De vel op ment of the Mid-Pol ish Trough ver sus Late Ju ras sic evo lu tion in the Carpathian Foredeep area
Bronis³aw Andrzej MATYJA
Matyja B. A. (2009) — De vel op ment of the Mid-Pol ish Trough ver sus Late Ju ras sic evo lu tion in the Carpathian Foredeep area. Geol.
Quart., 53 (1): 49–62. Warszawa.
Late Ju ras sic is the key ep och for an idea of the ex is tence of the south east ern seg ment of the Mid-Pol ish Trough. New data on the evo lu - tion of Up per Ju ras sic de pos its in the Carpathian Foredeep sub strate pro vide in for ma tion that there is a com plete Oxfordian through Valanginian suc ces sion in the area of thick Oxfordian and Kimmeridgian de pos its, prov ing the oc cur rence of the trough. Thick ness of the Oxfordian and Kimmeridgian suc ces sion is twice to three times smaller than pre vi ously as sumed. The fa cies de vel op ment pat tern dis tin - guishes this area from the rest of the Late Ju ras sic ba sin. The sponge megafacies ranges up into the low er most Tithonian in this re gion.
Tithonian Štramberk-type reefs oc cur near the Carpathian thrust front and along side. The Late Ju ras sic and ear li est Cre ta ceous fa cies are lat i tu di nally ar ranged. Start ing from the lat est Mid dle Ju ras sic, the study area showed strong struc tural and fa cies re la tions to the Tethys do main. The col lected data con tra dict the hy poth e sis that the Mid-Pol ish Trough con tin ues in the Carpathian Foredeep sub strate.
Bronis³aw Andrzej Matyja, Fac ulty of Ge ol ogy, Uni ver sity of War saw, ¯wirki i Wigury 93, PL-02-089 Warszawa, Po land, e-mail:
Matyja@uw.edu.pl (re ceived: Sep tem ber 30, 2008; ac cepted: March 10, 2009).
Key words: Mid-Pol ish Trough, Late Ju ras sic, Carpathian Foredeep area, north ern Tethys shelf, sponge megafacies, Štramberk-type coral reefs.
INTRODUCTION
The hy poth e sis on the con tin u a tion of the Mid-Pol ish Trough into the Carpathian Foredeep sub strate was based mainly on the pres ence of thick Oxfordian and Kimmeridgian de pos its oc cur ring in this re gion (Po¿aryski, 1957b; Konarski, 1974; Morycowa and Moryc, 1976; Niemczycka and Brochwicz-Lewiñski, 1988).
The area of the pres ent strati graphic and fa cies anal y sis al - most en tirely be longs to that part of the Nida Synclinorium, which is cov ered by Mio cene de pos its of the Carpathian Foredeep. The Nida Synclinorium is fringed by a zone of Up - per Ju ras sic rocks. In both the Pol ish Jura Chain and south west - ern mar gin of the Holy Cross Moun tains, the rocks out crop at the sur face. Un like the Carpathian Foredeep area, knowl edge on the stra tig ra phy and fa cies pat tern of the out crop ar eas is much more com plete (e.g., Kutek, 1968, 1969; Matyja, 1977;
Kutek et al., 1977; Matyja and Wierzbowski, 2004; Zió³ko - wski, 2007).
The sed i men tary cy cle, to which be long the Up per Ju ras sic de pos its, in the Carpathian Foredeep sub strate started at the be -
gin ning of the late Bajocian (Moryc, 2006 — in the early Kuyavian, as in the orig i nal text) and ter mi nated in Valanginian or maybe Hauterivian times (Urbaniec and Œwietlik, 2003;
Dziadzio et al., 2004). De pos its of the cy cle un con form ably over lie an older sub strate and are un con form ably over lain by Up per Cre ta ceous rocks. Thus, they form a sep a rate struc tural stage. The re sults of in ves ti ga tions in sev eral tens of wells al - lowed me to pres ent a new hy poth e sis on the po si tion of the Late Ju ras sic ba sin in the Carpathian Foredeep area.
EVOLUTION OF THE VIEWS ON THE COURSE AND ORIGIN OF THE MID-POLISH TROUGH
An area show ing a trend for ac cu mu la tion of thick de pos its and par al lel to the edge of the East Eu ro pean Craton was a prom i nent palaeogeographic and struc tural el e ment of the epicratonic Perm ian and Me so zoic of Po land. The area was first dis tin guished by Po¿aryski (1957a) as the Dan ish–Pol ish Fur row. Slightly later (Po¿aryski, 1957b) that au thor de fined its course (see Fig. 1) and pointed to struc tural con straints on its evo lu tion. The north east ern limit of the fur row was strictly re -
lated to the so-called lower es carp ment of the East-Eu ro pean Craton (in the orig i nal text it was called the north east ern Eu ro - pean plate — op. cit.), and the fur row it self was be lieved to have been of geosynclinal na ture. The 1070 m thick Up per Ju - ras sic se quence en coun tered in the ¯ó³cza 1 bore hole (drilled in the Carpathian Foredeep area, for lo ca tion see Fig. 1) was to be in dic a tive of the south east ern con tin u a tion of the fur row.
In the 1970s, the geo log i cal ter mi nol ogy of the fur row was changed (Po¿aryski, 1975; Po¿aryski and Brochwicz- Lewiñski, 1978, 1979). The term fur row was re placed by the term aulacogen with a taphrogenic (graben) stage (see Fig. 2) with sed i men ta tion con trolled by a sys tem of faults and flex - ures, and a downwarp (syneclise) stage when sed i men ta tion of thick non-faulted se quences oc curred over a vast area. The time pe riod be tween these two stages cor re sponds to the late Early Cre ta ceous. Due to in de pend ent evo lu tion of the fur row be - tween the Dan ish and Pol ish seg ments, ob served from the Mid - dle Ju ras sic through Early Cre ta ceous, the term Dan ish–Pol ish Aulacogen was sub se quently re placed by the term Mid-Pol ish Trough (Po¿aryski, 1975). At the same time, its con tin u a tion to wards south east ern Po land was proved by in ter pre ta tions pre sented in pa pers by Kutek and G³azek (1972) and Konarski (1974). How ever, the prob lem of its fur ther ex ten sion into the Tethyan do main (Po¿aryski and ¯ytko, 1981) was sub ject to po lem ics (Wdowiarz, 1983). Re search on deeper-seated lithospheric zones (Guterch, 1968, 1977) al ready in di cated at that time that, within a 60–100 km wide area par al lel ling the Teisseyre-Tornquist line to the south-west, there is a zone where the Moho oc curs at greater depths than in the ad join ing ar eas. The zone is sep a rated from these ar eas by deep fault sys - tems. It was no ticed then that the zone fairly well co in cides with a syneclise stage of the Mid-Pol ish Aulacogen. How ever, it was also found out that it sig nif i cantly de vi ates from the axis of the Tri as sic–Ju ras sic graben in south east ern Po land (Po¿aryski and Brochwicz-Lewiñski, 1978, 1979).
Later re search of the litho sphere (Guterch et al., 1984;
Guterch and Grad, 2006) sup ported the view on the ex is tence of an elon gated crustal block be tween the East Eu ro pean Craton and the Palaeozoic plat form, re ferred to as the Trans-Eu ro pean Su ture Zone (TESZ) — Berthelsen (1993).
The TESZ is di vided by trans verse frac ture zones into three seg ments, but lo ca tions of these frac ture zones are dif fer ently marked by var i ous au thors (e.g. Guterch et al., 1984; Guterch and Grad, 1996; Dadlez, 1998; Fig ure 3).
Dadlez (1998) di vided the TESZ by trans verse crustal frac - ture zones into three seg ments of Pom er a nian, Kuiavian and Ma³opolska (Fig. 3). The Ma³opolska seg ment is sep a rated from the Kuiavian seg ment by the Grójec Fault. Al though in - cluded in the TESZ, the Ma³opolska seg ment dif fers so much from the Pom er a nian and Kuiavian seg ments that Dadlez (1997, 1998) made a con clu sion that, in south east ern Po land, the TESZ not only can not be iden ti fied with the Teisseyre-Tornquist Zone be cause it is wholly lo cated on the East Eu ro pean Craton, but also it is at all im pos si ble for rec og - ni tion. Any way, the crustal frac ture, bound ing the TESZ to the south-west, runs nearby or is a con tin u a tion of the Holy Cross Lin ea ment in the Ma³opolska seg ment (HCL on Fig. 3). It is sig nif i cant for the con sid er ations be cause the Me so zoic sed i - men tary fur row, un der stood as the main depocentral axis of the Pol ish Ba sin (Stephenson et al., 2003), was lo cated above the TESZ in North ern and Cen tral Po land (Dadlez et al., 1995;
Stephenson et al., 2003) and it di vorced from the TESZ in south east ern Po land. This ob ser va tion is in line with a view of Kutek (2001) who pos tu lated that the Mid-Pol ish Trough de - vel oped as an asym met ri cal rift ba sin.
Fig. 1. The course (shaded gray) of the Dan ish–Pol ish Fur row af ter Po¿aryski (1957b), sim pli fied
Denticulated line is re lated to north ern extention of Carpathian overthrust
Fig. 2. The course of the taphrogenic stage of the Mid-Pol ish Aulacogen (Trough) af ter Po¿aryski and Brochwicz-Lewiñski (1978, 1979) Lo ca tions of the bore holes men tioned by Konarski (1974) are in di cated;
note lo ca tion of Nieczajna Dolna 3, which is thought to mark a large thick - ness zone of the trough axis, is out side the zone
The idea that the Mid-Pol ish Trough evolved as the Mid-Pol ish Rift was pre sented by Kutek (1989, 1994b, 1996, 2001). That au thor sug gested that the south east ern part of the rift, ex tend ing south-east of the Holy Cross Lin ea ment, evolved as a prom i nent rift struc ture dur ing the late Mid dle Ju - ras sic, be ing ge net i cally re lated to the Carpathian rift sys tem (Kutek, 1989). In a later pa per, Kutek (1994b) re fined his hy - poth e sis claim ing that one of the rift sys tems, de vel op ing in
North ern and Cen tral Po land, was bor dered by the Holy Cross Lin ea ment. The other one, the Carpathian rift sys tem de vel op - ing in the south-east, formed as a re sult of north ward prop a ga - tion of the rift zone from the Carpathian do main into cratonic ar eas of West ern Ukraine and southeast ern Po land. Both the rift sys tems met at the Holy Cross Lin ea ment and amal gam ated dur ing Mid dle Ju ras sic times (Kutek, 1994b, p. 206). The Holy Cross Lin ea ment started to play a role of a trans fer fault at those times; hence, it was called the Holy Cross Trans fer Fault.
The Mid-Pol ish Rift was an asym met ric rift. Its prox i mal part in south east ern Po land was lo cated in a place of the pres ent day Lower San Anticlinorium. Its dis tal parts were sit u ated fur - ther south-west wards in the Nida Synclinorium, Silesia- Kraków Monocline and Up per Silesia Coal Ba sin (Kutek, 1996). A graben or half-graben stage of its evo lu tion, i.e. typ i - cal rift ing phase, com menced in the Callovian and the last rift - ing pulse oc curred in the Mid dle and Late Albian. The tran si - tion from a synrift to sag ba sin stage took place at the Albian/Cenomanian bound ary (Kutek op. cit.). The fun da men - tal the ses of the con cept of Mid-Pol ish Rift evo lu tion were re - cently re called (Kutek, 2001) in a broader con text of the Pol ish Ba sin evo lu tion. For these con sid er ations it is very im por tant to iden tify stron ger sub si dence rates dur ing the Oxfordian in ar eas sit u ated at a cer tain dis tance to the west of the rift. Such strong sub si dence is con sis tent with the sim ple-shear ex ten sion con - trol ling the Mid-Pol ish Rift.
Hakenberg and Œwidrowska (1997, p. 802), Dadlez et al.
(1998, p. 54) and Stephenson et al. (2003, p. 68) made some ob jec tions re gard ing var i ous as pects of the pre sented con cept on the rift ing evo lu tion of the Mid-Pol ish Trough. De tailed sed - i men tary and tec tonic evo lu tion of the SW mar gin of the East Eu ro pean Craton from Perm ian to early Maastrichtian time was pre sented now a days by Œwidrowska et al. (2008).
It should be noted in con clu sion that, since it has been dis - cov ered, the Mid-Pol ish Trough has also en com passed the area of south east ern Po land (Po¿aryski, 1957a). In the evo lu - tion of views on the trough, from a geosyncline-type sed i men - tary ba sin (Po¿aryski, 1957b) through an aulacogen (Po¿aryski and Brochwicz-Lewiñski, 1979) to a rift (Kutek, 1989, 1994b, 1996, 2001), the Late Ju ras sic evo lu tion ary stage played an es sen tial role.
All in ter pre ta tions are based on the pres ence of a huge 1300 m thick de pos its en coun tered in the sub strate of the Carpathian Foredeep (Fig. 4), as sumed to be of Oxfordian and Kimmeridgian age. More over, the de pos its are sit u ated broadly on the south east ern ex ten sion of the Mid-Pol ish Trough axis (Niemczycka and Brochwicz-Lewiñski, 1988; Kutek 1994, 2001 and Fig. 5 here). There fore, the prob lem of Late Ju ras sic his tory of the Carpathian Foredeep area seems to be es pe cially im por tant in terms of the above pre sented.
UPPER JURASSIC AND LOWER CETACEOUS DEPOSITS OF THE CARPATHIAN FOREDEEP
SUBSTRATE
The Up per Ju ras sic data are based on the most re cent strati - graphi cal in ves ti ga tions. Their pre lim i nary (Matyja and Barski,
Fig. 3. Teisseyre-Tornquist Tec tonic Zone af ter Guterch et al. (1984) and Guterch and Grad (1996) (spot ted); and crustal frac tures (shaded in grey be tween them) from deep seis mic sound ing (DSS) data af ter Dadlez (1997) sim pli fied
Fig. 4. Palaeoisopachs of the Up per Ju ras sic af ter Niemczycka and Brochwicz-Lewiñski (1988, fig. 5) sim pli fied
Grey-shaded ar eas in di cate re stored isopachs
2007) or fi nal but briefly pre sented (Barski and Matyja, 2008a, b) re sults have al ready been pub lished. A com pre hen sive re port on the strati graphi cal stud ies is cur rently un der prep a ra tion.
A num ber of lithostratigraphic units, hold ing the rank of for ma tions and mem bers, have been es tab lished within the en - tire con tin u ous Up per Ju ras sic–Lower Cre ta ceous se quence.
How ever, these are in for mal units and thus are used with uncapitalized lith o logic and unit-terms (Sal va dor, 1994). If pos si ble, the pre vi ously used unit names have been main tained be cause some of the suc ces sions in in di vid ual sec tions from the study area were very thor oughly ana lysed (Morycowa and Moryc, 1976; Golonka, 1978; Zdanowski et al., 2001; Bobrek et al., 2002). Due to the lim ited cov er age of the pa per, re search his tory and syn on ymy of the lithostratigraphic units are not pre sented.
The two old est for ma tions, £êkawica sponge lime stone For ma tion and Niwki lime stone-marly for ma tion, oc cur through out the whole Carpathian Foredeep area. The re main - ing for ma tions are lo cated in the north ern or south ern re gions.
The bound ary be tween them runs lon gi tu di nally south of D¹browa Tarnowska (see Fig. 6). Ear lier re ports on the vari - abil ity within the Up per Ju ras sic de pos its, with re gard to the Al gal-Oolitic Se ries, be tween the north and south were given by Golonka (1978).
£ÊKAWICA SPONGE LIMESTONE FORMATION
The lower por tion of the Up per Ju ras sic suc ces sion of the Carpathian Foredeep sub strate is com posed, like much of the
epicontinental Pol ish Ba sin, of the so-called Sponge Megafacies.
The Sponge Megafacies cor re sponds here to the £êkawica sponge lime stone for ma tion of very vari able thick ness re sult ing from both fa cies vari abil ity (bed ded and biohermal lime stones) and its dif fer ent strati graphi cal ranges in in di vid ual sec tions. The
£êkawica for ma tion is com monly over lain by the Niwki lime - stone-marly for ma tion. In ar eas of strong de vel op ment of biohermal fa cies, it is im me di ately over lain ei ther by the Swarzów lime stone for ma tion (north ern re gion) or by the Pilzno coral lifer ous lime stone for ma tion (south ern re gion). An interfingering of the £êkawica sponge lime stone for ma tion with the Niwki lime stone-marly for ma tion is ob served in a num ber of sec tions. There are also sec tions where sponge lime stones over - lie the Niwki for ma tion. There fore, the up per sponge lime stone mem ber has been es tab lished for this part of the £êkawica for - ma tion that over lies the Niwki for ma tion. The spa tial re la tion - ships be tween these for ma tions are il lus trated in Fig ure 7.
Thick ness1 of the £êkawica for ma tion is vari able and ranges from 68 m to 570 m.
NIWKI LIMESTONE-MARLY FORMATION
The lime stone-marly for ma tion was es tab lished by Morycowa and Moryc (1976). Golonka (1978) called these de - pos its the Niwki se ries. It is com posed of marls, marly lime - stones and pelitic lime stones con tain ing rare or ganic re mains.
The Niwki lime stone-marly for ma tion over lies or interfingers the £êkawica for ma tion, but is over lain by dif fer - ent lithostratigraphic units: the Pilzno coral lime stone for ma - tion or up per sponge lime stone mem ber in the south, and the Swarzów lime stone for ma tion in the north.
As men tioned above, the £êkawica for ma tion can oc cur as a lat eral equiv a lent to the Niwki for ma tion. It is man i fested by the oc cur rence of sponge lime stone interbeds in a num ber of bore hole sec tions in dif fer ent parts of the Niwki for ma tion.
Thick ness of the Niwki for ma tion var ies from 0 to 587 m.
SWARZÓW LIMESTONE FORMATION
This for ma tion was es tab lished by Morycowa and Moryc (1976) as the coral lifer ous-al gal for ma tion in the D¹browa Tarnowska re gion. It con sists mostly of var i ous types of grained lime stones (e.g., organodetrital, oolitic and oncolitic lime stones) with abun dant cor als and al gae. More de tailed lithological and well-log char ac ter is tics is given by Morycowa and Moryc (op. cit.). Thick ness of the Swarzów lime stone for - ma tion ranges be tween 118 and 177 m.
SMÊGORZÓW COQUINA FORMATION
This for ma tion was es tab lished by Morycowa and Moryc (1976) as the lime stone-dolomitic co quina for ma tion in the
Fig. 5. Up per Ju ras sic isopachs (af ter Niemczycka and Brochwicz- Lewiñski, 1988; see also Fig. 4) su per im posed on the Trans-Eu ro pean Su ture Zone (TESZ) (af ter Dadlez, 1997; see also Fig. 3)
1The values refer to complete thicknesses preserved within the Upper Jurassic–Lower Cretaceous succession. If part of the formation’s deposits was removed by subsequent erosion, it is clearly stated.
D¹browa Tarnowska re gion. The lower part of the for ma tion com monly con tains a 2–5 m thick marl bed, mostly slightly sandy and with glauconite. Above, there is a se ries of organodetrital lime stones con tain ing abun dant bi valves and cri noids, with interbeds of de tri tal and oolitic lime stones. This se ries is over lain by a more marly co quina layer com posed mostly of un bro ken shells rep re sent ing mainly oys ters.
The up per most por tion of the suc ces sion con sists largely of co quina lime stones and marls with abun dant Exogyra in di vid u - als. These de pos its rep re sent the Smêgorzów co quina for ma tion with its lithological and well-log char ac ter is tics given by Mory - cowa and Moryc (1976). The ex tent of the Smêgorzów co quina for ma tion is lim ited to the north ern fa cies re gion. The for ma tion is no where pre served in full; its up per bound ary is ero sional. The max i mum pre served thick ness of the for ma tion is 160 m.
PILZNO CORAL LIMESTONE FORMATION
This for ma tion, es tab lished by Matyja and Barski (2007) is rep re sented by a few hun dred metres thick reef-form ing coral - lifer ous lime stones. This for ma tion oc curs in the south ern re - gion and forms a lat i tu di nally ex tend ing zone near the Carpathian Thrust front be tween the ar eas lo cated about 20 km east of Dêbica and about 15 km west of Tarnów (Fig. 8). Their
west ern and east ern bound aries are ero sional. This for ma tion gen er ally over lies the Niwki for ma tion or the £êkawica for ma - tion, and is over lain by the Ropczyce for ma tion. There are also ar eas where the Pilzno for ma tion lat er ally interfingers with part of the Niwki for ma tion.
Thick ness of the Pilzno for ma tion var ies from 0 to 466 m.
ROPCZYCE LIMESTONE FORMATION
Golonka (1978) de fined the Ropczyce for ma tion as a dolomitic-lime stone se ries (Ropczyce se ries). This for ma tion is clearly bi par tite and thus sub di vided into two mem bers (Zdanowski et al., 2001; Maksym et al., 2001). The lower mem ber, re ferred to as the lime stone-dolomitic mem ber, is com posed mainly of lime stones and dolomites con tain ing pseudo morphs af ter gyp sum, evaporite-so lu tion col lapse brec - cia, Clypeina biomicrites and lam i nated bird’s-eye lime stones (Maksym et al., 2001). The up per mem ber, so-called lime - stone-marly mem ber, is char ac ter ized by a con sid er able in - crease in clay con tent and ad mix ture of de tri tal quartz grains (op. cit.).
Thick ness of the Ropczyce for ma tion is 312–423 m. Thick - nesses of the lime stone-dolomitic and lime stone-marly mem - bers are 92–319 m and 66–114 m, re spec tively.
Fig. 6. Lo ca tion map of area il lus trated in Fig ures 8–10 in the Geo log i cal Map of Po land with out Caino zo ic De pos its (Dadlez et al., 2000)
DÊBICA LIMESTONE FORMATION
The Ropczyce for ma tion is over lain by the up per al gal se - ries (Dêbica se ries) iden ti fied by Golonka (1978). It is rep re - sented by organogenic al gal lime stones and grainstones. The com plete thick ness of the Dêbica for ma tion is un known due to its ero sional up per bound ary. The max i mum pre served thick - ness is 94 m.
STRATIGRAPHIC POSITION OF THE LITHOSTRATIGRAPHIC UNITS
The most se ri ous dis ad van tage of the pre vi ous re ports on the Up per Ju ras sic de pos its from southeast ern Po land was the lack of strati graphi cal anal y ses. Stud ies of ammonites, as orthostratigraphic fos sils, en abled both es tab lish ing the strati - graphic po si tion and mak ing a very thor ough cor re la tion be - tween dif fer ent fa cies types within the Up per Ju ras sic suc ces - sion of the Kraków–Czêstochowa Up land (see Matyja and Wierzbowski, 2004) and the southwest ern mar gin of the Holy
Cross Moun tains (see Kutek, 1968; Matyja 1977), i.e. out crop ar eas fring ing the Nida Synclinorium.
Ammonite finds are not nu mer ous in these rocks, nei ther are il lus tra tions of the spec i mens (e.g., Król, 2004). Mid dle Oxfordian ammonites have been re ported by Król (2004).
From a pelitic lime stone se ries, that au thor re ports the pres ence of Cardioceras (Plasmatoceras) sp., whereas Perisphinctes (Dichotomosphinctes) sp. is known from the low er most part of the sponge lime stone suc ces sion. The for mer spec i men doc u - ments the lower part of the Plicatilis Zone, while the lat ter one
— the Mid dle Oxfordian Transversarium Zone. Both the men - tioned lithologies cor re spond to the low er most part of the
£êkawica for ma tion. All these data in di cate that the lower part of the £êkawica sponge lime stone for ma tion oc cu pies the same strati graphic po si tion as the Czêstochowa sponge lime stone for ma tion from the Pol ish Jura Chain (e.g., Matyja and G³owniak, 2003) and the south west ern mar gin of the Holy Cross Moun tains (Matyja, 1977).
Only two ammonites have been cited, but not il lus trated, from youn ger de pos its. One of them was found in the lower part (mem ber “b”) of the lime stone-dolomitic co quina for ma -
Fig. 7. Chronostratigraphic po si tion of the Up per Ju ras sic and Lower Cre ta ceous lithostratigraphic units in the Carpathian Foredeep area (based on Barski and Matyja, 2008b)
USLM — up per sponge lime stone mem ber
tion (Smêgorzów for ma tion in this re port) — see Morycowa and Moryc, 1976. This ammonite was iden ti fied by Cimaszewski (pers. comm. Moryc) as Ataxioceras sp. in di cat - ing the lower Kimmeridgian. The strati graphic po si tion of these de pos its is in a dra matic con tra dic tion to the re main ing age de ter mi na tions pre sented in this pa per (see be low). The other ammonite spec i men was found 30 m be neath the top of the Niwki for ma tion. It was iden ti fied as Orthosphinctes sp. by Gutowski (Gutowski et al., 2007) and is ac tu ally iden ti fied as rep re sen ta tive of much youn ger evo lu tion ary lin eage of Discosphinctoides–Sarmatisphinctes–Ilowaiskya oc cur ring from the up per Kimmeridgian Autissiodorensis Zone through the lower Tithonian (see Kutek and Zeiss, 1997). The pre - served spec i men re sem bles in di vid u als of the for mer gen era.
Pre vi ous biostratigraphic de ter mi na tions of other microfossils en able aug ment ing or sup port ing the Up per Ju ras - sic stra tig ra phy of the Carpathian Foredeep area, pre sented in this paper.
Since the 1970s, there has been a lot of in for ma tion about the oc cur rence of tintinnids in the Al gal–Oolitic Se ries (cor re - spond ing to the Swarzów and Pilzno for ma tions in the pres ent pa per) from which Golonka (1978) re ported the pres ence of a spec i men rep re sent ing “...prob a bly the gen era of Crassicolaria...”. Morycowa and Moryc (1976) also il lus trated
“...microfossils re sem bling tintinnids...” (op. cit., p. 250, pl. 14,
fig. 1a–e, h and fig. 2) from the mem ber “d” of the Coral lifer - ous-Al gal Lime stone For ma tion (Swarzów for ma tion in this re - port). In the light of the new data, those pre vi ously rec og nized oc cur rences cre ate a suprisingly co her ent im age of the stra tig - ra phy (Matyja and Barski, 2007; Barski and Matyja, 2008a, b).
Among other microfossils used as biostratigraphic in di ca - tors, cal car e ous dinocysts, foraminifers (Garlicka, 1974;
Olszewska, 1998, 1999; Bobrek et al., 2002); and re cently or - ganic dinoflagellate cysts (Matyja and Barski, 2007; Barski and Matyja, 2008a, b) are the most im por tant.
Anal y sis of or ganic as so ci a tions of dinoflagellate cysts in - di cates that most sam ples con tain rich and well-pre served palynological ma te rial. The most abun dant as so ci a tions were found in the Niwki for ma tion and part of the £êkawica sponge lime stone for ma tion. With few ex cep tions, poor but es pe cially im por tant re sults have been ob tained from youn ger de pos its.
The re sults of biostratigraphic anal y ses are pre sented be low (see also Fig. 7).
The on set of marly sed i men ta tion of the Niwki for ma tion falls on the late Oxfordian Bifurcatus Chron. The doc u mented up per bound ary of the Niwki for ma tion runs within the lower Tithonian in most of the bore hole sec tions. The only area where it ranges up at least to the up per Tithonian is the south-east of the south ern re gion. It is worth not ing that at least 200 m thick part of the Niwki for ma tion was as signed by Golonka (1978) to
Fig. 8. Dis tri bu tion of Early Kimmeridgian shal low wa ter car bon ate plat form and se lected for ma tions For area lo ca tion see Fig ure 6
the Kimmeridgian, based on foraminifera stud ies. Ana lys ing, among oth ers, cal car e ous dinocysts, Olszewska (1998) placed the up per bound ary of the Niwki for ma tion within the up per Kimmeridgian.
The strati graphi cal range of the £êkawica for ma tion is vari - able. Its lower bound ary runs within the lower Oxfordian whereas the up per one can range up into ei ther the up per Oxfordian Bifurcatus Zone or even the lower Tithonian.
Dinocyst de ter mi na tions, made on the Swarzów lime stone for ma tion, doc u ment a strati graphic in ter val com pris ing the up per lower Tithonian to up per Tithonian, and prob a bly up per - most up per Tithonian–Berriasian.
The age of the Smêgorzów co quina for ma tion re mains un - clear. It can not be pre cluded that it is late Tithonian or Berriasian.
The age of the Pilzno coral lime stone for ma tion was di - rectly de ter mined by the pres ence of an up per Tithonian tintinnid as sem blage (Barski and Matyja, 2008a). Be cause the Pilzno for ma tion over lies in gen eral both the Niwki and
£êkawica for ma tions, which range up into the lower Tithonian, it can be as sumed that the Pilzno for ma tion started to be de pos - ited not ear lier than dur ing the early Tithonian.
The up per bound ary of the Pilzno for ma tion is de fined by the age po si tion of the Ropczyce for ma tion. In the Zagorzyce 6 bore hole, in the lime stone–marly mem ber of the up per part of the Ropczyce for ma tion, the so-called small form of Calpionella alpina was found at a depth of 2836 m (Olszewska, 1999). Such forms first oc curred at the base of the calpionellid “zone B” and per sisted through the calpionellid
“zone D” cor re spond ing to the up per most Tithonian–low er - most Valanginian in ter val (Remane, 1985). Be tween the lime - stone–marly mem ber of the Ropczyce for ma tion and the Pilzno for ma tion there is the lime stone–dolomitic mem ber of the Ropczyce lime stone for ma tion (92–319 m in thick ness) rep re - sent ing an ex tremely shal low-ma rine, lo cally la goonal en vi - ron ment. As sum ing that the en vi ron ment’s de vel op ment re - sulted in a break ing of the ma rine com mu ni ca tion with the ba - sin in Cen tral Po land, and know ing that it oc curred pre cisely in the zarajskensis ho ri zon of the late Tithonian Scythicus Chron (Kutek, 1994a), I lean to the opin ion that the strati graphic po si - tion of the Pilzno coral lime stone for ma tion at the cur rent stage of study falls be tween the up per part of the lower Tithonian and the lower part of the up per Tithonian (Fig. 7).
The strati graphi cal anal y sis has shown that the strati graphic po si tion of the Up per Ju ras sic de pos its in the Carpathian Foredeep sub strate is char ac ter ized by a strong pe cu liar ity in re la tion to lithologically sim i lar Up per Ju ras sic de pos its from the mar gin of the Holy Cross Moun tains and Nida Synclinorium, which they were pre vi ously cor re lated with. The most im por tant at trib utes of the peculiarity are as follows:
— A much greater strati graphic range of the £êkawica sponge lime stone and Niwki lime stone-marly for ma tions. In the south ern re gion of the Carpathian Foredeep, the sponge megafacies, rep re sented by the £êkawica for ma tion, ranges up into the lower Tithonian, whereas to wards the north i.e. in the SW mar gin of the Holy Cross Moun tains it is re placed in the up per most Oxfordian by a shal low wa ter car bon ate plat form (Kutek, 1968; Matyja et al., 1989). In the Wieluñ Up land, the megafacies also cov ers lower Kimmeridgian de pos its
(Wierzbowski et al., 1983). The Niwki for ma tion was sup - posed to be of Oxfordian (Morycowa and Moryc, 1976;
Gliniak et al., 2004; Gutowski et al., 2007) or partly Kimmeridgian age (Golonka, 1978; Olszewska, 2004), but it ranges up into the lower Tithinian or even into the up per Tithonian in some sec tions.
— De vel op ment of the Tithonian shal low wa ter car bon ate plat form. Car bon ate plat form fa cies of the north ern re gion (Swarzów lime stone for ma tion) were so far con sid ered late Oxfordian (Morycowa and Moryc, 1976) or Kimmeridgian in age (Golonka, 1978; Olszewska, 1999, 2001, 2004; Gutowski et al., 2007).
— De vel op ment of reefal de pos its (Pilzno for ma tion) rep - re sent ing the up per most lower Tithonian through up per (but not up per most) up per Tithonian as an equiv a lent of the Štramberk lime stones.
The new biostratigraphic data served both for a mod i fi ca - tion of pre vi ously de vel oped Late Ju ras sic palaeogeographic re con struc tion and for a ver i fi ca tion of the dis tri bu tion and thick ness pat tern in in di vid ual Ju ras sic stages.
Stratigraphically, most of the Up per Ju ras sic se quence in the base ment of the peri-Carpathian Foredeep is com posed of two for ma tions:
1. The £êkawica for ma tion rep re sented by bed ded lime - stones and thick microbialite-sponge bioherms;
2. The Niwki for ma tion rep re sented by marls and marly lime stones, lo cally by micritic lime stones.
The Oxfordian por tion of the se quence is sim i lar to that found in ad ja cent ar eas. Es sen tial changes are ob served at the base of the Kimmeridgian suc ces sion. In the SW mar gin of the Holy Cross Moun tains, a shal low ma rine car bon ate plat form de vel oped in late the Planula Chrone of the late Oxfordian (Matyja et al., 1989), and con tin ued in the early Kimmeridgian (Kutek, 1968, 1969). How ever, it did not reach the foredeep area (Figs. 8 and 9). Only in the north ern most sec tions, the Niwki for ma tion con tains thin interbeds of de tri tal lime stones sup pos edly rep re sent ing a dis tal part of the plat form.
In the Pol ish Jura Chain, ero sional pro cesses re moved al - most all Kimmeridgian de pos its. Lime stones, con tain ing co lo - nial cor als, are pre served in a num ber of sites only in the east - ern most ar eas of the out crops (see Fig. 8). These lime stones cor re spond in age to the up per most Oxfordian or, more likely, to the low er most lower Kimmeridgian (see Matyja and Wierzbowski, 2006a).
In the area lo cated fur ther to the south along the Up per Ju ras - sic out crops there are Pilica for ma tion de pos its at the Oxfordian/Kimmeridgian bound ary, rep re sented by micritic lime stones with sub or di nate marl interbeds (Matyja and Wierzbowski, 2004). In the re con structed Late Ju ras sic palaeogeographic im age (op. cit.) this fa cies change is ob served in an area be tween the Kroczyce biohermal com plex and Pilica interbiohermal ba sin (see Fig. 10). It seems prob a ble that the zone of fa cies changes was as so ci ated with ac tiv ity of the lat i tu - di nally trending Zawiercie Lin ea ment iden ti fied by Kutek (1996, 2001). Kutek (1996, p. 60; 2001, p. 220) re ported a num ber of fea tures dis crim i nat ing the ar eas sit u ated to the north and south of the lin ea ment in both the Silesian–Kraków Monocline and the east ern mar gin of the Mid-Pol ish Anticlinorium. An ad di tional fea ture is that other fa cies changes are ob served also in the Ju ras -
sic suc ces sion of this area. De scrib ing the Mid dle and early Late Ju ras sic fa cies, Ró¿ycki (1953) sit u ated the bound ary be tween the ma jor fa cies units (north ern re gion of Czêsto - chowa–Zawiercie and south ern re gion of Olkusz–Kraków) slightly to the south of Zawiercie. An other change is ob served in the dis tri bu tion trend of Oxfordian biohermal com plexes along a line cross ing Zawiercie. South of Zawiercie, the biohermal com - plexes show a lat i tu di nal ex tent, whereas north of Zawiercie, NE–SW trends are also ob served (see Fig. 10). The ex tents of biohermal com plexes are re lated to the ori en ta tion of sub strate el e va tions de vel oped both prior to and dur ing Oxfordian times (Matyja and Wierzbowski, 2004).
The up per part of the Up per Ju ras sic–Lower Cre ta ceous se - quence also ex hib its lat i tu di nal fa cies vari abil ity. The Tithonian shal low ma rine car bon ate plat form (Swarzów for ma tion) and the over ly ing co quina-marly de pos its (Smêgo rzów for ma tion) are typ i cal of the north ern fa cies re gion in the peri-Carpathian Foredeep. Lat i tu di nally ex tend ing Tithonian coral reefs of huge thick nesses (Pilzno for ma tion) are ob served in the south ern re - gion near the pres ent-day Carpathian thrust front. They are over - lain by cal car e ous peritidal de pos its (lime stone-dolomitic mem - ber of the Ropczyce for ma tion) fol lowed by very shal low ma rine and con ti nen tal marly de pos its (lime stone-marly mem ber of the Ropczyce for ma tion — Zdanowski et al., 2001) rep re sent ing the Berriasian stage (Olszewska, 1998). The pre served part of the suc ces sion is topped by shal low ma rine car bon ate plat form de - pos its (Dêbica for ma tion) as signed to the Valanginian (Bobrek et al., 2002; Dziadzio et al., 2004). The bound ary be tween the north ern and south ern re gions, de lin eated by the south ern ex tent of the for ma tions, runs roughly lat i tu di nally slightly to the south of D¹browa Tarnowska (see Fig. 8).
The Oxfordian- Valanginian suc ces sion, for merly as signed to the Oxfordian and Kimmeridgian (Niemczycka and Broch - wicz- Lewiñski, 1988), is 1247–1373 m thick. The ¯ó³cza 1 bore hole, re ferred to by Po¿aryski (1957b), Grobla 28, Niecza - jna Dolna 3 bore holes (Konarski, 1974) and a num ber of sec - tions de scribed by Morycowa and Moryc (1976) were drilled through the se quence in the Carpathian Foredeep sub strate. All of the sec tions were used by Po¿aryski and Brochwicz-Lewiñski (1978, 1979), Niemczycka and Brochwicz- Lewiñski (1988) and Kutek (1994b, 2001) for re con struc tions of the Mid-Pol ish Trough.
New strati graphic data in di cates that the to tal thick ness of the Oxfordian and Kimmeridgian strata in the Carpathian Foredeep sub strates var ies from 371 up to 799 m (see Fig. 11)2. These fig ures are twice or three times smaller than those which were used for the re con struc tions of the ex tend of the Mid-Pol - ish Trough in the Carpathian Foredeep area.
A RELATION OF THE RECOGNIZED DEPOSITIONAL SUCCESSION TO THE TETHYS OCEAN DOMAIN
The Up per Ju ras sic de pos its of the Carpathian Foredeep sub strate are in cluded into two panregional fa cies pat terns, both re lated to the Tethyan area. The older fa cies pat tern is rep re - sented by the sponge megafacies de fined as bed ded or biohermal car bon ate de pos its (lime stones and marls) con tain - ing Lithistida and Hyalospongea (Hexactinosa and Lychniscosa) si li ceous sponges pre served as cal car e ous “mum - mies” (Matyja and Pisera, 1991). In this sense, the sponge
Fig. 9. Fa cies and bathymetry re la tion ships in the early Kimmeridgian be tween the SW mar gin of the Holy Cross Moun tains and the north ern and cen tral area of the Nida Synclinorium, and the peri-Carpathian Foredeep area
2Figure 11 illustrates the total thicknesses of the £êkawica and Niwki formations as roughly corresponding to the thicknesses of the Oxfordian and Kimmeridgian. The real thickness of the Oxfordian and Kimmeridgian deposits is lower because the upper boundary of the Kimmeridgian succession commonly runs several metres to a few tens of metres below the upper boundary of these formations, as evidenced by data from some borehole sections.
Thickness values are given only for individual sections because drawing isopachs requires obtaining more comprehensive data on structural constraints, which is outside the scope of the present paper.
megafacies was wide spread in the north ern Tethyan shelf and can be traced from Por tu gal through the Spain’s Celtiberic and Praebetic prov inces, Jura Moun tains in France and Swit zer - land, across Swabian Alb, Franconian Alb, Moravia and Po - land to wards Ukraine. The max i mum de vel op ment of the sponge megafacies in Eu rope took place dur ing the Oxfordian (see Matyja and Wierzbowski, 1995, Fig. 1), but lo cal oc cur - rences are ob served in all the Up per Ju ras sic stages (e.g., Ziegler, 1977; Leinfelder, 1993).
The de vel op ment of the sponge megafacies was pre ceded by a con sid er able deep en ing of the ma rine ba sin. In biostratigraphically well-dated Up per Ju ras sic sec tions of the Pol ish Jura Chain, the deep en ing is marked within the mid dle Callovian–low er most Oxfordian in ter val (Gi¿ejewska and Wieczorek, 1977; Dembicz and Praszkier, 2003). The ef fect of the deep en ing is ob served also in North ern and Cen tral Po land.
Among the three ma jor Permo-Me so zoic tec tonic sub si dence events, the mid dle one oc curred in the Late Ju ras sic (Dadlez et al., 1994). Ini tially (Dadlez et al., 1994), no synchroneity was seen be tween event II (extensional event) and geo log i cal pro - cesses in the Carpathian Ba sin, as ev i denced by the re sults of Birkenmajer’s stud ies (1985) who did not con sider the Mid -
dle/Late Ju ras sic tran si tion as the main rift ing phase in the Carpathians. Al though the event oc curred dur ing in ten si fi ca - tion of crustal ex ten sion within the Arc tic-North At lan tic rift sys tem (Ziegler, 1990), the event was also sup posed to have been re lated to the de vel op ment of rift ing pro cesses at the north ern flank of the Tethys (Dadlez et al., 1995). It was no - ticed then (Dadlez et al., 1998, p. 52) that the Late Ju ras sic in - crease in sub si dence rate is very weakly marked in the NW por - tion of the trough, more dis tinct in its cen tral part, and best pro - nounced along the pro file LT-5 sit u ated in the south-east ern - most part of the study area. In its later re con struc tion of the Tethyan Ocean evo lu tion, Birkenmajer (1986) pos tu lated the extensional re gime and the for ma tion of an oce anic crust for the Pieniny Klippen Ba sin and the Magura Ba sin “...dur ing Late Li assic or even Mid-Late Ju ras sic times...” (op. cit., p. 23).
The stage of rapid spread ing of the Tethys Ocean bas ins oc - curred at the Mid dle/Late Ju ras sic tran si tion. The range of the spread ing was de ter mined mainly by palaeomagnetic data from the Pieniny Klippen Belt of south west ern Ukraine (Lewandowski et al., 2005) and Slovakia (Lewandowski et al., 2006). Matyja and Wierzbowski (2006b) re ported the re la tion - ship of these dy namic extensional pro cesses at the turn of Mid -
Fig. 10. Dis tri bu tion of the Oxfordian biohermal com plexes (b.c. — in brown) and interbiohermal bas ins (i.b-b. — in blue) in the Kraków–Czêstochowa Up land (af ter Matyja and Wierzbowski, 2004)
dle/Late Ju ras sic in the outer bas ins of the Tethys Ocean to the pro cesses that oc curred in the ad join ing shelf area, call ing it the Me tis Geotectonic Event.
The youn ger panregional fa cies pat tern is rep re sented by the Štramberk lime stones. This fa cies was better stud ied in the west ern part of its range and treated as a belt fring ing (de lim it - ing) the Tethys shelf area (Mišik, 1974). The iden ti fi ca tion of the east ward con tin u a tion of this belt (Pilzno for ma tion) to the out side of the Bo he mian Mas sif mar gins al lows con sid er ing the Štramberk lime stones as a fa cies that rimmed the shelf. It is worth add ing that the Pilzno for ma tion reefs formed a very prom i nent lat i tu di nally elon gated belt. There was no de pend - ence of the reef lo ca tion on the ear lier basinal dif fer en ti a tion into biohermal and interbiohermal bas ins. The reefs are sit u - ated both in ar eas of de vel op ment of the £êkawica for ma tion basinal fa cies, and upon pre vi ously formed micro bialite- sponge bioherms of con sid er able thick nesses.
CONCLUSIONS
The Up per Ju ras sic and Lower Cre ta ceous de pos its of the Carpathian Foredeep sub strate show a num ber of dis tinc tive palaeogeographic fea tures dis crim i nat ing the area from ar eas lo cated to the north. These are the fol low ing features:
1. Lack of the early Kimmeridgian shal low ma rine car bon - ate plat form iden ti fied in the south west ern mar gin of the Holy Cross Moun tains (Kutek, 1968) and in the cen tral area of the Nida Synclinorium (Jurkiewicz et al., 1969).
2. Much greater strati graphic range of the sponge megafacies (reach ing into the lower Tithonian) than in the re - main ing area of Po land.
3. Lat i tu di nal pat tern of the Tithonian and Early Cre ta ceous fa cies in the Carpathian Foredeep area.
These fea tures, along with data on the to tal thick ness of the Oxfordian and Kimmeridgian suc ces sion (twice to three times smaller than pre vi ously as sumed) and the vari able thick ness dis tri bu tion, con tra dict the pres ence of a NW–SE-trending zone (i.e. in line with the Mid-Pol ish Trough axis) of in creased sub si dence in the Carpathian Foredeep area dur ing Late Ju ras - sic and earliest Cretaceous times.
The same fea tures, sup ported by the pres ence of a lat i tu di nal belt of coral reefs of the Štramberk fa cies (Pilzno for ma tion), sug gest that the study area is re lated to the Tethyan do main.
Ac knowl edge ments. The au thor would like to ex press his grat i tude to Prof. J. Michalik and Dr. M. Krobicki, for valu able re marks. The au thor also wishes to ex press his thanks to the Fac ulty of Ge ol ogy of the Uni ver sity of War saw, the Min is try of the En vi ron ment and the Na tional Fund for En vi ron ment Pro tec tion and Wa ter Man age ment for fi nanc ing the research project.
Strati graphi cal in ves ti ga tions were car ried out as part of a broader pro ject or dered by the Min is try of the En vi ron ment and fi nanced by the Na tional Fund for En vi ron men tal Pro tec tion and Wa ter Man age ment (No 629/2005/Wn-07/FG-bp-tx/D).
The re main ing stud ies, which are the es sence of the pa per, were per formed within the frame work of a pro ject No. BW 17.97.2 sup ported by the Fac ulty of Ge ol ogy, Uni ver sity of War saw.
Fig. 11. To tal thick ness in metres of the £êkawica and Niwki for ma tions in the Carpathian Foredeep area For area lo ca tion see Fig ure 6, ex pla na tions as in Fig ure 8
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