatial trends and results of the local denudation chronology studies. Local studies would take priority as a result of a more reliable information base, and their greater interpretative possibilities. Local denuda[ion chronology can be a powerful tool for dating in the cases where absolute dating methods fail, or are problematic. It can contribute to the evaluation of natural hazards and risks, as well as to the understanding of the behaviour of complex geosystems. The outlined conception of the general denudation chronology of the West Carpathians arises from older and for a long time generally accepted conceptions (Klimaszewski 1934,1965; Lukniś 1962,1964; Mazdr 1963, 1965; S t a rk e 1 1965,1969; C z u d e k et al.1965). However, these conceptions vary by more details (number, age and genesis of surfaces of planation) and mobilistic geotectonic theory now puts into ques[ion some s[arting points of these conceptions (e.g. time of relative tectonic calm needed for creation of the Midmountain level as a pediplain). The stratigraphic position of planation surfaces have to be revised continuously with the development of geological dating. We have attempted to show that the harmonization of older conceptions with the latest regional geoŁectonic [heory (Kovźć 2000) is possible. New data confirms and gives more precision to some of the older conceptions and can be an arbiter between them. We can summarize the more important conclusions follow: 20

The regional mobiljstic conception (Kovóć 2000) explains regional morphotectonic differentiation, which was considered earlier in papers of E. Mazrir (1965), L. Starkel (1965) or W. Zuchiewicz (1987). We suppose genera]]y W-E and S-N shiftings of the morphotectonic stages in the West Carpathians as a consequence of geotectonic trends. The origin of the Midmountain leveJ as a tectoplain is an altemative hypothesis, which explains the formation of the regional surface of planation in active orogene. [t is in line with the conception of "initial surface" of E. L u k n i ś (1962, 1964) to which it gjves a deeper geotectonic explanation. ]t is suitable to consider more then one stage of partial planatjon in the Plio- cene and Early Pleistocene in the line with M. Klimaszewski (1965) or L. Starkel (1965,1969) but contrary [o E. Mazur (1963,1965) and M. Lukniś (1962, 1964).

ACKNOWLEDGEMENT

The research has been supported by the Scientific Gran[ Agency of the Minis- try of Education of the Slovak Republic and Slovak Academy of Sciences - pro- jects No.1/8426/01 and 1/1037/04.

Comenius Uniuersiw, Faculw of Na[ural Sciences Deparirneri[ of Physical Geography and Geoecolosy Mlynskó dolina, 842 15 Bra[islaua 4, Slouakia [email protected]

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STRESZCZENIE

J. Minór, M. Bizubovź, M. Gallay

OGÓLNE ASPEKTY CHRONOLOGII DENUDACJI KARPAT ZACHODNICH

Au(orzy prezentują metodyczne podejście zmierzające do rewizji chronologii denudacji Karpa( Zachodnich, Opiera się ona na wykorzystaniu geo[ektonicznej rekons[rukcji Karpat w neogenie, da- Lowaniu bezwzględnym, kompleksowych badaniach geomorfologicznych, ujęciu i]ościowym i mo- delowaniu poprzez zastosowanie geomorfologicznego systemu informacji. Należy też rozróżnić me- iodologię badań chronologii denudacji w skali lokalnej i regionalnej. Ogólny charakter chronologii denudacii Karpat Zachodnich iest określony przez warunki tektoniczne i klimatyczne, kióre byy homogeniczne na większości [erytorium w określonych okresach. Ta jednorodność miała charakterystyczne trendy w przes(rzeni j czasie. Okres ekstensywnej tektoniki w badenie-pannonie pokazuje jak powiązać poligeniczną inicjalną powierzchnię (dla współczesnej rzeźby) poziomu śródgórskiego. Wginanie tektoniczne było istotnym czynnikiem dla tworzenia zró- wnań w obszarach aktywnych tek(onicznie. Stwierdzono, że przesunięcia faz denudacji w przekroju W-E i S-N bylo powiązane z (endencjami geotek(onjcznyrni. Obecność trzech generacji zi.ównań neogeńskich jes( jlustrowane dwoma przykładami: wspólczesnych ruchów tektonicznych koło Bratysławy (Devinska Kobyła) i da[owaniem cz`^rarto- rzędowego wulkanizmu kolo Nowej Bany.