Wapiennik Breccia Member (Pieniny Klippen Belt, Poland) - revised stratigraphy and origin

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Geo log i cal Quar terly, 2011, 55 (1): 49–62

Wapiennik Brec cia Mem ber (Pieniny Klippen Belt, Po land) – revised stratigraphy and or i gin

Agnieszka ARABAS, Magdalena SIDORCZUK, Marcin BARSKI and Barbara OLSZEWSKA

Arabas A., Sidorczuk M., Barski M. and Olszewska B. (2011) – Wapiennik Brec cia Mem ber (Pieniny Klippen Belt, Po land) – re vised stra tig ra phy and or i gin. Geol. Quart., 55 (1): 49–62. Warszawa.

The Wapiennik Brec cia Mem ber was orig i nally at trib uted to the Czorsztyn Lime stone For ma tion of the Czorsztyn Suc ces sion in the Pieniny Klippen Ba sin. The brec cia was as signed pre vi ously to the Callovian–Oxfordian. Based on micropalaeontological and microfacies stud ies we have de ter mined its age as late Albian. At this time the Czorsztyn Swell was af fected by extensional fault ing, with sub se quent sub ma rine ero sion of scarps. The re-eval u ated age of the brec cia, as well as the li thol ogy of its clasts and its ma trix that contains Cre ta ceous foraminifera, in di cate the as sign ment of the Wapiennik Brec cia Mem ber to the Chmielowa For ma tion.

Agnieszka Arabas, In sti tute of Geo log i cal Sci ences, Pol ish Acad emy of Sci ences, Twarda 51/55, PL-00-818 Warszawa, Po land, e-mail:

sobstyl@twarda.pan.pl; Magdalena Sidorczuk and Marcin Barski, Fac ulty of Ge ol ogy, Uni ver sity of War saw, Żwirki i Wigury 93, PL-02-089 Warszawa, Po land; Barbara Olszewska, Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Carpathian Branch, Skrzatów 1, PL-31-560 Kraków, Po land (re ceived: July 29, 2010; ac cepted: No vem ber 26, 2010).

Key words: Ju ras sic, Cre ta ceous, Pieniny Klippen Ba sin, brec cia, foraminifera, microfacies.

INTRODUCTION

The geotectonic evo lu tion of the Pieniny Klippen Ba sin has been widely dis cussed (e.g., Książkiewicz, 1972; Birkenmajer, 1986; Golonka et al., 2003; Jurewicz, 2005; Krobicki et al., 2006; Froitzheim et al., 2008; Aubrecht et al., 2009). Lower Ju - ras sic to Cre ta ceous de pos its filled the ba sin (e.g., Birkenmajer, 1977, 1986; Wierzbowski, 1994; Wierzbowski et al., 1999;

Aubrecht et al., 2006) that was trans formed into the Pieniny Klippen Belt (PKB), a long nar row struc ture sep a rat ing the Outer and Cen tral Carpathians (Plašienka et al., 1997; see Fig. 1A). An in ter est ing is sue is whether Me so zoic sed i men ta - tion in the Pieniny Klippen Ba sin was af fected by tec tonic move ments. The tec toni cally in duced in sta bil ity of the ba sin sub stra tum may be dem on strated by the pres ence of slumps, brec cias, faults, nep tu nian dykes and so on. Nu mer ous ev i - dence gath ered so far from the Ju ras sic and Cre ta ceous sed i - men tary rocks of the PKB points to a dy namic tec tonic en vi - ron ment (e.g., Birkenmajer, 1986; Golonka et al., 2003;

Plašienka, 2003; Jurewicz, 2005).

The brec cia from Wapiennik Quarry (Fig. 1B) has been re - garded so far as Callovian-Oxfordian in age, sug gest ing tec - tonic ac tiv ity on the Czorsztyn Swell dur ing this in ter val (Birkenmajer, 1977, 1979). In this study, we re-eval u ate the age of this brec cia and sug gest mid-Cre ta ceous tec tonic ac tiv ity in the Czorsztyn Swell area.

GEOLOGICAL SETTING

Red lime stone brec cias crop ping out in Wapiennik Quarry close to Szaflary vil lage near Zakopane (Fig. 1B) were at trib - uted to the Wapiennik Brec cia Mem ber of the Czorsztyn Lime - stone For ma tion by Birkenmajer (1977, 1979). This is the only known oc cur rence of these rock.

The brec cia ap pear ing in the east ern, older part of Wapiennik Quarry was de scribed by Birkenmajer (1952, 1958, 1963, 1977, 1979). It was ini tially lo cated be tween the Bajocian white crinoidal lime stones and the Callovian- Kimmeridgian red lime stones (Birkenmajer, 1952, 1958). In suc ceed ing years Birkenmajer (1977, 1979) de scribed the brec -

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cia as ly ing be tween the eroded sur face of the red crinoidal lime stones of the Krupianka Lime stone For ma tion and red nod u lar lime stone of the Czorsztyn Lime stone For ma tion (Figs. 2A and 3A).

The brec cia was firstly re ported to be com posed of red and white crinoidal limestone clasts in a red lime stone ma trix (Birkenmajer, 1952, 1958). Birkenmajer (1963) ob served that the lower part of the brec cia con sists of an gu lar frag ments of white and red crinoidal lime stones in a pink crinoidal lime stone ma trix, whereas its up per part com prises frag ments of red microcrystalline, crinoidal lime stones and subcrystalline lime - stones. Sub se quently, Birkenmajer (1977, 1979) re ported the brec cia to be com posed of an gu lar frag ments of red crinoidal lime stones of the Krupianka Lime stone For ma tion and white crinoidal lime stones of the Smolegowa Lime stone For ma tion, ce mented by a red or pink lime stone ma trix rich in man ga nese ox ides and scat tered cri noid frag ments.

The brec cia was at trib uted to the Bathonian or Callovian (Birkenmajer, 1952), Bathonian–Callovian? (Birkenmajer, 1958), mid dle Callovian (Birkenmajer, 1963) and fi nally

Callovian–Oxfordian based on its strati graphic po si tion (Birkenmajer, 1977, 1979).

A tec tonic or sed i men tary or i gin of the brec cia was pos tu - lated (Birkenmajer, 1958). Its for ma tion was linked with ver ti - cal tec tonic move ments of the sea-floor and un der wa ter or subaerial ero sion (Birkenmajer, 1963, 1979). The un der ly ing Mid dle Ju ras sic crinoidal lime stones were in ter preted to have been crushed in a fault zone, trans ported by sea cur rents and ce - mented with a red lime stone ma trix (Birkenmajer, 1979).

DESCRIPTION OF THE BRECCIA FROM WAPIENNIK QUARRY IN SZAFLARY

LITHOLOGY

To day, only a part of the ex po sure orig i nally de scribed by Birkenmajer ex ists (Fig. 2). The ac ces si ble ex po sure is about 13 m long and about 6 m high. It is lo cated in the east ern wall of

Fig. 1. Lo ca tion of: A – the Pieniny Klippen Belt (in black) within the Carpathians;

B – Wapiennik Quarry in Szaflary, Po land

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Wapiennik Breccia Member (Pieniny Klippen Belt, Poland) – revised stratigraphy and origin51

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the east ern, older part of Wapiennik Quarry, along a 170/85S-ori ented fault sur face.

White crinoidal lime stones of the Smolegowa Lime stone For ma tion con tact with a mas sive brec cia, re ferred to herein as the crinoidal lime stone brec cia (Fig. 2C). The brec cia con - sists mainly of clasts of white crinoidal lime stone in a red pelitic lime stone ma trix. The ex posed part of the brec cia is ap - prox i mately 2.40 m-thick. The clasts of the brec cia range mostly within 1.5–2 cm in di am e ter. The larg est clasts oc cur in the south of the quarry, where they reach 7 cm in size, whereas in the north ern part, the larg est clasts are up to 5 cm.

The clasts have an ir reg u lar shape. The clast round ness in - creases from the north, where they are mostly an gu lar, to the south, where they are mostly sub-rounded. The sort ing of the clasts in creases from very poor in the south ern part of the quarry to poor in the north. The brec cia has a com pact frame - work and a clast-sup ported fab ric. The tex ture of the brec cia is cha otic and clast/ma trix bound aries are sharp. The vol ume of the ma trix in creases south wards.

The crinoidal lime stone brec cia con tacts with an other mas - sive brec cia, re ferred to herein as the pelitic lime stone brec cia

(Fig. 2C) the larger part of this brec cia is ex posed in the south - ern side of the east ern wall of the quarry (Fig. 3B). The pelitic lime stone brec cia con sists mainly of clasts of red pelitic lime - stones in a red pelitic lime stone ma trix. The thick ness of the pelitic lime stone brec cia ranges from 1 to 1.3 m. Di am e ters of the an gu lar brec cia clasts are gen er ally in the range of 4 to 5 cm.

The clasts have a pre dom i nantly ir reg u lar shape and their sort - ing is poor. The pelitic lime stone brec cia has a com pact frame - work, clast-sup ported fab ric and a cha otic tex ture. The clasts and ma trix are partly coated with dark Fe-Mn crusts and the de - posit con tacts with red pelitic lime stones (Fig. 2C).

The red crinoidal lime stones of the Krupianka Lime stone For ma tion, which were doc u mented as com po nents of the Wapiennik Brec cia Mem ber (Birkenmajer, 1952, 1958, 1963, 1977, 1979), have not yet been found in the pres ent re search.

Sim i lar pelitic lime stone brec cias ap pear also in the south - ern and west ern walls of the east ern part of Wapiennik Quarry.

Crinoidal lime stone brec cias were also found in the south ern wall of the east ern part of the quarry, as well as in the south ern wall of its west ern part, where they oc cur in the vi cin ity of Ju - ras sic nep tu nian dykes (Sidorczuk, 2005).

Fig. 3. The south ern side of the east ern wall in the east ern part of Wapiennik Quarry in Szaflary

A – Czorsztyn Lime stone For ma tion, Czorsztyn Suc ces sion: 1 – Smolegowa Lime stone For ma tion, 2 – Krupianka Lime stone For ma tion, 3 – Wapiennik Brec cia Mem ber (nod u lar ma trix in quan tity: a – larger, b – smaller), 4 – Czorsztyn Lime stone For ma tion;

B – cur rent ex po sure: RL – red lime stone, for other ex pla na tions see Fig ure 2

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MICROFACIES

De pos its of the brec cias de scribed rep re sent sev eral microfacies types. The cri noid, fil a ment and Globuligerina microfacies are the most com mon in the crinoidal lime stone brec cia clasts. The Saccocoma microfacies and the Globuligerina-fil a ment microfacies are less com mon in crinoidal brec cia clasts. The crinoidal lime stone brec cia ma trix rep re sents the Hedbergella microfacies. The fil a ment, Globuligerina, Saccocoma, Hedbergella and Globuligerina-fil - a ment microfacies most of ten oc cur in the clasts of the pelitic lime stone brec cia. The cri noid, fil a ment-ju ve nile gas tro pod and micritic microfacies are less com mon in clasts of the pelitic lime - stone brec cia. The Hedbergella and micritic microfacies oc cur in the pelitic lime stone brec cia ma trix.

MICROFACIES OF THE CRINOIDAL AND PELITIC LIMESTONE BRECCIA CLASTS

Cri noid microfacies (Fig. 4A). Packstones and grainstones. The dom i nant com po nents are cri noid skel e tal el e - ments (80–90% of the clast area in thin sec tion). Frag ments of brachi o pod shells, bryo zoan col o nies, echinoid spines and grains of de tri tal quartz are less com mon.

The cri noid microfacies oc curs in the crinoidal and pelitic lime stone brec cia clasts.

Fil a ment microfacies (Fig. 4B). Packstones rich in fil a - ments, which are thin bi valve shells of the ge nus Bositra (60–80% of the clast area in thin sec tion). They are ac com pa - nied by frag ments of cri noids, Globochaete spores, shells of ju ve nile gas tro pods, grains of de tri tal quartz and foraminifera rep re sent ing the ge nus Lenticulina Lamarck.

The fil a ment microfacies oc curs in crinoidal and pelitic lime stone brec cia clasts.

Globuligerina microfacies (Fig. 4C). Wackestones and packstones with dom i nant of plank tonic foraminifera rep re - sent ing the ge nus Globuligerina (40–60% of the clast area in thin sec tion). Fil a ments, frag ments of cri noids, foraminifers of the ge nus Lenticulina, ju ve nile gas tro pods, frag ments of bryo - zoan col o nies and peloids are less com mon.

The Globuligerina microfacies oc curs in crinoidal and pelitic lime stone brec cia clasts.

Saccocoma microfacies (Fig. 4D). Packstones rich in frag - ments of plank tonic cri noids Saccocoma (50–80% of the clast area in thin sec tion). They are ac com pa nied by frag ments of ses sile cri noids, fil a ments, grains of de tri tal quartz, foraminifera of the ge nus Lenticulina, peloids, Globochaete spores and shells of ju ve nile gas tro pods.

The Saccocoma microfacies oc curs in crinoidal and pelitic lime stone brec cia clasts.

Hedbergella microfacies (Fig. 4E). Packstones, rich in plank tonic foraminifera (about 60–90% of the clast area in thin sec tion) with dom i na tion by the ge nus Hedbergella – H.

planispira Tappan (Fig. 5A), H. delrioensis Carsey (Fig. 5B), Ticinella sp., Globigerinelloides bentonensis Mor row (Fig. 5C), Heterohelix moremani Cushman (Fig. 5D),

Guembelitria cenomana Keller (Fig. 5E), and Rotalipora appenninica Renz (Fig. 5F). Ben thic foraminifera, e.g.

Dorothia tro chus d’Orbigny and Tritaxia sp. are less com mon.

They are ac com pa nied by fil a ments and peloids.

The Hedbergella microfacies oc curs only in the pelitic lime stone brec cia clasts.

Globuligerina-fil a ment microfacies (Fig. 4F). Packstones with dom i na tion by foraminifers of the ge nus Globuligerina (50% of the clast area in thin sec tion) and fil a ments (30% of the clast area in thin sec tion). Frag ments of bryo zoan col o nies are less com mon.

The Globuligerina-fil a ment microfacies oc curs in crinoidal and pelitic lime stone brec cia clasts.

Fil a ment-ju ve nile gas tro pod microfacies (Fig. 4G).

Packstones rich in fil a ments (35–45% of the clast area in thin sec tion) and shells of ju ve nile gas tro pods (15–20% of the clast in thin sec tion). Peloids and frag ments of other shells also oc cur.

The fil a ment-ju ve nile gas tro pod microfacies oc curs only in the pelitic lime stone brec cia clasts.

Micritic microfacies (Fig. 4H). Mudstones with nu mer ous peloids, frag ments of cri noids, fil a ments or grains of de tri tal quartz.

The micritic microfacies oc curs in crinoidal and pelitic lime stone brec cia clasts.

MICROFACIES OF THE CRINOIDAL LIMESTONE BRECCIA MATRIX

Hedbergella microfacies. Mudstones, wackestones and rarely packstones rich in foraminifers (30–60% sur face of the ma trix area in thin sec tion) with dom i na tion by the ge nus Hedbergella: H. planispira, Heterohelix moremani, Globige - rinelloides bentonensis, Guembelitria cenomana and Rotalipora appenninica. Fil a ments and peloids are less com mon.

MICROFACIES OF THE PELITIC LIMESTONE BRECCIA MATRIX

Hedbergella microfacies. Wackestones and packstones.

The dom i nant com po nents in this microfacies are foraminifers (40–70%), mostly of the ge nus Hedbergella: H. planispira, H.

delrioensis, Ticinella sp., Globigerinelloides bentonensis, Heterohelix moremani, Planomalina buxtorfi Gandolfi (Fig. 5G), Rotalipora appenninica, Praeglobotruncana delrioensis Plummer (Fig. 5H), and Rotalipora ticinensis Gandolfi. Fil a ments, grains of de tri tal quartz and ben thic foraminifera of the ge nus Dorothia tro chus are less com mon.

Micritic microfacies. Mudstones with sev eral frag ments of cri noids and grains of de tri tal quartz.

STRATIGRAPHIC ANALYSIS

The age of the brec cia stud ied is de ter mined on the ba sis of foraminifera rec og nized in thin sec tions. Thir teen foraminifera spe cies from 16 thin sec tions are doc u mented. Foraminifers

Wapiennik Breccia Member (Pieniny Klippen Belt, Poland) – revised stratigraphy and origin 53

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Fig. 4. Microfacies of the crinoidal and pelitic lime stone brec cias

A – cri noid microfacies, B – fil a ment microfacies, C – Globuligerina microfacies, D – Saccocoma microfacies, E – Hedbergella microfacies, F – Globuligerina-fil a ment microfacies, G – fil a ment-ju ve nile gas tro pod microfacies, H – micritic microfacies

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Fig. 5. Foraminifera of the crinoidal and pelitic lime stone brec cias

A – Hedbergella planispira Tappan, B – Hedbergella delrioensis Carsey, C – Globigerinelloides bentonensis Mor row, D – Heterohelix moremani Cushman, E – Guembelitria cenomana Keller, F – Rotalipora appenninica Renz,

G – Planomalina buxtorfi Gandolfi, H – Praeglobotruncana delrioensis Plummer

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from the brec cia ma trix and clasts have been ana lysed sep a - rately in or der to achieve the most pre cise age in di ca tions. The palaeontological con tent of the ma trix is un doubt edly most in - dic a tive for the age as sign ment of the brec cia. The clast stra tig - ra phy has an ad di tional value if the ma trix is de void of marker taxa. In such cases the youn gest clast age con strains the age of the brec cia. The strati graphi cal ranges of the most in dic a tive foraminifera spe cies of the ma trix and clasts of the crinoidal lime stone and the pelitic lime stone brec cias are shown in Fig - ures 6 and 7 and are pre sented af ter Robaszyński and Caron (1995), Gale et al. (1996), Ken nedy et al. (2004) and Premoli and Verga (2004).

CRINOIDAL LIMESTONE BRECCIA

The ma trix of the crinoidal lime stone brec cia con tains the fol low ing foraminifera taxa (Fig. 6): Hedbergella planispira, Globigerinelloides bentonensis, Rotalipora appenninica, Guembelitria cenomana and Heterohelix moremani. The co-oc cur rence of these spe cies de ter mines the strati graphi cal range be tween the Rotalipora appenninica Zone (up per most Albian) and the lower part of the Rotalipora cushmani Zone (up per Cenomanian; Premoli and Verga, 2004).

The as sem blage of the crinoidal lime stone brec cia clasts con sists of Globuligerina sp., Ticinella sp., Globigerinelloides bentonensis, Guembelitria cenomana, Rotalipora appenninica and Lenticulina sp. The in dex taxa (Fig. 6) are in ac cor dance with the strati graphi cal in ter val in di cated by spe cies from the brec cia ma trix.

PELITIC LIMESTONE BRECCIA

The foraminifera as sem blage from the ma trix of the pelitic lime stone brec cia con sists of: Hedbergella delrioensis, H.

planispira, Globigerinelloides bentonensis, Rotalipora ticinensis, R. appenninica, Praeglobotruncana delrioensis, Planomalina buxtorfi, Heterohelix moremani, Dorothia tro - chus and Ticinella sp. The co-oc cur rence of Planomalina buxtorfi, R. appenninica and R. ticinensis is in dic a tive of the lower part of the Rotalipora appenninica Zone (up per most Albian).

The foraminifera as sem blage col lected from the pelitic lime stone brec cia clasts con sists of taxa with a lower strati - graphic value. The as sem blage is com posed of Globigerina sp., Hedbergella planispira, H. delrioensis, Ticinella sp., Dorothia tro chus, Globigerinelloides bentonensis, Heterohelix moremani, Guembelitria cenomana, Rotalipora appenninica, Tritaxia sp. and Lenticulina sp. The co-oc cur rences of the taxa in di cate a strati graphi cal range be tween the Rotalipora appenninica Zone (up per most Albian) and the lower part of the Rotalipora cushmani Zone (up per Cenomanian; Premoli and Verga, 2004).

Due to un cer tain geo met ri cal re la tions be tween the two com po nents of the Wapiennik Brec cia Mem ber con sist ing of the pelitic lime stone brec cia and the crinoidal lime stone brec - cia, as well as the pres ence of highly tectonised de pos its, the dat ing of the mem ber is dif fi cult and should be based on foraminifera taxa from both brec cias. The most pre cise strati -

graphic data are pro vided from the ma trix of the pelitic lime - stone brec cia. They in di cate a lat est Albian age of the Wapiennik Brec cia Mem ber. The mem ber is lim ited to the lower part of the Rotalipora appenninica Zone (up per most Albian), which cor re sponds to the lower part of Stoliczkaia dispar ammonite Zone (Ken nedy et al., 2004).

DISCUSSION

The Wapiennik Brec cia Mem ber was orig i nally at trib uted to the Czorsztyn Lime stone For ma tion of the Czorsztyn Suc - ces sion and re ported to rep re sent the Callovian–Oxfordian (Birkenmajer, 1977). The strati graphic data pre sented herein con strain a new strati graphic as sign ment of the mem ber (Sobstyl et al., 2009).

The ma jor ity of the stud ied clasts of the Wapiennik Brec - cia Mem ber con sist of white crinoidal lime stones rep re sent - ing the Smolegowa Lime stone For ma tion and red pelitic lime - stones of the Czorsztyn Lime stone For ma tion. The clasts of red lime stones that con tain Cre ta ceous Hedbergellidae foraminifera rep re sent the Chmielowa For ma tion. More over, the ma trix of the Wapiennik Brec cia Mem ber also shows ev i - dence of Cre ta ceous Hedbergellidae foraminifera. This sug - gests close re la tion of the Wapiennik Brec cia Mem ber to the Chmielowa For ma tion (Birkenmajer, 1963, 1977;

Alexandrowicz, 1979; Birkenmajer and Jednorowska, 1987;

Gasiński, 1988; Bąk et al., 1995), which con sists of red or var ie gated marly lime stones and shaly or nod u lar lime stones with the Hedbergella microfacies (Birkenmajer, 1977), by means of li thol ogy, micropalaeontological con tent and age of the brec cia (Fig. 8).

Clasts of the brec cias from Wapiennik Quarry rep re sent var i ous types of lime stones known in the PKB area (Wierzbowski, 1994; Wierzbowski et al., 1999; Jaworska 2000; Sidorczuk, 2005). The fol low ing main clast types were iden ti fied: lime stones of cri noid microfacies (Bajocian), lime - stones of fil a ment-ju ve nile gas tro pod microfacies (up per Bajocian–lower Bathonian), lime stones of fil a ment microfacies (up per Bajocian–up per Callovian), lime stones of Globuligerina microfacies (up per Callovian–Oxfordian), lime - stones of Saccocoma microfacies (Kimmeridgian to lower Tithonian) and lime stones of Hedbergella microfacies (up per Albian). The clasts from the Wapiennik brec cias show a dis or - dered ar range ment, im ply ing a high en ergy en vi ron ment, typ i - cal of de po si tion in top o graph i cally dif fer en ti ated bas ins. The lime stones with the Calpionella microfacies and lime stones with Globochaete microfacies, which are char ac ter is tic of the up per Tithonian and lower-mid dle Berriasian parts of the Czorsztyn Suc ces sion, have not been rec og nized. This may sug gest ero sion, karstic dis so lu tion or non de po si tion pe riod in that time.

The bi otic com po nents of the red pelitic lime stone ma trix of brec cias from the Wapiennik Quarry, in clud ing foraminifera, fil a ments, ju ve nile gas tro pods and frag ments of echinoderms, clearly in di cate de po si tion of the brec cias in an open ma rine en - vi ron ment. These find ings, along with sedimentological fea - tures such as the pres ence of poorly sorted and sharp-edged

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Fig. 6. Strati graphi cal range of the most im por tant plank tonic foraminifera from the crinoidal lime stone brec cia ma trix (solid lines) and clasts (doted lines)

Ranges of taxa af ter Premoli and Verga, 2004

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Fig. 7. Strati graphic range of the most im por tant plank tonic foraminifera from the pelitic lime stone brec cia ma trix (solid lines) and clasts (doted lines)

Ranges of taxa af ter Premoli and Verga, 2004

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clasts, strongly sug gest a tec tonic, synsedimentary or i - gin of the brec cias.

Albian ma rine brec cias from the Czorsztyn Suc - ces sion are also known from Dolný Mlyn and Kamenica in Slovakia (Aubrecht et al., 2006). Youn - ger brec cias also oc cur in the PKB: lower Cenomanian microbreccias were de scribed from Vršatec in West - ern Slovakia (Aubrecht et al., 2006) and from Jarabina near Stará Lubovňa in East ern Slovakia (Aubrecht et al., 2006).

The up per Albian brec cia from the Wapiennik Quarry con tacts di rectly with Bajocian white crinoidal lime stones of the Smolegowa Lime stone For ma tion.

More over, the old est clasts of these cri noid lime stones were found in up per Albian ma trix. This im plies rel a - tively deep pre-Albian ero sion of the de pos its. Deep ero sion can be, how ever, dem on strated from a few other places in the PKB. The first is Horné Sŕnie (Aubrecht et al., 2006), where up per Aptian/Albian de - pos its over lie Bajocian crinoidal lime stones and where Albian or Albian-Cenomanian nep tu nian micro dykes were found. Deep ero sion and slight tilt ing be tween the Bathonian and the Albian has been noted.

A sec ond ex am ple of the con tact be tween Bajocian crinoidal lime stones and Albian shales of the Pomiedznik For ma tion is Szczobiny on the west ern side of the Homole Gorge (Jurewicz, 1997), where Albian nep tu nian dykes pen e trate a crinoidal base ment.

An other ex am ple is the con tact be tween the Bajocian and the Albian was dis cov ered at Vršatec (Mišík, 1979). It is in ter preted as the re sult of the pen e - tra tion of Albian nep tu nian dykes into Bajocian crinoidal lime stones.

Ad di tional ev i dence for tec tonic move ments is the pres ence of tiny veins con tain ing Albian to Cenomanian? plank tonic foraminifera (Hedbergella, Thalman ninella, Rotalipora) in the up per Titho - nian-low est Berriasian de pos its from the Rogoźnik Klippen (Reháková in Wierzbowski et al., 2006).

There is no ev i dence for emer gence in the Wapiennik Quarry in Szaflary. How ever, deep ero sion of de pos its from the up per Albian to the lower Bajocian is ob served. The brec cia or i gin may be re - lated to sub ma rine ero sion of scarps, con strained by synsedimentary tec tonic ac tiv ity, which cre ated faults.

The tec tonic pro cess could be re lated to the geotectonic evo lu tion of the PKB dur ing the Cre ta - ceous (e.g., Golonka et al., 2003; Plašienka, 2003;

Csontos and Vörös, 2004; Jurewicz, 2005; Froitzheim et al., 2008). Late Albian tec tonic ac tiv ity of the PKB may have been re lated to the mid-Cre ta ceous Benkovo Phase (Plašienka, 2002, 2003; Froitzheim et al., 2008). How ever, the or i gin of sub ma rine scarps, fur - nish ing clasts of the brec cias, can not be un equiv o cally con cluded, al though their ge netic re la tion to fault - ing-in duced sea bot tom to pog ra phy seems jus ti fied.

Fig. 8. Strati graphic ta ble

for the Czorsztyn Suc ces sion af ter Ber et al. (2008) Ver ti cal lines in di cate hi a tus, the grey star in di cates

the Wapiennik Brec cia Mem ber

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CONCLUSIONS

1. The brec cia from the Wapiennik Quarry in cludes: the crinoidal lime stone brec cia and the pelitic lime stone brec cia.

Both brec cias dif fer in clast com po si tion, but are in cor po rated into the same red lime stone ma trix.

2. The age of the brec cias, as de ter mined on the ba sis of foraminifera in the brec cia ma trix, is con fined to the late Albian. This age de ter mi na tion is not con sis tent with the Callovian-Oxfordian age, pro posed by Birkenmajer (1977).

3. The or i gin of the brec cia is re lated to the sub ma rine ero - sion of scarps, gen er ated by synsedimentary tec tonic ac tiv ity of the Czorsztyn Swell dur ing the late Albian. This event may be as so ci ated with the mid-Cre ta ceous Benkovo Phase.

4. The brec cia from the Wapiennik Quarry has been known as the Wapiennik Brec cia Mem ber and at trib uted to the

Czorsztyn Lime stone For ma tion (Birkenmajer, 1977). The late Albian age of the brec cia, as well as its li thol ogy and micropalaeontological con tent, al lowed us to sug gest the at tri - bu tion of the Wapiennik Brec cia Mem ber to the Chmielowa For ma tion.

Ac knowl edge ments. Pre lim i nary find ings from this study were part of the MSc. the sis of A. Sobstyl (first au thor):

“Or i gin and stra tig ra phy of the lime stone brec cia from the Wapiennik Quarry in Szaflary (Pieniny Klippen Belt)”, Fac - ulty of Ge ol ogy, Uni ver sity of War saw, 2008. This work was sup ported by the Fac ulty of Ge ol ogy, Uni ver sity of War saw (M.S. & M.B., pro ject No. BW 1837/2). The au thors are grate ful to the re view ers, dr M. Krobicki and dr hab. R.

Aubrecht for their thor ough re view of the manu script and to prof. A. Wierzbowski for help ful dis cus sions and com ments.

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