New palaeomagnetic re sults from the Pol ish part of the Pieniny Klippen Belt, Carpathians — ev i dence for the palaeogeographic po si tion
of the Czorsztyn Ridge in the Me so zoic
Jacek GRABOWSKI, Micha³ KROBICKI and Katarzyna SOBIEÑ
Grabowski J., Krobicki M. and Sobieñ K. (2008) — New palaeomagnetic re sults from the Pol ish part of the Pieniny Klippen Belt, Carpathians — ev i dence for the palaeogeographic po si tion of the Czorsztyn Ridge in the Me so zoic. Geol. Quart., 52 (1): 31–44.
Warszawa.
Mid dle and Up per Ju ras sic lime stones from the Pol ish part of the Pieniny Klippen Belt (PKB) were palaeomagnetically stud ied at six lo - cal i ties. The Mid dle Ju ras sic red crinoidal lime stones of the Krupianka Lime stone For ma tion and Oxfordian radiolarites of the Czajakowa Radiolarite For ma tion, sam pled in the east ern part of the Pol ish sec tion of the PKB, were ei ther un suit able for palaeomagnetic stud ies (Krupianka Klippe) or remagnetized in the Neo gene (Baba and Zaskalskie-Bodnarówka klippen). The Czorsztyn Lime stone For ma tion was in ves ti gated at the lo cal i ties of Krempachy (up per Mid dle Ju ras sic: up per most Bajocian?–Callovian?), Ob³azowa (mid dle Oxfordian) and RogoŸnik (Rogo¿a Co quina Mem ber — Kimmeridgian). A pre-fold ing, mixed po lar ity com po nent of mag ne ti za tion was re vealed, which was in ter preted as pri mary. Palaeoinclinations dif fer slightly, but not sig nif i cantly, be tween lo cal i ties. The palaeolatitude of the Pol ish sec tor of the PKB, av er aged for the Mid dle/Up per Ju ras sic, amounts to 22°N (±5°). It cor re sponds to the es ti mated palaeolatitudes of the north ern mar gins of the Adri atic microplate and in di cates a sig nif i - cantly large dis tance from the Eu ro pean plate. There is a grow ing ev i dence for a north ward drift of the PKB in the Late Ju ras sic up to the ear li est Cre ta ceous: from the palaeolatitude of 22°N in the Late Ju ras sic up to 28°N in the west ern part, in Po land/W Slovakia, and from 28° up to 36°N in the east ern part of the PKB in Ukraine. Sys tem at i cally lower palaeolatitudes in the west com bined with ex ist ing palaeogeographic and geotectonic sce nar ios would ac count for a NE–SW ori en ta tion of the Czorsztyn Ridge in the Late Ju ras sic/ear li est Cre ta ceous.
Jacek Grabowski and Katarzyna Sobieñ, Pol ish Geo log i cal In sti tute, Rakowiecka 4, 00-975 Warszawa, Po land; e-mails:
jacek.grabowski@pgi.gov.pl, katarzyna.sobien@pgi.gov.pl; Micha³ Krobicki, Fac ulty of Ge ol ogy, Geo phys ics and En vi ron men tal Pro - tec tion, AGH Uni ver sity of Sci ence and Tech nol ogy, Mickiewicza 30, 30-059 Kraków, Po land; e-mail: krobicki@geol.agh.edu.pl (re - ceived: May 7, 2007; ac cepted: Au gust 20, 2007).
Key words: Po land, Pieniny Klippen Belt, Carpathians, Ju ras sic, palaeomagnetism.
INTRODUCTION
The palaeomagnetic method is a sen si tive tool for de tec tion of tec tonic ro ta tions within fold- and thrust belts (e.g. Pea cock et al., 1998; Van der Voo, 2004) and terrane trans la tions along the ac tive mar gins of a con ti nent (e.g. Umhoefer, 2000). It is also widely used to de tect the tec tonic af fin ity of “sus pect” ter - ranes by com par i son of the palaeomagnetic di rec tion with a ref er ence curve from neigh bour ing cratons (Van der Voo, 1993; Mor ris and Tarling, 1996). The Pieniny Klippen Belt (PKB) is a nar row zone, from a few hun dreds metres to about 20 km wide, that stretches along the strike of the West ern Carpathian Arc from the Vi enna Ba sin to Poiana Botizei (Ro - ma nia) (Fig. 1). It con sti tutes a bound ary be tween the Cen tral
and Outer West ern Carpathians. The de tailed his tory of both orogens in the Me so zoic from the point of view of plate tec ton - ics is still in suf fi ciently known due to a scar city of palaeomagnetic data. It is rel a tively well es tab lished that, in the Berriasian, both the Pieniny Klippen Belt and Cen tral West Carpathians were sit u ated rather close to the Eu ro pean Craton:
Berriasian palaeolatitudes for the Fatric Unit in the Tatra Mts.
and PKB in the West ern Slovakia amount to 27–28°N (Houša et al., 1996; Grabowski, 2005) which is not sta tis ti cally dif fer - ent from the palaeolatitude of the south ern edge of the Eu ro - pean Plate, cal cu lated from the ref er ence Berriasian palaeopole (Galbrun, 1985). Also the Berriasian lat i tu di nal dif fer ence be - tween Eu ro pean Craton and the east ern part of the PKB in Ukraine is palaeomagnetically un de tect able (Lewandowski et al., 2005). Con trast ing re sults ex ist for the Late Ju ras sic for the
east ern and west ern part of the PKB. The re sults of Kruczyk and K¹dzia³ko-Hofmokl (2006) in di cate a palaeolatitude of 36°N for the broad Mid to Late Ju ras sic (Batho - nian–Oxfordian) time span for the Pol ish part of the Pieniny Klippen Belt, which is very close to the ref er ence palaeolatitude cal cu lated from the Besse and Courtillot (2002) ap par ent po lar wan der paths. Lewandowski et al. (2005) re port im por tant palaeolatitudinal changes of the Ukrai nian sec tor of the PKB in the Mid dle–Late Ju ras sic: from 41°N in the Bajocian–Bathonian, through 28°N in the mid dle Oxfordian to 36°N in the Berriasian. In this study we pres ent new data from the Pol ish part of the Pieniny Klippen Belt, from lo cal i ties which hith erto have not been palaeomagnetically stud ied. The re sults are com pared with the ex ist ing palaeomagnetic da ta base for the PKB and ad ja cent ar eas, in or der to pro vide more data for the palaeotectonics and palaeo ge ogra phy of the Carpathian do main dur ing the Me so zoic.
GEOLOGICAL SETTING
The Me so zoic of the PKB is com posed of sev eral suc ces - sions of pre dom i nantly deep and shal lower-wa ter lime stones, cov er ing a time span from the Early Ju ras sic up to the Late Cre -
ta ceous (Andrusov, 1938, 1959; Birkenmajer, 1958, 1977, 1986, 1988; Andrusov et al., 1973; Miëík, 1994; Golonka and Krobicki, 2001, 2004). Dur ing the Ju ras sic and Cre ta ceous within the Pieniny Klippen Ba sin the sub ma rine Czorsztyn Ridge (= “pe lagic swell” of Miëík, 1994, mainly Czorsztyn Suc ces sion) and sur round ing zones formed an elon gated struc - ture dom i nated by pe lagic sed i men ta tion (Fig. 2) (Birkenmajer, 1977, 1986; Miëík, 1994; Michalík and Reháková, 1995;
Aubrecht et al., 1997; Plaëienka, 1999; Wierzbowski et al., 1999; Golonka and Krobicki, 2001, 2004). Its deep est part shows the pres ence of deep wa ter Ju ras sic–Early Cre ta ceous de pos its (pe lagic lime stones and radiolarites). Basinal sed i - men tary zones have been oc cu pied by the Pieniny and Branisko suc ces sions, whilst the Niedzica and Czertezik suc ces sions have been lo cated be tween these basinal units and the shal low - est Czorsztyn Suc ces sion (Birkenmajer, 1977, 1986, 1988;
Aubrecht et al., 1997; Wierzbowski et al., 2004). Strongly con - densed Ju ras sic–Early Cre ta ceous pe lagic cherty lime stones (Maiolica-type fa cies) and radiolarites (of the Grajcarek Unit) were also de pos ited in the north west ern Magura Ba sin (Outer Carpathian Ba sin).
The Pieniny Klippen Ba sin prob a bly opened dur ing Pliensbachian–Aalenian time, form ing a part of the global sys - tem re lated to the open ing of the Al pine Tethys. The Al pine Tethys, that is the Ligurian, Penninic and Pieniny/Magura
Fig. 1. Lo ca tion of the study area (A — gen eral view, B — de tails) with sam pling points
Oceans, con sti tute an ex ten sion of the Cen tral At lan tic sys tem (Stampfli et al., 1998). The synrift stage lasted in the Pieniny Klippen Ba sin from the late Early Ju ras sic to the Tithonian.
Gen er ally, the Pieniny Klippen Ba sin sed i men tary his tory is con nected with three tec tonic/sed i men tary events re flected firstly by ox y gen-re duced dark/black terrigenous de pos its of the Early–early Mid Ju ras sic age (Gresten-type and Fleckenkalk/Fleckenmergel fa cies), sec ondly by Mid dle Ju ras - sic–ear li est Cre ta ceous crinoidal, nod u lar (of the ammonitico rosso type) or cherty (of the Maiolica = Biancone type) lime - stones and radiolarites and thirdly by Late Cre ta ceous pe lagic marls (i.e. Scag lia Rossa type) fa cies and/or flysch/flyschoidal de pos its (Fig. 3) (i.a. Birkenmajer, 1986, 1988; Miëík, 1994;
Aubrecht et al., 1997; B¹k, 2000; Golonka and Krobicki, 2004;
Krobicki and Golonka, 2006).
The Pieniny Klippen Ba sin was closed at the Cre ta - ceous/Ter tiary tran si tion as an ef fect of strong Late Cre ta ceous (Subhercynian and Laramian) com pres sion (Birkenmajer, 1977, 1986). The Me so zoic suc ces sions were de tached and thrusted to wards the pres ent-day north, with the Czorsztyn Unit in the lower plate, and the Niedzica, Branisko and Pieniny
units in the up per plate po si tion. The to tal crustal short en ing was es ti mated as min i mum of 100 km (Birkenmajer, 1986).
The next ma jor tec tonic events took place in the Early and Mid dle Mio cene. They were re lated to the tec tonic es cape of the com pos ite North Pannonian (ALCAPA) ter rain from the Al pine col li sion zone (Balla, 1987; Csontos et al., 1992). The lo ca tion of the PKB just at the ac tive north ern mar gin of the North Pannonian ter rain re sulted in soft con ti nen tal col li sion (e.g. Royden and Burchfiel, 1989; Lille et al., 1994) and sev eral compressional and transpressional phases (e.g. Ratschbacher et al., 1993); these were man i fested by refolding of the Cre ta - ceous nappes and the de vel op ment of a sys tem of strike-slip faults that con sti tute the north ern and south ern bound aries of the PKB (Birkenmajer, 1986).
SAMPLING AND METHODS
36 ori ented drill cores, taken with a gas o line pow ered drill ing ma chine, and 6 ori ented hand sam ples, were col lected
Fig. 2. Palaeo ge ogra phy of the circum-Carpathian area dur ing the lat est Late Ju ras sic — ear li est Early Cre ta ceous and palinspastic sec tion through the Pieniny Klippen Ba sin (be low)
Bl — Bal kan, Cr — Czorsztyn Ridge, Hv — Helvetic shelf, IC — Central Carpathians, Kr — Kruhel, Mg — Magura Ba - sin, Mr — Marmaros Mas sif, PKB — Pieniny Klippen Ba sin, Ra — Rahov Ba sin, RD — Rheno-Danubian Ba sin, SC — Silesian Ridge (Cor dil lera), Sl — Silesian Ba sin, Sn — Sinaia Ba sin, St — Štramberk, Tr — Transilvanian Ocean; black line in di cates po si tion of palinspastic cross-sec tion (be low); plate po si tion at 140 Ma (af ter Golonka and Krobicki, 2001;
Krobicki and Golonka, 2006, mod i fied), palinspastic re con struc tion (af ter Birkenmajer, 1986, 1988, mod i fied)
from the Up per Ju ras sic de pos its at 6 lo cal i ties (Fig. 1B). Five lo cal i ties were sit u ated within the Czorsztyn Unit and one lo - cal ity within the Niedzica Unit. In RogoŸnik, near Nowy Targ (1 in Figs. 1 and 3), 5 cores were drilled in the lower part of the aban doned quarry (Birkenmajer, 1979; Reháková and Wierzbowski, 2005) from the red micritic lime stones of the
Rogo¿a Co quina Mem ber of the Czorsztyn Lime stone For ma - tion. The sam pled part rep re sents most prob a bly the Kimmeridgian (Parvu la–Borzai zones; Reháková and Wierzbowski, 2005). Five cores were col lected from blocks of brec cia interfingering with the coquinas in or der to per form a con glom er ate test. In the Ob³azowa Klippe (2 in Figs. 1 and 3), 7 cores were taken from the of the Czorsztyn Lime stone For ma tion, 1.3 to 2.5 m above the con tact with the Krupianka Lime stone For ma tion. The age of the sam pled in ter val is es ti - mated as mid dle Oxfordian, bas ing on ammonites and microfacies (Krobicki et al., 2006b). From one of the klippen, south of Krempachy (3 in Figs. 1 and 3), 5 hand sam ples were col lected from the Czorsztyn Lime stone For ma tion. Fil a ment microfacies and a lack of protoglobigerinids in di cate the pre-Oxfordian (up per most Bajocian–Callovian) part of the for ma tion (Pszczó³ko wski pers. comm.; Wierzbowski et al., 1999), with out the pos si bil ity of closer age de ter mi na tion. In two klippen in the east ern part of the PKB (So³tysie Ska³ki — 4 in Figs. 1 and 3), red crinoidal lime stones of the Krupianka Lime stone For ma tion (Mid dle Ju ras sic) were sam pled: 8 cores were taken from the Baba and 8 cores from the Krupianka Klippe. In the sin gle lo cal ity of the Niedzica Unit (Zaskalskie-Bodnarówka — 5 in Figs. 1 and 3), 3 cores and one hand sam ple were taken from the Oxfordian radiolarites of the Buwa³d Radiolarite Mem ber of the Czajakowa Radiolarite For ma tion.
From each core and hand sam ple 1–3 spec i mens were ob - tained for fur ther palaeomagnetic anal y sis. Nat u ral remanent mag net is ation (NRM) was mea sured with JR-5 and JR6a spin - ner mag ne tom e ters (AGICO, Brno; noise level 10–5 A/m) in the palaeomagnetic lab o ra tory of the Pol ish Geo log i cal In sti tute (PGI) in War saw. Sam ples were de mag net ised ther mally us ing the non-mag netic oven MMTD (Mag netic Mea sure ments, UK, rest field <10 nT). NRM mea sure ments and de mag neti sa tion ex per i ments were car ried out in mag net i cally shielded space (a low-field cage, Mag netic Mea sure ments, UK, which re duces the am bi ent geo mag netic field by about 95%). Mag netic sus - cep ti bil ity was mon i tored with a KLY-2 bridge (AGICO, Brno;
sen si tiv ity 10–8 SI units) af ter each ther mal de mag neti sa tion step. Char ac ter is tic remanence mag net is ation (ChRM) di rec - tions were cal cu lated by prin ci pal com po nent anal y sis (Kirschvink, 1980) us ing the PALMAG pack age of Lewandowski et al., (1997) and, oc ca sion ally, a remagne - tization cir cle method (McFadden and McElhinny, 1988).
Rock mag netic stud ies in cluded mostly stepwise ac qui si tion of the iso ther mal remanent mag net is ation (IRM) and ther mal de - mag neti sa tion of a com pos ite IRM ac quired along 3 per pen dic - u lar axes (Lowrie, 1990); the IRM was im parted us ing a MMPM1 pulse mag net iser pro duced by Mag netic Mea sure - ments (UK).
RESULTS
IRM ex per i ments en abled dis tinc tion of dif fer ent mag netic min er als in the out crops stud ied. In the red crinoidal lime stones of the Krupianka Lime stone For ma tion (Baba Klippe), sat u ra - tion of the IRM was not achieved at 1.4 T, in di cat ing the dom i -
Fig. 3. Strati graphi cal cor re la tion be tween Ju ras sic lithofacies (lithostratigraphic units af ter Birkenmajer, 1977) of the Pieniny Klippen Belt suc ces sions (af ter Wierzbowski et al., 2004; Krobicki and Golonka, 2006, mod i fied) with po si tion of sec tions sam pled
nance of a high coercivity mag netic frac tion. Its max i mum un - block ing tem per a tures of be tween 600–700°C are char ac ter is - tic for he ma tite (Fig. 4A). In the red micritic lime stones of the Rogo¿a Co quina Mem ber (RogoŸnik quarry) rapid in creases of the IRM in ap plied fields of up to 200 mT in di cates low coercivity min er als. The char ac ter of the IRM/IRM0 curve re - vealed also the oc cur rence of a sub or di nate high coercivity min eral-he ma tite. The dom i nant soft mag netic frac tion is prob - a bly fine-grained mag ne tite, with an un block ing tem per a ture about 450°C, as shown by the three-axis ther mal de mag ne ti za - tion curves (Fig. 4B).
Rocks were mod er ately mag netic with NRM in ten si ties mostly be tween 0.5 and 4 mA/m and mag netic sus cep ti bil ity val ues be tween 10–80 × 10–6. Be cause of the pres ence of he - ma tite, only ther mal de mag ne ti za tion was ap plied. Two com - po nents of magnetizations were clearly de fined at RogoŸnik, Ob³azowa and Krempachy. Be tween 100 and 250°C a com po - nent A was de mag ne tized (Fig. 5A). Its di rec tion is quite sim i - lar to the pres ent-day geo mag netic field di rec tion in the area in RogoŸnik (Fig. 6). How ever, it re veals an al most ver ti cal down ward in cli na tion at Ob³azowa and Krempachy (Fig. 6) in - dic a tive of a near-pole lat i tude. As the rocks stud ied could not reach sub-po lar po si tion dur ing last 20 My, it can be in ter preted in terms of a re sul tant vec tor or, for in stance, a re cent block ro - ta tion around a hor i zon tal axis due to neotectonics. The
neotectonic ac tiv ity of the PKB is well known (Zuchiewicz, 1980) and Qua ter nary ro ta tions of the Me so zoic klippen around a hor i zon tal axis were re ported e.g. from the Szaflary area (Fig. 1) (see Birkenmajer 1979 p. 59). Re cent hor i zon tal mo tions in the area are di rected NNE (Hefty, 1998) and rates of ver ti cal move ments do not ex ceed 0.5 mm/yr (Z¹bek et al., 1993; Czarnecki, 2004).
Be tween 300 and 550°C an other com po nent B was re - vealed (Fig. 5B, C). It re veals a N to NNW dec li na tion with a mod er ate pos i tive in cli na tion at RogoŸnik and a sim i lar dec li - na tion but neg a tive in cli na tion at Ob³azowa and Krempachy (Figs. 7A and 8A). Af ter tec tonic cor rec tion the com po nent B from all three lo cal i ties is rea son ably well clus tered. (Figs. 7B and 8B). The po lar ity of com po nent B is nor mal, though in two spec i mens from Ob³azowa the re versed po lar ity was ob - served. In one spec i men from Ob³azowa an anom a lous mag - ne ti za tion was found which, in geo graphic co or di nates, cor re - sponds to a steep in cli na tion re versed com po nent C from lo - cal ity Baba (Fig. 9).
Spec i mens from brec cia in the RogoŸnik quarry re vealed the same struc ture of mag ne ti za tion, with com po nent A and B of com pa ra ble un block ing tem per a tures to those de scribed above (Fig. 5D). How ever, both com po nents are dis persed (Fig. 10) which in di cates that they were ac quired be fore the or i - gin of the brec cia.
Fig. 4. Stepwise ac qui si tion of IRM and ther mal de mag ne ti za tion of IRM (Lowrie test) for Baba Klippe (A) and RogoŸnik quarry (B) IRM — iso ther mal remanent mag ne ti za tion
In the Baba lo cal ity, all spec i mens of red crinoidal lime - stones re vealed the pres ence of com po nent C, de mag ne tized be tween 150 and 400°C (Fig. 5E). At higher tem per a tures, the de mag ne ti za tion paths show great cir cles to wards the NNW in - di cat ing the pres ence of an other, yet un de ter mined, com po nent of nor mal(?) po lar ity. How ever, sta ble end points have not been reached and this com po nent has not been de ter mined. De -
mag ne ti za tion paths for red crinoidal lime stones of the Krupianka Lime stone For ma tion in their type lo cal ity were highly vari able and it was not pos si ble to iso late any char ac ter - is tic com po nent that might be sta tis ti cally sig nif i cant.
At Zaskalskie-Bodnarówka, two low un block ing tem per a - ture (100–250°C) com po nents A1 and A2 were cal cu lated (Fig. 11A). They re veal ex clu sively nor mal po lar ity and the di -
Fig. 5. Ex am ples of or thogo nal pro jec tions (Zijderveld di a grams) of de mag ne ti za tion paths dur ing ther mal treat ment In ten si ties of NRM: × 10–6 A/m
rec tion of com po nent A2 af ter tec tonic cor - rec tion ap proaches that of com po nent A1 be fore tec tonic cor rec tion (Fig. 11B and Ta - ble 1). At higher tem per a tures (300–500°C) a re versed po lar ity com po nent ap peared in all spec i mens, al though, only in two cases was a well-de fined lin ear de cay to the or i gin ob served (Fig. 5F). In 5 spec i mens it was pos si ble to cal cu late the com po nent us ing a method of remagnetization cir cles (McFadden and McElhinny, 1988) (Fig. 12).
The com po nent was ten ta tively com pared to com po nent C from the Baba lo cal ity, be - cause it re veals the same steep neg a tive in - cli na tion in both in situ and tec tonic co or di - nates. How ever, the dec li na tion of com po - nent C from Zaskalskie-Bodnarówka is closer to that of its coun ter part from Baba af - ter ap pli ca tion of tec tonic cor rec tion (Fig. 13). Two pos si ble in ter pre ta tions of the com po nent C at Zaskalskie-Bodnarówka (in pre- and postfolding co or di nates) are given in Ta ble 2.
TIMING OF MAGNETIZATION
The age of the com po nent A in Rogo - Ÿnik must be Late Ter tiary or youn ger, as in - ferred from its in cli na tion (Fig. 6). Com po - nent A is surely older than the sam pled brec - cia be cause its di rec tion is dis persed be - tween the brec cia clasts (see Fig. 10). This im plies that the brec cia it self is also rel a - tively young. More care ful in spec tion of the brec cia re veals that it might be re lated to
Fig. 6. Ste reo graphic pro jec tion of low tem per a ture com - po nent A from RogoŸnik quarry, Ob³azowa Klippe and Krempachy; lower hemi sphere pro jec tion
Fig. 9. Ste reo graphic pro jec tion of high tem per a ture com po nent C from Baba Klippe;
up per hemi sphere pro jec tion
Fig. 7. Ste reo graphic pro jec tion of high tem per a ture com po nent B from RogoŸnik quarry, Ob³azowa Klippe and Krempachy
A — be fore tec tonic cor rec tion, B — af ter tec tonic cor rec tion; white sym bols — up per hemi - sphere pro jec tion, other — lower hemi sphere pro jec tion; for other ex pla na tions see Fig ure 6
Fig. 8. Mean di rec tions cal cu lated from RogoŸnik quarry, Ob³azowa Klippe and Krempachy with á95 ovals plot ted
For other ex pla na tions see Fig ures 6 and 7
Fig. 10. Ste reo graphic pro jec tion of low tem per a ture com po nent A (squares) and high tem per a ture
com po nent B (cir cles) from RogoŸnik Brec cia white sym bols — up per hemi sphere pro jec tion,
black sym bols — lower hemi sphere pro jec tion
Fig. 11. Ste reo graphic pro jec tion of low tem per a ture com po nents A1 and A2 from Zaskalskie-Bodnarówka,
lower hemi sphere pro jec tion A — be fore tec tonic cor rec tion,
B — af ter tec tonic cor rec tion
T a b l e 1 Low tem per a ture com po nents
Lo cal ity Tect. corr. Com po nent Pol. D/I á95 k Dc/Ic á95 k N no/n
RogoŸnik 92/12 A NR 16/73 6.3 59.7 45/67 6.3 59.7 5 10/11
Ob³azowa 199/55 A NR 212/86 6.2 62.3 200/31 6.2 62.3 7 12/10
Krempachy 197/50 A NR 177/80 5.9 49.6 193/31 5.9 49.6 5 13/13
Zakalskie-Bodnarówka 38–50/
35–40
A2 NR 20/54 12.2 57.3 31/18 13.1 49.7
4 7/4
A1 NR 297/72 8.8 195.0 16/53 8.9 192.8 7/3
Tect. corr. — tec tonic cor rec tion (az i muth of bed ding dip/ bed ding dip); Pol. — po lar ity; D/I — dec li na tion/in cli na tion be fore tec - tonic cor rec tion; Dc/Ic — dec li na tion/in cli na tion af ter tectonic cor rec tion; á95, k — Fisher sta tis tics pa ram e ters; N — num ber of in de - pend ently ori ented cores/hand sam ples; no/n — num ber of spec i mens de mag ne tized/num ber of spec i mens used for cal cu la tion of char ac ter is tic di rec tion; NR — nor mal
C?
Fig. 12. High tem per a ture com po nent C? from Zaskal skie-Bodnarówka, cal cu lated us ing a method
of rema gnetization cir cles (see McFadden and McElhinny, 1988)
Fig. 13. Ste reo graphic pro jec tion of high tem per a ture com po nent C from Zaskalskie-Bodnarówka and Baba
Klippe, up per hemi sphere pro jec tion A — be fore tec tonic cor rec tion,
B — af ter tec tonic cor rec tion
karst phe nom ena which are well de vel oped in the quarry. We pre sume that karstification of the lime stones might have taken place in the Late Neo gene. There fore com po nent A must have been ac quired ear lier, most prob a bly dur ing weath er ing in the warm cli mate of the Late Ter tiary. The di rec tion of com po nent A from Ob³azowa and Krempachy might have been sub se - quently mod i fied due to neotectonic phe nom ena (see above).
Com po nent B is in ter preted as pre-fold ing at all three lo cal i ties (RogoŸnik, Ob³azowa and Krempachy). It might be a pri mary mag ne ti za tion and this is ad di tion ally sup ported by its mixed po lar ity. The in cli na tions of com po nent B at par tic u lar lo cal i - ties, in pre-fold ing co or di nates, are not iden ti cal: the in cli na tion is the shal low est at Ob³azowa (Oxfordian) and slightly steeper in older (Krempachy — Mid dle Ju ras sic) and youn ger (RogoŸnik — Kimmeridgian) rocks. This might re flect a grad - ual lat i tu di nal drift of the area (Ta ble 3). How ever, as each stage is rep re sented by a sin gle lo cal ity, and 95% er ror bars for the in cli na tions of com po nent B largely over lap, it might be pos si ble that in cli na tion and palaeolatitude dif fer ences are not sta tis ti cally sig nif i cant and a mean palaeoinclination 39° (±7°) must be cal cu lated for the area, as rep re sen ta tive for the late Mid to early Late Ju ras sic. This will be dis cussed in the next sec tion. Com po nent C is in ter preted as Neo gene remagne - tization co eval with in tru sion of an de site dykes, one of which is
sit u ated just 300 m from the Baba Klippe (Birkenmajer, 1970), close enough to el e vate the tem per a ture of the host rock. The di rec tion of com po nent C also cor re sponds well to re versed po - lar ity com po nents of steep in cli na tions, noted from the Pieniny andesites (Birkenmajer and Nairn, 1968; Kruczyk, 1970;
Márton et al., 2004).
DISCUSSION
Palaeoinclination 39o (±7o) cal cu lated from com po nent B at 3 lo cal i ties im plies a palaeolatitude for the area stud ied of 22°N (±5°) in the late Mid to early Late Ju ras sic (Oxfordian–Kimmeridgian). This re sult clearly con tra dicts the con clu sion of Kruczyk and K¹dzia³ko-Hofmokl (2006) who ob tained a mean palaeolatitude of 36°N (±7°) for the Pol ish part of the PKB for the Bathonian–Oxfordian. We do not have a good ex pla na tion for this con tra dic tion. Con trast ing palaeolatitudes from sev eral lo cal i ties in the Ukrai nian and Slovakian sec tors of the PKB were re cently re ported by Lewandowski et al., (2006a) who pos tu lated that the Czorsztyn Ridge might be com posed of sev eral microblocks (ter ranes).
This ex pla na tion can not rec on cile our re sults and those of
T a b l e 2 Char ac ter is tic di rec tions from the stud ied lo cal i ties — high tem per a ture com po nents B and C
Lo cal ity Tect. corr. Com po nent Pol. D/I á95 k Dc/Ic á95 k
Paleopole:
Lat. N/
Long. E
Dp/Dm N no/n
RogoŸnik 92/12 B NR 335/38 4.7 95.7 344/43 4.7 95.7 63/233 3/6 5 11/11
Ob³azowa 199/55 B NR +RV 347/-12 7.9 38.4 341/34 7.9 38.4 56/234 5/9 7 12/10
Krempachy 197/50 B NR 15/-10 8.5 37.7 15/40 8.5 37.7 61/171 6/10 5 13/9
Zakalskie-Bodnarówka 38–50/
35–40 C? RV 92/-64 9.1 69.2 184/-63 10.6 51.0 33/323 (btc)
86/169 (atc) 8/10
9/11 4 7/6
Baba – C RV 148/-64 7.6 28.6 148/-64 7.6 28.6 68/293 10/12 8 14/14
Krupianka – no re sults 8 no re sults 0/13
Dp/Dm — 95% con fi dence ovals of palaeopole cal cu la tion; btc — be fore tec tonic cor rec tion; atc — af ter tec tonic cor rec tion; RV — re versed; di rec tions ac cepted for geo log i cal in ter sec tions are in di cated with bold; other ex pla na tions as in Ta ble 1
T a b l e 3 Com par i son of Me so zoic palaeolatitudes from the west ern (Po land)
and east ern part of the PKB (Ukraine)
PKB west ern part PKB east ern part
Lo cal ity Age Palaeolatitude Lo cal ity Age Palaeolatitude
Brodno1 Tithonian/
Berriasian 27°N (±5°) Kamenets2 Berriasian 36°N (±8°)
RogoŸnik3 Kimmeridgian 25°N (±4°) Kimmeridgian 30°N (±10°)
Ob³azowa3 Oxfordian 21°N (±5°) Oxfordian 28°N (±6°)
Krempachy3 Callovian 23°N (±5°) Bajocian/Bathonian 41°N (±5°)
Mean
Callovian–Kimmeridgian 22°N (±5°) Mean
Bajocian–Berriasian 31°N (±3°)
1 — Houša et al. (1996), 2 — Lewandowski et al. (2005), 3 — this study
Kruczyk and K¹dziako-Hofmokl (op. cit.). It is dif fi cult to ac - cept that nearby lo cal i ties in the Pol ish part of the PKB (e.g.
RogoŸnik and Czorsztyn) were sep a rated in the Late Ju ras sic by as much as 14° (±6°) of lat i tude which equals al most 1500 km! The dif fer ence must re sult from in ter pre ta tion of the palaeomagnetic data. In gen eral, con cern ing the re sults of Kruczyk and K¹dzia³ko-Hofmokl (op. cit.), the mag netic re - cord in their rocks is much more com pli cated than that in ours, with many com po nents in ter preted as in ter me di ate di rec - tions. Their sam pling area em braced mostly a cen tral part of the Pieniny Klippen Belt in Po land (be tween Czorsztyn and Niedzica) with an iso lated lo cal ity in the east ern part (Homole).
Only two lo cal i ties be longed to the Czorsztyn Unit, while five other lo cal i ties were sit u ated in the Niedzica and Branisko units which are more dis turbed tec toni cally. Our re sults from the west ern part of PKB in Po land (RogoŸnik, Ob³azowa, Krempachy — ex clu sively Czorsztyn Unit) re veal a rel a tively sim ple struc ture of mag ne ti za tion with out sig nif i cant Neo gene remagnetization. On the other hand, more east erly lo cal i ties were ei ther remagnetized in the Neo gene (Baba and Zaskal - skie-Bodnarówka) or did not give any co her ent re sults (Kru - pianka). It may be pos tu lated that the east ern lo cal i ties might have been af fected ther mally in the Neo gene due to an de site in - tru sions, what prob a bly re sulted in more than one remagne - tization event and sig nif i cant loss of pri mary mag ne ti za tion.
The gen er ally con vinc ing re sults of Kruczyk and K¹dzia³ko- Hofmokl (op. cit.) from the Czorsztyn Cas tle Klippe (al though also af fected by Ter tiary remagnetization) re vealed a palaeo - latitude of 34° (±7°) dur ing de po si tion of the nod u lar lime - stones. How ever, it is not cer tain which part of the Czorsztyn Lime stone For ma tion was stud ied. If the sam ples were taken from the low er most part of the for ma tion they might rep re sent even the up per most Bajocian/low er most Bathonian Parkinsoni Zone (Wierzbowski et al., 1999; Krobicki et al., 2006a), thus the re sults are not com pa ra ble with ours.
PALAEOGEOGRAPHIC IMPLICATIONS
ORIENTATION OF THE CZORSZTYN RIDGE IN THE LATE JURASSIC
As in ter pre ta tion of palaeomagnetic data from the PKB, at the pres ent state of knowl edge, is equiv o cal, the geo log i cal im pli ca tions based on them must also be ac cepted with some cau tion. Nev er the less, we be lieve that our re sults, when com - pared to those of Lewandowski et al. (2005) shed some light on the orig i nal ori en ta tion of the Czorsztyn Ridge.
The struc tural ori en ta tion of the Czorsztyn Ridge re mains a mat ter of de bate. Var i ous trends have been drawn on palaeotectonic maps but mostly with lit tle com ment. Rakús et al.
(1988) sug gested an E–W to ENE–WSW ori en ta tion of the Czorsztyn Ridge, roughly par al lel to the Carpathian pro lon ga - tion of the Penninic ocean. The re con struc tions of Vašíèek et al.
(1994) and Michalík (1994) (in his fig. 5B), al though es sen tially sim i lar to those of Rakús et al. (1988), in di cate a NW–SE di rec - tion of the Czorsztyn Ridge in the Late Ju ras sic, thus sub-per - pen dic u lar to the NE–SW trend of the Penninic ocean. The same ori en ta tion of the Czorsztyn Ridge is sup ported by Channell and
Kozur (1997). An al ter na tive po si tion of the Pieniny Klippen Ba sin (and also of the Czorsztyn Ridge), par al lel to the Penninic NE–SW trend is given by Stampfli et al. (1998).
Golonka et al. (2000) in their fig ures 4 and 5, sug gest an E–W di rec tion of the Czorsztyn Ridge in Mid Ju ras sic–Early Cre ta ceous time with out any dis cus sion. Some geo log i cal ar gu - ments for NE–SW ori en ta tion of the Czorsztyn Ridge in the Tithonian–Berriasian were given by Golonka and Krobicki (2001). They in clude in di rect ev i dence bas ing on gen eral palaeo - geographic con sid er ations and ac cept also an E–W ori en ta tion as a pos si ble op tion. The NE–SW ori en ta tion, how ever, con forms with their mod eled wind and upwelling di rec tions in the Al - pine–Carpathian sec tor of the West ern Tethys. Aubrecht and Túnyi (2001) pos tu lated NE–SW ori en ta tions of nep tu nian dykes, cut ting the Czorsztyn Ridge at some lo cal i ties in W Slovakia. The orig i nal ori en ta tion of nep tu nian dykes was ob - tained us ing new palaeomagnetic data from the Vršatec, Babina, Bolesovska Dol ina and Meste¹sk« skala lo cal i ties. The re sults are, how ever, con fus ing and should be re in ter preted. They were par tially ques tioned by the au thors (Túnyi et al., 2004), who re - jected the re sults from Vršatec. More over, new palaeomagnetic re sults from the same lo cal i ties (e.g. Babina klippe — Lewan - dowski et al., 2006b) dif fer mark edly from those re ported by Aubrecht and Túnyi (2001). Palaeomagnetic ar gu ments for a NE–SW ori en ta tion of the Czorsztyn Ridge in the Mid Ju ras sic were given by Golonka et al. (2003), us ing the pre lim i nary data of Lewandowski et al. (2000, in the fi nal form as Lewandowski et al., 2005). The palaeolatitudes of the east ern ter mi na tion of the Czorsztyn Ridge in the Bajo cian–Bathonian cor re spond to the “ex pected” palaeolatitudes of the SE Eu ro pean mar gin (Lewandowski et al., 2005). This im plies a NE–SW ori en ta tion of the struc ture, par al lel to the edge of the Eu ro pean Plat form, at least in the Bajo cian–Bathonian.
When we ac cept that the Czorsztyn Ridge was a roughly con tin u ous struc ture of un vary ing length and that the Kamenets lo cal ity, stud ied by Lewandowski et al. (2000, 2005), was lo - cal ized on the ridge, we might com pare the co eval palaeolatitudes in the pres ent-day west ern and east ern part of the Czorsztyn Unit (Ta ble 3). It ap pears that palaeolatitudes from the west ern part are sys tem at i cally lower than from the east ern part. The dif fer ence amounts to 6–8° be tween the Oxfordian and the Berriasian. At the pres ent-day, the stud ied west ern part of the PKB is sit u ated 1° more to the north than the east ern part (Kamenets lo cal ity, Ukraine). That means that the west ern part of the PKB must have been pushed con sid er ably north wards, in re la tion to the east ern part, dur ing Late Me so - zoic and/or Ter tiary orogenic phases. This also im plies an orig - i nal NE–SW ori en ta tion of the Czorsztyn Unit in the Oxfor - dian–Berriasian, con sis tent with the palaeo ge ogra phy pos tu - lated by Stampfli et al. (1998), Golonka and Krobicki (2001), Golonka et al. (2003) and Krobicki and Golonka (2006). Ex ist - ing palaeomagnetic data ac count for a north wards drift of the PKB in the Late Ju ras sic up to the ear li est Cre ta ceous (Fig. 14):
from the palaeolatitude of 22°N in the Late Ju ras sic up to 28°N in the west ern part, and from 28° up to 36° in the east ern part (Lewandowski et al., 2005; this pa per). The method im ple - mented does not al low es ti ma tions of palaeolongitude, which is why there is only a sche matic in ter pre ta tion on Fig ure 14.
POSITION OF THE CZORSZTYN RIDGE WITH RESPECT TO MAJOR PLATES
A pos si ble age of mag ne ti za tion was es ti mated by plot ting in cli na tions from RogoŸnik, Ob³azowa and Krempachy against ref er ence in cli na tion trends for Eu rope, South (Fig. 15A) and North Af rica (Fig. 15B), cal cu lated for the Pieniny Klippen Belt geo graphic co or di nates (49°N, 20°E) as a func tion of time.
The Me so zoic Ap par ent Po lar Wan der Paths (APWP) of Besse and Courtillot (2002) was used for Eu rope (Fig. 15).
The main prob lem in the Af ri can APWP con struc tion is the rel a tive lack of re li able Af ri can Me so zoic poles. This could be com pen sated for by us ing palaeomagnetic data from other con - ti nents ro tated into Af ri can co or di nates ac cord ing to their age as did Besse and Courtillot (2002).
To de fine a mas ter APWP for Af rica, they used orig i nal Eur asian, North Amer i can and In dian data, trans ferred to the South Af ri can co or di nates and com bined with Af ri can data.
Av er age poles were cal cu lated ev ery 10 Ma with a 20 Ma win - dow (Fig. 15A).
Agree ment be tween data from Af rica and Adria in di cate their af fin ity and co her ent mo tion in the Late Ju ras sic/Early Cre ta ceous time in ter val. This is why palaeomagnetic data from Adria are com monly used to im prove the poorly doc u - mented Me so zoic APW path of Af rica. A com pos ite APW path in North Af ri can co or di nates was cre ated from Adria and West Gond wana data in te gra tion by Muttoni et al. (2001) (Fig. 15B).
An in cli na tion ver sus time plot shows in cli na tion which would be ex pected if the Czorsztyn Ridge re mained at tached to Eu rope or Af rica and al lows mea sure ment of its rel a tive dis - place ments with re spect to the ma jor plates. Com par i son of the mean PKB in cli na tions with the ex pected Eu ro pean and Af ri - can in cli na tions and sig nif i cant large dis tance from the Eu ro - pean trend in the Me so zoic lead to the con clu sion that Czorsztyn Ridge might have been very close to the Af ri can plate in the Late Ju ras sic. This con clu sion is in line with re cent data by Lewandowski et al. (2006b).
More over, com puted in cli na tions are very close to those ex - pected from the strati graphic age of the rocks sam pled. Good qual ity data en able de ter mi na tion of mag netic remanence age for the Me so zoic: Late Ju ras sic or Early/Late Cre ta ceous. We be lieve that the mag ne ti za tion in sam pled lo cal i ties is pri mary of Ju ras sic age, which is sup ported by its mixed po lar ity in
Fig. 14. Sche matic ori en ta tion and drift of the Czorsztyn Ridge in the Late Ju ras sic/ Early Cre ta ceous time in ter val pro posed on the ba sis of palaeogeographic and palaeomagnetic con sid er ations
Fig. 15. Ex pected Eu ro pean (af ter Besse and Courtillout, 2002) and Af ri can palaeoinclinations ( A — af ter Besse and Courtillout, 2002;
B — af ter Muttoni et al., 2001) cal cu lated for the geo graphic co or di nates of a given lo cal ity in the Pol ish sec tor of the Pieniny Klippen Belt and in cli na tions of the B com po nent cal cu lated in this study
Ob³azowa. A Cre ta ceous age of mag ne ti za tion is less prob a ble.
There is no ev i dence for any Cre ta ceous ther mal event in the Czorsztyn Ridge re gion, which could have led to remagne - tization. In the Early Cre ta ceous, the Ju ras sic rocks were cov - ered by rel a tively thin layer (about 50 m) of rock. A Late Cre ta - ceous age of sec ond ary mag netic remanence was re ported by Grabowski (2000) and Grabowski and Michalík (2005) in the Fatric Unit of the Cen tral West Carpathians. How ever, this remagnetization is ac com pa nied by ther mal re set of d18O ra tios in the Cen tral West Carpathians which, so far, have not been ob served in the PKB (Michalík et al., 1995).
CONCLUSIONS
1. Palaeomagnetically in ves ti gated Mid dle and Up per Ju - ras sic lime stones of the Czorsztyn Lime stone For ma tion (Pol - ish sec tor of the Pieniny Klippen Belt) re vealed a pre-fold ing, mixed po lar ity com po nent, in ter preted as pri mary. A mean Mid dle/Late Ju ras sic palaeolatitude of 22°N (±5°) was cal cu - lated for the area stud ied.
2. There is a grow ing ev i dence for a north ward drift of the PKB in the Late Ju ras sic up to the ear li est Cre ta ceous: from a
palaeolatitude of 22°N (this study) in the Late Ju ras sic up to 28°N (Houša et al., 1996) in the west ern, Pol ish–Slovakian part, and from 28° up to 36° in the east ern, Ukrai nian part (Lewandowski et al., 2005). Sys tem at i cally lower palaeo - latitudes in the west would im ply a NE–SW ori en ta tion of the Czorsztyn Ridge in the Me so zoic.
3. The mean pre-Oxfordian–Kimmeridgian palaeolatitudes from the west ern part of the PKB (this study) are lower by about 10° from those sug gested by Stampfli and Borel (2002).
They are con cor dant with Adri atic/Af ri can rather than with Eu - ro pean palaeolatitudes.
Ac knowl edge ments. The in ves ti ga tions were sup ported by the Min is try of Ed u ca tion and Sci ence (pro ject no.
6.14.0005.00.0 of the Pol ish Geo log i cal In sti tute) (JG and KS) and AGH Uni ver sity of Sci ence and Tech nol ogy (no.
11.11.140.447) (MK). Tech ni cal as sis tance from ing. T.
Sztyrak is also grate fully ac knowl edged. Spe cial thanks are due to prof. A. Pszczó³kowski (In sti tute of Geo log i cal Sci ences, Pol ish Acad emy of Sci ences) for in spec tion of thin sec tions from Krempachy. We wish to thank R. Aubrecht and M.
Lewandowski, the jour nal ref er ees, for their con struc tive re - views and help ful sug ges tions.
REFERENCES
ANDRUSOV D. (1938) — Geologický výskum vnitøního bradlového pásma v Západních Karpatech. III. Tektonika: Rozpravy Státneho Geologickeho Ústavu ÈSR, 9.
ANDRUSOV D. (1959) — Geológia èeskoslovenských Karpát II. SAV, Bratislava.
ANDRUSOV D., BYSTRICKÝ J. and FUSÁN O. (1973) — Out line of the struc ture of the West Carpathians. Guide Book, X Con gress CBGA, GÚDŠ, Bratislava.
AUBRECHT R. and TÚNYI I. (2001) — Orig i nal ori en ta tion of Nep tu - nian dykes in the Pieniny Klippen Belt (West ern Carpathians): the first re sults. Contribut. Geophys. Geod., 31 (3): 557–578.
AUBRECHT R., MIŠÍK M. and SÝKORA M. (1997) — Ju ras sic synrift sed i men ta tion on the Czorsztyn Swell of the Pieniny Klippen Belt in West ern Slovakia. In: Al pine Evo lu tion of the West ern Carpathians and Re lated Ar eas (eds. D. Plaaienka, J. Hók, J. Vozár and M.
Ellecko): 53–64. Dionýz Stur Pub lisher, Bratislava.
BALLA Z. (1987) — Ter tiary palaeomagnetic data for the Carpatho-Pannonian re gion in the light of Mio cene ro ta tion ki ne mat - ics. Tectonophysics, 139: 67–98.
B¥K K. (2000) — Biostratigraphy of deep-wa ter ag glu ti nated Foraminifera in Scag lia Rossa-type de pos its of the Pieniny Klippen Belt, Carpathians, Po land. In: Pro ceed ings of the Fifth In ter na tional Work shop on Ag glu ti nated Foraminifera (eds. M. B. Hart, M. A.
Kaminski and C. W. Smart). Grzybowski Foun da tion Spe cial Pub li ca - tion, 7: 15–41. Kraków.
BESSE J. and COURTILLOT V. (2002) — Ap par ent and true po lar wan - der and the ge om e try of the geo mag netic field over the last 200 Myr. J.
Geophys. Res., 107(B11), 2300, doi: 1029/2000JB000050. EPM 6.
BIRKENMAJER K. (1958) — Sub ma rine ero sional breaks and Late Ju ras - sic synorogenic move ments in the Pieniny Klippen Belt geosyncline.
Bull. Acad. Polon. Sc., Sér., Sc. Chim., Géol. Géogr., 8: 551–558.
BIRKENMAJER K. (1970) — Pre-Eocene fold struc tures in the Pieniny Klippen Belt (Carpathians of Po land). Stud. Geol. Pol., 31: 1–77.
BIRKENMAJER K. (1977) — Ju ras sic and Cre ta ceous lithostratigraphic units of the Pieniny Klippen Belt, Carpathians, Po land. Stud. Geol.
Pol., 45: 1–158.
BIRKENMAJER K. (1979) — Przewodnik geologiczny po pieniñskim pasie ska³kowym. Wyd. Geol., Warszawa.
BIRKENMAJER K. (1986) — Stages of struc tural evo lu tion of the Pieniny Klippen Belt, Carpathians. Stud. Geol. Pol., 88: 7–32.
BIRKENMAJER K. (1988) — Ex otic Andrusov Ridge: its role in plate-tec tonic evo lu tion of the West Carpathian Foldbelt. Stud. Geol.
Pol., 91: 7–37.
BIRKENMAJER K.and NAIRN A. E. M. (1968) — Palaeomagnetic stud - ies of Pol ish Rocks. III. Neo gene ig ne ous rocks of the Pieniny Moun - tains, Carpathians. Ann, Soc. Geol. Pol., 38: 475–489.
CHANNELL J. E. T.andKOZUR H. W. (1997) — How many oceans?
Meliata, Vardar and Pindos oceans in Me so zoic Al pine paleogeography. Ge ol ogy, 25: 183–186.
CSONTOS L., NAGYMAROSY A., HORVÁTH F.andKOVÁ M. (1992)
— Ter tiary evo lu tion of the Intra-Carpathian area: a model.
Tectonophysics, 208: 221–241.
CZARNECKI K. ed. (2004) — Geo dy nami cal stud ies of the Pieniny Klippen Belt — Czorsztyn Re gion (in Pol ish with Eng lish sum mary).
Instytut Geodezji Wy¿szej i Astronomii Geodezyjnej. Warszawa.
Monography.
GALBRUN B. (1985) — Magnetostratigraphy of the Berriassian stratotype sec tion (Berrias, France). Earth Planet. Sc. Lett., 74: 130–136.
GOLONKA J.andKROBICKI M. (2001) — Upwelling re gime in the Carpathian Tethys: a Ju ras sic–Cre ta ceous palaeogeographic and palaeoclimatic per spec tive. Geol Quart., 45 (1): 15–32.
GOLONKA J. and KROBICKI M. (2004) — Ju ras sic paleogeography of the Pieniny and Outer Carpathian bas ins. Rivista Italiana di Paleontologia e Stratigrafia, 110 (1): 5–14.
GOLONKA J., KROBICKI M., OSZCZYPKO N., ŒL¥CZKA A. and S£OMKA T. (2003) — Geodynamic evo lu tion and palaeo ge ogra phy
of the Pol ish Carpathians and ad ja cent ar eas dur ing Neo-Cim mer ian and pre ced ing events (latest Tri as sic–Ear li est Cre ta ceous). In: Trac ing tec tonic de for ma tion us ing the sed i men tary re cord (eds. T.Mc Cann and A. Saintot). Geol. Soc. Lon don, Spec. Publs., 208: 138–158.
GOLONKA J., OSZCZYPKO N. andŒL¥CZKA A. (2000) — Late Car - bon if er ous–Neo gene geodynamic evo lu tion and paleogeography of the circum-Carpathian re gion and ad ja cent ar eas. Ann. Soc. Geol. Pol., 70: 107–136.
GRABOWSKI J. (2000) — Palaeo- and rock mag ne tism of Me so zoic car - bon ate rocks in the sub-Tatric se ries (Cen tral West Carpathians) — palaeotectonic im pli ca tions. Pol. Geol. Inst., Spec. Pap., 5: 1–88.
GRABOWSKI J. (2005) — New Berriasian palaeopole from the Cen tral West Carpathians (Tatra Moun tains, south ern Po land): does it look Apulian? Geophys. J. Internat., 161 (1): 65–80.
GRABOWSKI J. and MICHALÍK J. (2005) — Remagnetization and thrust ing in the Krizna nappe of the Cen tral West Carpathians: a case study from the Tatra and Stražov Mts. TSG An nual Meet ing 2005.
Univ. Plym outh. Ab stract vol ume.
HEFTY J. (1998) — Es ti ma tion of site ve loc i ties from CEGRN GPS cam - paigns referred to CERGOP ref er ence frame. Rep. Ge od esy, 9 (36):
67–79.
HOUŠA V., KRS M., KRSOVÁ M. and PRUNER P. (1996) — Magnetostratigraphy of Ju ras sic-Cre ta ceous lime stones in the West - ern Carpathians. In: Palaeomagnetism and Tec ton ics of the Med i ter ra - nean re gion (eds. A. Mor ris and D. H. Tarling). Geol. Soc. Spec. Publ., 105: 185–194.
KIRSCHVINK J. L. (1980) — The least square line and plane and the anal y sis of palaeomagnetic data. J. Roy. Astr. Soc., 62: 699–718.
KROBICKI M. and GOLONKA J. (2006) — Field trip A — from Tethyan to Plat form Fa cies. Pieniny Klippen Belt. In: Ju ras sic of Po land and Ad ja cent Slovakian Carpathians. Field trip guide book (eds. A.
Wierzbowski, R. Aubrecht, J. Golonka, J. Gutowski, M. Krobicki, B.
A. Matyja, G. Pieñkowski and A. Uchman): 15–22. 7th In ter na tional Con gress on the Ju ras sic Sys tem, 6–18 Sep tem ber 2006, Kraków, Po land.
KROBICKI M., SIDORCZUK M. and WIERZBOWSKI A. (2006a) — Field trip B3 — In side Tethys. Pieniny Klippen Belt (Po land). Stop A1 –— Czorsztyn Cas tle Klippe–Czorsztyn Suc ces sion (Bajocia-Berriasian). In: Ju ras sic of Po land and Ad ja cent Slovakian Carpathians (eds. A. Wierzbowski, R. Aubrecht, J. Golonka, J.
Gutowski, M. Krobicki, B. A. Matyja, G. Pieñkowski and A.
Uchman): 23–28. Field trip guide book. 7th In ter na tional Con gress on the Ju ras sic Sys tem, 6–18 Sep tem ber 2006, Kraków, Po land.
KROBICKI M., SIDORCZUK M. and WIERZBOWSKI A. (2006b) — Field trip B3 – In side Tethys. Pieniny Klippen Belt (Po land). Stop B3.15 – Ob³azowa Klippe: stra tig ra phy and microfacies of the Czorsztyn Lime stone For ma tion (Bathonian-Tithonian, Czorsztyn Suc - ces sion). In: Ju ras sic of Po land and ad ja cent Slovakian Carpathians (eds. A. Wierzbowski, R. Aubrecht, J. Golonka, J. Gutowski, M.
Krobicki, B. A. Matyja, G. Pieñkowski and A. Uchman): 116–117.
Field trip guide book. 7th In ter na tional Con gress on the Ju ras sic Sys tem, 6–18 Sep tem ber, 2006, Kraków, Po land.
KRUCZYK J. (1970) — Palaeomagnetic in ves ti ga tions of the Mt. W¿ar andesites (in Rus sian). Publs. Inst. Geophys. Pol. Acad. Sc. 35.
KRUCZYK J. and K¥DZIA£KO-HOFMOKL M. (2006) —
Palaeomagnetic study of Mid dle–Up per Ju ras sic sed i ments from the Pol ish seg ment of the Pieniny Klippen Belt. Acta Geophys., 54:
205–224.
LEWANDOWSKI M., NOWO¯YÑSKI K. and WERNER T. (1997) — PDA — a pack age of FORTRAN pro grams for palaeomagnetic data anal y sis (manu script).
LEWANDOWSKI M., KROBICKI M., MATYJA B. A. and WIERZBOWSKI A. (2000) — Rekonesans paleomagnetyczny w jurajskie ska³y pieniñskiego pasa ska³kowego Ukrainy Zakarpackiej.
Polska Grupa Robocza Systemu Jurajskiego, I Spotkanie, Wiktorowo, 28–29.09.200; Ab stracts, Polskie Towarzystwo Geolo - giczne, Kraków.
LEWANDOWSKI M., KROBICKI M., MATYJA B. A. and WIERZBOWSKI A. (2005) — Palaeogeographic evo lu tion of the Pieniny Klippen Ba sin us ing strati graphic and palaeomagnetic data
from the Veliky Kamenets sec tion (Carpathians, Ukraine).
Palaeogeog., Palaeoclim., Palaeoecol., 216: 53–72.
LEWANDOWSKI M., ZIÓ£KOWSKI P. and SIDORCZUK M. (2006a)
— Palaeo ge ogra phy of some Ju ras sic bas ins of the Cen tral Eu rope — palaeomagnetic ap proach. In: Ju ras sic of Po land and Ad ja cent Slovakian Carpathians (eds. A. Wierzbowski, R. Aubrecht, J.
Golonka, J. Gutowski, M. Krobicki, B. A. Matyja, G. Pieñkowski and A. Uchman). Field trip guide book of the 7th In ter na tional Con gress on the Ju ras sic Sys tem. Po land, Kraków, Sep tem ber 6–18, 2006.
LEWANDOWSKI M., AUBRECHT R., KROBICKI M., MATYJA B. A., REHÁKOVÁ D., SCHLÖGL J., SIDORCZUK M. and WIERZBOWSKI A. (2006b) — Palaeomagnetism of the Pieniny Klippen Belt (Carpathians): ev i dence for low-lat i tude or i gin and palaeogeographic dis per sion of the Ju ras sic car bon ates. Vol. Jurassica, IV, 56–58. 7th In ter na tional con gress on the Ju ras sic Sys tem, Ab stracts.
LILLE R. J., BIELIK M., BABUŠKA V. and PLOMEROVÁ J. (1994) — Grav ity mod el ling of the litho sphere In the Eakstern Alpine — west ern Carpathian–Pannonian Ba sin re gion. Tectonophysics, 231: 215–236.
LOWRIE W. (1990) — Iden ti fi ca tion of fer ro mag netic min er als in a rock by coercivity and un block ing tem per a ture prop er ties. Geophys. Res.
Lett., 17: 159–162.
MÁRTON E., TOKARSKI K. and HALÁSZ D. (2004) — Late Mio cene coun ter-clock wise ro ta tion of the Pieniny andesites at the con tact of the In ner and Outer West ern Carpathians. Geol. Carpath., 55:
411–419.
MCFADDEN P. L.andMCELHINNY M. W. (1988) — The com bined anal y sis of remagnetization cir cles and di rect ob ser va tions in palaeo - magnetism. Earth Planet. Sc. Lett., 87: 161–172.
MICHALÍK J. (1994) — Notes on paleogeography and paleotectonics of the West ern Carpathian area dur ing the Me so zoic. Mitt. Osterr. Geol.
Ges., 86: 101–110.
MICHALÍK J. and REHÁKOVÁ D. (1995) — Sed i men tary re cords of Early Cre ta ceous tec tonic ac tiv ity in the Al pine-Carpathian re gion.
Slo vak Geol. Mag., 2: 159–164.
MICHALÍK J., REHÁKOVÁ D., HLADÍKOVÁ J. AND LINTNEROVÁ O. (1995) — Lithological and bi o log i cal in di ca tors of or bital changes in Tithonian and Lower Cre ta ceous se quences, West ern Carpathians, Slovakia. Geol. Carpath., 46 (3): 161–174.
MIŠÍK M. (1994) — The Czorsztyn sub ma rine ridge (Ju ras sic-Lower Cre - ta ceous, Pieniny Klippen Belt): an ex am ple of a pe lagic swell. Mitt.
Österr. Geol. Gess., 86: 133–140.
MORRIS A.andTARLING D. H. (1996) — Palaeomagnetism and tec ton - ics of the Med i ter ra nean re gion: an in tro duc tion. In: Palaeomagnetism and Tec ton ics of the Med i ter ra nean re gion (eds. A. Mor ris and D. H.
Tarling). Geol. Soc. Spec. Publ., 105: 185–194.
MUTTONI G., GARZANTI E., ALFONSI L., CIRILLI S., GERMANI D.
andLOWRIEW. (2001) — Mo tion of Af rica and Adria since the Perm ian: palaeomagnetic and paleoclimatic con straints from north ern Libya. Earth Planet. Sc. Lett., 192: 159–174.
PEACOCK D. C. P., ANDERSON M. W., MORRIS A. and RANDALL D.
E. (1998) — Ev i dence for the im por tance of “small” faults on block ro - ta tion. Tectonophysics, 299: 1–13.
PLAŠIENKA D. (1999) — Tektonochronológia a paleotektonický model jursko-kriedového vývoja centralnych Západných Karpat. Veda, Bratislava.
RAKÚS M., MIŠÍK M., MICHALÍK J., MOCK R., ÏURKOVIÈ T., KORÁB T., MARSCHALKO R., MELLO J., POLÁK M. and JABLONSKÝ J. (1988) — Paleogeographic de vel op ment of the West Carpathians: Anisian to Oligocene. In: Evo lu tion of the North ern Mar - gin of Tethys (eds. M. Rakus, J. Dercourt and A. E. M. Nairn). Mem.
Soc. Geol. France, 154 (3): 39–62.
RATSCHBACHER L., FRISCH W., LINZER H-G., SPERNER B., MESCHEDE M., DECKER K., NEMCOK M., NEMCOK J. and GRYGAR R. (1993) — The Pieniny Klippen Belt in the West ern Carpathians of north east ern Slovakia: struc tural ev i dence for transpression. Tectonophysics, 226: 471–483.
REHÁKOVÁ D.andWIERZBOWSKI A. (2005) — Microfacies and strati graphic po si tion of the Up per Ju ras sic Rogo¿a Coquinas at RogoŸnik, Pieniny Klippen Belt, Carpathians. Tomy Jurajskie, 3:
15–27.
ROYDEN L. H. andBURCHFIEL B. C. (1989) — Are sys tem atic vari a - tions in thrust belt style re lated to plate bound ary pro cesses? (The West ern Alps ver sus the Carpathians). Tec ton ics, 8 (1): 51–61 STAMPFLI G. M., MOSAR J., MARQUER D., MARCHANT R.,
BAUDIN T.andBOREL G. (1998) — Subduction and obduction pro - cesses in the Swiss Alps. Tectonophysics, 296: 159–204.
STAMPFLI G. M.andBOREL G. D. (2002) — A plate tec tonic model for the Pa leo zoic and Me so zoic con strained by dy namic plate bound aries and re stored syn thetic oce anic isoch rones. Earth Planet. Sc. Lett., 196:
17–33.
TÚNYI I., JELEÑSKA M.andAUBRECHT R. (2004) — Mid dle/Late Ju - ras sic ex ten sion in the Pieniny Klippen Belt in ferred from the ori en ta - tion of nep tu nian dykes. Contribut. Geophys. Ge od esy, 34: 156–157.
Spe cial Is sue. Paleo, Rock and En vi ron men tal Mag ne tism 9th Cas tle Meet ing, Ab stracts.
UMHOEFER P. J. (2000) — Where are the miss ing faults in trans lated ter - ranes? Tectonophysics, 326: 23–35.
VAN DER VOO R. (1993) — Palaeomagnetism of the At lan tic, Tethys and Iapetus Oceans. Cam bridge Univ. Press.
VAN DER VOO R. (2004) — Palaeomagnetism, oroclines and growth of the con ti nen tal crust. GSA To day, 14 (12): 4–9.
VAŠÍÈEK Z., MICHALÍK J. and REHÁKOVÁ D. (1994) —Early Cre ta - ceous stra tig ra phy, paleogeography and life in West ern Carpathians.
Beringeria, 10: 3–168.
WIERZBOWSKI A., JAWORSKA M. and KROBICKI M. (1999) — Ju ras - sic (Up per Bajocian-low est Oxfordian) ammonitico rosso fa cies in the Pieniny Klippen Belt, Carpathians, Po land: its fauna, age, microfacies and sed i men tary en vi ron ment. Stud. Geol. Pol., 115: 7–74.
WIERZBOWSKI A., AUBRECHT R., KROBICKI M., MATYJA B. A.
and SCHLÖGL J. (2004) — Stra tig ra phy and palaeogeographic po si - tion of the Ju ras sic Czertezik Suc ces sion, Pieniny Klippen Belt (West - ern Carpathians) of Po land and East ern Slovakia. Ann. Soc. Geol. Pol., 74: 237–256.
Z¥BEK Z., BARLIK M., KNAP T., MARGAÑSKI S. and PACHUTA A.
(1993) — Con tin u a tion of geodynamic in ves ti ga tions in the Pieniny Klippen Belt, Po land, from 1985 to 1990. Acta Geophysica Polonica, 41: 131–150.
ZUCHIEWICZ W. (1980) — Young tec tonic move ments and mor phol ogy of the Pieniny Mts, Pol ish West ern Carpathians. Ann. Soc. Geol. Pol., 50: 263–300.
