Neotectonic Mobility of the Roztocze Region, Ukrainian Part, Central Europe: Insights from Morphometric Studies

Annales Societatis Geologorum Poloniae (2010), vol. 80: 167–183.

NEOTECTONIC MOBILITY OF THE ROZTOCZE REGION, UKRAINIAN PART, CENTRAL EUROPE: INSIGHTS FROM MORPHOMETRIC STUDIES

Teresa BRZEZIÑSKA- WÓJCIK, £ukasz CHABUDZIÑSKI & Leszek GAWRYSIAK

Insti tute of Earth Science s, Maria Curie-Sklodow ska Uni ver sity, Al. Kraœnicka 2c, d, 20-817 Lublin, Poland; e- mails: tbrzezin@poc zta.umcs.lublin.pl; lchabudz in [email protected]; Leszek.Gaw [email protected]

Brzeziñska- Wójcik, T., Chabudzi ñski, £. & Gawry siak, L., 2009. Neo tec tonic mo bil ity of the Roz tocze re gion, Ukrain ian part, Cen tral Europe: in sights from morphomet ric stud ies. An nales So cie ta tis Ge olo go rum Po lo niae, 80: 167–183.

Ab stract: The re sults of geo logi cal, geo mor phic and hydro geo logi cal re search in di cate spa tially vari able neo - tec tonic ac tiv ity of the Ukrain ian part of the Roz tocze re gion. This ac tiv ity is con firmed by analy sis of some geo met ric and mor phomet ric co ef fi cients (es pe cially drain age ba sin elon ga tion ra tio, drain age ba sin cir cu la tory ratio, drain age basin shape and lemnis cate coef fi cient), which were cal culated for 1646 drainage areas of the 3rd to 6th or der, and mor phomet ric lin ear co ef fi cients (mountain- front sinu os ity in dex and val ley floor width- valley height ratio coef fi cient), which charac ter ise the fault scarps. The south-wester n mar gin of the Rava Roztocze and Ya niv Roz tocze re gions, fol low ing NW–SE-trending faults, be longs to struc tures of the 1st or 2nd class of relative tec tonic ac tiv ity. On the other hand, in the north- eastern mar ginal zone in the Ukrain ian part of the Roz tocze region, a relatively ac tive seg ment comprised between Maheriv and Zhashkiv shows a charac ter is tic NW–SE ori en ta tion of val leys, con trolled by a net work of sec on dary sub-paralle l faults. In the south ern part of the ana lysed area, the Stavchanka River drainage ba sin re lated to the NW-striking fault zone, and the sub-paralle l edge of the zone of the Vereshytsia-upper Mlynivka transverse depres sion are relatively ac tive. Some relatively in active areas are those of smaller drain age ba sins of the 3rd to 6th or der, lo cated within the zone of the main wa ter shed be tween the Rata and Lu bac zówka riv ers in the Rava Roz tocze re gion and the Zubra and Poltva riv ers in the Lviv Roz tocze re gion.

Key words: neo tec tonic mo bil ity, mor phomet ric co ef fi cients, Ukrain ian part of the Roz tocze re gion, Cen tral Europe.

Manu script re ceived 15 De cem ber 2009, ac cepted 15 May 2010

IN TRO DUC TION

The Ukrainian part of the Roz tocze region is a tectoni c tinct mor pho log i cal mar gin, re lated to the Rava-Rus’ka– horst, stretching NW–SE, elevate d by 110–120 m (Palien- Krehiv fault zone (Khiznyakov & ¯elichowski, 1974), and ko, 1993) with respec t to the adja cent areas : Sandom ierz to the Zhovkva–Lviv tectoni c area (Bogutsky et al., 1993), Basin in the west, Upper Bug and Styr Basin in the east, and known as the Lysynets’kyi fault (Andreyeva, 1986). It sepa - Lviv Opilli a in the south (Rosly i, 1990; Hnati uk, 2002) rates the Roztocze region from the Upper Bug and Styr Ba- (Fig. 1). The area rep re sents the wa ter shed between the Vis- sin (Fig. 1). In its northern secti on, the margin has a NW– tula and Dnister river basins . SE ori enta ti on, typi cal of Roztocze region, and in the south - The boundari es of the region, parti cu lar ly the southern secti on, a NNW–SSE ori enta ti on prevails. The northern west ern and the north-eastern ones, clearly show tectoni c boundary of the Ukrai nian part of the Roztocze region fol - control relat ed to the south-west ern marginal area of the lows the sub-par al lel Early Variscan faults sep a rat ing the East-Eu ro pean Plat form, es pe cially the mar ginal block of Mazowsze–Lublin mega-block from the Lviv block (Rava- the Lviv mega-block in the slope area of the platform (Fig. Rus’ka–Horyniec). The southern boundary of the region is 2). The south-western boundary of the region is connect ed control led by the Lviv–Mal’chytsi fault (Holohory), sepa - with a set of the Stavchanka-Vereshytsia (Nemyriv-Shklo- rat ing the Lviv and Peri-Dniestrian mega-blocks (Hofsh- Mal’chytsi) nor mal faults (Bogutsky et al., 1998), sepa rat - teyn, 1979; Znamienskaya & Chebanenko, 1985; Hnatiuk, ing the Carpathian Foredeep basin from Roztocze region 2001). (Ney, 1969). The north-east ern boundary is visi ble as a dis- 168 T. BRZEZIÑSKA-WÓJCIK ET AL.

Fig. 1. Surface fea tures in the Ukrai nian part of the Roztocze re gion. Geomorphic re gions and subre gions in Roztocze ac cord ing to Roslyi (1990) and Hnatiuk (2002). 1 – towns and places; 2 – the highest hills; 3 – rivers; 4 – boundary be tween Po land and Ukraine; 5 – bound aries of re gions and sub re gions

In a surfic ial im age of the geologi cal struc ture of the been a subject of geologi cal (Hofshte yn, 1979; Sobakar’ et Ukrainian part of the Roz tocze region, lithologi cally varied al., 1975; Pali enko, 1990), geo mor pho logi cal (Bo gut sky et Palaeo gene and early Neo gene (Mio cene) rocks (Wy socka, al., 1993; Hna tiuk, 2001; Burac zyñs ki, 2002) and hydro- 2002) and Upper Creta ceous (Maastri chtian) strata (Andre- geo logi cal (Mi chalc zyk & Ko val chuk, 2002) re search. yeva, 1986) are prevalent (Fig. 2), local ly covered by Pleis- An as sess ment of the to tal ampli tudes of ver tical crus tal tocene loess (Ma ruszc zak, 1967) and Holocene sedi ments movem ents in the Roz tocze region showed that the aver age (Hna tiuk, 1997). rate of post-Bade nian upli ft was 0.2 mm/year (Pali enko, The problem of Neogene tectoni c ac tivit y within the 1990). Moreover, the aver age gra dient of the movem ent ra- boundarie s of the Ukrainian part of the Roz tocze region has tio was 0.2–0.3 mm/year in the hill top zone of the region NEOTECTONIC MOBIL ITY OF THE ROZTOCZE REGION 169

Fig. 2. Geo log i cal set ting of the Ukrai nian part of the Roztocze re gion, with out Qua ter nary sed i ments (compiled by T. Brzeziñska- Wójcik af ter: £omnicki, 1887, 1898; Teisseyre, 1938; Naidyn, 1953; Cieœliñski & Wyrwicka, 1970; Khiznyakov & ¯elichowski, 1974; Glushko, 1988; Vyshniakov, 1990; Buraczyñski & Krzowski, 1994; Popielski, 2000; Hnatiuk, 2001; 2002; Wysocka, 2002; Wysocka et al., 2007; Œwidrowska, 2007). Caino zo ic: 1 – clays, silts (Sarmatian), 2 – reef and de tri tal lime stones, sand stones (Upper Badenian), 3 – quartz and glauconitic sands (Upper Badenian), 4 – de tri tal lime stones, sand stones and sands (Upper Badenian), 5 – detri tal limestones , sand stones and sands (Lower Badenian), 6 – sands and glauconitic sand stones (Eocene); Me sozoic: 7 – marls, marly opokas and chalk (Upper Maastrichtian), 8 – marly opokas and marls (Lower Maastrichtian), 9 – gaizes and marly gaizes (Lower Maastrichtian), 10 – opokas and gaizes (Upper Campanian), 11 – gaizes and opokas (Lower Campanian); 12 – Palaeozoic faults; 13 – Meso- and Caino zo ic faults; 14 – bor ders of Roztocze ac cord ing to Roslyi (1990) and Hnatiuk (2002); 15 – Polish-Ukrai nian bor der and 0.4 mm/year – in the east ern marginal zone (Pali enko, vial depos it s within the region suggest s that af ter the Middle 1993). Accord ing to Hofshte yn (1979), the am pli tude of the Pleisto cene the area was upli fted by 30–40 m (Hofshte yn, post- Sarmatian tectonic move ments in the Roz tocze re gion 1979). The result s of repeat ed precis e level li ngs carrie d out reached 300–350 m. An analysis of Pleisto cene glacio flu - along a transverse profil e through the Roztocze–Lviv 170 T. BRZEZIÑSKA-WÓJCIK ET AL.

Opillia zone indi cat e peri odic varia tions of the rates of con - re gion (An dreyeva, 1986; Bo gut sky et al., 1998; Œwidrow- tem po rary tec tonic move ments. The larg est gra di ents of the ska, 2007). Smaller areas built from Cam panian gaize and gravit y field have also been noted in this zone (in the Lviv silicate chalk are docu mented be tween Rava- Rus’ka, Ne - area more than 0.2 mGal betwee n 1966 and 1970), along myriv and Ma heriv in the Rava Roz tocze region. Less resis - with increa sed values of the heat flow (Sobakar’ et al., tant marl, as well as Maas trichtian chalk oc cur in the north- 1975). eastern part of the region. Small, eroded patches of Eocene As fol lows from geo mor phic re search (Bo gut sky et al., strata (sands and quartz and glauco nit ic mudstone ) have 1993), the most im portant tec tonic zones are accom panied been identi fied local ly in the southern segm ent of the by parallel-tre nding river val leys, most of them showing an So³okija River val ley (Burac zyñs ki & Krzowski, 1994) and asym metric cross sec tion; one of them is the sub- parallel in the north of Ma heriv (Rogala , 1912; Kudrin, 1966; Bo- valley of the Stavchanka River. Boreholes drilled in this gut sky et al., 1998) in the Rava Roz tocze region. Thin valley reveal ed a 150 m deep, NW–SE striking tectoni c de- (20–60 m) Badenian form ati ons do not form a conti nuous pression over a 30-km -long stretch. Towards the north, in cover. Gen er ally, shallow- water, marginal- type fa cies show the di rec tion of the Vere shyt sia River val ley, the de pres - vari able de vel op ment and thick ness. Sedi men ta tion gaps, sion’s am pli tude changes to 20–30 m. Sim ulta ne ously , an erosiona l surface s and great changeabil ity of de posit s are analy sis of the valley pattern in the Vere shyt sia drain age ba - char acter istic of Mio cene for mations. Over a large area, es - sin (Bo gut sky et al., 1993) and longi tu di nal secti ons of the pecia lly in the marginal south-west ern part of the Roztocz e valley bottom (Burac zyñs ki, 2002) lead to a conclu sion that re gion, the Lower Bade nian or gan ode tri tal lime stone with the sub-paral lel Lviv–Mal’chytsi (Holohory) tectoni c zone sandstone and sand, crop out (Wysocka , 2002). Near Lviv is current ly acti ve. This is also confirm ed by obser va ti ons of and Ra dru¿ towns, Ratine limestone occurs, which is a discharge s of springs in this area. Accord ing to Mi chalczyk counter part of evaporitic-chem ical beds in the Carpa thi an and Koval chuk (2002), the largest discharge s (20–110 l/s) Foredeep ba sin (Peryt & Peryt, 1994). The most com mon in are noted in the springs in the upper Shklo drainage ba sin in the Roztocz e region are vari ous Upper Badenian carbon ate the Yaniv Roztocz e region, whereas within the boundarie s and ter ri ge nous de pos its clas si fied as supra- evaporitic- of the rem aining part of the Ukrainian Roztocz e region, the chemical beds. Ter ri ge nous for ma tions have emerged as discharge of more than 70% of acti ve springs does not ex- sands and quartz and glauco nit e sandstone , covered by ceed 0.5–2.0 l/s. highly eroded reef and organ ode tri tal limestone , as well as The aim of this study is to assess the neotec tonic mobil - coquina beds and lime sands with sandstone and clay inter - ity of the Ukrainian part of Roztocz e region using mor- cala ti ons (Palienko, 1993; Wysocka , 2002; Wysocka et al., phomet ric co ef fi cients. The as sess ment was made us ing a 2007). digital ter rain model (DTM; Nita et al., 2007) and calcu - The Up per Cre taceous, Eo cene and Bade nian strata are lated on its basis geom etric and morphom etric param eter s covered with Pleis tocene and Holocene sedi ments of vary - for drainage ba sins of the 3rd–6th order, as well as morpho- ing lithol ogy, thickness and origin (Bachynskiy & Zubrit - met ric lin ear co ef fi cients, which char ac ter ise fault scarps in skiy, 1979; Burac zyñs ki et al., 2003; Maruszc zak, 1994). the marginal zones of the study area and in some val leys Pleisto cene sedi ments in the Roz tocze re gion are only pre - cutti ng the south-west ern margin of the Ukrainian part of served as frag ments of loess cov ers be tween Ma heriv and the Roz tocze re gion. Krehiv towns, and along the eastern edge of the Roztocz e region near Lviv (Maruszc zak, 1967). In river val leys and basin- shaped de pres sions (Rata River val ley, Vereshytsia GEO LOG I CAL AND GEOMORPHIC River ba sin), there oc cur Holo cene or gano genic de pos its of SET TINGS up to a- few- metre thick ness. Holo cene min eral-or ganic muds are also docum ented in the val leys (Bogut sky et al., Struc tural fea tures of the area have been shaped by its 1993; Bu rac zyñski, 2002). loca ti on within the marginal zone of the East-Europea n Three major NW–SE oriente d tec tonic zones (south- Platform , the marginal part of which was affect ed by over- western – Stavchanka-Veres hytsia, middle – Zubra and lap ping ver ti cal crus tal move ments of large am pli tude (Pa- south-east ern – Zhovkva-Lviv, called Lysy nets ’ka) are lienko, 1993). The overlap ping of the structura l plans: the clearly visible in the Ukrainian part of the Roz tocze region, prim ary NW–SE plan and the sec ondary W–E plan, ex - as they follow the deeply entre nched, discon ti nuous Palae o - plains the ex is tence of a char ac ter is tic block ar range ment of zoic struc tures (Fig. 2). The zones stretching sub-paral lel the struc tures (Fig. 2). Fault-contr olled lines di vide the Roz - are of sub or di nate char ac ter. The south- western bound ary tocze region into three subregions (Fig. 1): Rava Roztocz e of the Roztocz e region and the relati vely narrow and rec ti - (its northern part being locat ed in Poland) , and Yaniv and lin ear val leys of the Vereshyt sia and Stavchanka riv ers are Lviv Roztocz e in the Ukraine (Rosly i, 1990; Hnati uk, re lated to the Stavchanka- Vereshytsia zone (Ney, 1969; 2002). Khiznyakov & ¯elichowski , 1974). The Zhovkva–Lviv, In terms of li thol ogy, the Ukrainian part of the Roz - also called Ly synets’k a, zone is fol lowed by the eastern tocze re gion is char acter ised by the preva lence of Mio cene boundary of the Roztocz e region. In the south-eas t of Lviv, over Eocene and Upper Creta ceous strata (Fig. 2). The Up- it is express ed as an elevate d step rising at about 60 m. per Cre taceous car bon ate and carbonate- siliceous rocks of Within the bounda ries of Lviv city, the structure is exposed dif fer ent re sis tance (ga izes, silicate chalk, marl) are typi cal as an overthrust of Maastri chtian marls over Badenian of the northern and east ern parts of the Ukrainian Roztocz e sands, dipping at an angle of 30–40°. In the north-west of NEOTECTONIC MOBIL ITY OF THE ROZTOCZE REGION 171

Lviv, the zone is repeat edly dislo cat ed, and it shifts towards lated for an upland area, i.e. the Polish part of the Roztocze the cen tral part of the Roz tocze re gion (Fig. 2). Be tween region (Brzeziñska-Wójcik, 1994, 1995, 1998, 1999; these two struc tures the Zubra zone occurs, be ing par allel ed Brzeziñska-Wójcik & Mi³kowska, 2002; Brzeziñska-Wój- by the narrow and rec ti linear valley s of the Zubra and cik & Superson, 2004; Brzeziñska-Wójcik & Ho³ub, 2007; Mlynivka rivers. Sub-paral lel faults are consid ered to be Brzeziñska-Wójcik et al., 2003). younger and overlappe d with the NW–SE sys tem. This Despit e some am bigu it y com prised in this methodo- overlap ping of the structura l plans was a pre condi ti on for a logy, it is pos si ble to es ti mate the dy namic di ver si fi ca tion char ac ter is tic block- type char ac ter of the Roz tocze struc ture within a geo log i cally het er o ge neous sys tem. Such con di- (Bo gut sky et al., 1993). tions are met in the Ukrai nian part of the Roztocze region, Char ac ter is tic morphologic pa ram e ters: rel a tively high built up of Meso zoic , Palaeogene (Eocene) and Lower Neo - ab so lute and rel a tive heights, struc tural lev els, out li ers and gene (Miocene ) strata (Bogutsky et al., 1998; Wysocka et the dom inant orien ta ti ons of the valley network – W–E al., 2007). The area is also char acter ised by a high de gree of and/or NW–SE, all re sult from lithological and tectoni c fea - cli mate continentality (Kaszewski et al., 2002). tures of the area (Fig. 1). Maxi m um ele va ti ons change from A Digi tal Terrai n Model (DTM) was de veloped for the 389.5 m a.s.l. in the Rava Roztocze region (Wielki Dzia³ Ukrai nian part of the Roztocze region using 1:50,000 topo - within the borders of Poland) through 396.9 m a.s.l. (near graphic maps at the “1942” set ting. The maps were regis - Dubrovytsia) to 401.4 m a.s.l. in the Lviv Roztocze region tered in a set of coor di nate s and then the river net work, con- (Chortova Hora), while the mini m um heights range from, tour lines and al ti tude points were digi ti zed giving them the respec tively: 227.5 m a.s.l. in the So³okija River valley attri bute of alti tude. Using the Topo_to_Ras ter tool, part of through 260.0 m a.s.l. in the Fuyna River val ley to 248.5 m ArcGIS software, a nu mer ical model of the sur face fea tures a.s.l. at the mouth of the Mlynivka River val ley. Thus, the at a reso lu ti on of 20 m was obtai ned. On the basis of the reli ef energy of these three units is 162.0 m, 136.9 m, and model, assis ted by a contour line drawing, the drainage ar- 152.9 m, respectively. eas of the 3rd to 6th or der were marked, dig itized and clas si- Within the bor ders of the subre gions, three ba sic struc - fied in accordance with a classic hydrographic model. tural lev els can be dis tin guished at the fol low ing al titud es: The data pre pared in such a way served then to cal cu - 310–330 m a.s.l. (in the Rava Roztocze region), 350–360 m late geo met ric pa ram e ters and co ef fi cients: max i mum ba sin a.s.l. (in the Rava Roztocze and in the Yaniv Roztocze re - length L, drain age ba sin area A, drain age ba sin per im e ter P, gions), and 380–390 m a.s.l. (in the Yaniv Roztocze and in drainage ba sin mean width W, drain age ba sin elon ga tion ra- the Lviv Roztocze re gions) (Buraczyñski, 2002). Isolat ed tio Re, drain age ba sin cir cu la tory ra tio Rk, form ratio Rf, hills – de nuda ti on rem nants – are rising above hilltop level lemniscate co ef fi cient k, as well as morphometric pa ram e- up to a height of 20 to 30 m, mainly in the watershed zone. ters and co ef fi cients: max i mum height Hmax, min i mum The Roztocze re gion shows a pecu li ar ori enta ti on of the height Hmin, mean height Hœr, max i mum re lief H, re lief ra tio drainage network. Val leys, which play an im portant role in Rh (CF), and rel ative re lief ra tio Rhp, char ac ter is ing the dis - the regional subdi vi sion, are mostly re lated to tectoni c tin guished 3rd – 6th order basins (Table 1). zones, includ ing grabens filled with depos it s of differ ent In ad di tion, morphometric lin ear co ef fi cients were age – from Eocene sands in the So³okija River valley to cal cu lated, i.e. the moun tain-front sin u os ity in dex Smf and Quaternary sedi m ents in the val leys of Stavchanka, upper the valley shape index Vf, which descri be fault scarps in the Vereshytsia, Fuyna and Poltva rivers (Teisseyre, 1938; mar ginal area zone and in some valleys dis secting these Buraczyñski & Krzowski, 1994; Buraczyñski et al., 2003). margins, respec tively (Figs 7, 8). The mountai n front sinu - os ity in dex Smf (Bull, 1977, 1978) is calcu lat ed as a rati o of the length of the mountai n front measured along the foot of METH ODS AND MA TE RI ALS the mountai n at the pronounced break of slope Lmf to the straight line length of the mountai n front Ls (Table 1). The Geo met ric and morphometric co ef fi cients, which de - valley floor width and valley height rati o Vf pa ram e ter scribe drain age ar eas, and morphometric lin ear co ef fi- (Bull, 1977, 1978; Bull & McFadden, 1977) is calculated cients de scribing fault scarps within the margins of the area as: and in some val leys cut ting through the margins, are param - Vf = 2Vfw/[(Eld – Esc) + (Erd – Esc)]; e ters which il lus trate well the re la tion ships be tween the river sys tem and ampli tudes of ver tical crustal move ments. where Vf is the width of the val ley floor, Eld and Erd are the Most of the param eter s and coef fi cie nts appli ed in this study ele va ti ons of the left and right valley divides , respec tively, were used more than thirty years ago to analyse semi-desert and Esc is the ele va tion of the val ley floor. mountai n areas in Ne vada and Cal ifor nia (cf. Bull, 1977; 1978; Bull & McFadden, 1977) and some mountai n areas in the monsoon clim ate zone (Cuong & Zuchiewicz, 2001), as RESULTS well for moun tains situ ated in the temper ate cli mate zone: the Carpathian Mountai ns (Zuchiewicz, 1980, 1981, 1995a, Geo met ric pa ram e ters obtai ned for 1,646 drainage 1995b, 2000; Krawczyk & Zuchiewicz, 1989; Forma & basins of the 3rd–6th order vary signif i cant ly (Table 2). The Zuchiewicz, 2002), and the Sudety Mountai ns (Badura & drain age ba sin sur face A ranges betwee n 0.01 km2 (5th or- Przybylski, 1995; Sroka, 1997; Badura et al., 2003, 2007). der drainage basins) and 315.34 km2 (4th order drainage Some of the pa rame ters and co ef fi cients were also calcu - bas ins), at tain ing av er ages of 1.26 km2 (6th order drainage 172 T. BRZEZIÑSKA-WÓJCIK ET AL.

Ta ble 1 Pa ram e ters de scrib ing 3rd–6th order drainage basins in the Ukrai nian part of the Roztocze region

Parameter Symbol Formula References Geometric parameters of drainage basins Total area A [km2] Horton (1945) Maximum basin length L [km] Horton (1945), Schumm (1954) Basin perimeter P [km] Smith (1950) Mean width of the basin W [km] A/L Basin elongation ratio Re 2(A/p)0.5/L Schumm (1954) Circulatory ratio Rk 4pA/P2 Miller (1953), Gregory & Walling (1973) Form ratio Rf A/L2 Horton (1945) Lemniscate coefficient k pL2/4A Chorley (1971), Gregory & Walling (1973) Morphometric parameters of drainage basins

Hmax [m a.s.l.]

Hmin [m a.s.l.]

Hmed [m a.s.l.] (Hmax – Hmin)/2

Maximum relief H [m] Hmax – Hmin Strahler (1954), Schumm (1954) Relief ratio Rh H/L Strahler (1954), Schumm (1954) Relative relief Rhp H/P Melton (1957, 1958) Morphometric linear coefficients Mountain-front sinuosity index Smf Lmf/Ls Bull (1977, 1978) 2Vfw/[(Eld – Esc) + Valley floor width and valley height ratios Vf Bull (1977, 1978), Bull & McFadden (1977) (Erd – Esc)]

basins) to 4.58 km2 (3th order drainage basins). The maxi - The cir cu la tory ra tio Rk (Miller, 1953; Gregory & mum basin length L (Horton, 1945; Schumm, 1954) is the Walling, 1973) compares the drain age ba sin area to a cir cle, distanc e betwee n the most distant points of the drainage ba - whose per im eter is the same as that of the ba sin. The val ues sin measured along a straight line (Dobija, 1979). The cal- of Rk lower than 1.0 are typi cal of elongate d basins. In the culat ed val ues vary from 0.35 to 31.94 km (4th order drain- Ukrai nian part of the Roztocze region, the extre me val ues of age basins), attai ning aver ages of 1.64 km (6th order drain - the coef fi cie nt vary from 0.20 (4th order drainage basins) to age basins) to 2.47 km (3th order drainage basins). Extre me 0.89 (5th and 6th order bas ins) and aver age 0.61–0.62 (Table val ues of the per im eter of the ana lysed bas ins P change 2, Fig. 4). from 0.85 to 136.34 km for the 4th order drainage basins, The form ratio Rf (Horton, 1945) com pares the out line and aver age 4.36 km (6th order drainage basins) to 6.92 (3th of the drain age ba sin to a rect an gle. Lower val ues are typ i- order drainage basins). The mean width of the basin W var- cal of elongate d basins, while Rf > 1.0 typify wide basins, ies betwee n 0.01 km (5th order bas ins) to 11.11 km (3rd or- whose out line is close to a square. The value of the Rf co ef - der bas ins), aver ag ing 0.55 km (6th order drainage basins) fi cient de creases with the in crease of the ba sin area (Eagle- to 0.86 (3th order drainage basins). son, 1970; Gregory & Walling, 1973). In the Ukrai nian part The drain age ba sin elon ga tion co ef fi cient Re (Bull & of the Roztocze re gion, ex treme values of Rf change from Mc Fadden, 1977) is one of indi rect indi ca tors of young tec - 0.05 to 1.00 (extre me coef fi cie nts for basins of the same or- tonic ac tiv ity. It is cal cu lated as a ra tio of the cir cle di ame - der, char ac ter ised by min i mum and max i mum Re values) ter, the area of which is equal to the area of a drain age ba sin, and average 0.35–0.37 (Table 2, Fig. 5). to the maxi m um basin length (Schumm, 1954; Eagleson, The lemniscate co ef fi cient k varies betwee n 0.74 (6th 1970). Accord ing to Strahler (1964) and Eagleson (1970), order bas ins) and 14.49 (5th order bas ins) to 2.56 (3th order values close to 1.0 are typi cal of poorly dissec ted basins, drain age bas ins), av er ag ing 2.42 (4th order drainage basins) while val ues around 0.6–0.8 charac ter ise basins with steep to 2.56 (3th order drainage basins) (Table 2, Fig. 6). slopes and varied topog ra phy. Drainage basins in arid and It appears from the analy sis of the differ en ti ati on of the semiarid cli mates tend to show Re values ranging from sur face val ues of Re, Rk , Rf and k geo met ric in di ca tors (cf. <0.50, through 0.50–0.75 to >0.75 for tectoni cally acti ve, Figs 3–6) that the drainage ba sin elonga ti on rati o Re and the slightly ac tive and in ac tive setting s, re spec tively (Bull & drain age ba sin shape co ef fi cient Rf cor re late very well McFadden, 1977). Extre me val ues of the basin elonga ti on (Pearson corre la ti on coef fi cie nt 0.99), in contra st to the val- ra tio Re in the Ukrai nian part of the Roztocze region vary ues of the cir cu latory ra tio Rk (0.05–0.11). In order to better betwee n 0.26 (5th order bas ins) and 1.00 (4th and 6th order il lus trate the spa tial dif fer en ti a tion of the in ten sity of tec - basins), and average 0.66–0.67 (Table 2, Fig. 3). tonic ac tiv ity through out drain age bas ins, a com pi la tion of NEOTECTONIC MOBIL ITY OF THE ROZTOCZE REGION 173

Ta ble 2 Av er age, max i mum and min i mum val ues of se lected geo met ric and morphometric pa ram e ters of the 3rd–6th order drainage basins in the Ukrai nian part of the Roztocze region

Drainage basins of selected orders Parameter 3rd order (172) 4th order (412) 5th order 6th order average max min average max min average max min average max min Geometric parameters of drainage basins A [km2] 4.58 188.83 0.12 3.88 315.34 0.05 2.15 137.36 0.01 1.26 34.56 0.08 L [km] 2.47 23.14 0.70 2.37 31.94 0.35 1.94 31.92 0.44 1.64 10.96 0.38 P [km] 6.92 82.92 1.60 6.60 136.34 0.85 5.17 86.21 1.25 4.36 37.31 1.20 W [km] 0.86 11.11 0.16 0.80 9.87 0.12 0.63 4.91 0.01 0.55 3.15 0.14 Re 0.66 0.96 0.43 0.67 1.00 0.33 0.67 1.00 0.26 0.67 1.00 0.33 Rk 0.61 0.84 0.30 0.62 0.92 0.20 0.62 0.89 0.23 0.62 0.89 0.23 Rf 0.35 0.89 0.15 0.37 1.00 0.09 0.36 0.97 0.05 0.36 1.00 0.09 k 2.56 5.37 0.88 2.42 8.99 0.77 2.48 14.49 0.81 2.47 8.98 0.74 Morphometric parameters of drainage basins H max 349.814 401.590 280.720 337.702 404.250 226.290 328.080 404.250 231.170 330.007 404.250 235.310 [m a.s.l.] H min 298.721 344.080 237.960 285.866 359.410 209.930 274.478 349.180 208.690 273.120 345.520 215.310 [m a.s.l.] Hmed 326.033 367.100 257.530 311.718 378.580 219.300 301.493 374.670 222.510 302.651 369.370 222.190 [m a.s.l.] H [m] 51.093 121.830 16.510 51.835 190.950 8.590 53.601 191.950 13.480 56.887 169.040 9.570 Rh 0.039 0.086 0.003 0.032 0.106 0.005 0.038 0.196 0.006 0.044 0.146 0.009 0,01 Rhp 0.011 0.036 0.001 0.012 0.044 0.001 0.063 0.002 0.017 0.057 0.003 5

the values of Re, Rk, Rf and k co ef fi cients has been made tonic ac tiv ity (10–12 points), slight tectonic activity (7–9 (Fig. 7). The follow ing princi ples were adopted in such a points) and weak activity/no activity (4–6 points) (Fig. 7). com par i son: val ues of the co ef fi cients rang ing be tween In the light of the adopted value brackets for the Re, Rk, 0.00–0.50 (Re, Rk), 0.00–0.25 (Rf) and 4.1–15.0 (k) were al - Rf and k coef fi cie nts (Fig. 7), the val ues of Re < 0.50 (after locat ed 3 points and then, re spec tively, 0.50–0.75, 0.25– Bull & McFadden, 1977) and the values of Rk < 0.50, 0.50 and 2.1–4.0 – 2 points each, and 0.75–1.00, 0.50–1.00 Rf < 0.25 and k – 4.1–15.0, define d by us in this paper (Ta - and 1.0–2.0 – 1 point each. This is how a spa tial im age was ble 2, 3), the follow ing drainage basins are tectoni cally rel a- create d of the distri buti on of basins of a rel ati vely high tec- tively ac tive: (1) Stavchanka River (3rd order) basin; (2)

Ta ble 3 Tec tonic ac tiv ity classes in the light of se lected val ues of geo metric and morphometric param e ters

Selected geometric and morphometric parameters Vf parameter Smf Re (Bull, 1977, (Bull & Rk Rf k 1978; Rockwell Tectonic (Keller & Tectonic Tectonic (Bull, 2007) McFadden, (this paper) (this paper) (this paper) et al., 1984; activity classes Pinter, 1996) activity classes activity classes 1977) Wells et al., 1988) 1 and 2 1 (tectonically 1 (tectonically 0.00-0.50 0.00-0.50 0.00-0.25 4.1-15.0 < 1.4 0.43-0.80 0.06-0.51 (tectonically active) active) active) 2 (moderately 2 (moderately 3 (moderately 0.50-0.75 0.50-0.75 0.25-0.50 2.1-4.0 1.4-3.0 1.8-1.9 1.2-1.7 active) active) active) 4 (slightly 3 (slightly 3 (slightly 1.0-7.0 0.75-1.00 0.75-1.00 0.50-1.00 1.0-2.0 > 3.0 active or >1.9 active or active) inactive) inactive) 2.0-7.8 5 (inactive) 174 T. BRZEZIÑSKA-WÓJCIK ET AL.

rd th rd Fig. 3. Spa tial dis tri bu tion of val ues of the ba sin elon ga tion co ef fi cient Re in the 3 –6 or der drain age bas ins. A – 3 or der bas ins; B – 4th or der bas ins; C – 5th or der bas ins; D – 6th or der bas ins

drainage basins transverse to the south-west ern margin of namely: the Rata and Lubaczówka rivers in the Rava the Rava Roztocze re gion betwee n Nemyriv and Shklo (4th Roztocze region, and the Zubra and Poltva rivers in the Lviv order); (3) drainage basins of the Bila, Derevenka and Svi- Roztocze region. nia, and Mlynivka rivers (4th–5th order), transverse to the Morphometric char ac ter is tics obtai ned for the 3rd– north-east ern margin of the Roztocze region; and (4) bas ins 6th or der drain age bas ins are also con sid er ably di ver si fied transverse to the south-west ern margin of the Roztocze re- (Ta ble 2). The max i mum al ti tude Hmax ranges from 226.29 gion betwee n Horyniec and Nemyriv (5th–6th order). (4th order bas ins) to 404.25 m a.s.l. (5th and 6th order bas - Slight ac tiv ity (Fig. 7) has been iden tified in the bas ins ins), av er ag ing 328.08 (5th order drainage basins) to 349.81 of the upper Vereshytsia and Zubra rivers (3rd–4th or der). (3th order drainage basins), while the mini m um alti tude th Rela tively inac tive are the ar eas of small drain age bas ins of Hmin change from 208.69 (5 order bas ins) to 359.41 m the 3rd–6th order, locat ed in the zone of main water shed, a.s.l. (4th order bas ins) and aver age 273.12 (5th order bas - NEOTECTONIC MOBIL ITY OF THE ROZTOCZE REGION 175

rd th rd th Fig. 4. Spa tial dis tri bu tion of val ues of the ba sin cir cu la tory ra tio Rk in the 3 –6 or der drain age bas ins. A – 3 or der bas ins; B – 4 or der bas ins; C – 5th or der bas ins; D – 6th or der bas ins

ins) to 298.72 m a.s.l. (3th order drainage basins). Mean alti - (3th order drainage basins) and 58.89 m (6th order drainage tudes in the ana lysed drainage basins are situ ate d within the basins) (Table 2). range of 219.30 to 378.58 m a.s.l. and re flect extre me val ues The re lief ra tio Rh (Strahler, 1954; Schumm, 1954, typ ical of the 4th order drainage basins. 1956) repre sent s the mean incli nati on of a drainage ba sin. The max i mum re lief H (Strahler, 1954; Schumm, 1954) Accord ing to Morisawa (1962), it is parti cu lar ly useful to is calcu lated as a dif fer ence be tween the mini m um and max- char ac ter ise elon gated bas ins. Lower val ues of this co ef fi- im um alti tude and informs about the de gree of re ju vena ti on cient are typi cal for drainage basins built from resis tant bed- of the landsca pe (Krawczyk & Zuchiewicz, 1989). In the rock and suggest a tectoni c upli ft of the area. The rel ati ve ana lysed Roztocze bas ins, the max im um relief H index var- re lief ra tio Rhp (Melton, 1957, 1958) refle cts the rati o of ies betwee n 8.59 m (4th order drainage basins) and 191.95 maxi mum re lief in a drain age ba sin to its per ime ter. The m (5th or der drain age bas ins), av er ag ing be tween 51.09 m val ues of Rh and Rhp co ef fi cients, cal cu lated for the 3rd–6th 176 T. BRZEZIÑSKA-WÓJCIK ET AL.

rd th rd Fig. 5. Spa tial dis tri bu tion of val ues of the drain age ba sin shape co ef fi cient Rf in the 3 –6 or der drain age bas ins. A – 3 or der bas ins; B – 4th or der bas ins; C – 5th or der bas ins; D – 6th or der bas ins

order drainage basins in the Roztocze re gion vary, re spec - greater than 3.0 are relat ed to inac ti ve fronts, in which the tively, from 0.0009 and 0.003 (3rd order bas ins) to 0.063 ini tial range-front fault may be more than 1 km away from and 0.196 (5th order basins) (Table 2). the present erosional scarp (Bull & McFadden, 1977). The lin ear pa ram e ter, moun tain front sin u os ity in dex In the Ukrai nian part of the Roztocze region, the low est Smf, at tains val ues of 1.0–16 for rec tilin ear, tec toni cally ac- values of the Smf index (1.11–1.43) were obtai ned for the tive scarps de veloped in dry clim ate condi ti ons in the Ba sin sub-par allel escarp ment framing the zone of trans verse de - and Range Province . Areas of weak or insig nif i cant tec tonic pression of the Vereshytsia-Stara-upper Mlynivka rivers acti vit y show values within the range of 1.4–3.0 and from valley (Fig. 8) in the north. Sim ilar values (1.16–1.80) were 1.8 to > 5.0, respec tively (Bull, 1977, 1978). Gener all y, the obtai ned for the sub-paral lel escarp m ent fram ing the val ley Smf val ues less than 1.4 in di cate tectoni cally active fronts of the Svinia River west of Zhovkva town. Slightly higher (Rockwell et al., 1984; Wells et al., 1988), whereas those values (1.23 to 1.60) were define d for the south-western NEOTECTONIC MOBIL ITY OF THE ROZTOCZE REGION 177

Fig. 6. Spa tial dis tri bu tion of the lemniscate co ef fi cient k in the 3rd–6th or der drain age bas ins. A – 3rd or der bas ins; B – 4th or der bas ins; C – 5th or der bas ins; D – 6th or der bas ins

mar gin of the Rava Roztocze and the Yaniv Roztocze re - paral lel margin – slope of the valley of Svinia River to the gions be tween the sub-par allel valleys of the Baszenka and west of Zhovkva town. the upper Vereshytsia rivers. The highest values (1.43– The valley floor width and valley height rati o Vf (Bull, 1.88) were obtai ned for the north-eastern margin of the Lviv 1977, 1978; Bull & McFadden, 1977) helps to differ en ti ate Roztocze region, SE of Lviv. A com pila ti on of these values betwee n wide-bottom valley s with high Vf values and nar- shows that a rel a tively high tec tonic ac tiv ity oc curs in: the row canyons with uneven gra dient and low Vf values. Ab- marginal edge sepa rat ing the inver sion horst of the nor mally low val ues of this ra tio usu ally in di cate ac tively Roztocze region from the Carpathian Foredeep basin, and a upli fting ar eas (Keller & Pinter, 1996). The values quoted per pen dic u lar to it sub-par al lel mar gin fol low ing the Vere- by Bull and Mc Fadden (1977) for the Garlock Fault zone in shytsia-Stara-up per Mlynivka rivers zone, as well as a sub- Cal ifor nia are contai ned within the 0.05–47.0 range and are 178 T. BRZEZIÑSKA-WÓJCIK ET AL.

Fig. 7. Tec tonic activ ity in the 3rd–6th or der drain age bas ins, on the ba sis of ac cu mulated val ues of the fol lowing co ef fi cients: Re elon - rd th ga tion co ef fi cient, Rk cir cu la tory ra tio, Rf drain age ba sin shape co ef fi cient and lemniscate co ef fi cient k. A – 3 or der bas ins; B – 4 or der bas ins; C – 5th or der bas ins; D – 6th or der bas ins betwee n 1.3–11.0 on aver age. Tectoni c ac tivit y classes of inter val be tween 12.89 and 28.42 (Fig. 9). The low est value mountai n fronts in west-centra l Nevada (Bull, 2007) reveal (12.89) was noted in the Radru¿ka River val ley, trans- the follow ing mean values of Vf: classes 1 and 2 (tec toni - versely dissec ting the edge south of Horyniec town, while cally acti ve) 0.06–0.51, class 3 (moder ate ly acti ve) 1.2–1.7, the highest (28.42) was observe d in the Vronka River val- class 4 (slightly acti ve) 1.0–7.0, and class 5 (inac ti ve) ley, sit uate d south-west of Nemyriv town. 2.0–7.8. For the West ern Transverse Ranges (Cali for nia) , in In the context of Vf values obtai ned for var ious fault turn, these values fall into inter vals of 0.43–0.80 (class 1), scarps from other regions (Bull & Mc Fadden, 1977; Keller 1.8–1.9 (class 2), and >1.9 (class 3) (Keller & Pinter, 1996). & Pinter, 1996; Bull, 2007), it is pos sible to assum e that The values of Vf co ef fi cient, cal cu lated for val leys equiva lent values obtai ned only for a small part of the ana- transverse ly dissec ting the south-west ern margin of the lysed area sug gest a lack of tectonic ac tiv ity. How ever, cal - Rava Roztocze and the Yaniv Roztocze regions, fall into the cula ti ons were based on 1:50,000 topo graphi c maps, avail - NEOTECTONIC MOBIL ITY OF THE ROZTOCZE REGION 179

Fig. 8. Spa tial dis tri bu tion of the val ues of Smf mountain front sin uos ity in dex in the Ukrai nian part of the Roztocze re gion

able at the mom ent. In future , when 1:10,000 or more de- that the fea tures specific to rec tilin ear scarps of young faults tailed maps be come available, cal cu lations will be repeated, are to be found in the south-western margin of the Rava and then it will be pos sible to com pare Vf values with those Roztocze and the Yaniv Roztocze re gions be tween the ob tained for other tectoni cally active areas in a more sub-par allel valleys of the Baszenka and the Vereshytsia reliable way. rivers (Fig. 10). Low values of such indi ces , such as: drainage ba sin elon ga tion co ef fi cient, drain age ba sin cir cu la tory CON CLU SIONS ra tio, drain age ba sin shape, lemniscate co ef fi cient, moun - tain-front sinu os it y index and valley floor width-valley An analy sis of the values of se lected geo met ric pa - height ra tio make it pos si ble to clas sify this area, de vel oped ram e ters (Re, Rk, Rf, k) of drainage basins and of lin ear along NW–SE faults, as com posed of struc tures showing morphometric co ef fi cients and in di ces (Smf, Vf) shows the 1st and 2nd class of rela tive tec tonic ac tiv ity. 180 T. BRZEZIÑSKA-WÓJCIK ET AL.

The fol lowing ar eas of smaller 3rd–6th order drainage bas ins, lo cated within the main wa ter shed zone, are rela - tively inac tive: the Rata and the Lubaczówka river bas ins in the Rava Roztocze re gion and the Zubra and the Poltva river basins in the Lviv Roztocze region. The changeable values of the rem aining basin pa ram e- ters (per im eter, mean width, as well as re lief ra tio and rela - tive al ti tude co ef fi cient) re flect con sid er able di ver sity of the area with re spect to hypsometry. It re sults from its lithological and tec tonic fea tures, which will be a subject of future research.

Ac knowl edge ments We ac knowledge with thanks con struc tive com ments as well as care ful, in-depth re views of fered by L. Marks and P. Migoñ on the first draft of this paper.

REF ER ENCES

Andreyeva, H. J., 1986. Geologicheskaya karta Lvovskoi oblasti 1:200 000. (In Ukrai nian). Lviv. Bachynskiy, G. O. & Zubritskiy, J. G. (eds), 1979. At las mista Lviv. (In Ukrai nian). UDINTR, Lviv. Badura, J. & Przybylski, B., 1995. Neotectonic as pects of the East Sudetic Fore land re lief (In Pol ish, Eng lish summary ). Fig. 9. Spa tial dis tri bu tion of the val ues of Vf valley floor width Przegl¹d Geologiczny, 43: 760–766. and val ley height ra tio in trans verse pro files of se lected drain age Badura, J., Zuchiewicz, W., Górecki, A., Sroka, W., Przybylski, bas ins in the south-west ern mar gin of the Ukrai nian part of the B. & ¯yszkowska, M., 2003. Morphotectonic prop er ties of Roztocze region the Sudetic Mar ginal Fault, SW Poland. Acta Montana IRSM AS CR Ser. A, 24: 21–49. Badura, J., Zuchiewicz, W., Štepanèiková, P., Przybylski, B., Kontny, B. & Cacoñ, S., 2007. The Sudetic Mar ginal Fault: A young morphotectonic fea ture at the NE mar gin of the Bo he - The enti re north-eastern marginal zone of the Ukrai nian mian Massif, Cen tral Eu rope. Acta Geodynamica et Geo- part of the Roztocze region appears to be more differ en ti - materialia, 4, 4 (148): 7–29. ated in terms of geom orphol ogy and shows charac ter isti cs Bogutsky, A., Gruzman, H. & Voloshyn, P., 1993. Alpejska of an area of rel atively weak con tem po rary tec tonic ac tiv ity. tektonika Roztocza i karpacki pas rafowy. (In Pol ish). In: It is only the area sit uate d betwee n Maheriv and Zhashkiv Harasimiuk, M., Krawczuk, J. & Rzechowski, J. (eds), towns, with a char acter istic valley pattern of the up per Tektonika Roztocza i jej aspekty sedymentologiczne, hy dro- Svinia and upper Mlynivka rivers control led by a net work geologiczne i geomorfologiczno-krajobrazowe. Materia³y of sec ondary sub-paral lel faults, that in the light of differ en - polsko-ukraiñskiej konferencji terenowej, 16-20 czerwca ti a tion of morphometric co ef fi cients (es pe cially the drain - 1993, Lublin-Lwów. Zak³ad Geologii UMCS, Towarzystwo Wolnej Wszechnicy Polskiej, Lublin: 50–55. age ba sin elon ga tion ra tio, drain age ba sin cir cu la tory ra tio, Bogutsky, A., Voloshyn, P., Gerasimov, L. & Wysocka, A., 1998. drain age ba sin shape, lemniscate co ef fi cient and moun - Budowa geologiczna Roztocza Ukraiñskiego. (In Pol ish). In: tain-front sin u os ity in dex) be longs to struc tures as signed to st nd Przewodnik LXIX Zjazdu Naukowego Polskiego Towarzystwa the 1 or 2 class of relative tectonic activity. Geologicznego. Budowa geologiczna Roztocza (100-lecie The south ern part of the ana lysed area is also in ter est- badañ polskich geologów), Krasnobród, 23-26.09.1998. rd ing, as far as tec tonic ac tiv ity is con cerned. The 3 order Wydawnictwo UMCS, Lublin: 245–256. drain age ba sin of the Stavchanka River is rela tively active Brzeziñska-Wójcik, T., 1994. Pres ent tec tonic ac tiv ity of So³okija (showing the low est values of drainage ba sin elonga ti on river ba sin of the Roztocze by co ef fi cient of elon ga tion drain - ratio, drain age ba sin cir cu la tory ra tio and drain age ba sin age ba sin. (In Pol ish, Eng lish summary ). Annales Universi- shape), relat ed to the NW–SE ori entat ed fault zone and the tatis Mariae Cu rie-Sk³odowska, B, 49: 137–146. sub-paral lel margin fram ing the zone of the transverse de- Brzeziñska-Wójcik, T., 1995. Qua ter nary tec tonic ac tiv ity in the Tanew River ba sin in Roztocze. (In Pol ish, Eng lish sum- pression of the Vereshytsia-upper Mlynivka rivers in the mary). Annales Universitatis Mariae Cu rie-Sk³odowska, B, north (with the low est values of the mountain-front sinuo- 48 (1993): 25–43. sity index). Brzeziñska-Wójcik, T., 1998. Tec tonic ac tiv ity of the es carp ment The multi-stage char acter and vari able thick ness of sed - zone of Tomaszowskie Roztocze in the light of morphometric i men tary infill largely re flect Qua ter nary tec tonic mo bil ity co ef fi cients. (In Pol ish, Eng lish sum mary). Annales Universi- of the Stavchanka and upper Vereshytsia rivers. tatis Mariae Cu rie-Sk³odowska, B, 52: 57–75. NEOTECTONIC MOBIL ITY OF THE ROZTOCZE REGION 181

Fig. 10. Rela tive tectonic activ ity ar eas of the Ukrainian part of the Roztocze region. 1 – ar eas of rel a tive tec tonic ac tiv ity dis tin guished on the ba sis of the low est val ues of the fol lowing co ef fi cients: Re ba sin elon ga tion ra tio, Rk cir cu la tory ra tio, Rf drain age ba sin shape co ef - fi cient and lemniscate co ef fi cient k; 2 – areas rela tively up lifted in the light of Vf val ley floor width and val ley height ra tio; 3 – rela tively tec tonically ac tive fronts/escarp ments in the light of Smf mountain front sinuosity index

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