NEO TEC TON ICS OF PO LAND: AN OVER WIEV OF AC TIVE …ac tiv ity, es ti ma tion of the para me tres of the neo tec tonic stress field, ampli tudes and rates of Qua ter nary and re

Studia Quaternaria, vol. 24: 5–20.

NEO TEC TON ICS OF PO LAND:AN OVER WIEV OF AC TIVE FAULT ING

Wi told Zuchiewicz1, Janusz Badura2, Marek Ja ro si ñski3 and Com mis sion on Neo tec ton ics,Com mit tee for Qua ter nary Re search, Pol ish Acad emy of Sci ences

1In sti tute of Geo logi cal Sci ences, Jagiel lo nian Uni ver sity, Ole an dry 2A, 30063 Kraków, Po land;e- mail: wi [email protected]

2Pol ish Geo logi cal In sti tute, Lower Sile sian Branch, al. Ja wor owa 19, 50- 122 Wroc³aw, Po land;e- mail: [email protected]

3Pol ish Geo logi cal In sti tute, Ra kow iecka 4, 00- 975 Warszawa, Po land; e- mail: marek.ja rosin [email protected]

Ab stractNeo tec tonic stud ies in Po land con cern mainly mani fes ta tions of those tec tonic move ments that have been ac tive inLate Neo gene and Qua ter nary times, as well as geo deti cally meas ured re cent ver ti cal and hori zon tal crus tal mo tions.Among prob lems of par ticu lar in ter est, the fol low ing should be listed: pe rio dic ity of neo tec tonic (mostly Qua ter nary)ac tiv ity, es ti ma tion of the para me tres of the neo tec tonic stress field, am pli tudes and rates of Qua ter nary and re centmove ments, de vel op ment of neo tec tonic troughs and young faults, mu tual re la tion ships among pho to linea ments, geo -logi cal struc tures and re cent seis mic ity, as well as the role of tec tonic re ac ti va tion of fault zones due to hu man ac tiv ity. Neo tec tonic faults in Po land have de vel oped in Neo gene and Qua ter nary times due to re ac ti va tion of La ramian orolder struc tures, or in the Qua ter nary due to re ac ti va tion of Neo gene faults. The size of throw of Qua ter nary faultschanges from 40–50 m and >100 m in the Sude tes and the Lublin Up land, to sev eral – sev eral tens of me ters in the Car -pa thi ans. The av er age rate of fault ing dur ing Qua ter nary times has been 0.02 to 0.05 mm/yr, what en ables one to in -clude these struc tures into the do mains of in ac tive or low- activity faults. A simi lar con clu sion can be drawn from there sults of re peated pre cise lev el lings and GPS cam paigns. Strike- slip dis place ments have been pos tu lated for some ofthese faults. Iso lated faults in Cen tral Po land have shown mid dle Qua ter nary thrust ing of the or der of 40–50 m, andsome of the Outer Car pa thian over thrusts tend to re veal young Qua ter nary ac tiv ity, as in di cated, i.a. by con cen tra tionsof frac tured peb bles within the thrust zones. Epi sodes of in creased in ten sity of fault ing took place in the early Qua ter -nary, in the Ma zo vian (Hol stein ian) In ter gla cial, and dur ing or shortly af ter the Odra nian (Dren the) gla cial stage.Some of the faults have also been ac tive in Holo cene times. Re cent seis mic ac tiv ity is of ten re lated to strike- slip faults, which in the Car pa thi ans trend ENE–WSW and NE–SW, whereas out side the Car pa thi ans they are ori ented par al lel tothe mar gin of the East- European Plat form and the Sudetic Mar ginal Fault. Fu ture in ves ti ga tions should put more em -pha sis on pa laeo seis mo tec tonic phe nom ena and prac ti cal ap pli ca tion of neo tec tonic re search.

Key words: neo tec ton ics, ac tive fault ing, Po land

NEO TEC TONIC SUB DI VI SION

From among dif fer ent defi ni tions of the neo tec tonic pe -riod (cf. Zuchiewicz 1995), for the pur pose of this pa per wehave cho sen that pro posed by ªengör et al. (1985): ..."thetime that elapsed since the last ma jor whole- scale tec tonicre or gani za tion“. Ex ten sive bib li og ra phy per tain ing to theneo tec ton ics of Po land can be found in Zuchiewicz (2003),whereas abridged re views of mani fes ta tions of young tec -tonic move ments are com prised in a few pub li ca tions (e.g.Rühle 1973, Ostafic zuk 1995, Zuchiewicz 1995, 2002, Ja ro -si ñski 1999, 2005; and ref er ences therein). Be neath, we shalldeal with some as pects of young fault ing only, and par ticu -larly in ar eas situ ated out side the Al pine oro gen, i.e. north ofthe Car pa thi ans (Fig. 1).

A pro posal of neotectonic- structural sub di vi sion of Po -

land, pre sented by IGCP Pro ject 346 Neo geo dy namica Bal -tica (Kara ba nov, Schwab 1997) for the Bal tic coun tries,in cludes the fol low ing 1st- order units (Fig. 2):

– Baltic- Belarus Syne clise, in clud ing both the ar eas sub -sid ing since the on set of the Oli go cene, and those origi nallysub sided and then up lifted;

– Central- European Sub si dence Zone, in clud ing theOdra De pres sion and West Bal tic Step (sub sided since theOli go cene), as well as the Pom era nian De pres sion and Cen -tral-European High;

– Central- European Zone of Up lift, in clud ing the Lu sa -tian-Sudetic and Holy Cross blocks, as well as South- Polish– Po do lian Up lift, up lifted since the Oli go cene;

– Car pa thian Fore deep, show ing dif fer en ti ated sub si -dence and up lift;

– Car pa thi ans, show ing dif fer en tial up lift.

To the mem ory of Prof. Jerzy Lisz kowski

The great est geo dy namic haz ard, apart from the Car pa -thi ans, can be ex pected in the Central- European Zone of Up -lift, and par ticu larly in the Lusatian- Sudetic Block.

AM PLI TUDES AND RATES OFQUA TER NARY CRUS TAL MOVE MENTS

The am pli tudes and spa tial dis tri bu tion of zones show -ing Qua ter nary tec tonic mo bil ity have been treated dif fer -ently by dif fer ent authors, de pend ing on the time scale

con sid ered (cf. Zuchiewicz 1995, 2000). Ac cord ing to Rühle (1969, 1973), the am pli tude of Qua ter nary up lift ex ceeded100 m in NE Po land, as well as in south ern Lublin Up landand Roz tocze re gion, while sub si dence ten den cies (–50 to<–100 m) were con fined to the lower Vis tula River val leyand NW Po land (Figs. 3, 4). Large thick nesses of Qua ter narysedi ments (>200 m) within tec tonic gra bens and de pres sionsin the Kuyavian- Pomeranian Swell and in the East- EuropeanPlat form, how ever, in di cate higher am pli tudes of ver ti calmove ments (Rühle 1973, Ba ra niecka 1975, 1980). There -

6 W. ZUCHIEWICZ et al.

Fig. 1. Tec tonic sketch- map of Po land (based on Zno sko (ed.) 1998; modi fied). Ar eas of Al pine fold ing: I – Car pa thi ans, II – Car pa thianFore deep. Ar eas of Pa laeo zoic fold ing. Cale doni des and Varis ci des at the ground sur face or un der thin sedi men tary cover: III – East Sude tes,IV – West Sude tes and Fore- Sudetic Block, VIII – Holy Cross Mts. Varis can oro genic troughs: V – Up per Sile sian Coal Ba sin, VI –Wa³brzych Coal Ba sin, VII – North- Sudetic Trough. Pa laeo zoic plat form: IX – Fore- Sudetic Mono cline and Silesian- Cracow Mono cline, X– ba sins (from NW to SE): Szcze cin, Mo gilno-£ódŸ, Miechów, XI – Mid- Polish An ti cli nor ium (Kuyavian- Pomeranian Swell), XII – Mar -ginal De pres sion. East- European Plat form. Low ered parts of crys tal line base ment over lain by thick sedi men tary cover: XII – Mar ginal De -pres sion, XIII – £eba High, XIV – Peri bal tic Syne clise, XVI – Pod la sie Low, XVIII – Bug Syne clise. Up lifted parts of crys tal line base mentover lain by thin sedi men tary cover: XV – Mazury- Suwa³ki An te clise, XVII – S³awatycze High (Horst).

NEO TEC TON ICS OF POLAND 7

Fig. 2. Neotectonic- structural units (based on Kara ba nov, Schwab 1997; modi fied).


Fig. 3. Neo tec tonic map of Po land (based on dif fer ent sources elabo rated by Zuchiewicz 2000; modi fied). KG – Kleszc zów Gra ben, OB –Orava Ba sin.


Fig. 4. Young faults in Po land (based on: Kow al ski, Lisz kowski 1972, Rühle 1973, Lisz kowski 1982, 1993, Hen kiel 1984, 1993, Dy jor1993, 1995, Ba ra niecka 1995, Dy jor et al. 1995, Krzysz kowski et al. 1995, Jura 1995, 1999, Ostafic zuk 1995, Ni tycho ruk 1996,Brzeziñska- Wójcik 1999, Ka si ñski, Pi wocki 1999, Ber 1999 and oth ers; modi fied by Zuchiewicz 2000). Ar eas in which neo tec tonic faultswere mapped: A – Lower Sile sia, B – Up per Sile sia, C – Lublin Up land and Roz tocze re gion, D – Pod la sie re gion, E – San dom ierz Ba sin, F –Holy Cross Mts., G – NE Po land (Suwa³ki area), H – NW Po land (in clud ing Szcze cin Low land), I – North- Polish Low land and up lands ofsouth- central Po land, K – Car pa thi ans. Neo tec tonic faults in Lower Sile sia: 1 – Mid dle Odra Fault Zone, 2 – Sudetic Mar ginal Fault (SMF),3a – pos si ble con tinua tion of SMF, 3 – Intra- Sudetic fault, 4 – Za toñ fault, 5 – Rêbiszów fault, 6 – Jerz ma nowice fault, 7 – G³êbinów fault, 8 –Bagieniec- Paszowice fault, 9 – Legnica- Chojnów fault, 10 – Sobótka fault, 11 – Strze lin fault, 12 – Prze worno fault, 13 – mar ginalKarkonosze fault, 14 – Z¹bkowice Œl¹skie fault, 15 – Do boszowice fault, 16 – Po mi anów Górny and Nysa faults, 17 – Bia³a G³ucho³askafault, 18–20 – faults as so ci ated with the Up per Nysa K³odzka Gra ben, 21 – Toszek fault. –100 – ten den cies of Qua ter nary ver ti cal move -ments (in me tres); KG – Kleszc zów Gra ben.

fore, the av er age rates cal cu lated for the en tire Qua ter naryap pear to be 0.04–0.06 and 0.08 mm/yr, re spec tively. TheQua ter nary neo tec tonic am pli tudes dur ing in di vid ual epi -sodes of in creased ac tiv ity ranged from 15–20 m (sub si dence in the Kleszc zów Gra ben dur ing the Pilica/Drenthe- WartheIn ter gla cial stage; cf. Brodzikowski 1987) and 20–30 m (up -lift of the Roz tocze re gion dur ing the Ma zo vian/Hol stein ianIn ter gla cial; cf. Hara simiuk, Hen kiel 1980) to 30–40 m (up -lift of some por tions of the Sude tes Mts., in the Ma zo -vian/Hol stein ian In ter gla cial; cf. Krzysz kowski et al.1995)and 70–100 m (early Pleis to cene up lift of some struc tures ofthe West Car pa thi ans; cf. Zuchiewicz 1991). The rates of

these move ments in the Pol ish Outer Car pa thi ans range from0.02 to 2 mm/yr (Zuchiewicz 1991, Zuchiewicz et al. 2002).

In North ern Po land, epi sodes of in creased neo tec tonicac tiv ity oc curred at the end of Plio cene, in mid dle (1.45–1.35Ma) and late Eo pleis to cene (1.15–1.00 Ma), and late Meso-pleis to cene (0.60–0.45 Ma) times (Mo jski 1991). The sub si -dence of the Ma zo vian De pres sion and the Bal tic De pres sionwas in ter rupted by gla cioi so static up lift that fol lowed everyScan di na vian ice- sheet re treat, be ing com bined with the re -ac ti va tion of base ment struc tures of the Kuyavian- Pomera-nian Swell (Ba ra niecka 1975, Lisz kowski 1993, Zuchiewicz1995).


Fig. 5. Re cent crus tal move ments and his tori cal seis mic ity in Po land (based on Pa gac zewski 1972, Wyrzykowski 1985, Hefty 1998, Ja ro -si ñski 1999, Zuchiewicz 2000).

The lat est ver sion of the map of re cent ver ti cal crus talmove ments in Po land, based on re peated lev el ling (Wyrzy-kowski 1985), ap pears to in di cate pre vail ing sub si dence(usu ally be tween 0 and –3 mm/yr) all over the coun try, ex -cept for weakly up lifted parts of Pom era nia and the SE por -tion of the Car pa thi ans (Fig. 5). The strong est sub si dence(<–3.5 mm/yr) is re corded in the Paczków Gra ben, LowerSile sia, up per Odra River val ley, and P³ock Ba sin (Figs. 4, 5). The re sults of re peated GPS cam paigns are avail able for se -lected ar eas of Lower Sile sia only (cf. Kontny 2003).

YOUNG FAULTS

Seis mo tec tonic faults in Po land have de vel oped in Neo -gene and Qua ter nary times due to re ac ti va tion of La ramian or older struc tures, or in the Qua ter nary due to re ac ti va tion ofNeo gene faults (Kow al ski, Lisz kowski 1972, Rühle 1973,Lisz kowski 1982, 1993, Hen kiel 1983, 1984, 1993, Dy jor1983, 1993, 1995, Ba ra niecka 1995, Dy jor et al. 1995,Krzysz kowski et al. 1995, Jura 1995, 1999, Ostafic zuk 1995, Ni tycho ruk 1996, Brzeziñska- Wójcik 1999, Ka si ñski, Pi -wocki 1999, Ber 1999, Zuchiewicz 2000, and oth ers; see Fig. 4). The first group in cludes, i.a. faults bor der ing the lowerVis tula River val ley, the es carp ment zone of the Roz tocze re -gion, SE Po land, and many fault zones in the Sude tes andFore- Sudetic Block, SW Po land, of throws rang ing from 100m (Leg nica - Cho jnów fault) through 600 m (Paczków andKêdzierzyn gra bens) to 800 m (Roz toka-Mok rzeszów gra-ben). In NE Po land, mani fes ta tions of Qua ter nary re ac ti va -tion of the Teisseyre- Tornquist zone and of faults per pen-dicu lar to it (NE–SW) have been en coun tered, ow ing tocombined ef fects of the mid- Atlantic ridge- push and com -pres sion ex erted by the Car pa thi ans (Czar necka 1993). Mostof these faults co in cide well with the pho to linea ments seenon sat el lite im ages and to po linea ments iden ti fied on digi talele va tion mod els (Ba¿yñski et al. 1984, Granic zny 1991,Ostafic zuk 1995, 1999).

The sec ond group of faults in cludes those of Lower Sile -sia (Wroc³aw - Ozimek, Prze worno - Wêgliniec, SudeticMar ginal Fault, a fault along the north ern mar gin of theKarkonosze Mts.; Dy jor 1983, 1993, 1995, Mi goñ 1991) andUp per Sile sia re gions (i.a. a se ries of E–W trend ing faultsshow ing re cently down faulted north ern limbs, cf. Czar necka1988), the NW–SE, N–S, NE–SW, E–W, and ESE–WNWori ented faults of the Lublin Up land and Roz tocze re gion(Hara simiuk, Hen kiel 1984, Hen kiel 1984, Bu rac zyñski1984), NNE–SSW and NE–SW ori ented faults in the north -ern part of the San dom ierz Ba sin (Laskowska- Wysoczañska1979, 1983), as well as sev eral oblique- slip, strike- slip, andthrusts faults in the Car pa thi ans (Zuchiewicz 1995, Zuchie-wicz et al. 2002; and ref er ences therein).

In NW Po land (Kopczyñska- Lamparska 1979) and onthe NW mar gin of the Holy Cross Mts. (Lind ner 1978), Qua -ter nary fault ing pro ceeded in the Cro merian and Hol stein ianin ter gla cials, while on the NE mar gin of the Holy Cross Mts.it took place in the War the and Eemian stages (Kosmowska- Suffczyñska 1986). In the cen tral part of the Holy Cross Mts.re ac ti va tion of Pa laeo zoic faults was no tice able in the earlyand mid dle Qua ter nary (Kow al ski 1995). Dur ing the Mid -dle-Polish (Saalian) gla cia tions and Eemian in ter gla cial, in -

ten sive sub si dence of some gra bens in north- eastern (Koci-szewska-Musia³ 1978) and north ern Po land (cf. Ostafic zuk1981) be came ap par ent. Gra bens of throws up to 40–50 morigi nated in the £ódŸ Up land dur ing Hol stein ian times (cf.Zuchiewicz 1995). Re cently ini ti ated stud ies of frac turedclasts in Qua ter nary flu vial se ries in the Car pa thi ans (To kar -ski, Œwierc zewska 2005, To kar ski et al. 2005b) point to re ac -ti va tion of some map- scale thrusts.

The size of throw of Qua ter nary faults (Fig. 4) changedfrom 40–50 m to more than 100 m in the Sude tes, Lublin Up -land, and In ner Car pa thi ans, and from sev eral to sev eral tensof me tres in the Outer Car pa thi ans. The av er age rate of fault -ing dur ing Qua ter nary times has been 0.02 to 0.05 mm/yr,what en ables one to in clude these struc tures into the do mainsof in ac tive (D) or low- activity (C) faults (cf. Slem mons &De polo 1986). Simi lar con clu sions re sult from re peated lev -el lings and GPS cam paigns.

Strike- slip com po nent has been sug gested for some Qua -ter nary faults, in clud ing the Sudetic Mar ginal Fault (Masta-lerz, Wo je woda 1990, To kar ski et al. 2005a) or JanowiceFault in the Lublin Up land (Hen kiel 1984). Soli tary faults inCen tral Po land (Kleszc zów Gra ben) rep re sent Mid- Quater-nary thrusts of dis place ments up to 40–50 m (cf. Ha³uszc zak1999, Go towa³a, Ha³uszc zak 2002).

Epi sodes of in creased in ten sity of fault ing took place inthe early Qua ter nary, in the Ma zo vian (Hol stein ian) In ter gla -cial and dur ing or shortly af ter the Odra nian (Dren the) gla cial stage. Some of the faults have also been ac tive in Holo cenetimes (Karkonosze Mts., Roz tocze re gion, Outer Car pa thi -ans).

The Qua ter nary fault ing is re flected in in creased thick -nesses of young de pos its on down thrown blocks (in clud ingstacks of colluvial- solifluction wedges; cf. Hen kiel 1993),de for ma tion of river ter races and al lu vial fans, changes of the drain age pat tern, clast frac tur ing, as well as in the for ma tionof cracks within Pleis to cene ice- sheets, con trol ling the pre -ferred ori en ta tion of gla ci flu vial ac cu mu la tion forms (e.g.Klajn ert 1984).

Faults ac tive in young Qua ter nary times are fre quentlyac com pa nied by pho to linea ments, nearly 70% of which co -in cide with mani fes ta tions of his toric and present- day seis -mic ity (Granic zny 1991).

SEIS MIC ITY

His tori cal seis mic ac tiv ity is of ten re lated to strike- slipfaults, which in the Car pa thi ans trend ENE–WSW andNE–SW (Ba¿yñski et al. 1984, Granic zny 1991), whereasout side the Car pa thi ans they are ori ented par al lel to the mar -gin of the East- European Plat form and the Sudetic Mar ginalFault (Lisz kowski 1982, Guterch, Lewandowska- Marciniak2002; see also Fig. 5).

A de tailed list of his tori cal earth quakes re corded in Po -land was pre sented by Pa gac zewski (1972), Guterch andLewandowska- Marciniak (1975, 2002), Pro chazková et al.(1977, 1978) and Pro chazková and Kar nik (1978). In theyears 1000–1970 AD, 89 earth quakes oc curred, half of themin the Lower Sile sia and usu ally along the Sudetic Mar ginalFault. The re cur rence in ter val for the Sude tes is 22 yrs, themaxi mum in ten sity of earth quakes at tain ing 8° MCS (Paga-


czewski 1972). Within the Car pa thi ans, earth quake foci usu -ally clus ter along the in ner (south ern) side of the Pi en inyKlip pen Belt and along some strike- slip and oblique- slipfaults (Orava Ba sin in 1995 and 2004; Krynica area in 1992and 1993); in other re gions they oc cur spo radi cally. Seis micin ten si ties of the Pol ish Car pa thian earth quakes range from 4to 7.5° MCS, whereas their mag ni tudes are be tween 3 and 5(Orava Ba sin, on 30 Nov. 2004, Ml = 4.3, Ms = 4.4; cf.Guterch et al. 2005). The strong est earth quakes were re -ported in 1785- 86 from the Žil ina area (Slo vak West ern Car -pa thi ans, close to the Pol ish bor der). Fo cal depths reach up to23 km, av er ag ing at 10–12 km, al though in the Orava Ba sinthese are usu ally around 5–6 km. Cu mu la tive mag ni tudes ofthe Car pa thian earth quakes point to a close re la tion ship be -tween epi sodes of in creased seis mic en ergy re lease and cli -matic fluc tua tions of the Lit tle Ice Age (cf. Zuchiewicz1989).

The dis tri bu tion of earth quake foci in Po land fol lowstwo prin ci pal di rec tions: the “Sudetic” (NW–SE) and “Scan -di na vian” (NE–SW) ones, be ing par al lel to the ori en ta tion ofmaxi mum shear stresses (cf. Lisz kowski 1982).

An other ques tion is the seis mic ity within ar eas of stronghu man im pact, fre quently re lated to re ac ti va tion of olderfaults due to sub sur face and open- cast min ing, as well as con -struc tion of ar ti fi cial wa ter res er voirs.

CASE STUD IES

As far as Qua ter nary fault ing is con cerned, the best stud -ied re gions are rep re sented by the Lower Sile sia, Kleszc zówGra ben, Lublin Up land, and San dom ierz Low land within the Car pa thian Fore deep (Fig. 4).

Lower Sile sia

Neo tec tonic map of Lower Sile sia, SW Po land, byBadura and Przy byl ski (2000) is the only de tailed neo tec -tonic map of a large frag ment of Po land that shows dis tri bu -tion of faults ei ther re ac ti vated or formed in Neo gene andQua ter nary times (see sim pli fied ver sion of this map in Fig.6). This map also por trays the dis tri bu tion of young- Alpinefolds and thrusts, ex po sures of young vol can ics, dis tri bu tionof hy dro ther mal and min eral wa ters, traces of young min er -ali za tion, and heat flow val ues.

From among faults re ac ti vated in Qua ter nary times, themost im por tant is the Sudetic Mar ginal Fault (SMF), nearly300 km long, which marks the bound ary be tween the up lifted Sude tes and sta ble and/or sub sided Fore- Sudetic Block (cf.Dy jor 1995, Dy jor et al. 1995, Krzysz kowski et al. 1995,Badura et al. 2003, Kontny 2003). Its NW seg ment shows,apart from dip- slip, a mi nor sin is tral com po nent, while theSE seg ment is char ac ter ised by pre domi nant dip- slip and,per haps, in sig nifi cant dex tral com po nent. This prob lem willbe solved ow ing to fu ture de tailed stud ies, in clud ing those offrac tured peb bles in Pleis to cene strata situ ated in the faultzone.

The SMF is con sid ered to have been ac tive in the LateOli go cene and re ac ti vated later on, al though it proba blyorigi nated al ready dur ing the Varis can orog eny. Qua ter nary

ac tiv ity of this struc ture has been a mat ter of de bate. Some re -search ers sug gested Qua ter nary up lift of the foot wall rang -ing from 20–30 m to 60–80 m, and even 80–100 m, a largepor tion of it hav ing been due to gla cioi so static re bound af terthe Saalian gla cia tion. Fault ing of Qua ter nary ter races, rec ti -line ar ity of the fault scarp, pos si ble seis mo tec tonic de for ma -tions within Pleis to cene al lu vial fans, as well as his tori calseis mic ity, and con tem po ra ne ous, GPS- detected mo bil ity,all tes tify to re cent ac tiv ity of this zone.

We have ana lysed the south east ern, nearly 100- km- long, por tion of this fault. This por tion of the SMF has beensub di vided into seven seg ments show ing slightly dif fer entori en ta tion (N28°W to N55°W), geo logi cal set ting, length(8.8–22.9 km), height of the fault and fault- line scarp (40–300 m), as well as the val ues of mor phomet ric para me tres ofsmall catch ment ar eas of streams that dis sect the scarp. Thelat ter para me tres, par ticu larly those char ac ter is ing the elon -ga tion, re lief, and av er age slope of in di vid ual catch mentareas, to gether with ab nor mally small val ues of the val leyfloor width to val ley height ra tios, and moun tain front sinu -os ity in di ces which are in dica tive of a nearly rec ti lin ear traceof the moun tain front, al low us to con clude about Qua ter naryup lift ten den cies of the SMF foot wall in the Sowie Mts. seg -ment (cf. Badura et al. 2003).

The re main ing faults re ac ti vated in the Qua ter nary areclus tered in the Sudetic Block, in the Karkonosze Mts., Iz eraMts., Up per Nysa K³odzka Gra ben, and in some por tions ofthe Fore- Sudetic Block (Figs. 4, 6).

Kleszc zów Gra ben

The Kleszc zów Gra ben, Cen tral Po land, 80 km long and2–3 km wide, is situ ated in the Szcze cin-£ódŸ- MiechówSyn cli nor ium (Figs. 4, 7). This gra ben be longs to one of themost thor oughly stud ied Late Ce no zoic struc tures of the Pol -ish Low lands (cf. Rühle et al. 1978, Krzysz kowski 1991,1992, Ha³uszc zak 1999, Go towa³a, Ha³uszc zak 2002). Thegra ben is com posed of a number of seg ments whose ori en ta -tions in the east ern (WNW–ESE) and west ern (WSW–ENE)parts co in cide with those of re gional faults (Go towa³a 1987,Go towa³a, Ha³uszc zak 2002; see Fig. 7). The 250–600- m- thick Neo gene–Qua ter nary in fill is un der lain by Ju ras sic andCre ta ceous strata that be came folded and faulted dur ing theEarly Palaeo gene La ramian move ments. The cen tral por tionof the gra ben is oc cu pied by the open- cast brown coal mine“Be³chatów”.

Within the Kleszc zów Gra ben three struc tural stageswere iden ti fied: the Va la chian (folded and faulted Mio cenestrata), Be³chatów (strongly tec ton ized Plio cene and Lowerand Mid dle Pleis to cene strata), and up per (poorly de formedOdra nian/War the through Holo cene sedi ments) ones (cf.Krzysz kowski 1989, 1991). Dif fer en ti ated sub si dence oc -curred dur ing the Augus to vian In ter gla cial (Bave lian Com -plex), South- Polish (El ste rian) gla cia tions, Ma zo vian(Hol stein ian) In ter gla cial, and – much more weaker – dur ingthe War the gla cial stage (Krzysz kowski 1991), whereasmain epi sodes of fault ing took place at the turn of the Plio -cene and Pleis to cene, in the Ma zo vian In ter gla cial, and dur -ing the War the stage, in the so- called “Be³chatów phase”(Krzysz kowski 1991, Ha³uszc zak 1994). The amount of sub -


si dence be tween the Odra nian (Dren the) and War the stagesat tained 15–20 m (Brodzikowski 1987).

The Kleszc zów Gra ben origi nated in Late Oli go -cene–Early Mio cene times due to tran sten sional re ac ti va tionof base ment faults, ori ented WSW–ENE to NW–SE (Go -towa³a, Ha³uszc zak 2002). Later on, a se ries of WSW- striking pull- apart ba sins was formed, and in the Late Sar ma -tian–Early Pan nonian, ex ten sional re ac ti va tion of NE- orientated nor mal faults took over. An other epi sode oc curred in the Late Neo gene through Mid- Pleistocene, when dex traltran spres sional mo tions along re verse NW- striking faultstook place (Fig. 7). The be gin ning of this stage (Late Mio -cene – South- Polish/El ste rian gla cia tion) was char ac ter isedby tec tonic qui es cence, while in ten sive fault ing oc curred atthe end of the South- Polish (El ste rian) gla cia tion, re sult ing in the for ma tion of NW- striking faults and fold ing of Ce no zoicstrata (see also: Krzysz kowski 1991, 1992, Ha³uszc zak1994, Ha³uszc zak et al. 1995). It was proba bly at that time,

when a NW- striking thrust- fault show ing top to the NE dis -place ment, in the north ern part of the gra ben, was formed(Ha³uszc zak et al. 1995, Ha³uszc zak 1999). This epi sode ter -mi nated ca. 260 ka, shortly be fore the War the stage. The re -cent de vel op ment of the Kleszc zów Gra ben con sists inre ac ti va tion of some of the pre- existing faults, partly due tomin ing ex ploi ta tion, and also ow ing to present- day seis mic -ity of mag ni tudes up to 4.6 and epi cen tres aligned par al lel toone of the re gional base ment faults. Fo cal mecha nisms ofthese earth quakes in di cate oblique- slip kine mat ics (Go -towa³a, Ha³uszc zak 2002).

Lublin Up land

Ce no zoic fault ing in the Lublin Up land, SE Po land,post- dating La ramian move ments, pro ceeded in the Early orMid dle Eo cene, Mid dle and Late Sar ma tian, as well as in theEarly Qua ter nary (e.g. Hen kiel 1983, 1984, Hara simiuk,


Fig. 6. Neotectonic map of Lower Silesia (based on Badura, Przybylski 2000; sim pli fied), show ing faults ac tive in the Neo gene and thoseac tive/re ac ti vated in Qua ter nary times, as well as Laramian folds.

Hen kiel 1984, Bu rac zyñski 1997, Brzeziñska- Wójcik 2002). The thick ness of Qua ter nary sedi ments within tec tonic gra -bens is be tween 50 and 120 m (Hen kiel 1984). An other epi -sode of fault ing was con fined to the Elsterian-2 gla cial stage

and the Ma zo vian (Hol stein ian) In ter gla cial, when 20–30 mof sub si dence oc curred in some of the gra bens (Hara simiuk,Hen kiel 1981). The Mid dle and Late Pleis to cene fault ingwas of con sid era bly smaller am pli tude.

The prin ci pal fault zones in the Lublin Up land in clude(Fig. 8): the dex tral Kock-£êc zna fault (NW–SE); theWieprz River val ley fault zone (N–S), com posed of al ter nat -ing asym met ric gra bens and half- grabens re ac ti vated inEarly Qua ter nary times; the Early Qua ter nary fault zone ofthe north ern mar gin of the Lublin Up land (E–W), em brac ingthe Mo giel nica and So bi anowice gra bens filled with morethan 70 m thick Qua ter nary al lu vium; the pre- QuaternaryBystrzyca River val ley fault zone (NE–SW), com posed ofnor mal faults bound ing nar row gra bens and horsts; theW³odawka River fault zone; as well as the pre- QuaternaryKap lonosy fault (NNW–SSE).

The NW por tion of the Lublin Up land bears theJanowice fault (NE–SW), con sid ered by some authors as aQua ter nary sin is tral fault zone of up to 1 km off set (Hen kiel1983, 1984). The mor pho tec tonic scarp at Do bre (NW–SE),Na³êc zów Pla teau, was in ter preted as a seis mo tec tonic nor -mal fault, as so ci ated with a se ries of su per im posed col lu vialwedges, proba bly formed due to re peated pa laeo seis micevents (Hen kiel 1993). The es carp ment zone (NW–SE) ofthe Roz tocze re gion be came up lifted by 20–30 m fol low ingthe South- Polish/El ste rian gla cia tions (e.g. Hara simiuk,Hen kiel 1980, Laskowska- Wysoczañska 1984).

Car pa thian Fore deep

The sub stra tum of the Car pa thian Fore deep be tweenKraków and San dom ierz, South Po land, is cut by sev eralfault zones (Fig. 9). These in clude: a sys tem of pre- Laramian, usu ally NE- trending strike- slip faults of the Kurdwanów- Zawichost zone (cf. Osmól ski et al. 1978, Krysiak 2000),and a sys tem of nor mal faults that bound La ramian horsts and gra bens, ori ented NW–SE. These struc tures be came re ac ti -vated in Neo gene and, pos si bly, also Qua ter nary times, as


Fig. 7. Faults as so ci ated with the Kleszc zów Gra ben (based on Go towa³a, Ha³uszc zak 2002; sim pli fied).

Fig. 8. Young fault zones in the Lublin Up land (based on Hen kiel 1983, 1984; modi fied).

shown by the re sults of struc tural stud ies of the Late Mio cene fresh- water mo las ses of the Witów Se ries (cf. Brud et al.2003). The mo las ses are cut by joints, and nor mal and strike- slip faults which were formed in two suc ces sive events: (1) asyn- depositional one, pro ceed ing un der NNW–SSE to N–Sori ented hori zon tal com pres sion, pos si bly coe val with re ac -ti va tion of a NE- striking sin is tral fault of the Kurdwanów- Zawichost Fault Zone in the base ment; and (2) a post- depositional one, dur ing N–S to NE–SW- oriented ex ten sion. In the first event, re ac ti va tion of the NE- striking sin is tralfault led to for ma tion of N–S- oriented joints, as well as NW- striking dex tral, and NNW- trending nor mal faults. Thisevent was proba bly con tem po ra ne ous with sin is tral re ac ti va -tion of some thrusts in the West ern Outer Car pa thi ans, in -duced by eastward- directed ex tru sion of crus tal blocks in theCar pa thian in ter nides. In the sec ond event, both W–E andNW–SE- oriented joints and WNW- striking nor mal faultswere formed. The lat ter most proba bly origi nated due to re ac -ti va tion of the Early Pa leo cene WNW- and NW- striking nor -mal faults in the base ment. Simi lar con clu sions re sult fromanaly ses of small- scale tec tonic struc tures at other lo cali ties

situ ated in the me dial por tion of the Car pa thian Fore deep and in mar ginal slices of the Outer Car pa thi ans (Rauch et al.2006).

In the west ern part of the Car pa thian Fore deep, the pre- Eemian up lift be came re placed by sub se quent sub si dence as -so ci ated with re ac ti va tion of nor mal faults (Niedzia³kowskaet al. 1985, Niedzia³kowska, Szcze panek 1993- 94).

Plio cene–Qua ter nary tec tonic ten den cies in the Pol ishseg ment of the Car pa thian oro gen are marked in Fig. 10. This area has been domi nated in Qua ter nary times by re ac ti va tionof ma jor thrust faults, prin ci pally due to NNE- oriented hori -zon tal stresses; mi nor nor mal fault ing be ing con fined to in -tra mon tane ba sins and some por tions of the Car pa thianFore deep (Zuchiewicz et al. 2002).

RE CENT STRESS FIELD

Re cent stress meas ure ments in di cate that the Car pa thi -ans are be ing ex posed to tec tonic push from the hin ter land,which gen er ates NNE- oriented com pres sion in the east ernpart of the Outer Car pa thian fold- and- thrust belt (Ja ro si ñski


Fig. 9. Fault pat tern in the me dial Car pa thian Fore deep (based on Krysiak 2000 and Rauch et al. 2006; modi fied).

1999, 2005). This push is trans mit ted far ther to the northalong the mar ginal part of the East- European Plat form (Fig.11). Suc ces sive ac com mo da tion of this push is evi denced bysys tem atic dis tor tion of tec tonic com pres sion fromNNE–SSW in the south ern seg ment to NNW–SSE in theBal tic por tion of the East- European Plat form, where the Car -pa thian push is bal anced with the North At lan tic ridge push.Within the Trans- European Su ture Zone, fre quent stress ro -ta tions be tween N–S and NW–SE in ver ti cal bore hole sec -tions and among bore holes sug gest a dis crete strike- slipac com mo da tion of the Car pa thian push (Ja ro si ñski 2005). Asur vey of natu ral and mining- induced trem ors pro vides ad di -tional source of in for ma tion about re cent geo dy nam ics(Guterch, Lewandowska- Marciniak 2002). For the in ner part of the Outer Car pa thi ans, i.e. close to the Pi en iny Klip penBelt, ei ther strike- slip or thrust fault stress re gime is in ferredfor the nap pes (Wie jacz 1994). The strike- slip stress re gimewas de ter mined also for sin gu lar earth quakes in the Kleszc -

zów Gra ben (Go towa³a, Ha³uszc zak 2002) and the Ka lin in -grad dis trict near the Pol ish bor der (Wie jacz 2004).Domi nance of strike- slip fault stress re gime was con strainedby hy drau lic frac tur ing tests in bore holes lo cated in SE Po -land, while in west ern Po land ex ten sional stress re gime withsome amount of strike- slip com po nent pre vails (Ja ro si ñski2005).

FU TURE TASKS

Re li able es ti ma tion of geo dy namic haz ards in Po landwill re quire in te gra tion of the ex ist ing, usu ally scat tered,geo logi cal, geo physi cal, geo mor pho logi cal, pa laeo seis mol -ogi cal, and geo detic data, com bined with sup ple men ta tionand veri fi ca tion of the char ac ter is tics of young tec tonic struc -tures and pro cesses. Such an ap proach should en able for thecon struc tion of a new model of the neo tec tonic stress field inthis part of Cen tral Europe.


Fig. 10. Neo tec tonic sketch- map of the Pol ish Car pa thi ans (based on Zuchiewicz et al. 2002): A – physio graphic units and dis tri bu tion ofyoung up lifted zones, B – pat tern of neo tec tonic ele va tions and de pres sions.

Ac know ledge ments

We ac knowl edge with thanks care ful re view by A. K. To kar ski and help ful edi to rial com ments of fered by T. Go slar.

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NEO TEC TON ICS OF PO LAND: AN OVER WIEV OF AC TIVE …ac tiv ity, es ti ma tion of the para me tres of the neo tec tonic stress field, ampli tudes and rates of Qua ter nary and re

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