the ti tho nian–ear li est ber ria sian nan no co nus...

S T U D I A G E O L O G I C A P O L O N I C AVol. 132, Kraków 2009, pp. 7–38.

Ge ol ogy of the Pi en iny Klip pen Belt and the Ta tra Mts, CarpathiansEd ited by K. Birk en ma jer

Part XX

Andrzej PSZCZÓ£KOWSKI1

The Ti tho nian–ear li est Ber ria sian Nan no co nus zonesin se lected sec tions of the Pi en iny Klip pen Belt

and the West ern Ta tra Moun tains (south ern Po land)2

(Figs 1–20; Tabs 1, 2)

Ab stract. In com pari son with the Span ish sec tions, first ap pear ance (FAD) of the Ti tho nianNan no co nus spe cies is re corded ear lier in the Pi en iny Klip pen Belt and the West ern Ta tra Moun tains(West ern Car pa thi ans). The Early Ti tho nian Nan no co nus com pres sus Zone cor re lates with theup per most part of the “Pulla- Tithonica” Zone and the lower part of the Mal mica Zone. The N. in fansZone cor re sponds to the up per part of the Mal mica Zone and the lower part of the Chiti noi della Zone(Do beni Sub zone) in clud ing the low er most in ter val of the Boneti Sub zone. The N. win ter eri Zone isequiva lent to the up per most part of the Chiti noi della Zone, en tire Cras si col laria Zone, and the ba salin ter val of the Ber ria sian Alpina Sub zone. In the Kryta Val ley sec tion (Ta tra Mts), the In fans/Win ter eri zo nal bound ary is lo cated within the Boneti Sub zone and is cor re lated with the lower part ofthe CM20n mag ne to zone. Speci mens re ferred to Nan no co nus sp. A oc cur in the stud ied sec tions;these speci mens dif fer from the pub lished de scrip tions of all pre vi ously es tab lished Ti tho nianspe cies. In the Lower Ti tho nian lime stones nan no co nids are scarce be ing more nu mer ous in the lowerin ter val of the N. win ter eri Zone. In crease in abun dance of the ge nus Nan no co nus cor re lates with theMid- to Late Ti tho nian Nan no fos sil Cal ci fi ca tion Event (NCE) re ported from the Cen tral At lan ticOcean.

Key words: Nan no co nus, stra tigra phy, Ti tho nian, Ber ria sian, Pi en iny Klip pen Belt, West ern Ta traMoun tains, Car pa thi ans, Po land.

IN TRO DUC TION

This study of the Ti tho nian Nan no co nus as sem blages was con ducted in thePieniny Klip pen Belt (PKB) and the Ta tra Moun tains, south ern Po land (Fig. 1).These as sem blages have been stud ied in the fol low ing sec tions (Fig. 1C and 1D):

1 In sti tute of Geo logi cal Sci ences, Warsaw Re search Cen tre, Pol ish Acad emy of Sci ences,ul. Twarda 51/55, 00-818 Warszawa, Po land. E- mail: [email protected]

2 Manu script ac cepted for pub li ca tion May 30, 2009.

Stare Bystre, Wapi en nik, Ka puœnica I, Gacówka (PKB, the Brani sko Suc ces sion),Grajcarek (the Ma gura Suc ces sion) and the Kryta Val ley (West ern Ta tra Moun -tains). The nan no co nids have been stud ied un der the JEOL scan ning elec tron mi -cro scope (JSM 840A) in fresh chips taken from the lime stone sam ples. The mi cro -fos sils have been iden ti fied and pho to graphed from thin sec tions un der the OLYM -PUS and NIKON Eclipse LV100 POL light mi cro scopes. In this Nan no co nus-

8 A. PSZCZÓ£KOWSKI

Fig. 1. A – Po si tion of the Pieniny Klippen Belt in the Carpathian Moun tains (af ter Birkenmajer,1977); in set shows the area pre sented in 1B; B – Lo ca tion of the ar eas shown in 1C (Pieniny KlippenBelt) and 1D (Tatra Moun tains); C – Lo ca tion map of the stud ied sec tions in the Pieniny Klippen Belt(af ter Birkenmajer, 1977, gen er al ized): 1 – Pieniny Klippen Belt Suc ces sions and Magura Unit(Ju ras sic and Cre ta ceous strata); 2 – Paleogene of the Magura Unit and of Pieniny Klippen Belt; 3 –Paleogene of the Podhale autochthone; D – Lo ca tion map of the Kryta Val ley sec tion in the WesternTatra Mountains

oriented study only fi nal re sults of the mi cro fos sil analy sis nec es sary for stra -tigraphi cal lo ca tion of the stud ied sam ples are re ported. The main ob jec tive of thispa per was to pres ent all data im por tant for the Nan no co nus zo na tion of the Ti tho -nian strata stud ied in the above- mentioned sec tions. The zo na tion pro posed hereinis also com pared with the pre vi ous pub li ca tions per ti nent to this topic.

PRE VI OUS RE SEARCH

Brön ni mann (1955) has de scribed and il lus trated 10 Nan no co nus spe cies fromthe Lower Cre ta ceous lime stones of north- central Cuba. This author con sid ered N.ste in manni Kampt ner, 1931, to be the old est Nan no co nus spe cies oc cur ring in thelow er most Cre ta ceous lime stones. In Mex ico, Trejo (1960) has es tab lished 6 Nan -no co nus zones (A–F) be tween Up per Ti tho nian and Al bian. His Zone A em braceda part of the Up per Ti tho nian, whereas the Zone B com prised the top most Ti tho nian and Lower Ber ria sian. How ever, the age of the Zone A was un cer tain as no Late Ti -tho nian spe cies of Cras si col laria have been re ported to oc cur to gether with Nan no -co nus bron ni manni3 (Trejo, 1960). Ac cord ing to Báldi- Beke (1964), the old estnan no co nid spe cies are known from the Lower Ti tho nian. How ever, the spe ciesNan no co nus dolo miti cus Cita et Pasquaré, 1959 and N. bro en ni manni Trejo, 1959have not been iden ti fied in the Lower Ti tho nian strata from Hun gary (Báldi- Beke,1964). Deres and Aché ri té guy (1980) cor re lated their Nan no co nus ste in man niiZone with the Up per Ti tho nian–Ber ria sian. Bra lower et al. (1989) have dis tin -guished the Ber ria sian Nan no co nus ste in man nii mi nor Sub zone (=NJK-D Sub -zone) and N. ste in man nii ste in man nii Zone (=NK-1 Zone). Also, these authors cre -ated new spe cies and sub spe cies of the ge nus Nan no co nus Kampt ner, 1931 (N.com pres sus, N. in fans, N. win ter eri, N. kampt neri mi nor and N. globu lus mi nor) oc -cur ring in the stra tigraphic in ter val from the Mid dle and Up per Ti tho nian to Mid dle Ber ria sian. In Spain, Tav era et al. (1994) sub di vided the NJK Zone of Bra lower etal. (1989) on the ba sis of first oc cur rences of Nan no co nus in fans Bra lower, N. win -ter eri Bra lower et Thier stein and N. ste in man nii mi nor Deres et Aché ri té guy (Tab.1). Tav era et al. (1994) placed the first oc cur rence (FO) of N. in fans within thelower part of the cal pi onel lid In ter me dia Sub zone of the Cras si col laria Stan dardZone. The first oc cur rence of N. in fans was con sid ered by these authors to be an ear -lier event as com pared with data pre sented by Bra lower et al. (1989). The FO of N.win ter eri was placed in the up per part of the In ter me dia Sub zone and the FO of N.ste in man nii mi nor was slightly older than the Cras si col laria/Cal pi onella zo nalbound ary (Tav era et al., 1994). Pszczó³kowski et al. (2005) have iden ti fied the N.win ter eri Sub zone in the lat est Ti tho nian and ear li est Ber ria sian of west ern Cuba. Itbe came clear that ex ist ing Ti tho nian zo nal scheme based on Nan no co nus spe ciesneeds some changes. Sub se quently, a new Nan no co nus-based zo nal scheme for theTi tho nian was pro posed (Pszczó³kowski, 2006).

TITHONIAN-EARLIEST BERRIASIAN NANNOCONUS ZONES 9

3 This original name used by Trejo (1960) was later changed for N. broennimanni (Deres &Archéritéguy, 1980).


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STUD IED SEC TIONS: LO CA TION, LITHOSTRATIGRAPHICPO SI TION OF SAM PLED STRATA AND CAL CAR E OUS

NANNOFOSSILS

Stare Bystre sec tion (B in Fig. 1C)

This sec tion was named (“Stare Bystre - school”), de scribed and as signed to theBranisko Suc ces sion by Birkenmajer (1958, 1979). The whole sec tion is over -turned, so the rock units ap pear in re versed po si tion (Birkenmajer, 1958, 1979).The red radiolarite of the Buwa³d Radiolarite Mem ber (Czajakowa Radiolarite Fm.– Birkenmajer, 1977) is Late Oxfordian in age (Fig. 2) as in di cated by pres ence of“Colomisphaera” fibrata (Nagy, 1966). Up-sec tion, thin red radiolarite is tec toni -cally wedged be tween the lime stones of the Czorsztyn Lime stone For ma tion. Inthis sec tion, the Early Tithonian age of the red radiolarite re ported by Golonka andSikora (1981) is not con firmed by the pres ent study. The Czorsztyn Lime stone For -ma tion is rep re sented mainly by red nod u lar lime stones about 8 m thick (Figs 3 and4: 1). These lime stones are mas sive in the lower part (Fig. 4: 1-a) and slightly marlyin the up per one (Fig. 4: 1-b); their age is Kimmeridgian (Late Kimmeridgian,mainly)–Early Tithonian (Fig. 5).

The Early Tithonian ammonites have been col lected from the up per part of theCzorsztyn Lime stone For ma tion (Myczyñski, in Pszczó³kowski & Myczyñski,2008), be tween sam ples By-9 and By-10 (Figs 2 and 3). These ammonites in di catethat the Kimmeridgian/Tithonian bound ary is lo cated be low the sam ple By-9(Fig. 2). Chitinoidellids and/or calpionellids have not been found in the CzorsztynLime stone Fm. in the Stare Bystre sec tion. There fore, it seems that the up perbound ary of this for ma tion does not cor re spond to the up per bound ary of the “rednod u lar lime stones” de scribed by Golonka and Sikora (1981, p. 9 and fig. 3). Thebound ary be tween the Czorsztyn Lime stone For ma tion and the Dursztyn Lime -stone For ma tion (Birkenmajer & Myczyñski, 2000) is lo cated at the base of theEarly Tithonian Malmica Zone (Fig. 2). The Dursztyn Lime stone For ma tion iscom posed of (1) cream to white platy lime stone 1.5 to 2 m thick (Fig. 4: 2), some -times bioturbated (Fig. 4: 3) and (2) red dish nod u lar lime stone, yel low on weath -ered sur faces, about 5 m thick (Fig. 5). The lat ter lith o logic ho ri zon was named thecalpionellid lime stone, tran si tional be tween the Dursztyn Lime stone For ma tionand the Pieniny Lime stone For ma tion (Birkenmajer, 1979). The Dursztyn Lime -stone For ma tion ex posed in the Stare Bystre sec tion is Early Tithonian–EarlyBerriasian in age (Fig. 2). The basal part of the for ma tion has been as signed to theMalmica Zone (sensu Reháková, 2000b), whereas the youn gest lime stone beds rep -re sent the Alpina Subzone (Fig. 2). A strati graphi cal con den sa tion (or hi a tus?) isprob a ble at the bound ary of the Chitinoidella and Crassicollaria Zones. The J/Kbound ary is in di cated at the base of the Alpina Subzone, 5.6 m above the contact ofthe Czorsztyn Limestone Formation with the Dursztyn Limestone Formation.

The Up per Kimmeridgian–Lower Tithonian nod u lar lime stones of the Czorsz-tyn Lime stone For ma tion con tain few nannofossil taxa only (Fig. 6). The spec i -mens ob served and doc u mented in SEM be long mainly to gen era Watznaueria



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Reinhardt, 1964 (Fig. 7: 7, 8) and Cyclagelosphaera Noël, 1965. First oc cur renceof Nannoconus was re corded from the Lower Tithonian lime stone, slightly be lowthe base of the Malmica Zone, close to the base of the Dursztyn Lime stone For ma -tion. The po si tion of the base of Malmica Zone may be de fined in di rectly, as theTithonica/Malmica bound ary was cor re lated with the Darwini/Semiforme bound -


Fig. 3. Up per part of the Czorsztyn Lime stone For ma tion ex posed in the Stare Bystre sec tion.Lo ca tion of sam ples By-9 and By-10 is in di cated (see also Fig. 2). The nod u lar lime stone oc curs in are versed po si tion and the strata are dip ping to the left

ary in ter val (Reháková, 2000a). The Early Tithonian Darwini/Semiforme bound -ary was cor re lated with the up per part of the M22n magnetozone (Gradstein et al.,2004). There fore, the Malmica Zone sensu Reháková (2000a, b) is sig nif i cantlynar rower than the zone used by Nowak (1976).


Fig. 4. 1 – Late Kimmeridgian strata of the Czorsztyn Lime stone For ma tion at Stare Bystre:con tact be tween red (thick-bed ded) nod u lar lime stone (a) and marly nod u lar lime stone (b); theex posed lime stones are over turned, with older beds at left; 2 – White-yel low ish platy lime stone of thebasal Dursztyn Lime stone For ma tion at Stare Bystre: CL – Czorsztyn Lime stone For ma tion, DN –Dursztyn Lime stone For ma tion; 3 – Lo cally bioturbated platy lime stone of Dursztyn Lime stoneFor ma tion at Stare Bystre (top at the bot tom of the pho to graph, the marker is 12 cm long)

Five Nannoconus biozones have been iden ti fied in the Stare Bystre sec tion (Fig. 6). The low er most N. compressus Zone is thin and poorly doc u mented, with N. cf.compressus Bralower et Thierstein 1989, only. The youn ger N. infans Zonel is ten -ta tively rec og nized on the ba sis of N. cf. infans Bralower, 1989 (Fig. 7: 4) pres ence.Spec i mens as signed to Conusphaera mexicana Trejo subsp. mexicana Bralower,Monechi et Thierstein 1989 (Fig. 7: 1), Nannoconus sp. A (Fig. 7: 2) and N. cf.compressus Bralower et Thierstein 1989 (Fig. 7: 3) also oc cur in this NannoconusZone. The next N. wintereri Zone, based on the in dex taxon oc cur rence (Fig. 7: 6),em braces the Up per Tithonian–basal Berriasian lime stones. The taxa N. compre-ssus (Fig. 7: 5) and N. sp. A, are also pres ent. The Lower Berriasian lime stone (sam -


Fig. 5. Thick-bed ded nod u lar lime stones, lat est Tithonian–ear li est Berriasian in age, ex posed atthe road in Stare Bystre (Dursztyn Lime stone For ma tion ac cord ing to Birkenmajer & Myczyñski,2000). The strata oc cur in tec toni cally re versed po si tion with youn ger beds sit u ated in the lower partof the out crop (see Fig. 2, in ter val be tween samples By-18 and By-20)


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Fig. 7. Cal car e ous nannofossils from the Czorsztyn Lime stone For ma tion (7, 8) and the DursztynLime stone For ma tion (1–6) at Stare Bystre (Pieniny Klippen Belt): 1 – Conusphaera mexicana Trejomexicana Bralower, Monechi et Thierstein, 1989, sam ple By-13A (Chitinoidella Zone, Early Titho-nian); 2 – Nannoconus sp. A (slightly oblique lon gi tu di nal sec tion), sam ple By-10B (Malmica Zone,Early Tithonian); 3 – Nannoconus sp. cf. N. compressus Bralower et Thierstein, 1989 (lon gi tu di nalsec tion), sam ple By-13A (Chitinoidella Zone); 4 – N. cf. infans Bralower, 1989 (slightly obliquelon gi tu di nal sec tion), sam ple By-13 (Chitinoidella Zone, Early Tithonian); 5 – N. compressusBralower et Thierstein, 1989 (slightly oblique lon gi tu di nal sec tion), sam ple By-14 (Boneti Subzone,Late Tithonian); 6 – N. wintereri Bralower et Thierstein, 1989 (trans verse sec tion), sam ple By-16(Intermedia Subzone, Late Tithonian); 7 – Watznaueria barnesae (Black 1959) Perch-Niel sen, 1968(dis tal view), sam ple By-8C (Late Kimmeridgian); 8 – W. ovata Bukry, 1969 (dis tal view), sam pleBy-8-A1 (Borzai Zone, Late Kimmeridgian)

ple By-19) con tains Nannoconus kamptneri Brönnimann subsp.mi nor Bralower, 1989. This taxon was re ported to co-oc cur withN. steinmannii mi nor (FAD – Bralower et al., 1989; see also Tab. 1). There fore, pres ence of N. kamptneri mi nor in the Stare Bystre sec tion (Fig. 6) doc u ments the N. steinmannii mi nor (Sub)Zone.The top most lime stone bed (By-20) yielded taxa N. steinmanniimi nor and N. steinmannii steinmannii and N. wintereri; there -fore, it be longs to the lower in ter val of the N. steinmanniisteinmannii Zone (NK-1) of Bralower et al. (1989).

Wapiennik klippe sec tion (W in Fig. 1C)

The Wapiennik klippe is lo cated at the out let of the Harcy-grund Val ley (Birkenmajer, 1977, fig. 7), but now is no lon gerex posed ex cept its up per most part com posed of the Valanginianlime stones about 1 m thick. The klippe was blown up and sub se -quently sub merged when the dam was con structed and theCzorsztyn ar ti fi cial lake has formed. The orig i nal cross-sec tionof the klippe was shown by Birkenmajer (1958, 1979). Wiêtczak (1999) stud ied stra tig ra phy and microfacies of the ex posedCzorsztyn and Pieniny Lime stone for ma tions there. The mainre sults of the Wiêtczak’s (1999) un pub lished study of the Wa-piennik klippe are shown in the left col umn in Fig. 8. Prof.Andrzej Wierzbowski (Ge ol ogy Fac ulty of the War saw Uni ver -sity) kindly made ac ces si ble for this study the rock sam plestaken by R. Wiêtczak (right col umn in Fig. 8). These sam ples, la -belled HR, cor re spond to the orig i nal ones used by Wiêtczak(1999), al though a part of them have been re-named (as RW/1/1to 11). Dur ing the pres ent study, ad di tional sam ples have beencol lected (MRW, PM) from the rub ble of the de stroyed klippeused for the dam con struc tion. The strati graphic po si tion ofthese sam ples is based on the re sults of microfossil anal y sis (Fig. 8), al though their pre cise lo ca tion in the orig i nal sec tion couldnot be re stored.

The pres ent study has shown that the Czorsztyn Lime stoneFor ma tion ex posed in the Wapiennik klippe com prises also theLower Tithonian lime stones in the basal part of the sec tion (Fig.8). Some of the stud ied sam ples from the rub ble are rich in smallammonite shells and Saccocoma os si cles, but do not con tain anyin dex Tithonian microfossils. These sam ples are not in cluded inthe set of data pre sented in Fig. 8; their age is an open ques tionand may be Early Tithonian or even Kimmeridgian (?). The sam -ples PM-4a and MRW-1 (from the rub ble) con tain chitinoi-dellids of the Dobeni Subzone (Chitinoidella Zone). The for mer


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Fig. 9. Nannoconus spp. from the Czorsztyn Lime stone For ma tion (Upszar Lime stone Mbr) in theWapiennik klippe near Harcygrund Val ley (1–7) and the Kapuœnica I sec tion (8, 9); for lo ca tion seeFig. 1C and Birkenmajer (1977, fig. 7H): 1, 2 – Nannoconus sp. A (lon gi tu di nal sec tions), sam plePM-4a, Dobeni Subzone, Early Tithonian; 3 – N. wintereri Bralower et Thierstein, 1989 (obliquesec tion), sam ple HR-6, Intermedia Subzone, Late Tithonian; 4 – N. infans Bralower, 1989 (obliquesec tion), sam ple MRW-5, Praetintinnopsella Zone, Late Tithonian; 5,6 – N. wintereri Bralower etThierstein, 1989 (oblique sec tions), sam ple MRW-5 (5) and HR-6 (6); 7 – N. cf. compressus Braloweret Thierstein, 1989 (slightly oblique lon gi tu di nal sec tion), sam ple MRW-5; 8, 9 – N. compressusBralower et Thierstein, 1989 (oblique sec tions), sam ples K-03 (8) and K-04 (9), Early Tithonian

sam ple (PM-4a in Fig. 8) con tains also cal car e ous nannoplankton with Watzna-ueria ovata Bukry, 1969, Conusphaera mexicana Trejo, 1960 and Nannoconus sp.A (Fig. 9: 1, 2). The sam ple PM-4a prob a bly be longs to the older Nannoconus as -sem blage, but its zonal as sign ment is un clear. The sam ples col lected from the youn -ger strata (PM-1, MRW-5, HR-4, HR-5 and HR-6) yielded Nannoconus spec i mensbe long ing to N. wintereri (Fig. 9: 3, 5, 6), N. infans (Fig. 9: 4), N. cf. compressus(Fig. 9: 7) and N. sp. A. These sam ples can be as signed to the lower part of N.wintereri Zone. The up per part of this Zone is not doc u mented in the Wapiennikklippe sec tion. Also, the basal in ter val of the N. wintereri Zone is not de tected as the sam ples be long ing to the Boneti Subzone of the Chitinoidella Zone have not beenfound in the stud ied rock ma te rial. Ac cord ing to Wiêtczak (1999), the Tithonian/Berriasian bound ary is sit u ated be tween sam ples HR-5 and HR-6, that is, at the con -tact of the Czorsztyn Lime stone For ma tion with the Pieniny Lime stone For ma tion(Fig. 8). The pres ent study re vealed that the Tithonian/Berriasian bound ary (=J/Kbound ary) is lo cated higher up in the sec tion above the sam ple HR-9, which be -longs to the up per most Tithonian. There fore, the lower part of the Pieniny Lime -stone For ma tion 3.5 do 4 m thick was de pos ited dur ing Late Tithonian time. Thebase of this for ma tion is cor re lated with the mid dle part of Late TithonianCrassicollaria Standard Zone (A2 Subzone in the calpionellid subdivision ofRemane, 1964, 1985).

Kapuœnica I sec tion (K in Fig. 1C)

This sec tion is lo cated in the Kapuœnica klippe at the dam’s level (Pszczó³-kowski & Myczyñski, 2004). The bound ary be tween the Buwa³d Radiolarite Mem -ber of the Czajakowa Lime stone For ma tion and the Upszar Lime stone Mem ber ofthe Czorsztyn Lime stone For ma tion is in di cated (Fig. 10) 60 cm be low the pre vi -ously as sumed lo ca tion (see Pszczó³kowski & Myczyñski, 2004, fig. 3). Thischange is sup ported by thin sec tions study of the beds as signed here to the basal in -ter val of the Upszar Lime stone Mem ber. Rare spec i mens as signed to N. compre-ssus Bralower et Thierstein, 1989 (Fig. 9: 8, 9) oc cur in the basal beds of the UpszarMem ber (Fig. 11).. Be low the Nannoconus compressus Zone, the low er mostTithonian strata may oc cur in the top most part of the Buwa³d Radiolarite Mem berabove the bed K-01 (Fig. 11) or, al ter na tively, there is a hi a tus at the bound ary of the Czajakowa Radiolarite Fm. and Czorsztyn Lime stone For ma tion in the Kapuœnica I sec tion.

Gacówka sec tion (G in Fig. 1C)

In the Gacówka sec tion (Branisko Suc ces sion ac cord ing to Birkenmajer, 1979),the Upszar Lime stone Mem ber of the Czorsztyn Lime stone For ma tion is com posed of two in for mal units: (1) lay ered lime stone (up per most Kimmeridgian–LowerTithonian) and (2) mas sive pseudonodular lime stone of Late Tithonian age(Fig.12). In this sec tion, the first nannoconids oc cur in the Early Tithonian lime -stones of the Dobeni Subzone (Chitinoidella Zone) – Fig. 12 and Fig. 13: 3. The


spe cies Nannoconus infans Bralower (Fig. 13: 1, 2) and N. wintereri Bralower etThierstein 1989 ap pear in the basal in ter val of the Boneti Subzone. The taxon N. cf.compressus (Fig. 13: 4) has been ob served in the lower part of the Boneti Subzone.The spe cies N. wintereri (Fig. 13: 5) and N. steinmannii mi nor (Fig. 13: 6) oc cur inthe Lower Berriasian lime stone of the Pieniny Lime stone For ma tion (Fig. 12).Thus, in the Gacówka sec tion, the Late Tithonian oc cur rences of Nannoconus be -long to N. wintereri Zone, al though strong in flu ence of tec tonic de for ma tion doesnot per mit to ap ply more de tailed zonal (Nannoconus-based) sub di vi sion of the ex -posed strata.


Fig. 10. Bound ary be tween the Buwa³d Radiolarite Mem ber (Czajakowa Radiolarite For ma tion –CZ) and the Upszar Lime stone Mem ber (Czorsztyn Lime stone For ma tion – CL), ex posed in thenorth ern klippe at Kapuœnica (Kapuœnica I sec tion in Pszczó³kowski & Myczyñski, 2004); K-01 toK-3: sam ples taken from the beds ex posed in the outcrop


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Fig. 12. Nannoconus oc cur rence in the Tithonian–ear li est Berriasian strata, Gacówka sec tion(Branisko Suc ces sion, Pieniny Klippen Belt). 1 – radiolarite; 2 – thin-bed ded green and redbiomicrites; 3 – thick-bed ded to mas sive light grey pseudonodular lime stone; 4 – grey micriticlime stone; 5 – cal cite veins and strongly tectonized strata; 6 – tec tonic con tact; 7 – taxon oc cur rence(con firmed); 8 – prob a ble oc cur rence of a taxon (cf.)

Grajcarek sec tion (Gr in Fig. 1C)

Birkenmajer (1979) pre sented an out line of lithostratigraphy and a de scrip tionof this sec tion (= slaugh ter house at Szczawnica Wy¿na). The Palenica Marl Mem -ber of the Czorsztyn Lime stone For ma tion (Birkenmajer, 1977) is up to 1.2 m thick(Fig. 14). Nowak (1971, 1976) has as signed this unit to the Early TithonianMalmica Zone.

In the stud ied sec tion, the lower bound ary of the Palenica Marl Mem ber is tec -toni cally dis turbed against the Czajakowa Radiolarite For ma tion. This Mem ber issub di vided into three in for mal lith o logic units: (1) green shaly marl in the lowerpart (mz in Fig. 14), (2) red marl in the up per part (mc in Fig. 14), and (3) red nod u -lar marly lime stone (Fig. 15). The green marl and a large part of the red marl be longto the Early Tithonian “Pulla-Tithonica” Zone sensu Borza (1984), al though spec i -


Fig. 13. Se lected spec i mens of nannoconids found in the Czorsztyn Lime stone For ma tion (1–4) and in the basal part of the Pieniny Lime stone For ma tion (5, 6) in the Gacówka sec tion (BraniskoSuc ces sion): 1, 2 – N. infans Bralower, 1989 (tan gen tial and oblique sec tions), sam ples G-12 (1) andG-12A (2), Boneti Subzone, Late Tithonian; 3 – N. sp. ex gr. N. infans-wintereri (oblique transversalsec tion), sam ple G-10, Dobeni Subzone, Early Tithonian; 4 – N. cf. compressus Bralower etThierstein, 1989 (oblique lon gi tu di nal sec tion), sam ple G-15, Boneti Subzone, Late Tithonian; 5 – N.wintereri Bralower et Thierstein, 1989 (oblique sec tion), sam ple G-21, Alpina Subzone, EarlyBerriasian; 6 – N. steinmannii Kamptner mi nor Deres et Achéritéguy, 1980 (oblique lon gi tu di nalsec tion), sample G-21, Alpina Subzone

mens of Carpistomiosphaera borzai (Nagy, 1966) are also pres ent. Only the up per -most part of the red marl and the marly lime stone do con tain spec i mens ofParastomiosphaera malmica, so it is as signed here to the Malmica Zone (Fig. 15).This strati graphi cal scheme is not ex actly the same as the for mer one (Nowak,1976, fig. 7), al though con firms the (mainly) Early Tithonian age of the PalenicaMarl Mem ber (="Aptychi Shales") reported by the cited author.

The spec i mens of Nannoconus have not been found in the lower and mid dleparts of the Palenica Marl Mem ber. Rare Watznaueria bri tan nica (Stradner 1963)Reinhardt 1964 (Fig. 17: 1) and Watznaueria sp. oc cur in the green and red marls(Fig. 16). The Nannoconus infans Zone com prises the up per most part of thePalenica Marl Mem ber and the low er most in ter val of the Pieniny Lime stone For -ma tion. Aside of the in dex taxon (Fig. 17: 5, 8-a), the nannofossil as sem blage char -ac ter is tic for this zone con tains Nannoconus sp. A (Fig. 17: 6, 7), N. compressusBralower et Thierstein, 1989 (Fig. 17: 3), N. cf. compressus (Fig. 17: 4) andPolycostella(?) sp. (Fig. 17: 8-b). Also, Conusphaera mexicana Trejo subsp.mexicana Bralower, Monechi et Thierstein, 1989 (Fig. 17: 2) ap pears in the top -most sam ple (Gr-4a) col lected from the red marl. The first ap pear ance (FAD) of C.mexicana mexicana in the Grajcarek sec tion seems to be roughly co eval with the


Fig. 14. The Czajakowa Radiolarite For ma tion (CZ), the Palenica Marl Mem ber (PM) of theCzorsztyn Lime stone For ma tion, and the Pieniny Lime stone For ma tion (PL) ex posed in the Graj-carek sec tion (Magura Suc ces sion). Green radiolarite (CZ) un der lies the Aptychus-bear ing green(mz) and red (mc) marls of the Palenica Member


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Fig. 17. Cal car e ous nannofossils from the Palenica Marl Mem ber (Czorsztyn Lime stone Fm.) andthe lower part of the Pieniny Lime stone For ma tion in the Grajcarek sec tion: 1 – Watznaueriabri tan nica (Stradner, 1963) Reinhardt, 1964 (dis tal view), sam ple Gr-3-1 (“Pulla-Tithonica” Zone,Early Tithonian); 2 – Conusphaera mexicana Trejo mexicana Bralower, Monechi et Thierstein, 1989, sam ple Gr-4a (Malmica Zone, Early Tithonian); 3 – Nannoconus compressus Bralower et Thierstein,1989 (lon gi tu di nal sec tion), sam ple Gr-7 (Chitinoidella Zone, ?Early Tithonian); 4 – N. cf. compre-ssus Bralower et Thierstein, 1989 (ax ial sec tion), sam ple Gr-6 (Malmica Zone, Early Tithonian); 5 –N. infans Bralower, 1989 (lon gi tu di nal sec tion), sam ple Gr-4 (Malmica Zone, Early Tithonian); 6, 7 –Nannoconus sp. A (lon gi tu di nal sec tions), sam ples Gr-4 and Gr-6 (Malmica Zone, Early Tithonian); 8– (a) N. infans Bralower, 1989, Chitinoidella Zone, (b) Polycostella(?) sp. (sample Gr-7)

event named “base of (this) taxon” in the basal in ter val of the C. mexicana Zone(NJ-20) and at the top of the CM22n magnetozone (Bralower et al., 1989, fig. 14).The N. wintereri Zone is in com plete as its up per part is miss ing (Fig. 16). Un for tu -nately, sub di vi sion of the Chitinoidella Zone was not achieved in this sec tion (seealso Obermajer, 1986), thus the lower bound ary of the N. wintereri Zone could notbe cor re lated with the cor re spond ing subzone of the Chitinoidella Zone. Nev er the -less, a change to wards an as sem blage char ac ter ized by more fre quent Nannoconusspec i mens is con spic u ous. The N. compressus Zone was not found in the Grajcareksec tion. As the lower bound ary of the N. infans Zone is close (al though be low) tothe top of the red marl, this sug gests that the late ap pear ance of Nannoconus in thissection could be influenced by local paleoceanographic factors.

Kryta Val ley sec tion, West ern Tatra Mts (KV in Fig. 1D)

Stra tig ra phy of the de pos its ex posed in this sec tion lo cated in the Kryta Val ley,West ern Tatra Moun tains, was stud ied by Grabowski & Pszczó³kowski (2004,2006a, b). These Tithonian de pos its be long to the Jasenina For ma tion and con sistof lime stone with marl interbeds (Fig. 18); their up per part is as signed to thePoœrednie Mem ber of this for ma tion (Pszczó³kowski, 2003).

In the Kryta Val ley sec tion, the Nannoconus infans and N. wintereri Zones arecor re lated with the ear li est Late Tithonian Boneti Subzone of the ChitinoidellaZone. The spe cies N. infans Bralower (Fig. 20: 5, 6) oc curs in the lower part of theBoneti Subzone (Fig. 19), whereas N. wintereri Bralower et Thierstein (Fig. 20:


Fig. 18. Interbedded platy lime stones and marls of the Jasenina For ma tion (Chitinoidella andPraetintinnopsella Zones, Up per Tithonian, pro parte) ex posed in the Kryta Val ley, West ern TatraMoun tains

2–4) ap pears in the up per part of the stud ied sec tion, that is, within the BonetiSubzone and con tin ues in the Praetintinnopsella Zone. Spec i mens of N. compre-ssus Bralower et Thierstein 1989 (Fig. 20: 1) and N. cf. compressus are pres ent inboth above-men tioned Nannoconus Zones. How ever, the up per bound ary of the N.wintereri Zone is lo cated in the youn ger lime stones not ex posed in this sec tion. Incon trast with the N. infans Zone, nannoconids are more nu mer ous in the lower in -ter val of the N. wintereri Zone, equiv a lent to the up per part of the Late TithonianBoneti Subzone (Tab. 1). Michalík et al. (2008, 2009) re ported that in the Brodno


Fig. 19. Nannoconus spp. dis tri bu tion in the Kryta Val ley sec tion (West ern Tatra Moun tains)

sec tion (Kýsuca Suc ces sion, Pieniny Klippen belt, Slovakia) Polycostella Thier-stein, 1971, in creased in abun dance dur ing the Boneti Subzone. The in crease inabun dance of Nannoconus spec i mens cor re lates very well with the Mid- to LateTithonian Nannofossil Cal ci fi ca tion Event (NCE) of Bornemann et al. (2003), butap par ently pre ceded a change from microgranular chitinoidellid loricas to calcitic(hyaline) calpionellids (Reháková & Michalík, 1993).

TITHONIAN NANNOCONUS ZONES: THEIR DEF I NI TION,STRATI GRAPHIC PO SI TION AND COR RE LA TION WITH

STAN DARD NANNOFOSSIL ZONATION

The Nannoconus-based zonation pro posed ear lier (Pszczó³kowski, 2006, 2008) and con firmed in this pa per (Tab. 1) fol lows the def i ni tion of the Subzones NJK-band NJK-c of Tavera et al. (1994), re lated to the first ap pear ances of N. infansBralower and N. wintereri Bralower et Thierstein, re spec tively. How ever, it ap -pears from the data pre sented herein that the Tithonian biostratigraphic scheme


Fig. 20. Nannoconus spp. from the Up per Tithonian lime stones of the Jasenina For ma tion (BonetiSubzone of the Chitinoidella Zone); Kryta Val ley, West ern Tatra Moun tains: 1 – Nannoconuscompressus Bralower et Thierstein, 1989 (oblique sec tion), sam ple K-D; 2–4 – Nannoconus wintereriBralower et Thierstein, 1989 (lon gi tu di nal sec tions), sam ple K-E; 5, 6 – N. infans Bralower, 1989(oblique sec tions), sam ples K-B and K-C

based on nannoconids needs changes in re spect to NJK-a, NJK-b and NJK-c(Tavera et al., 1994). The Subzone NJK-a was based on a pres ence of N. compre-ssus Bralower et Thierstein (Tavera et al., 1994), but the lower bound ary of thisSubzone was not de ter mined by these au thors. Ac cord ing to Bralower et al. (1989),at site 534A the FAD of N. compressus oc curs within the CM21 mag netozone and(prob a bly) be low the Chitinoidella Zone (Tab. 1). How ever, also in the Cen tralAtlantic, Bornemann et al. (2003) have placed this event at the base of the NJ-20BZone (across the M21/M20 magnetozonal bound ary). Also Tremolada et al. (2006)have marked first oc cur rence (FO) of Nannoconus spp. at the CM21–CM20 bound -ary. In Spain, all the above-men tioned subzones of the NJK Zone (a–c) have beencor re lated with the Late Tithonian Durangites (ammonite) Zone and the lower partof the Jacobi Zone (Tavera et al., 1994). In terms of the calpionellid stra tig ra phy,these Nannoconus subzones cor re sponded to the calpionellid Intermedia Subzone(Tavera et al., 1994; see also Tab. 1). The NJK-c Subzone of Tavera et al. (1994)ter mi nated be low the Crassicollaria/Calpionella zonal bound ary. There fore, infact the NJK-d Subzone of Tavera et al. (1994) was not an ex act equiv a lent ofNJK-D (=N. steinmannii mi nor) Subzone of Bralower et al. (1989).

In the stud ied sec tions from the Pieniny Klippen Belt and the West ern TatraMts., the Nannoconus compressus Zone was iden ti fied in the Stare Bystre (Fig. 6)and Kapuœnica I (Fig. 11) sec tions, only. The strati graphic po si tion of its lowerbound ary is prob a bly be low the Malmica Zone, whereas the up per bound ary isplaced within the Malmica Zone (Tab. 1). This first Nannoconus as sem blage isvery poor in taxa and spec i mens, as well. The N. infans Zone oc curs in the fol low -ing sec tions: Stare Bystre (Fig. 6), Grajcarek (Fig. 16) and Kryta Val ley (Fig. 19).Its lower bound ary co in cides with the up per one of the N. compressus Zone and thetop of this zone oc curs within the Chitinoidella Zone (Tab. 1). The nannoconid as -sem blage of the N. infans Zone con sists of the fol low ing taxa: N. infans, N.compressus and N. sp. A. In the Grajcarek sec tion, Conusphaera mexicanamexicana ap pears (FAD?) within the basal in ter val of the N. infans Zone; as shownin Tab. 1, this po si tion seems to be slightly above the FAD of the taxon as in di catedfor the Cen tral At lan tic Ocean (Bralower et al., 1989). There fore, N. infans Zoneprob a bly cor re lates with a part of the NJ-20 Zone (C. mexicana) and the basal in ter -val of the NJK-A (=H. noelae) Subzone of Bralower et al. (1989), al thoughNannoconus spe cies have not been men tioned from the nannofossil as sem blage oc -cur ring in their C. mexicana Zone. Also, this zone may cor re spond to a lower part of the Polycostella beckmannii Subzone (NJ-20B) in the Brodno sec tion (Michalík etal., 2009). In the Kryta Val ley sec tion, the Infans/Wintereri zonal bound ary is lo -cated within the Boneti Subzone (Fig. 19). This lo ca tion may be cor re lated with thelower part of the CM20n magnetozone (Grabowski & Pszczó³kowski, 2004).

The N. wintereri Zone is re ported from all the stud ied sec tions, ex cept theKapuœnica I one (Fig. 11). Be sides the Kryta Val ley sec tion (Fig. 19), its lowerbound ary is ten ta tively des ig nated at Stare Bystre (Fig. 6), di rectly above the baseof the Boneti Subzone. How ever, the Dobeni/Boneti subzonal bound ary could notbe pre cisely de ter mined in the Stare Bystre sec tion. The up per bound ary of the N.


wintereri Zone is lo cated in the up per most part of the Dursztyn Lime stone For ma -tion di rectly be low the sam ple By-19 (Fig. 6). The nannoconid as sem blage con sistsof N. wintereri, N. infans, N. compressus, N. sp. A, and rare N. globulus mi nor. TheN. wintereri Zone should cor re spond to the NJK Zone (Bralower et al., 1989) orNJ-20B and NJK-A-C (Bornemann et al., 2003). How ever, the FAD of N. wintereriwas placed within the NJK-C Subzone (Bralower et al., 1989) or at the base ofNJK-c Subzone (Tavera et al., 1994). Such a high strati graphic po si tion of thisevent, cor re spond ing to the up per most in ter val of the Late Tithonian CrassicollariaZone (Tab. 1), is not con firmed by the data re ported in this study. Ac cord ing toMichalík et al. (2006), N. wintereri ap pears di rectly above the base of theCrassicollaria Zone in the Brodno sec tion (Kýsuca Suc ces sion, Pieniny KlippenBelt, Slovakia). In the re cent pa per on the Brodno sec tion stra tig ra phy (Michalík etal., 2009, fig. 9), the first oc cur rence of this taxon is shown within the Up perTithonian (Crassicollaria colomi Subzone), about 0.5 m above the J/K bound arypre vi ously des ig nated by Houša et al. (1999).

The Nannoconus steinmannii mi nor Zone was iden ti fied in the Stare Bystre(Fig. 6) and Gacówka sec tions (Fig. 12), whereas the N. steinmannii steinmanniiZone oc curs in the mid dle and up per in ter vals of the Early Berriasian AlpinaSubzone (Tab. 1) and con tin ues into the Mid dle Berriasian C. elliptica Subzone(Bralower et al., 1989, 1995; Pszczó³kowski & Myczyñski, 2004).

TAX O NOMIC RE MARKS

In the stud ied sec tions, spec i mens re ferred here to Nannoconus sp. A oc cur inthe Tithonian strata, which be long to the N. infans and N. wintereri Zones, mainly.These spec i mens dif fer from pub lished de scrip tions of other spe cies (N. compre-ssus, N. infans and N. wintereri – Bralower et al., 1989). The spec i mens as signed toNannoconus sp. A are larger than N. infans and do not pos sess a wide ax ial ca nal asis char ac ter is tic for N. wintereri (Ta ble 2). The cone-shaped Nannoconus spec i -mens dif fer also from rect an gu lar to elon gate oval rep re sen ta tives of N. compressus(Tab. 2). Spec i mens shown in Figs 7: 2, 9: 1 and 17: 7 are typ i cal rep re sen ta tives ofthe taxon Nannoconus sp. A. The larg est spec i mens at tain di men sions 7 × 7 µm.The re la tion of the de scribed ear li est cone shaped forms to the Early Berriasian N.steinmannii Kamptner subsp. mi nor Deres et Achéritéguy, 1980 is not clear. Ac -cord ing to Bralower et al. (1989, fig. 2), the evo lu tion ary lin eage con sisted of taxaN. compressus-N. infans-N. wintereri-N. steinmannii mi nor-N. kamptneri mi -nor-N. steinmannii steinmannii. How ever, Tithonian forms sim i lar to Nannoconussp. A have not been in cluded in this lin eage.

CON CLU SIONS

In the in ves ti gated sec tions of the Pieniny Klippen Belt (south ern Po land) theEarly Tithonian Nannoconus compressus Zone cor re lates with the up per most partof the “Pulla-Tithonica” Zone (Borza, 1984) and lower part of the Malmica Zone.The N. infans Zone is equiv a lent to the up per part of the Malmica Zone and the


lower part of the Chitinoidella Zone (Dobeni Subzone and the low er most in ter valof the Boneti Subzone). The N. wintereri Zone cor re sponds to the up per most part of the Chitinoidella Zone, the en tire Crassicollaria Zone and the basal in ter val of theBerriasian Alpina Subzone. In the Kryta Val ley sec tion (West ern Tatra Mts), theInfans/Wintereri zonal bound ary is lo cated within the Boneti Subzone and is cor re -lated with the lower part of the CM20n magnetozone (Grabowski & Pszczó³-kowski, 2004). Spec i mens re ferred to Nannoconus sp. A oc cur in the stud iedTithonian Nannoconus Zones; these spec i mens dif fer from the pub lished de scrip -tions of all pre vi ously es tab lished Tithonian spe cies. In the Lower Tithonian lime -stones Nannoconus spec i mens are scarce, be ing more nu mer ous in the lower in ter -val of the N. wintereri Zone. This in crease in abun dance of Nannoconus cor re lateswith the Mid- to Late Tithonian Nannofossil Cal ci fi ca tion Event (NCE) of Borne-mann et al. (2003).

Ac knowl edge mentsThis study was done as a stat u tory re search at the In sti tute of Geo log i cal Sci ences, Pol ish

Acad emy of Sci ences. Prof. Andrzej Wierzbowski (Fac ulty of Ge ol ogy, War saw Uni ver sity) kindlypro vided nine sam ples col lected by R. Wiêtczak (1999) from the Wapiennik klippe sec tion. I thankalso to Dr Ryszard Myczyñski for co-op er a tion dur ing the field work and to Dr Ryszard Or³owski fortech ni cal as sis tance with SEM pho to mi cro graphs prep a ra tion. I am grate ful to Au thor i ties of thePieniny Na tional Park and Tatra Na tional Park for per mis sion to work in the ar eas of these Parks. I amalso grate ful to the Man ag ers of the Res er voirs in Czorsztyn-Niedzica-Sromowce Wy¿ne S.A. forper mis sion to ac cess the Kapuœnica klippe dur ing field work. I thank Prof. Krzysztof Birkenmajer forvalu able ed i to rial re marks. Prof. Jerzy Lefeld kindly ex pressed critical observations on the manu-script of this paper.


Ta ble 2

Di men sions and out line of se lected Tithonian Nannoconus spe cies(af ter Pszczó³kowski, 2008, slightly mod i fied)

Taxon

Dimensions

Outline Source of dataLength[µm]

Width[µm]

Axial canal

Nannoconus compressusBralower et Thierstein

3–8 2–4Narrow(common lackof axial canal)

Rectangular toelongate oval

Bralower et al.(1989)

Nannoconus infansBralower

1–6 Less than 3 Very narrowVariable (square, elongate orsausage shaped)

Bralower et al.(1989)

Nannoconus wintereriBralower et Thierstein

4–8 4–8 Bowl-shaped Cone shapedBralower et al.(1989)

Nannoconus sp. A 4.5–7 4.5–7 Very narrow Cone shaped This paper

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the ti tho nian–ear li est ber ria sian nan no co nus...

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