Landform Analysis, vo!. 3: 13-24 (2002)
The dependence of relief on tectonics in the South-West Escarpment Zone ofTomaszowskie Roztocze (SE Poland)
Teresa Brzezinska-W6jcik
Zaklad Geografi; Regionalnej, hlStylllt Nauk 0 Ziem; UMCS. "I. Akademicka 19, 20-033 Lublin c·mail: [email protected]
Abstract: The relatively undeformed South-West escarpment zone (SWEZ) ofRo7.toczc. SE Poland, ismarginal to the East European Platfonn, which is covered by a thick succession of Palaeozoic and Mcsozoic rocks. Cain()7.oK: LA sedimenls, previously much more widely distributed and largely destroyed by erosion, still fill some valleys and also crop out in the hills ofthe inner and outer escarpments. The escarpment zone comprises severnl morphological --- c:!ements: an OUler hill zone, inner inselbergs and a median depression lone of teclonic origin. Transverse 10 tbe escarpment, these elements arc compartmcntaliscd by transverse valleys. many of which are fauh-control1ed. Morphometric and geomorphological studies show that thc SWEZ ofRoZloczc was repeatedly leclonically activated. NCOletlonie redevelopmenl has resulted from controls in the underlying basement. Hence there arc IUany young faulls, a large numtx.T ofopen faull-fissures and a complex system ofjoints, all ofwhich have influenced landform developmenl in this area 10 a eon.~iderab1c: degree. The main scarps have been developed along the longitudinal fRUlt zones and. along the transverse fault 7.ones, breach valleys. Joint systems have controlled the development of sl:condary relief forms. The close association of relief and various elements of the geological struClure in the SWEZ of Roztoc1.e mean that canol,'f3phic methods can reliably be employed in studil;:s oflhe landfonns in this area.
Key words: geology, geomorphology, tectonil:S, relief, Roztocze
Introduction Tamowola, Pardysowka and Nowiny (280 m a.s.l.) are delimiled by a group of SW-throwing border The SWEZ of Rozlocze is marginal to the East faults and by antithctic Ihrust faults to thc North European Platfonn and lics within the Radom-Krasnik East (Jaroszewski, 1977). Thesc hills have Sleep Elevation, a structural unit ofthe Palacozoic bascment southern slopes and gentle northcrn slopes. (Zclichowski, 1974; 1983). Thc Palaeozoic rocks are According to Jabn (1956), their northern inclination covered by a lithologically-variablc succession of is caused by recent teclonic tilling. JaJOszewski Mesozoic sedimcnls.ln the Cimmerian and Laramian (1977) considered lhat Ihe antilhetic rotation of phases, the sedimentary pile was defonned into gentle individual blocks was due 10 tectonic extension. teclonic StnlClUrCS which follow prc-exisling elements Padol Jozcfowa is a second-order tectonic trough of horsl and graben (Ney. 1969; Pozaryski, 1974; developed in a zooe ofthrusts which accompany the Cieslinski et al., 1994). Miocene sediments, once border faults. Between Tereszpo1, Gomiki Nowe and widespread but now largely removed by erosion, arc Narol, the outer inselberg hills (310-320 m a.s.l.) stiU preserved along the foothills, where they form a are situated in the zone of the Tereszpol-Majdan zone of narrow, extended periclines (Aren, 1962; Ncpryski-Narol border faults. 10 lhis respeCl, they 1968). resemble lhose of the inncr edge. These hills, The escarpment zone comprises threc parallel confined to a structural trough to the Soulh·West of morphological elements: a zone of outer hills and Padol J6zcfowa (270-280 m a.s.I.), are arrangcd in inncr inselbergs separated by a zone of tectonic two parallel chains fonned by separatc semicircular depressions (Fig. 1). The asymmclric outer hills of ridges.
13 Teresa Brzezinska-W6jcik The dependence ofrelief on tectonics in the South-West Escarpment Zone...
matian clays and mudstones with sandy bands (Krakowieckie loarns) occur below ------zwl<1~ the scarp (Le. just within the Carpathiao ,Km' _omC' , Forcdeep Basin) (Aren, 1962; Musial, _Km} 1987; Ciesliilski et al., 1994). - The intra-Miocene movements oc curred in two slages: Middle Badenian and late Sarmmian. In the Bade!1ian, ma rine LithOlhamnium limestones and sands werc depositcd along the contemporary inncr edge of tbe SWEZ. Later move ments led to the development of regular step faults, the intervening blocks of which were antithetically rotated. Sedi "'". - mentation ofthe biogenic limestones took place on the slTUctural benches formed in -~ - --- this way but the sandy and Lithothamnj lilll-detrital scdimcnts accumulated in Cl --~ -...... ----" __of__ lagoons and bays. In the Sarmatian, sed ..~ J. Btnc:zyNIrl(ttl1): ...... - [...--'1 imentation was accompanied by tecton ic movements. The crustaI stress field ... o _JtricM... - probably had a large honzomal compo -- .".. 1 ,.u.. .",;I"*'Yp.u..dllQtlOmt.-M~ ....ig."-I. Localioo of South·Wesl Escarpment Zone ofTomaszowskic Roztoczc 1 nent at times, which is why the field was .K.. ",.".,OIltCt/I4I.aI_~"-"-/ltln reoriented. This Icd to the development _ ...1 ",.".,lIl"JOQ' ¥Id __d top ~ MMWieItIl... Geological setting ofdip-slip transverse faults. Also, older nomlal faults _"..1 ...."._~~ld_U"".,MM_i:ln became redevelopcd as thrusts. Rejuvenation of the ~ "'NalL.o_C'~ The SWEZ corresponds to an importanl geologi fault steps and both longitudinal and transverse ~ l¥IO'<..,IId,>UN aI Upper e-.u" cal boundary which is often regarded as the edge of troughs gradually led to a relatively large-scale deniv o "'ucI_,.IOd~dS-_ tbc Carpathian Foredeep Basin. According to Ney elation in the escarpment zone ofthe Carpatbian Fore _ .'me_,..1/IdI _UIId._.ofa-"",,, (1969), Jaroszewski (i974) and Zelichowski (1974) deep Basin. For some lime afterwards, the SWEZ 1-::::=1 _ llId ~ fl~1fI in",. conop/I. oIlo4&.ozoI<: , CaillOZoI<: rodll it was fomlcd along the deep-scatcd thrust zone which along the present inner scarp of Roztocze was tec 1-"'11 "'''lgflplW; bo 14 15 The dependence ofrelief on tectonics in the South~West Escarpment Zone... Teresa Brzezinska-W6jcik of morphotectonie elements in the escarpment zone and the higher tcrmces (Buraczytiski, 1980/1981). In is a direct result of the presence of active linear the Sopot Gorge, between Nowiny and Hamernia, '\ structures, to which morpbotectonic scarps ofNW there are two series of steep rapids: the higher in SE and WNW-ESE orientation are related. Lower Campanian gaizes and the lower in Badcman Recent detailed geological investigations in Roz organodetritallimestones (Figs. 2, 3, 4, 5). tocze have produced radically new interpretations In the escarpment zone of the Tomaszowskie concemingthe relationship between reliefand structural Roztocze, three topolioeaments are dominant 281 elements. The main rclieffonns ofthe SWEZ express 290" (24,7%), 51-70"(19,2%) and 31 H30" (11,2%). the tectonic fragmentation of tbe Mesozoic and In respect of the morphological scarps, two trends Cainozoic rock foundation. The tectonic activity took may be identified: 301-330" (44,7%) and 71-1 IQ<' place intennittcotJy from the Mioccne to lhe Early (33,9%). The tectonic scarps trend at 29l-320ll Plcistocene and was accompanied by erosion and (61,2%). The azimuths of the known faults are denudation (Jahn, 1956; Maruszczak & Wilgat, 1956; concentrated in two ranges: 301-320" and 51-600; Buraczyitski, 1980/1981; 1984; Harasimiuk, 1980; the 341-360° trend is poorly developed (Brzezin Brzezllisk.-W6jcik, 1996; 1997.). ska-W6jcik, 1996; 1997.). Breach valleys developed in the zones of SW The joints in the Lower Campanian gaizes in the NE transvei'5C faults. Between G6recko KOScielne and Sopot channel near Nowiny (Fig. 4) and those in the G6recko Stare the narrow valley ofthe Szum fonns a Lower Maestricbtian gaizes and marly gaizes near deep gorge in tbe escarpment zone ofRoztocze (Figs. Tereszpol (Fig. 6) are closely parallel with the trends 2, 3). In its floor, gaizes of Lower Campanian age offaults and main scarps. As the extensive longitudi give rise to steep rapids wbich trend 305-325°. On nal, orthogonal joint systems are dominant. it is f-;==,----"-----'----L-----, S'''~.J--"---7":_ the NW side of Brzezinska Gera, where it reaches reasonable to conclude that they may have been acti I'''' .. j SQtJtStNMv 10_ L.._~,:.J<, the greatest gradient (12,5%0), the river has cut as vated quite reccntly; these parallel the courses ofthe ~ _~fO~1igr4PftIC~ ~ much as 10 m into the outer hill zone (Buraczynski, longitudinal faults. A similar system of longitudinal ~=~=-- 1980/1981). The Niepryszka valley intersects Pad61 joint fissures has detennined the orientation the inner ~alJays on IIta r8lHlli'Knn cl IIta St~ooOw Arrtdt>e J6zefowa obliquely and crosses the outer edge ofthe hills ofthe Roztocze SzciebrzeszyIiskie escarpment ...le' ~MJ~.,..",...... $l....~ SWEZ in the transverse fault zone (Jaroszewski, zone. ..* __~II_1 Ion /Ite.u.01/". St....JIa'ooow AMd"1ta) ~~-"-" HUla"\. 1977). In the escarpment zone, the valley reveals the The comparisonofjoint trends in Lithothamnjum ~ ~mntIMl"'" RManlea.a denud._ ot -.._ -~ fracture in the profile ofboth the present floodplain limestones in the TereszpoJ Hills and those in the o 2 4 &km I I --_I ,...... _.. - ~ l'ig. J. Structural elements in the relief ;·f--r"'------K-"'-~ . '- ,.... The relationship between directions of systems: NW-SE and WNW-ESE, patterns also 3 -l.ao.dfomL. 17 16 Teresa Brzezinska-W6jcik The dependence ofrelief on tectonics in the South-West Escarpment Zone... I. £ 1 ! .. , transverse fissures of the Badeoian Litbothamnium limestones are not parallel with those in the Mae • \ stricbtian rocks. The longitudinal and transverse \ orthogonal fractures in the Badenian rocks areequaUy \ 0"'.' • i ,.• \ represented in field surveys. Therefore, no particular \ •, trend in the fracture system is evident. Theorthogonal • ,. \ • , system of joiots in tbe Badenian limestones has \ • \ o i detennined the form of inner inselberg hills in the \ • . , / Tercszpol region. • ,l __ .... / \ • In the Upper Badenian organodetritallimestones \ • .., of the Pardys6wka Hills, the ortbogonal fracture o , • , system is accompanied by an oblique set, in which tbe transverse trend (61-90°) is dominant; this is also • : • ,I present in the Lithotbamnjum limestones of the • , Tereszpol region. The existence of two overlapping o • • joint systems in the Upper Badenian organodetrital • limestones accounts for the irregularity ofthe lower o • • o steep rapids in the Sopot channel and the great ·I variation in the height of the rapids is attributed • to the generally massive form of the limestones. • m • Diagonal, transverse joints are significantly re •, , .".' • sponsible for manyofthe features ofthe SoPOl Gorge --_... .-- : -. B area. Fig. 6. The gcologyoftbe Tereszpol (1;gion (after Jaroszewski, 1977; CteSlmski, Kubica. Rzechowski. : i ..... ! There is a clear correlation of changes between 1994; Kur\::owski. 1994; Popielski. 1994) .;.... / Q the trends of the major relief elements and those of I- tmwoI atod poaumcol fluID:; 2 - .,..;~ ~ } - &Km' - pitts atod nwty pozfS 0(l..ower ~htiaI, , . pP.Nb - ~ SlII>ds orthe Badmian, pcNb - AN!sIooon of the Back:niaa, ...~ - rcd~ of..BadmIaot, , joint sets. In the southern part of the escarpment "1'Nb' - oopoodtbilallimesmbrs r:Jfdoe border _ of the Bodtroiaa. pNb-' - quua:ie and alaoocoooiric .....oflfRa zone (the Pardys6wka Hills) NNE-SSW joints are Ibdeouaol. wNb' -! j,lqbampiwu lirronu>nel ofupper Dadenian, i."lo-clIyo: aDd IOlLOds&ora wiltl and)'"-lI(KnkI;owicdie [[] KOimml1nnSpOrl'b~ ,! ! dominant and these are parallel with the scarps, lounI) ofthe Sonnatim; 4 - directiooo of from coua bcddina [J whereas to the NW ofTereszpol they arc replaced by • a more-or-less meridional set; this has fashioned the • main elemcDts of thc escarpment zone. The main • • elements ofrelief(the outer and inner scarps and the • Pad6l 16zefowa) of the Roztocze escarpment zone • >...., parallel the course ofthe longitudinal faults and those o of secondary importance - tbe orthogonal and • • ! diagonal joint sets (Figs. 3, 4. 6, 7, 8). • In order to identify the scarps and valleys con· • trolled by the lithostratigrapbic boundaries. trends of • the main relief elements, tbe course of faults and " • fractures and litbostratigraphic boundaries, have been " " analysed Numerous short denudation scarps which arc • " o Dot paraDel with any ofthe dominant trends have also " • been recognised (BrzeziJ\ska-W6jcik, 19973) (Fig. J). ! Some relief elements are parallel with the fold ! axes. The Ciotusza Nowa·Kunki depression follows ..... Fig. S. Longitudinal profile ofthe Sapot valley the lacnia-Werchrata Syncline. Therefore. it may be 1 - ADdy plain; 2-~ ~} _ boo"'D rauh$; 4_p=uoooed .... faults; S - SIC'q)"",,(Is in the ri...... bed; 6 - mIjor ..np regarded as a synclinal depression which follows the courses of the NW-SE faullS. According to Bura 1~~~I-1 ~ I.. Upper Badenian organodetrital limestones in the czynski (1995), the rescquent elevations in the NE 1--1- ~- Pardys6wka Hills indicates a rcoricntation oftile stress part of the Sopot Hills and the NE part of tbe Gra ,- field during thc Miocene in the escarpment zone bowica Plateau follow the Stanislaw6w Anticline. The betwcen Nowiny and Tereszpol (Figs. 3, 4, 6). The valleys between Ciotusza Nowa and Grabowica and Fig. 7. Structural elemenlS in the relief of the Sopot breach valley ---- orthogonal system is predominant in the wholcoflhis Dtugi K4t and Ciotusza Nowa follow the radial joint t - primary K&IJlS n:1alins to main fauits; 2 - _ondMy JeVP:!I n:latinl to lioull3;} - KafPS n:Winllf) lithostralipphic boundaries: 4 - dcmodarion scarp;; , - vallo:ys KCOrdiul to faultJ; 6-~ n:lllli"i to lithosuatignphi< \lolmdaries; 1 ~ zone. The longitudinal joint fissures parallel the fissures of Staoislaw6w Anticline (Brzezinska-W6j dmlOClatlon valley$; I - raidual hills n:laiinllOpM rlAUfa; 9 - ruiduo.l bills n:btiollDjoinl fl$$Ul'a andlitbno:lnOIigr2phic fractures in the Lower Maestrichtian gaizes but the cik, 19973) (Figs. 2, J). bouoocluiea; 10 -Iboes; ! I -lan 18 ). 19 Teresa Brzezif'lska-W6jcik The dependence ofrelief on tectonics in the South-West Escarpment Zone... Adam6w Pasieki ~ OI/fIlroaqnd/09't_-..,.. Fig. 8. Sln1ctura1 elements in the reliefoftbe Ten::szpol region ~ _~d/09'tlKftlnoC~ I- pn.-y lIC:IrJS rdIcilIIlO maiII fadta; Z - ~ IQtpI: Id..10 faults; 1 - sc:arpI Rbrlq 10 htllollrlti»...... botmcIario$; .. - ~~ S- SIrUClIInlI-rKe;6 -valkyt!'dalull1O (ouhs; 7 - ~aIIeYS rriall,,&1O li&llOslP~ ~ ~aI_t"""_-.orr ~ ~ boomcIarics; 1-dcnudau.:. valleys;: 9 - resocIuallulll 10 joiIII r..-, 10- Ililh rda!m& 11>JOInt r__ IedfJ'lk'_"""""'-_ ~ I>'Ot9I'* ~ c!eJn_ ~bouDcbncs; 11 -dunes ~_..., Morphotectonics of the escarpment zone partially follow thc morphological ones which were -'" first described by Harasimiuk (1980). o When the morphometric coefficients of drainage In the outer hills zone, the Tamowola and Ha ""--~~ ~j~ jrJi~rl E.J ..,.-.rJ_ I". _oIit>temi.. basin shape (RJ and of the mountain-front sinuosity memia Blocks arc the most strongly uplifted. The /l'lClo'p'lG1eCtonoc 0I0c:1<• I!:;;] •• IJ!Ie<1••• ,.,_ (S) of Bull and McFadden (1977) are applied 10 the Nowiny and Helacin Blocks are less so and the ,, ,, •, .~, new geological data, it is clear that the Miocene rocks Pardys6wka Block least of all. The blocks of Tar ...... - of the escarpment zone of Tomaszowskie Roztocze nowola and Hamernia, whieh are inclined anti -_ __ display features of a tensional regime. Tilted blocks thetically towards NE, arc cut by the border fault in Fig. 9. Morphoteclonics ofthe SWEZ (after: Bn.ezinsh-W6jeik, 1996, modified) along the outer edge (Pardys6wka, Nowiny), thrust the West and by the transverse faults in (he North (in faults which have led to the fonnation ofgrabens and the Szum valley) and in thc South (in the Sopot 1980/1981). The Pardys6wka Block, which is a geological structure of the block is rcOected in ils half·grabcns (Zwierzyniec, J6zef6w, Tanew) and valley). The sinuous nature of the ourer scarp re comf,X>site of several smaller blocks, has undergone relief. Valleys have dcveloped along the faults there; uplifted blocks in the inner zone (Tereszpol-G6recko presents the clearest evidence for the intensive uplift only limited uplift. The smaller blocks have been the faults separate the block into western and eastern Stare and Majdan Nepryski·Narol) are all readily of the blocks along the border fault (311-3200). In rotated antithetically and translocated along transverse structu.ral units. The coefficients of drainage basin identified. Valleys such as those of the Szum, the the zone ofthe borderfault system. the deeply incised, faults. The Niepryszka valley divides this block into shape (R) and ofmountain-front sinuosity (.5) indicate Nieprysz.ka, the Sopot, and the Tanew Gorge at narrow valleys oftbe Szum and Sopot, botb ofwhich an inactive northern part and a southern, where there that different parts oftbc block have been affected by Losiniccki Potok all appear to have developed along have steep rapids in their river beds, and Darrow has been intense activity. The coefficient of the movements of different intensity and direction. The the lines of the transverse faults which separate the erosion terraces on valley sides, are further evidence mountain-front sinuosity (.5) suggests considerable valleys which divide the block are depressed whereas blocks. Further, there is little doubt that the faults are of this uplift. Near Pad61 J6zefowa (Figs. 2, 9), the activity in the border dislocation and uneven and the northern edge ofthe western part ofthe block, on still active (Bn:eziitska-W6jcik, 1996; 1997b) (Fig. 9). blocks have becn slightly depressed. As indicated limited uplift ofthe blocks (Brzezinska-W6jcik, 1996; the transverse fault line, is strongly uplifted. The Szum Antithetic outer blocks of Helacin, Tamowola, by the values of the coefficient of mountain-front 1997b) (F;gs. 2, 3, 9). valley has evidently suffered tectonic depression in Pardys6wka, Hamemia and Nowiny and inner ones sinuosi()' (5), the Nowioy Block is weakly uplifted In the inner blocks zone, that of G6rniki Nowe the Quaternary. The eastcrn edge ofthe block exhibils of G6recko Stare, G6rniki Nowe, Majdan Sopocki, along the border fault and the transverse fault ofSopot. is the most strongly uplifted whereas the G6recko little evidence of tectonic uplift. The complicated Grabowica and Paary have all been identified in the The northern part of the block does not show any Stare, Majdan Sopocki and Grabowica Blocks have geological structure of the G6rniki Nowe Block escarpment zone. These are separated by troughs tectonic activi()'; this may be due to a superimposition undergone only limited uplift. The G6rniki Nowe appears to reflect a variable tectonic activity in the which trend NW-SE (Sopol. J6zef6w, Susiec, Ta· of various movements acting on this block and the Block is one ofthe better understood structures. both Quaternary (Figs. 2, 3, 9). The G6recko Stare Block new) as well as by valleys developed in the zones of area of the Sopot Gorge (Fig. 9). The steep gradient in terms of its geological foundation and its tectonic is cut by a systcm of faults (Jaroszewski, 1977) and the SW-NE faults (Szozdy-Tereszpol Zygmunty, ofthe river channel (up to 27,9%0) (Fig. 5) and thrce history. In the Nonh it is intersected by the Szum SW exhibits only limited tectonic activily. The coefficient Floriallka, Szum, Niepryszka, Sopot, Tanew with systems of erosion tcrraces represent finn evidence NE transverse fault and also by the antithetic NW of the mountain·front sinuosi()' (5') indica.tes only Jelen and Losiniecki Potok) (Figs. 2, 9). These blocks for uplift of the Sopot breach valley (Buraczyrlski, SE oriented faults (Jaroszewski, 1977). The complex weak uplift along the faul! which separates it from 20 21 Teresa Brzezinska-W6jcik The dependence ofrelief on tectonics in the South-West Escarpment Zone... Pad61 J6zcfowa and the Florianka vaUey. The Majdan coefficients ofdrainage basin shape and ofmountain following the methods of Bull & McFadden (1977), Buraczynski, J., 1984: The influence of neotec Sopocki Block is confined by fauhs in the West front sinuosity as well as the thin cover ofQuaternary also indicate that the border fault system is still tonics on development of valleys ofthe escarpment and South. It has sulTered weak uplift along the deposits (Figs. 2, 3, 9). tcctonically active; also that there has been recent zone of the Roztocze [Summ.]. Rocznik Po/skiego longitudinal inner fault and the transverse fault of intensive uplift ofboth inner and outer SC3Ips. They Towarzyslwa Ge%gicznego 54, 112: 209-225. Sopot and Dlugi K:tt whereas tbe north-eastern part confirm that, in Roztocze, the zone ofthe south-west Buraczytlski, J., 1995: Geomorphological regions has been depressed. The Grabowiea Block is very Conclusions escarpment is the most variable in terms of recent ofthe Roztocze [Summ.]. Annales UMCS, LubLin, B, compact and slopes to the NE. The south-west edge tectonic activity. The values ofmorphometric indices 48 (1993): 59-73- ofthe Grabowica Block is composed ofseveral steps At present, the SWEZ has a striking morphological confirm earlier views about thecontemporary tectonic Chalubiilska, A., K~ik, A., Maruszczak, H. & which descend to the Susiec Depression. The block identity. But there is much evidence that this zone is activity ofthis part ofRoztocze. They also indicate a Wilgat, T., 1954: Przewodnik wycieczki na Roztocze. is cut by W-8E faults along which dry valleys have an old geological and paleogeomorphological element distinct differentiation oftectonic activity within the In: Pnewodnik V Zjazdu Polskiego Towarzyslwa developed. According to Harasimiuk (1980), open which has been redeveloped tectonically many times. various morphotectonic blocks. Geograjicznego. Lublin: 87-124. (in Polish only). joints are present in the chalk bedrock, along which The evidence includes: the disappearance of the CieSliflski, S. & Rzechowski, J.• 1993: Mapa vertical translocations of5-7 m amplitude have taken deep water facies of the Krakowieckie clays at the geologiczna podloza czwartorz~uRoztocza mi~ References place. The values ofthe coefficients ofdrainage basin escarpment zooe; the traces of Badenian cliffs Dear Tomaszowem Lubelskim a Hrebennem. 1n: M. shape (R) and of the mountain-front sinuosity (S) J6zef6w and a wide range ofBadenian reefsediments. Harasimiuk, J. Krawczuk & J. Rzechowski (Ed.). Areti B., 1962: The Mioceneofthe Lublin Roztocze point to a considerable uplift ofthe south-eastem part Neotectonic effects simply followed old influences Tekloni/ca Rozlocza i jej aspekly sedymenlologiczne, Region between the Sannaand Tanew RivCTS [Summ.]. oflhe block and a depression in its north-eastern part. in the basement. Hence, new faults and open joints hydrogeologiczne i geomoryologicznQ-krajobrazowe. Prace Instylulu Geo/ogicznego 30: 5-86. TheGrabowica Block suffered antithetic rotation from largely control the contemporary appearance of the Wyd. TWWP, Lublin: 38-46 (in Polish only). Areri B., 1968: Mapa geologiczna Rozlocza SE to NW, as is shown by measurements oftectonic escarpment zone. Dcformed river terraces in the CieSliilski, S., Kubica, B. & Rzechowski, J., 1994: LubelsJciego mii;dzy Sannq a Tanwiq 1:200 000. activity during the Quaternary (Brzezitiska-W6jeik, breach valleys are also evidence for new tcctonic Mapa ge%giczna Po/ski. 1:200000. Tomaszow Wydawnictwo Instytutu GeologicZllcgo, Warszawa. 1996; I997b) (Figs. 2, 3, 9). redevelopment ofthe area. Certainly, the conclusions Lubelski, Do/hobycz6w. B - Mapa bez utworow (in Polisb only). The grabens which separate the outer from the inner ofJabn (1956) concerning postglacial vertical tectonic czwartoTZi;dowych. Wydawnietwo Kartograficzne Baraniecka, M. D., 1983: The Malopolska, Ku· blocks (the Szum, J6zef6w and Susiec Depressions) movements in the escarpment zone and those of Ha Polskiej Ageneji Ekologicznej S.A., Warszawa 1996. jawska and Mazowiecka phases treated as tectonic have been depressed only slightly. The Szum Trough, rasimiuk (1980) concerning the relationship between (in Polish only). phases in Quaternary of Poland. In: Malerialy 111 which is founded on the tectonic lines ofthe orthogonal the reliefelements and the nature ofthe disjunctive Czyzewski, J., 1929: Z badail nad sp~kaniem Krajowego Sympozjum: Wsp61czesne i neolekloniczne system (NW-8E and NE-5W), was generaUy weakly tectonic structure in Roztocze have amply been con krcdy senonskiej poludniowcgo RoZlOCza. Pneglqd ruchy skorupy ziemskiej w Polsce. 4, Ossolineum, depressed in the Quaternary, as indicated by the firmed by recent investigations. Geograjiczny9: 1-12. Wroclaw: 183-193. coefficient ofdrainage basin shape and ofthe mountain The main elements ofthe escarpment zone relief Harasimiuk, M., 1980: Rzeiba Slruktura/na Brzeziilska-W6jcik, T., 1995: Quaternary tectonic front sinuosity as well as the considerable thickness in Roztocze are directly related to the geological nyzyny Lubelskiej i Roztocza. Rozprawa habilita activity in the Tanew river basin in Roztocze [Summ.]. (>50 m) ofQualemary deposits it contains. The values structure. Normal, shallow longitudinal and transverse cyjna Wydz. BiNoZ UMCS, Lublin: 1-136. (in Po Annales UMCS, B, 48 (1993): 25-43. ofthe coefficients obtained for its southern-west part faults andjoints in the rocks ofUpper Cretaceous and lish only). Brzezinska-W6jcik, T. 1996. Unpublished: Wp/yw indicate great activity in the vicinity ofthe Szum Gorge. Miocenc havc been vcrY important in the development Harasimiuk, M., 1984: Rola tektoniki i litologii blldowy geoJogicznej na rozwoj rzeiby Roztocza This is indicated by the steep rapids in its channel, a ofthe main relief fonns. The main scarps (outer and w ewolucji sieci dolinncj Wyzyny Lubelskiej i Roz Tomaszowskiego i Rawskiego. Praca doktorska. deep incision (up to 10 m), a steep gradient (13,3 %0) inner), the valleys (e.g. the Tanew valley) and the tocza. Pnewodnik LV1 Zjazdu Polskiego Towarzy Archiwum Bibtioteki GI6wnej UMCS, Lublin, 1996: and a convex profile ofthe raised terrace which COD depressions (J6zef6w, Stanistaw6w-Kunki) have been stwa Geologicznego, 13-15 IX 1984 Lublin, Cz. 1: 1-120 (in Polish only). trasts to a concave profile in the lloodplain tcrracc (Bu developed in the zones of longitudinal faults or 66-68. (in Polish only). Brzezinska-W6jcik, T., 1997a: Topolineaments of raczyilski, 1980/1981). The Susiec Depression is also Tertiary fault troughs. The valleys of the Szum, Jabn, A., 1956: Geomorphology and Quaternary the escarpment zone ofthe Tomaszowskie Roztocze founded on the faults ofthe orthogonal system; these Niepryszka, Sopot and Potok Losiniccki and certain history of Lublin Plateau [Summ.]. Prace Geo and their connection with the structural plan of took place in the Sarmatian and relate to a phase ofthe scarps appear to follow transverse faults. In the grajicz"e PAN, Warszawa 7: 1-453. bedrock [Summ.]. Annales UMCS, B, 52, 3: 41-56. EastCarpathian movements. They created an hiatus in escarpment zone, an orthogonal joint system is Jaroszewsk..i, W., 1974: Tekronikn uskokOw i /al Brzcziilska-W6jcik, T., I 997b: Tectonic activity the Miocene succession. The coefficient ofmountain predominant. Joints of the diagonal system are of dOw. Wydawnictwa GeologicZlle. Warszawa: 1-295. of the escarpmcot zone of Tomaszowskie Roztocze front sinuosity (5) indicates a considerable activity considerable importance in the development of (in Polish only). in the light of roorphomeuic coefficients [Summ.]. along the northern and eastern scarps as well as secondary forms ofthe border zone relief, particularly Jaroszewski, W., 1977: Sedimentary' evidence for Annal.. UMCS, B, 52, 4: 57-75. pronounced depression below these scarps. Pad61 in the Tereszpol region ofthe escarpment zone. Miocene tectonic activity in the Central Roztocze Bull, W. B., McFadden, L. D., 1977: Tectonic J6zefowa is an exampleofa second~rder fault trough The distribution and trends oftopoLineaments are [Summ.]. Przeg/qd Geologiczny 25, 8-9: 418-427. geomorphology north and south ofthe Garlock fault, which was developed in the zone ofreverse faults and a function of differentiated neotcctomc movements Jaroszewski, W.• 1994: eotcktonika i rucby California. In: D. O. Doehring (Ed.). Geomorphology associated antithetic step faults. An antithetic rotation on a regional scale: this supports earlier conclusions wspOlczesne./n: R Dadlez&W. Jaroszewski (Eds.), in arid regions. Binghamton symposia in geomor is manifested by the depression ofthe trough towards based on hydrological data (Liszkowski, 1975; Mali Telclonika. PWN, Warszawa: 423-485. pholo&>, 8: 115-138. the NE and an increase in the thickness ofQuaternary nowski, 1977). Jaroszewski, W., Pi:ttkowska, A., 1988: On the BuraCZ}'liskiJ., 1974: Essai geomorphologique du deposits in this direction. The western part of Pad61 The very clear correlations between relief and nature ofsome lineaments (exemplified by the Roz Roztocze Rawskie [Summ.]. Annales UMCS, B, 29: J6zefowa has suffered only limited depression; this is various elements ofgeological structure in Roztocze, toczc Rigde, SE Poland). Annales Socielalis Geo 47-76. presumably due to lheantithetic uplift ofthe outerhills. particularly in its south-west escarpment zone, imply /ogonlm Poloniae 58: 423-443. Buraczyfuiki, J., 1980/1981: Development ofVal· The Majdan Ncpryski Block;o the eastern pan ofPadOl that this area is particularly suitable for analysing these Kosmowska-SuffczyIiska, D., 1998: Dependence leys in the Escarpment Zoneafthe Roztoczc. Annales J6zefowa has suffered weak antithetic uplift along its relationships by cartometric methods (Brzezinska ofreliefdireclionalily on joint panern (exemplified UMCS, B, 35/36: 81-102. western edge; this is shown by the values of the W6jcik, 1996; 1997b). Morpbometric calculations, by nonh·eastem margin ojSwii;tokrzyskieMoumains) 22 23 Teresa Brzezjr'lska-W6jcik [Summ..]. Wydzial Geografii i Studiow Regiooalnych Ney, R., 1966: Wgl~bny przekr6j kraw~dzi Roz UW, Warszawa: 1-165. tocza w Jozefowie. Sprawo-diania z posiedze1i Komisji Kowalski, W. C. & Liszkowski, J., 1972: The Nauk PAN, Oddzial w Krakowie 9, 2: 520--524. (in dependence between the recent vertical movements Polisb only). of the Earth crust in Poland and its geological struc Ney, R.. 1969: Pi~tra strukturalne w pOlnocnQ ture. [Summ.]. Biuletyn Geologiczny UW, Warszawa, -wscbodnim obramowaniu zapadliska przedkarpa 14: >-19. ckiego. Prace Geologiczne PAN. Oddzial Krakowski Krzywiec, P. & PielSCh, K., 1996: Tectonics and 53, s. 106. (in Polish only). depositional conditions of the Carpathian Foredeep Oszczypko, N., 1996: The Mioccne dynamics of Basin between Krak6w and Przemysl as a results of tbe Carpathian Foredccp in Poland [Summ.]. Przeglqd regional seismic profiles [Summ.]. Zeszyty Nallkowe Geologiczny44, 10: 1007-1018. AGH, Gcolog;a, 22: 49-59. Pawlowski, S., 1938: Sur la morpbologie de la Krzywiec, P. & Jochym, P., 1997: Characteristics Iisiere meridionalc du plateau de Lublin. Bull. Intern. ofthe Miocene subduction zone ofthe Polish Carpa de L'Ac. Pol. et de Lettr. Cl. de Se. Mat. et Nal. Serie thians: results of flexural modelling [Summ.]. Prze A. (Se. Mat.). Cracovic: 366-372. glqd Geologiczny 45, 8: 785-792. Popielski, W., 1994: Objainienia do "Szczego Kurkowski, S., 1994: Objainienia do "Szczegolo lowej mapy geologicznej Polski. arkusz Tereszpol wej mapy geologicznej Polski, arkusz KrasnobrOd (893), 1:50000". Wydawnictwo PaJistwowego Insty· (894), 1:50000". Wydawnictwo PaJistwowego Insty tutu Geologicznego, Warszawa: Tab. n, 1-35. (in tutu Geologicznego, Warszawa: Tab. n, 1-34. (in Polish only). Polish only). Poiaryski, W., 1974: Obszar swi~toknysko-Iu· LindnerL., WojtanowiczJ., Bogutsky A. B., 1998: bclski.ln: Budowa geologiczna Polski.W: Tektonika. Main stratigraphical units of the Pleistocene in Cz. I. Wydawnictwo Panstwowego lostytUtu Geolo southeastern Poland and the noIthwestern Ukraine, gicznego, Warszawa: 314-362. (in Polish only). and their correlation in Western and mid-eastern ROhle, E., 1976: The dynamics of litosphere in Europe. Geological Quarterly 42(1): 7>--86. the area o/Polandduring rhe youngAlpinestroctural Liszkowski, J., 1975b: The influence of crustal stage [Summ..].ln: Materia/y I Kraj. Symp. ,. Wspal movements on hydrogeological conditions in fracture czesne i neotektoniczne ruchy skorupy ziemskiej aquifers [Summ.]. WspOlczesne i neotektoniczne ruchy \J Polsce". T. n. Wydawnictwo Panstwowego Insty skonlpy ziemskiej w Polsce. J Krajowe Sympozjum. tutu Geologicznego, Warszawa: 112-125. Wydawnictwa Geologicznc, Warszawa, I: 279-290. Wyrwicka, K., 1977: Wyksztaiccnie litologiczoe Lomnicki, A. M., 1898: Atlas geologiczny Galieji. wC(glanowych surowc6w skalnych mastrychtu Tekst do zeszyw 10. Cz. 2, Krak6w (in Polish only). lubelskiego. Billletyn Instyrurll Geologieznego, 299: Malinowski, J., 1977: The influence of the neo Z badan zlOi surowcow ska/nych 9: 5-97. (in Polish tectonics on changes in hydrogeological conditions only). in the Roztocze area [Sunun.]. Kwartalnik Geolo Wyrzykowski, T., 1971: Map ofrecent absolute gicz1ly21,1: 51~8. velocities of vertical movements ofthe earths crust Malinowski, l., 1993: Wanmki hydrogeologicz surface on the territory of Poland, 1:2500 000. ne Roztocza w swietJe tektoniki.In: M. Harasimiuk, Instytut Geodezji i Kartografii, Warszawa. J. Krawczuk & J. Rzechowski. (Ed.) Telc101lika Rozto Zelicbowski, A. M., 1974: Obszar radomsko cza ijejaspe/ay sedymentologiczne, hydrogeologicz1le -krasnicki W: Budowa geologiczna Polski. lY. j geomorfologiczno-krajobrazowe. Wyd. TWWP, Tektonika. Cz. 1. Wydawnicrwo Patistwowego Insty Lublin: 109-117. (in Polish only). tutu Geologicznego, Warszawa: 113-128. (in Polish Maruszczak. H. & Wilgat, T., 1956: Le reliefde only). la zone Iisiere du Roztocze Central [Summ.]. Annales Zelicbowski, A. M., 1983: Tectonic map UMCS, Lub1in, B, 10: 1-107. 1:300 000. Tab. 43./n: Arias ofgeological structure Musial, T., 1987: Miocen Roztocza (Polska and mineral deposits in the Lublin region. Wy potudniowo-wschodnia). Biuletyn Geologiczny 31: s.... dawnictwo Panstwowego Instytutu Gcologicznego, 149. (in Polisb only). Warszawa. 24