Electrical resistivity tomography (ERT) and sedimentological analysis applied to investigation of Upper Jurassic limestones from the Krzeszowice Graben (Kraków Upland, southern Poland)

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Elec tri cal re sis tiv ity to mog ra phy (ERT) and sedimentological anal y sis ap plied to in ves ti ga tion of Up per Ju ras sic lime stones from the Krzeszowice Graben

(Kraków Up land, south ern Po land)

Tomasz WOZNIAK^1, *, Grzegorz BANIA¹, W³odzimierz J. MOŒCICKI¹and Micha³ ÆWIKLIK¹

1 Fac ulty of Ge ol ogy, Geo phys ics and En vi ron ment Pro tec tion, AGH Uni ver sity of Sci ence and Tech nol ogy, al.

A. Mickiewicza 30, 30-059 Kraków, Po land

WoŸniak, T., Bania, G., Moœcicki, W.J., Æwiklik, M., 2018. Elec tri cal re sis tiv ity to mog ra phy (ERT) and sedimentological anal - y sis ap plied to in ves ti ga tion of Up per Ju ras sic lime stones from the Krzeszowice Graben (Kraków Up land, south ern Po land).

Geo log i cal Quar terly, 62 (2): 287–302, doi: 10.7306/gq.1403

This pa per high lights the ap pli ca tion of shal low non-in va sive geo phys ics (elec tri cal re sis tiv ity to mog ra phy) sup ported by sedimentological anal y sis ap plied to the in ves ti ga tion, de scrip tion and in ter pre ta tion of Up per Ju ras sic lime stones ex posed in the aban doned quarry near the vil lage of Tomaszowice (Kraków Up land, south ern Po land). Within this site, on the north ern mar gin of the Krzeszowice Graben, a fa cies di ver sity of Up per Ju ras sic lime stones can be ob served. Field ex po sures were ana lysed to broadly char ac ter ize these Up per Ju ras sic lime stones in terms of fa cies and microfacies de vel op ment. Three fa - cies types, in clud ing pelitic lime stones, bed ded lime stones and car bon ate grav ity-flow de pos its, com posed of nu mer ous microfacies, have been dis tin guished. ERT study us ing a di pole-di pole ar ray has been car ried out, along 5 par al lel 110 m long pro files and along a per pen dic u lar 110 m long pro file, north of the Tomaszowice Quarry wall. The use of ERT in com bi - na tion with the geo log i cal data al lowed char ac ter iza tion and de scrip tion of the ge ol ogy at the re search site as well as the de - ter mi na tion of the lithological com po si tion and in ter nal ar chi tec ture of the subsurface. Fur ther more, the ERT in ter pre ta tion re sults in di cated the pres ence of a se ries of a sec ond ary faults closely linked with the Krzeszowice Graben. The dis tri bu tion of the grav ity-flow de pos its re flects the fault zone pat tern of the graben and Late Ju ras sic fault ac tiv ity.

Key words: elec tri cal re sis tiv ity to mog ra phy (ERT), Up per Ju ras sic lime stones, Oxfordian, Krzeszowice Graben, southern Po land.

INTRODUCTION

Elec tri cal re sis tiv ity to mog ra phy (ERT) is an ef fec tive, non-in va sive geo phys i cal tech nique, widely ap plied for the de - ter mi na tion of shal low subsurface prop er ties as well as the spa - tial dis tri bu tion of these prop er ties em bod ied in the 2D and 3D im ages. Be cause of this, ERT has been suc cess fully in te - grated, in par tic u lar, in sedimentological stud ies in ge ol ogy (see e.g., Hirsh et al., 2008; Šilhán and Pánek, 2010; Pellicer and Gib son, 2011; Æwiklik, 2013; Moœcicki et al., 2014; Koz³owska et al., 2016).

The Kraków Up land, and in par tic u lar the tec tonic mar gins of the Krzeszowice Graben (Fig. 1) are per fect places at which Up per Ju ras sic lime stones of di verse fa cies can eas ily be ob - served (see e.g., D¿u³yñski, 1952; Matyszkiewicz, 1997). Along the graben mar gins, these Up per Ju ras sic lime stones are com - monly ex posed, and show con sid er able sedimentological, lithological and tec tonic vari abil ity across short dis tances (see

e.g., Matyszkiewicz, 1996; Matyszkiewicz and Krajewski, 1996;

Krajewski, 2000) while their lat eral ex tents, re stricted by the size of ex po sures, re main poorly con strained.

We fo cus here on the com bi na tion of ERT with geo log i cal anal y sis to pro vide com ple men tary data on these Up per Ju ras - sic lime stones. While such geo phys i cal sur veys have in gen eral be come more widely ap plied, the use of ERT in this study is its first ap pli ca tion to the Krzeszowice Graben, though ERT has been ap plied north of the Kraków Up land (in the area of Bydlin) by Barski and Mieszkowski (2014).

This case study was car ried out in a small aban doned quarry lo cated near the vil lage of Tomaszowice, near Kraków, in the south ern part of the Kraków Up land (Figs. 1 and 2). Al - though the Up per Ju ras sic lime stone fa cies from this quarry, have al ready been briefly de scribed by Zió³kowski (2007b), who rec og nized three fa cies in these Up per Ju ras sic lime stones as well as ero sive con tacts be tween some of them, their de vel op - ment has un til now not been stud ied in de tail.

Our ob jec tive, in this pa per, has fo cused on: (1) high light ing the po ten tial of ERT for in ves ti ga tion and re con struc tion of these Up per Ju ras sic rocks, (2) iden ti fy ing and de scrib ing the car bon ate fa cies en coun tered in the study site, (3) de fin ing the spa tial dis tri bu tion to gether with bound aries be tween each fa - cies by cor re lat ing the ob tained ERT re sults with lithological char ac ter is tics as well as (4) pro vid ing in for ma tion about the pos si ble pres ence of tec tonic struc tures in the re search area.

* Corresponding author, e-mail: twozniak@geol.agh.edu.pl Received: June 12, 2017; accepted: December 20, 2017; first published online: April 3, 2018

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288 Tomasz WoŸniak, Grzegorz Bania, W³odzimierz J. Moœcicki and Micha³ Æwiklik

Fig. 1. Position of the Upper Jurassic limestones analysed in the area of Tomaszowice (asterisk) superimposed on a geological map of the southern part of Kraków Upland (after Gradziñski, 2009, simplified and modified)

Position of the KLFZ (Kraków–Lubliniec Fault Zone) and KCHF (Krzeszowice–Charsznica Fault) disturbing the Paleozoic basement after Habryn et al. (2014); white dots with annotations indicate Upper Jurassic outcrops mentioned in the text: U – Ujazd; G – Giebu³tów

Fig. 2A – location map of the abandoned quarry at Tomaszowice with the marked positions of the ERT survey lines (green lines), the part in the rectangle is magnified in Figure 2B; B – detailed location of the ERT survey lines superimposed on the

digital orthophotomap of the area investigated (source of orthophotomap: Google Earth web site)

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GEOLOGICAL SETTING

The Krzeszowice Graben is one of the larg est of all nu mer - ous grabens that oc cur within the re gional tec tonic unit of the Silesian–Kraków Homocline, and is the most eas ily ap par ent struc ture among the mod ern land forms of the Kraków Up land (Fig. 1).

The homocline is built of Me so zoic sed i men tary rocks (Tri - as sic, Ju ras sic and Cre ta ceous) that dip gently, at a low an gle, to wards the NE, and rest un con form ably on the pre-Me so zoic base ment of the homocline, which con sists of folded Pre cam - brian and Pa leo zoic rocks. The homocline base ment is cut by the Kraków–Lubliniec Fault Zone (KFLZ) and the Krzeszowice–Charsznica Fault (KCHF; Bu³a et al., 2002;

Habryn et al., 2014; Narkiewicz and Petecki, 2017). The KLFZ, which di vides the homocline base ment into the Up per Silesian Block and the Ma³opolska Block (¯aba, 1995, 1999) has been ac tive since the ear li est Pa leo zoic (Morawska, 1997; ¯aba, 1999). More over, this tec tonic zone, es pe cially along the bound ary of the Ma³opolska Block, in cludes many Pa leo zoic in - tru sions (Bu³a et al., 1997; ¯aba, 1999).

The unique read abil ity of the Krzeszowice Graben within the Silesian–Kraków Homocline has been con di tioned by the dif fer ences in ero sion be tween the Mio cene strata fill ing the graben and the rocks form ing the graben mar gins (mainly Up - per Ju ras sic lime stones). A sec ond fac tor was the Paleo - gene–Neo gene move ments which en abled ero sion of the Mio - cene infill.

The south ern mar gin of the Krzeszowice Graben was de - fined by D¿u³yñski (1953) as the Tenczyñski Horst while the north ern mar gin has been re ferred to as the Ojców Pla teau (Bogacz, 1964, 1967; Fig. 1); they re flect the nar row zones of this com pli cated faulted struc ture. Al though it is gen er ally rec - og nized that Ce no zoic tec ton ics (linked with the overthrusting Carpathian nappes) was re spon si ble for gen er at ing the faults that framed the tec tonic struc ture of the Krzeszowice Graben (D¿u³yñski, 1953; Gradziñski, 1972), this pro cess may have been ini ti ated in the Late Ju ras sic or even ear lier (Matyszkiewicz, 1996; Matyszkiewicz et al., 2007; Nawrocki et al., 2008; Habryn et al., 2014; Matyja and Zió³kowski, 2014).

The Up per Ju ras sic strata of the pres ent-day Kraków Up - land, the thick ness of which reaches ~250 m (Matyszkiewicz et al., 2015b), are di verse, con sist ing of mas sive and bed ded fa - cies as well as re worked sed i ments that are re lated to grav ity flow pro cesses (Fig. 3).

The Up per Ju ras sic bed ded fa cies (also called a “nor mal fa - cies”; vide Gwinner, 1976) are rep re sented by thin-bed ded marl-lime stone al ter na tions, bed ded pelitic lime stones and bed - ded lime stones with early diagenetic cherts, and bed ded lime - stone-marl strata known from well logs (Burzewski, 1969). It is com monly ac cepted that the sed i men tary en vi ron ment of the bed ded fa cies was placed in the in ner-de pres sions (intrabiohermal de pres sions) be tween el e vated, by up to 100 m (cf. Matyszkiewicz, 1999), parts of the car bon ate build ups and on their slopes (cf. D¿u³yñski, 1952).

The Up per Ju ras sic mas sive fa cies, de fined by D¿u³yñski (1952) as un bed ded lime stones with out cherts, con sist of pre - served frag ments of var i ous types of sponge-mi cro bial, mi cro - bial-sponge as well as mi cro bial car bon ate build ups (Matyszkiewicz et al., 2012). Lo cally, within these build ups, rare ac cu mu la tions of brachi o pods infill nep tu nian dykes (Matyszkiewicz et al., 2016).

Fig. 3. Lithostratigraphic sec tion of Up per Ju ras sic strata in the south ern part of the Kraków Up land (af ter Matyszkiewicz et al., 2016, mod i fied) with prob a ble strati graphic po si tion (black line) of Up per Ju ras sic lime stones ex posed at the site

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Al most the en tire Up per Ju ras sic suc ces sion of the Kraków Up land hosts a wide va ri ety of grav ity flow sed i ments. These sed i ments re veal a high lithological va ri ety, among which are grain flow and de bris flow de pos its as well as calciturbidites and tempestites (Bukowy, 1960; G³azek and Wierzbowski, 1972;

Hoffman and Matyszkiewicz, 1989; Matyszkiewicz, 1993, 1996, 1997; Koszarski, 1995; Matyszkiewicz and Krajewski, 1996;

Matyszkiewicz et al., 2007, 2015b; Matyszkiewicz and Olszewska, 2007). These de pos its are widely en coun tered along the bound aries that de fine the graben mar gins, es pe cially length wise along the nar row north ern zone of the Krzeszowice Graben (Matyszkiewicz, 1996; Zió³kowski, 2007a, b; Matysz - kie wicz et al., 2012).

Re worked sed i ments are the most ac cen tu ated at the bound ary be tween the Up per Oxfordian and Lower Kimmeridgian (Matyszkiewicz, 1996). In ad di tion, grav ity flow de pos its were iden ti fied in the part of the pro file that be longs to the Mid dle and Lower Oxfordian (Koszarski, 1995). The fac tors that af fected the for ma tion, de vel op ment and size of the grav ity flow de pos its were closely re lated to: (1) the dif fer en tial sea-bot - tom re lief be tween the car bon ate build ups and the bas ins be - tween them; (2) a tem po rary de te ri o ra tion of con di tions con trol - ling the growth of the car bon ate build ups (ini tial drown ing, cf.

Bice and Stew art, 1990); (3) the synsedimentary tec ton ics as - so ci ated with the KLFZ ac tiv ity as well as (4) sea level fluc tu a - tions (see e.g., Matyszkiewicz, 1996, 1997, 1999;

Matyszkiewicz et al., 2007, 2015b, 2016).

Our geo log i cal stud ies were car ried out in a small aban - doned quarry (50°08’29.13”N; 19°50’09.79”E) lo cated in the com plex area that sep a rates the Ojców Pla teau from the vast, east-west trending Krzeszowice Graben, near the vil lage of Tomaszowice, in the south ern part of the Up land (Figs. 1 and 2). The pre cise strati graphic level of the suc ces sion ana - lysed, gen er ally as cribed as be long ing to the Oxfordian, re - mains un known due to a lack of zon ally sig nif i cant ammonite fau nas. Pre cise strati graphic lev els have been de fined in Up per Ju ras sic lime stones ex posed near Ujazd (the bound ary be - tween the Oxfordian and the Lower Kimmeridgian), ~2 km west of the ex po sure stud ied and at Giebu³tów (Lower Kimmeridgian) ~4 km east of the suc ces sion stud ied, re spec - tively (Zió³kowski, 2007a, b).

METHODS

The ex po sure was de scribed and sam pled prior to the geo - phys i cal sur vey. Sedimentological anal y sis fo cused on fa cies and microfacies char ac ter iza tion of the ex posed lime stones.

Sam ples were col lected from the quarry wall, span ning the en - tire thick ness of the Up per Ju ras sic lime stones. De tailed microfacies anal y ses was car ried out on 18 thin sec tions and 12 pol ished slabs. All lime stone sam ples were sub se quently clas -

si fied us ing Dun ham (1962) scheme with its later mod i fi ca tions by Embry and Klovan (1972).

ERT ac qui si tion was per formed us ing a SuperSting R8 re - sis tiv ity me ter, con nected to a lin ear ar ray of 56 elec trodes si - mul ta neously (setup) with ba sic elec trode spac ing Dx = 2 m. In this pa per, the di pole-di pole ar ray type was used, as it is highly sen si tive to hor i zon tal changes in re sis tiv ity and is widely used in the in ves ti ga tion of near-sur face re sis tiv ity vari a tions (cf.

Szalai and Szarka, 2000; Dahlin and Zhou, 2004). Lengths of cur rent and po ten tial di poles a = 1, 2, 3, 4, 5, 6 Dx and sep a ra - tion fac tors (dis tances be tween cur rent and po ten tial di poles), n = 1, 2, 3, 4, 5, 6 a have been used. In to tal, 5 par al lel (P1–P4, P6) 110 m long sur vey lines, sep a rated by each other by 10 m as well as one sur vey line per pen dic u lar to the quarry wall 110 m long (P5) were ac quired. ERT sur vey was made in two stages. Dur ing the first phase of ERT mea sure ment (June, 09.2016) two sur vey lines (P1–P2) were es tab lished, whereas the re main ing sur vey lines (P3–P6) were con ducted dur ing the sec ond stage (Sep tem ber, 09.2016). In or der to avoid quarry wall ef fects on the mea sure ment re sult, the first sur vey line P1 was placed ~21 m from the quarry edges. The per pen dic u lar sur vey line P5, which starts at the edge of the quarry, cuts the P1 line at 56 m length. Lo ca tions and mea sure ment pa ram e ters of each sur vey line are shown in Fig ure 2 and Ta ble 1.

Geo detic mea sure ments, with the use of the Jog ger 20 lev - eler of Leica Geosystems, were con ducted si mul ta neously with the geo phys i cal sur veys for the pur pose of es tab lish ing elec - trode el e va tions along each pro file. Such mea sure ments are nec es sary to de ter mine the ter rain mor phol ogy which sig nif i - cantly in flu ences the data in ver sion pro cess (Bania, 2011).

The ob tained ap par ent re sis tiv ity datasets, along the des ig - nated sur vey lines, were in verted us ing Res2Dinv of Geotomo Soft ware (Loke, 2010). The in ver sion pro cess based on the L1-norm (ro bust, blocky) and L2-norm (smooth) in ver sion method was tested. In this pa per, we pro vide in verted re sis tiv ity sec tions only for the ro bust in ver sion method, which tends to pro duce mod els with a much sharper and straighter bound ary be tween dif fer ent re gions with dif fer ent re sis tiv ity val ues (Loke et al., 2003). All in ver sion data pro vide root mean square er ror (RMS) of be tween 0.99 and 2.50% (with a mean value of 1.60%) which re flects high data qual ity.

In or der to ana lyse the re sis tiv ity sec tions in terms of the oc - cur rence of sharp “struc tural” bound aries, anal y ses of the ver ti - cal and hor i zon tal gra di ents of the in ter preted re sis tiv ity dis tri bu - tion was per formed. Gen eral in ter pre ta tion of the ob tained ERT re sults was pri mar ily based on cor re la tion with the ex posed Up - per Ju ras sic lithologies, for which dif fer ent fa cies were as - signed. To show a gen eral pic ture of the geo log i cal struc ture, con tour maps of first and sec ond class top sur faces have been cre ated. The depths for each con tour map were de ter mined over a height point ‘0’, which was adopted from the ERT data.

No. ERT

sur vey lines

Pa ram e ters Pro file

ori en ta tion

Pro file length [m]

Electrodes used

Electrodesse paration [m]

Elec trodes con fig u ra tions (ar ray)

Data points

num ber RMS er ror [%]

1 P1

NW–SE

110 56 2

di pole-di pole a = 1–6 n = 1–6

~1323

1.0

2 P2 1.2

3 P3 2.5

4 P4 1.7

5 P5 NE–SW 2.2

6 P6 NW–SE 0.99

T a b l e 1 Main char ac ter is tics of the ERT sur vey lines

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RESULTS

MACROSCOPIC OBSERVATIONS AND MICROFACIES DEVELOPMENT OF LIMESTONES EXPOSED IN THE TOMASZOWICE QUARRY

In the W–E trending wall of the aban doned Tomaszowice Quarry, the fa cies re la tion ships in the lime stones can be ob - served (Fig. 4).

The lower part of the Up per Ju ras sic suc ces sion be gins with yel low ish pelitic lime stones (F1; Fig. 4). This part of the suc ces - sion is only ex posed in the low er most east ern bot tom part of the quarry, and a sin gle sam ple was col lected for microfacies study.

Thin sec tions show fine bioclastic wackestones with abun dant sponge spicules, frag ments of thin-shelled bi valves and radio - lar ians (Fig. 5A) while sin gle echinoderm plates and foraminifers are also pres ent. Pres sure dis so lu tion fea tures rep re sented by hor i zon tal (lo cally subhorizontal) and/or subordinately ver ti cal sty lo lites lined with Fe-ox ides are very com mon. More over, the wackestones are in tensely bioturbated, though the di ver sity of the trace-fos sil as so ci a tions through out this microfacies is very low. Gen er ally, two types of bur rows, Chondrites isp. and ?Planolites isp., were ob served.

Up wards, the pelitic lime stones are re placed by ~3 m thick suc ces sion con sist ing of bed ded fa cies vary ing in thick ness, which are rep re sented by lime stones with cherts and lo cally with marly in ter ca la tions (F2, Fig. 4). Weath ered lime stone sur - faces show nu mer ous cal ci fied si li ceous sponges up to sev eral tens of centi metres across. The chert nod ules, lo cally densely frac tured, rep re sented by el lip ti cal bod ies up to 13 cm across and elon gated hor i zon tally bod ies up to 25 cm long, are dis trib - uted mainly par al lel to the bed ding planes. To wards the cen tral part of the wall, the bed ding is less dis tinct and ob scured by cha ot i cally dis trib uted cherts. Mi cro scop i cally, the bed ded lime - stones are de vel oped as bioclastic wackestones-packstones as well as boundstones (Fig. 5B). In mi cro scopic view, the dom - i nant wackestone-packstone com po nents are enig matic microencrusting fos sils such as Crescentiella morronensis (for - mer Tubiphytes sp., cf. Senowbari-Daryan et al., 2008) ac com - pa nied by nu mer ous bioclasts dom i nated by bi valves shells, a va ri ety of si li ceous sponge spicules, Terebella lapilloides, plates of echinoderms, bryo zoans, serpulid tubes, cal car e ous sponges as well as foraminifers and holuthurian sclerities.

Some of the bioclasts have ev i dent thin micritic en ve lopes.

Among the main re cog nis able de tri tal com po nents, tuberoids, oncoids, intraclasts and sub or di nate small ooids are also ev i - dent. Lo cally in the wackestones, small, ir reg u lar bor ings are also ap par ent. The prom i nent com po nents of the boundstones are microbialites to gether with the cal ci fied si li ceous sponges which form so-called “uni tary sed i men tary se quences” (cf.

Gaillard, 1983; Matyszkiewicz, 1989; Olóriz et al., 2003; Reolid et al., 2005). The sponges pro vided suit able sub strates for en - crust ing or at tach ing epifauna on their lower sur faces (mainly serpulids and bryo zoans), whereas the op po site, up per sponge-sur faces were over grown by di verse microbialites. The spec trum of microbialites is very wide and in cludes stromatolite and thrombolite struc tures. Sponges bear ing nu mer ous bor ings as well as some in hab it ants re lated to Bullopora sp. within the skel e tal sponge mesh work could be ob served. Fur ther more, nu mer ous Crescentiella morronensis show ing up to 0.3 mm thick walls, ag glu ti nated, oval annelid worm tubes that cor re - spond to Terebella lapilloides and in di vid ual ben thic foraminifers are also fre quent. Sty lo lites, which are com monly ac com pa nied by brown ish Fe-ox ides within the boundstone microfacies, are very com mon.

The up per most part of the Up per Ju ras sic suc ces sion is rep re sented by mas sive as sem blages of lime stone clasts and cha ot i cally dis trib uted cherts, re ferred to grav ity-flow de pos its (F3, Fig. 4A–B). The lime stone clasts are poorly sorted and their di men sions var ied from sev eral cm up to sev eral tens of cm. Clast pack ing within this unit is vari able and shows clast-sup ported and to a lesser ex tent ma trix-sup ported fab ric (Fig. 4C). More over, the lime stone clasts are gen er ally dis trib - uted fairly ran domly and their ori en ta tion is cha otic. Lo cally, sub tle in verse grad ing could be ob served (Fig. 4C). The microfacies de vel op ment of the lime stone clasts within the grav ity-flow struc ture are no ta bly di verse, both ver ti cally and lat - er ally (Fig. 5C–F). The clasts are de vel oped as: (1) de tri tal sed i - ments, mostly as packstones, grainstones and wackestones with very abun dant Crescentiella morronensis; (2) mi cro - bial-Crescentiella boundstones; (3) bioclastic packstones- wacke stones as well as (4) mi cro bial-sponge boundstones with Crescentiella.

The bound ary that sep a rates the grav ity-flow de pos its from the un der ly ing bed ded fa cies ex tends along sharp ir reg u lar dis - con ti nu ity sur faces. Es pe cially in the ex treme west ern part of the quarry wall, this sur face is un du lat ing and forms a pre sum - ably N–S or NE–SW ero sional trending chan nel (Fig. 4B). Lo - cally, this bound ary is also em pha sized by the oc cur rence of a thick layer, up to 15 cm thick, of brown ish-green ish marl (Fig. 4D). The marl con tains small an gu lar lime stone clasts up to sev eral cm across and abun dant microfossils among which foraminifers (Ammobaculities sp., Dentalina sp., Paalzowella turbinella, Rumanolina elevata, R. seiboldi, Spirillina elongata, Sp. infima, Sp. tenuissima), radio lar ians (Spumelaria), nu mer - ous spicules and skel e ton frag ments of si li ceous sponges, echinoids, holothurian scler ites, coccoliths as well as oto liths were iden ti fied.

The Up per Ju ras sic suc ces sion ex posed in the quarry wall hosts dis con ti nu ities of var i ous or i gins. No ta bly, in the west ern part of the quarry wall, the lime stones are cut by a ~2 m long ver ti cal joint, wid en ing up to 16 cm across in its bot tom part (Fig. 6A). This joint is filled with sev eral cm thick ac cu mu la tions of epigenetic si li ceous pre cip i tates as well as with a brown clayey karstic re sid uum. Other in dis tinct dis con ti nu ities could also be ob served within the grav ity-flow struc ture. These wavy, ir reg u lar and/or nearly-flat sur faces di vided the en tire de posit into sev eral units (Fig. 4B). In the east ern part of the quarry wall, the lime stone fa cies are dis sected by a pre sum ably ENE–WSW strik ing fault, dip ping at a high an gle (Fig. 6B), ac - com pa nied by brec cias.

GEOELECTRICAL SURVEY RESULTS

The ERT in ver sion re sults, which are given in Fig ure 7, show that the range of in ter preted re sis tiv ity val ues is con sid er - able, from 10 to >1000 Wm. At the same time the fol low ing pat - terns are ap par ent in the in ter preted sec tions:

(1) The near-sur face zone is dom i nated by a low-re sis tiv ity layer, of vari able thick ness, whose re sis tiv ity val ues are

<20 Wm. In the cen tral part of the P1 sec tion the thick - ness of this layer is ~3–5 m (ca. x = 24–86 m) while at the ends of the cross-sec tion it is sig nif i cantly smaller (~1 m). In the fur ther sec tions a con sid er able in crease in thick ness of the low re sis tiv ity layer can be ob served. In the P6 sec tion their thick ness is >10 m (ca. x = 56 m;

Fig. 7).

(2) The layer un der ly ing the low re sis tiv ity layer is char ac - ter ized by much higher re sis tiv ity val ues (sev eral hun - dred Wm or more). The sig nif i cant vari abil ity of this layer

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Fig. 4. Field pictures

A – gen eral view of the ex po sure en coun tered in the aban doned Tomaszowice Quarry: three di verse Up per Ju ras sic fa cies among which pelitic lime stones (F1), bed ded lime stones (F2) and car bon ate grav ity-flow de pos its (F3) can be ob served (cf. Zió³kowski, 2007b). Ar eas in the dashed rect an gle mag ni fied in Fig ure 4B and in grey rect an gles mag ni fied in Fig ure 6A, B; B – De tail of the sharp, ero sive con tact with chan nel struc ture (ar rows) be tween Up per Ju ras sic car bon ate grav ity-flow and bed ded lime stones (re spec tively F3 and F2, Fig. 4A). Up per part: in ter nal lay er ing of in di vid ual grav ity-flow units (red dot ted lines). Ar eas in rect an gles mag ni fied in Fig ure 4C, D; C – densely packed clast-sup ported car bon ate grav ity-flow de pos its com posed of an gu lar to subrounded lime stone clasts with only mi nor fine-grained ma trix.

Su tured edges of the lime stone clasts are com monly stylolitized. Lower left part: sub tle in verse grad ing in the basal part (ar row; Nikon lens cap for scale); D – a layer of marls with platy, mm-scale fissility dip ping at a low an gle to wards the N or NE, oc curs lo cally within the ero sional chan nel at the top of the bed ded lime stones (pen for scale)

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Fig. 5. Thin-section photomicrographs of Upper Jurassic limestones from the Tomaszowice Quarry

A – bur rowed fine-bioclastic wackestones; cen tre and right: an dis tinct bur row en riched with abun dant echinoderm de tri tus with com mon echinoid spines, the whole bur row struc ture is cross-cut by subhorizontal, low-an gle sty lo lites lined by iron-bear ing ox ides (white ar rows); B – mi cro bial-sponge boundstones with Crescentiella, the outer sur faces of cal ci fied si li ceous sponges (up per right and right) are bor dered by sty lo lites (white ar rows); C – wackestones with com mon Crescentiella; lower left: Crescentiella sur rounded by bryo zoans in which the cyanobacterian crust con tin ues around and pen e trates partly into the bryo zoan cav i ties (white ar row); D – packstones, with com mon Crescentiella, oncoids with bioclasts in the nu clei (red ar row), tuberoids, intraclasts and nu mer ous un iden ti fied crushed bioclasts, some of the bioclasts tend to have a micritic en ve lopes (cortoids; white ar rows); E – mi cro bial-Crescentiella boundstones, the pres ent po si tion of the bot tom-top di rec tion is in di cated by the white ar row, while the red ar row in di cates the orig i nal top; F – mi cro bial-sponge boundstones with Crescentiella, upper part: re ori ented geopetal infills con sist ing of fine-grained in ter nal sed i ments and blocky ce ment (white ar rows) above the cav ity

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is ap par ent be tween sec tions. In sec tion P1, this layer oc curs shal low est at the NW and SE ends of the elec tri - cal sec tions, while a clear de pres sion can be seen on its course (in clud ing at 30–70 m; Fig. 7). Clear dif fer ences in the re sis tiv ity val ues within this zone, both in the hor i - zon tal and ver ti cal di rec tions, are pres ent. The de pres - sion noted is also clearly vis i ble within the next, P2 sec - tion, where sig nif i cantly lower resistivities (<200 Wm) are ap par ent in the SE part of the sec tion. In the next sec tions, P3 and P4, the high re sis tiv ity layer has con - sis tently much higher re sis tiv ity val ues than in pre vi ous sec tions, and the top sur face of this layer oc curs at greater depths. A clear change ap pears be tween the sec tions P4 and P6. The top sur face of the high re sis tiv - ity layer in sec tion P6 is weakly marked and is lo cated at least 20 m be low ground level.

(3) The ERT P5 sec tion, per pen dic u lar to the par al lel sur - vey lines grid, shows a stepwise struc ture of the high re - sis tiv ity layer (Fig. 7).

DISCUSSION

INTEGRATION OF SHALLOW GEOPHYSICAL SURVEY WITH GEOLOGICAL DATA

Com pre hen sive geo phys i cal-geo log i cal in ter pre ta tion.

The value de ter mined in the DC re sis tiv ity mea sure ments is de - fined as the ap par ent re sis tiv ity, which is a func tion of many pa -

ram e ters, such as true re sis tiv ity dis tri bu tion, type of elec trode ar ray, and its size and po si tion in re la tion to the geo log i cal struc - tures (Moœcicki and Antoniuk, 1999). In or der to ob tain the in for - ma tion about the true re sis tiv ity dis tri bu tion, the ap par ent re sis - tiv ity mea sured in the field un der goes a quan ti ta tive geo phys i - cal in ter pre ta tion (in ver sion), in which am bi gu ity is an in her ent fea ture (Loke, 2011). An ad di tional com pli ca tion is that the ob - tained 2D model re sis tiv ity sec tion as sumes that the mea sure - ments were car ried out on a pro file per pen dic u lar to the axis of the geo log i cal struc ture. This is rarely met be cause the geo log i - cal struc ture is un known. It causes the “er ror” in the in ter pre ta - tion, re sult ing from the 2D ap prox i ma tion of the real, spa tially di - verse geo log i cal struc ture (Loke and Barker, 1996). There fore, the re sis tiv ity sec tion ob tained from in ver sion should be treated as an ap prox i ma tion of the true re sis tiv ity dis tri bu tion.

The in te gra tion of geo phys i cal and sedimentological data has led us to the re con struc tion of the shal low fa cies ar chi tec - ture of the Up per Ju ras sic lime stones in the area of Tomaszowice. In or der to fa cil i tate the re sis tiv ity dis tri bu tion anal y sis that was ob tained from the in ver sion pro cess, three re - sis tiv ity classes were dis tin guished (Fig. 8). Tak ing into ac count all the data ob tained, the ap pro pri ate lithologically di verse fa - cies type (Fig. 9) has been as signed to a par tic u lar re sis tiv ity class.

The first re sis tiv ity class, which rep re sents the range of re - sis tiv ity >300 Wm (cf. Fig. 8), most likely cor re sponds to solid lime stones and pre sum ably rep re sents two dis tinct fa cies types. One of these, in cross-sec tions P1 and P2 (Fig. 9), can be in ter preted as a con tin u a tion of the car bon ate grav ity-flow 294 Tomasz WoŸniak, Grzegorz Bania, W³odzimierz J. Moœcicki and Micha³ Æwiklik

Fig. 6. Discontinuity surfaces

A – high-an gle frac tures, cut ting through Up per Ju ras sic bed ded lime stones (F2, Fig. 4), filled with the epigenetic pre cip - i tates (white ar rows) and karstic clayey re sid uum; B – weath ered fault brec cia: con tact be tween brec cia and sur round ing Up per Ju ras sic lime stones ex tends along the steep sur face (white ar rows); see lo ca tions in Fig ure 4A

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Fig. 7. ERT field data inversion results The position of each survey line is indicated on Figure 2

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Fig. 8. ERT field data inversion results with three adopted resistivity classes along with contours representing calculated maximum positive and negative values of the vertical and horizontal gradients based on the interpreted resistivities for ERT

survey lines P1–P6

The classifications based on the resistivity classes should be regarded as an attempt to simplify the lithological identification based on the resistivity values

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de pos its ap par ent in the quarry wall (cf. F3, Fig. 4). The line of the max i mum neg a tive val ues of the ver ti cal gra di ent, out lined on the P1 sec tion (black dot ted line, Fig. 8), emphasises the course of the lower bound ary of these de pos its. Un for tu nately, the same sur face is not ap par ent within the next P2 sec tion, with the re sult that this bound ary is un clear. Cu ri ously, it re ap - pears in the fur ther cross-sec tion P3 (white ques tion mark, P3, Fig. 8). It should be noted that the po si tion of this line, in the P3 sec tion, can not be treated with high con fi dence, be cause in this part of the in ter preted sec tion we are deal ing with a ho mo ge - neous zone with a rel a tively high val ues of in ter preted re sis tiv - ity. This am bi gu ity may be due, e.g. from the na ture of the in ver - sion pro cess (cf. Loke and Barker, 1996).

As sign ing a par tic u lar fa cies type to the de pos its of the first re sis tiv ity class that are vis i ble in other cross-sec tions P3–P4–P6 (Fig. 8) seems to be dif fi cult due to the pres ence of con sid er ably higher val ues of re sis tiv ity in re la tion to the ini tial pro files P1–P2 (Fig. 7). These de pos its may be in ter preted as a con tin u a tion of the car bon ate grav ity-flow de pos its, or as a dif - fer ent fa cies that rep re sents e.g. mas sive lime stones (cf.

Fig. 9). Am bi gu ity in the fa cies in ter pre ta tion (based on the re - sis tiv ity dis tri bu tion) may be con nected with the fact that the mea sure ments were per formed at two dif fer ent stages and there fore the weather con di tions (gov ern ing hu mid ity and wa ter dis tri bu tion in over bur den de pos its) may have af fected the mea sure ment re sults (e.g., Clément et al., 2009).

Fig. 9. Geological interpretation of the ERT survey lines (P1–P6) obtained by integration of all the research data

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The sec ond re sis tiv ity class, which rep re sents re sis tiv ity in the range of 100–300 Wm (cf. Fig. 8), can be in ter preted in two ways. On the one hand, the zone that oc curs im me di ately above the high re sis tiv ity sed i ments of the first class can be com bined with a layer of weath ered lime stone (Fig. 9) ex cept for the sur face layer that is high lighted in sec tion P6 (at 6–47 m), which in this case is one of the over bur den layer (e.g., sandy soil). The line of the max i mum pos i tive val ues of the ver - ti cal gra di ent (red dot ted line, Fig. 8), emphasises the top sur - face of the weath ered zone of the Up per Ju ras sic lime stones (Fig. 9). This zone oc curs in the shal low est parts of the ex treme SE and NW ends of the P1, P2 cross-sec tions as well as at the NW end of the P3 sec tion (Figs. 9 and 10A). Within the cen tral parts of the first three cross-sec tions, these de pos its are at a depth >9 m, thus con sis tent with an eroded trough (cf. zone D;

Fig. 10A).

The same re sis tiv ity zone (100–300 Wm) that oc curs im me - di ately be low the high re sis tiv ity sed i ments well up on P1 sec - tion, sug gests the oc cur rence of a dif fer ent lime stone fa cies type. In this case, this zone may be as so ci ated with the bed ded lime stones (Fig. 9) that are pres ent di rectly be low the grav - ity-flow de pos its (cf. F2, Fig. 4). Pre sum ably this lime stone type also ap pears in the next P2 cross-sec tion where it is lim ited to the NW mar gin of the sec tion (Fig. 9).

An in ter est ing case of the sec ond re sis tiv ity class oc curs within the SE part of the P2 cross-sec tion (at 72–96 m; Fig. 8).

This par tic u lar part of the cross-sec tion can be pre sum ably as - signed to the car bon ate grav ity-flow de pos its to gether with zone of the weath ered lime stones (ques tion mark in cir cle, Fig. 9). More over, the sec ond re sis tiv ity class marked on the per pen dic u lar sec tion P5 (Fig. 8) can be equated with the rock that rep re sents the fa cies va ri ety de scribed in the first re sis tiv ity class along with the zone of weath ered lime stones (Fig. 9). The dif fer ence in the re sis tiv ity dis tri bu tion be tween par al lel and per - pen dic u lar sur vey lines (e.g., P1 and P5) can be as so ci ated with a dif fer ent elec tric cur rent dis tri bu tion within a com plex geo log i cal struc ture.

Other de pos its that have a re sis tiv ity of <100 Wm rep re sent the third re sis tiv ity class (cf. Fig. 8) and can be iden ti fied with

the post-Up per Ju ras sic de pos its that form the over bur den (Fig. 9).

Tec tonic in ter pre ta tion. The geo phys i cal in ter pre ta tion has also per mit ted us to iden tify tec tonic phe nom ena, es pe - cially zones likely to rep re sent se ries of faults or, more pre cisely fault zones, in the re search area. These struc tures may cause the char ac ter is tic con tour dis tri bu tion, rep re sent ing the value of the in ter preted re sis tiv ity, which can be ex am ined and in ves ti - gated by nu mer i cal mod el ling (cf. Nguyen et al., 2005). The course of the faults was sug gested based on the sec tions that had been com piled with the cal cu lated val ues of the ver ti cal as well as the hor i zon tal gra di ents of the in ter preted re sis tiv ity (Fig. 8). The pres ence of four fault zones in the study area is pos tu lated (Fig. 9).

In the cross-sec tion P1 over the dis tance of the ~60–72 m, a dis tinct break in the con ti nu ity of the max i mum pos i tive and neg a tive val ues of the ver ti cal gra di ent of the in ter preted re sis - tiv ity as well as in the strata at trib ut able to the first and sec ond re sis tiv ity class by a zone that re veals a lower re sis tiv ity value is ev i dent (LRZ; Fig. 8). This sit u a tion is better re flected on the map that shows the top sur face of the strata of the first re sis tiv ity class (Fig. 10B) with a re sis tiv ity of >300 Wm. It is ap par ent that these rocks do not oc cur in cer tain parts of the maps, as is par - tic u larly vis i ble in sec tions P1 and P2 (zone A, Fig. 10B). The lat eral lim i ta tions of this zone match per fectly to the mu tu ally par al lel hor i zon tal gra di ents of the in ter preted re sis tiv ity po si - tioned within cross-sec tion P1 (at 60 and 72 m) and P2 cross-sec tion (at 66 and 72 m; Fig. 8). The same zone on the fur ther P3 sec tion is less vis i ble and is pre sum ably lim ited only to the SE mar ginal part of the sec tion. In our opin ion, this zone, with an al leged NE–SW course, may be in ter preted as fault fis - sure en larged by karst pro cesses (Fig. 9). An other fault which was prob a bly re shaped by karstification is ap par ent at the SE end of cross-sec tion P5 (Fig. 9) in the close prox im ity to cross-sec tion P1. The lat eral ex tent of this zone, which ex tends in a pre sum ably WNW–ESE di rec tion, is marked by the oc cur - rence of two par al lel zones of hor i zon tal gra di ents (X = ~16 and 22 m; Fig. 8).

Fig. 10. Contour maps of Upper Jurassic limestone top surfaces (without tectonic phenomena)

A – top surfaces of the sediments assigned to the second resistivity class (cf. Fig. 8), which have been identified as zones of weathered limestone (cf. Fig. 9); B – top surfaces of the strata assigned to the first resistivity class (cf. Fig. 8), which have been identified as

carbonate gravity-flow deposits and/or another facies type (cf. Fig. 9); source of orthophotomap( Google Earth web site)

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A dis tinct break in the con ti nu ity of the max i mum pos i tive val ues of the ver ti cal gra di ent within the NW part of the P3 cross-sec tion (be tween 22 and 26 m; Fig. 8) in di cates an other fault zone. The pre sumed NNE–SSW course of this fault has been de fined on the ba sis of the hor i zon tal gra di ents ap par ent on the sub se quent P1–P2–P4 and P6 cross-sec tions. The last hy po thet i cal fault, of al leged WNW–ESE course, is po si tioned in the zone be tween the P2 and P3 cross-sec tions. The faults emphasise the com plex geo log i cal struc ture with small, dis - tinctly tilted (to ward the NE) fault blocks, clearly vis i ble on the per pen dic u lar P5 cross-sec tion (Fig. 9).

Fig ure 11 de picts the sche matic course of the in ter preted fault zones based on the geo log i cal in ter pre ta tion de rived from Fig ure 9. All es tab lished faults rep re sent a se ries of sec ond ary faults, which are more or less per pen dic u lar to the main faults which frame the struc ture of the Krzeszowice Graben (cf.

Fig. 1).

REMARKS ON THE DEVELOPMENT OF THE UPPER JURASSIC LIMESTONES IN TOMASZOWICE QUARRY

Ac cord ing to Zió³kowski (2007b), the Up per Ju ras sic pelitic lime stones (F1, Fig. 4) ex posed in the low er most part of the Tomaszowice Quarry rep re sent a pre sum ably sim i lar sed i men - tary en vi ron ment and time in ter val (?Mid dle Oxfordian) to the Up per Ju ras sic lime stones de scribed from the area of Korzkiew (~7 km north-east of the stud ied out crop; Zió³kowski, 2005).

The bed ded lime stones from the mid dle part of the Tomaszowice Quarry (F2, Fig. 4), were de pos ited in Late Ju - ras sic shal low-wa ter and open-ma rine epicontinental con di - tions (e.g., Leinfelder et al., 1996; Matyszkiewicz, 1997;

Krajewski et al., 2016) and rep re sent the Tubiphytes–Terebella as so ci a tion widely de scribed from the lit er a ture (Leinfelder et al., 1996).

The Up per Ju ras sic de pos its from the up per most part of the quarry (F3, Fig. 4) dis play char ac ter is tics as so ci ated with car - bon ate grav ity-flow de pos its, such as de bris flow de pos its (cf.

Flügel, 2004), in line with the ob ser va tion of Zió³kowski (2007b).

Based on the sedimentological study it can not be ex cluded that these Up per Ju ras sic de bris flow de pos its might have formed by aggradational growth of sev eral stacked in di vid ual de bris flow surges (see e.g., Ma jor, 1997; Sohn et al.,1999; Sohn, 2000; Tripsanas et al., 2003). How ever, the ERT meth ods did not dis crim i nate de tails within the de bris flow sed i men tary body.

Post-depositional pro cesses such as dewatering, com pac tion and/or amal gam ation may have led to the weld ing of sin gle surges, which are not stratigraphically dis tin guish able, into the one unit that can be ob served right now in the quarry (cf. Ma jor, 1997; Sohn, 2000). The high pro por tions of lime stone clasts with rel a tive low ma trix con tent, that ac cord ing to Flügel (2004) is noncohesive in a car bon ate de bris flow, sug gest that this de - bris must have been weak dur ing de po si tion (cf. e.g., Surlyk, 1984). Such a com po si tion re sults in pre sum ably stiff plas tic flow prop er ties in which in ter nal fric tion and clast shear ing are re spon si ble for a de cel er at ing flow speed (Henrich, 2016). Such ma te rial within the flow struc ture could not be trans ported for long dis tances from the source area due to the lack of buoy ancy (e.g., Drzewiecki and Simó, 2002).

The lower bound ary of the de bris flow de pos its (re veal ing their typ i cal ero sive na ture) may be iden ti fied with a basal shear sur face where the downslope ori ented shear stress ex ceeds the shear strength of a sed i ment (vide Frey-Mar ti nez, 2010).

How ever, such sur faces may re sult in the de po si tion of de bris flow de pos its that have high in ter nal shear near the base of the flow (Middle ton, 1970).

The de po si tion of the de bris flows ana lysed prob a bly took place in the zones that rep re sent the prox i mal parts of the slopes of car bon ate build ups or their com plexes and sup pos - edly cor re sponds to the Up per Ju ras sic Oxfordian–Kim - meridgian stage bound ary (Fig. 3; cf. Matyszkiewicz, 1996;

1997). With re spect to the grav ity-flow de pos its at Tomaszowice, sim i lar de pos its (in close prox im ity to the site ex - am ined) of com pa ra ble age have been com pre hen sively iden ti - fied at Ujazd and Giebu³tów. In agree ment with ob ser va tions pro vided by Zió³kowski (2007a), the Up per Ju ras sic de pos its rep re sent the Bimmamatum–Platynota zone at Ujazd and the Low er most Kimmeridgian sublevel Polygyratus–Desmoides of the Platynota zone at Giebu³tów.

The di rec tion of the ero sional chan nel (Fig. 4B) doc u ments the pre sum ably N–S or NE–SW sed i ment trans port di rec tion to wards the pres ent-day cen tre of the Krzeszowice Graben.

Fur ther more, the ob served chan nel ori en ta tion is al most par al - lel to that of the nearby faults (Fig. 9), which cor re sponds to the north ern bound ary of the Krzeszowice Graben (Fig. 1). It is widely ac cepted in the lit er a ture (e.g., Matyszkiewicz, 1996;

Zió³kowski, 2007a) that at least a por tion of the faults which bound the struc ture of the Krzeszowice Graben al ready ex isted in Late Ju ras sic or even ear lier times and were sub ject to mul ti - ple Al pine re ac ti va tion (Matyszkiewicz et al., 2007; Nawrocki et al., 2008; Habryn et al., 2014; Matyja and Zió³kowski, 2014).

The same sit u a tion ap pears to hold for the faults (Fig. 8) which were iden ti fied in the re search area.

The pres ence of Up per Ju ras sic de bris flow de pos its at Tomaszowice re cords Late Ju ras sic synsedimentary fault tec - ton ics, which was a re per cus sion of the transregional fac tors that were re spon si ble for open ing both the North At lan tic and Tethys Oceans (Ziegler, 1990; Allenbach, 2002). Fault tec tonic ac tiv ity plays a ma jor role in the ini ti a tion of grav ity flows, and also af fects their char ac ter by in flu enc ing fac tors such as sed i - ment pro duc tion and slope mor phol ogy (cf. Pochat and Van Den Driessche, 2007; Quiquerez et al., 2013). In the re search Fig. 11. Sketch map with the positions of the faults identified

in the research area

Source of orthophotomap (Google Earth web site)

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area, tec tonic ac tiv ity was ac com pa nied by the re ju ve na tion of older Pa leo zoic struc tures in the homocline base ment, in par tic - u lar the Kraków–Lubliniec Fault Zone (e.g., Brochwicz- Lewiñski et al., 1984; ¯aba, 1999; Matyszkiewicz et al., 2006, 2007, 2012, 2015a, b).

CONCLUSIONS

1. Elec tri cal re sis tiv ity to mog ra phy to gether with sedimentological study was used to in ves ti gate the Up per Ju - ras sic lime stones at the Tomaszowice Quarry, lo cated within the north ern mar gin of the Krzeszowice Graben (south ern Po - land).

2. The cor re la tion be tween the ex posed Up per Ju ras sic lime stones and the ERT im ages ob tained (on which re sis tiv ity classes have been es tab lished) has al lowed their in ter pre ta tion in the subsurface as con straint of their lat eral dis tri bu tions. The first re sis tiv ity class (>300 Wm) was iden ti fied for the most part as de bris flow de pos its, per haps with mas sive lime stones. A sec ond re sis tiv ity class (100–300 Wm) was cor re lated with bed - ded lime stones, zones of weath ered lime stones and rocks at - trib ut able to the first re sis tiv ity class. Both of these classes re fer only to the Up per Ju ras sic lime stones, while a third re sis tiv ity class (<100 Wm) rep re sents over bur den lay ers that are youn - ger than Up per Ju ras sic. On gen eral grounds, the ob tained re -

sults pro vide and sup plied in for ma tion to the its geo log i cal in ter - pre ta tions.

3. The ERT re sults (anal y ses of the ver ti cal and hor i zon tal gra di ents) showed the use ful ness of this tech nique for the de lin - eat ing zones that may be in ter preted as fault zones. The data pre sented sug gest oc cur rence of four fault zones, of which two are en larged, pre sum ably by karst pro cesses.

4. The pres ence of grav ity-flow sed i ments such as de bris flow de pos its in the mar ginal zones of the Krzeszowice Graben re flects Late Ju ras sic ac tiv ity of the faults that formed the graben. This phe nom e non was con nected with the re ac ti va tion of the pre ex ist ing Kraków–Lubliniec Fault Zone.

Ac knowl edge ments. We are grate ful to Prof.

J. Matyszkiewicz (AGH Uni ver sity of Sci ence and Tech nol ogy, Kraków, Po land) for his sci en tific sup port and con struc tive com - ments, which sig nif i cantly helped to im prove the manu script.

We are in debted to Mrs. M. Simons for cor rec tions to the manu - script, Prof. B. Olszewska for kindly help ing with micro fauna de - ter mi na tion as well as Mr. S. Szczurek for help ing with the field - work. We would like to thank the two re view ers Dr. K. Wójcik (Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Warszawa, Po land) and Dr. M. Gradziñski (Jagiellonian Uni ver - sity, Kraków, Po land) for their con struc tive com ments that con - sid er ably im proved this pa per. The re search was fi nan cially sup ported by the AGH Uni ver sity of Sci ence and Tech nol ogy grant No.15.11.140.637.

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