VARI A TION IN CLASTIC IN PUT IN THE BERRIASIAN
OF THE LOWER SUB-TATRIC (KRÍŽNA) SUC CES SION
IN THE TATRA MOUNTAINS (CEN TRAL WEST ERN
CARPATHIANS, PO LAND): DATA FROM MAG NETIC
SUS CEP TI BIL ITY AND IN OR GANIC GEOCHEMISTRY
Jacek GRABOWSKI & Katarzyna SOBIEÑ
Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute, Rakowiecka 4, 00-975 Warszawa, Po land; e-mails: jacek.grabowski@pgi.gov.pl, katarzyna.sobien@pgi.gov.pl
Grabowski, J. & Sobieñ, K., 2015. Vari a tion in clastic in put in the Berriasian of the Lower Sub-Tatric (Krížna) suc ces sion in the Tatra Mountains (Cen tral West ern Carpathians, Po land): data from mag netic sus cep ti bil ity and in or ganic geo chem is try. Annales Societatis Geologorum Poloniae, 85: 139–150.
Ab stract: The pa per deals with the age and palaeoenvironment in ter pre ta tion of the Late Berriasian sed i men tary tran si tion from micritic calpionellid lime stones to marls, cor re spond ing to the pas sage from the Osnica For ma tion to the Koœcieliska Marl For ma tion, Lower Sub-Tatric suc ces sion, Tatra Mts., Cen tral West ern Carpathians. Since only re li ably dated sec tions are an ap pro pri ate ba sis for palaeoenvironmental study, the fol low ing pe lagic and hemipelagic sec tions were cho sen ow ing to en rich ment in fine, clastic ma te rial and the ex ist ing biostratigraphic and magnetostratigraphic frame works: Poœrednie III, Rówienka, G³adkie Up³aziañskie and Gêsia Szyja. The au thors in te grated and in ter preted new, de tailed data on mag netic sus cep ti bil ity (MS), rock mag ne tism and el e -ment geo chem is try from all of the sec tions. Well de fined biostratigraphy per mit ted the test ing of the po ten tial of MS as a strati graphic method. Ow ing to its close con nec tion to se lected terrigenous el e ments (e.g., Al, Th, Zr), MS could be used here as a proxy for de tri tal in put into the ba sin. Its value as a cor re la tion tool in a pe lagic and hemi-pelagic set ting was con firmed. MS per mit ted not only de tailed cor re la tion of the out crops stud ied, but also the com par i son of them with the Barlya sec tion (West ern Bal kans) of the same age.
This study proves that in creased de tri tal in put be gan in the Calpionellopsis sim plex Subzone and con tin ued into the lower part of the Calpionellopsis oblonga Subzone. It might be re garded as syn chro nous event within the Zliechov Ba sin and it is not ev ery where cor re lated with the for ma tion bound aries. The change in sed i men ta tion was not only a lo cal phe nom e non. The on set of de po si tion of the terrigenous frac tion can be iden ti fied in many sec tions of the West ern Tethys. Two in de pend ent fac tors, re gional re gres sion and an in crease in hu mid ity might have con trib uted si mul ta neously to the in creased de tri tal in put in Late Berriasian time. How ever, this pic ture is fur ther com pli cated by tec tonic ac tiv ity on lo cal and re gional scales.
Key words: Mag netic sus cep ti bil ity, geo chem is try, Berriasian, Lower Sub-Tatric suc ces sion, de tri tal in put, palaeoenvironmental changes, Tatra Mts.
Manu script re ceived 5 De cem ber 2014, ac cepted 4 March 2015
IN TRO DUC TION
The dat ing and quan ti fi ca tion of clastic in put into an -cient ma rine bas ins pro vide im por tant in for ma tion about rel a tive sea level changes (e.g., Haq, 2014; Wendler et al., 2014), tec tonic ac tiv ity (e.g., McCann and Saintot, 2003) and cli ma tic events (e.g., Adatte et al., 2002; Tucker, 2003). Mag netic sus cep ti bil ity (MS), which is a mea sure of the amount of para- and fer ro mag netic min er als, usu ally distri-buted within the dia mag netic ma trix (e.g., SiO2 or CaCO3),
has of ten been ap plied in re cent years as a use ful pa ram e ter for the es ti ma tion of terrigenous in flux (e.g., Ellwood et al.,
2000; Riquier et al., 2010; Da Silva et al., 2012, 2013). The ap pli ca tion of MS as a cor re la tion and palaeoenvironmental tool re quires re li able dat ing of the sec tions stud ied. The Berriasian pe lagic sec tions of the Lower Sub-Tatric (Krížna) suc ces sion of fer a good ba sis for test ing the po ten tial of MS for use as strati graphic method. The sec tions in the Pol ish part of the Tatra Mts. are well dated bio- and magnetostra-tigraphically (Pszczó³kowski, 1996; Grabowski and Pszczó³-kowski, 2006). As well, they are rel a tively rich in fine clastic ma te rial and the first re sults from the Poœrednie III sec tion
(Grabowski et al., 2013) in di cate that long-term changes in MS might be cor re lated with sea level trends (Hardenbol et
al., 1998) and/or cli ma tic events (Schnyder et al., 2006,
2009; Tremolada et al., 2006). In this pa per, the au thors pres ent the in te grated re sults of a new MS and geo chem i cal study of three new Berriasian sec tions and com pare them with the Poœrednie III sec tion. The au thors fo cus on dat ing and de ter mi na tion of the palaeoenvironment of a change in sed i men ta tion, which oc curred in the Late Berriasian and was man i fested in the tran si tion be tween micritic calpio-nellid-rich lime stones (Osnica Fm) and wide spread marls (Koœcieliska Marl Fm).
GEO LOG I CAL SET TING
AND STRA TIG RA PHY
The sec tions stud ied are lo cated in the Tatra Mts. (Po land) and be long to the Krížna Nappe (Fig. 1; Fatric do -main, Lower Sub-Tatric suc ces sion; see e.g., Bac-Mosza-szwili, 1998; Plašienka, 1997; Lefeld, 1999). They are (from west to east): Poœrednie III (PS), Rówienka (RO), G³adkie Up³aziañskie (GU) and Gêsia Szyja (GS). They were pri mar ily sit u ated within the extensional Zliechov Ba -sin, which was the site of deep-wa ter pe lagic and hemipelagic sed i men ta tion in the Late Ju ras sic and Early Cre ta -ceous (Lefeld, 1974; Vašíèek et al., 1994; Michalík et al., 1995a, b; Michalík, 2007). Af ter the Cenomanian, the Zlie-chov Ba sin was closed and thrusted north wards, to gether with other tec tonic el e ments of Fatric-Hronic nappe sys tem (e.g., Plašienka, 1997, 2003a, 2012; Prokešova et al., 2012;
Jurewicz, 2005). Dur ing thrust ing, the Krížna Nappe be -came dif fer en ti ated into nu mer ous smaller units (par tial nappes, du plexes; see Guzik and Kotañski, 1963; Prokešová
et al., 2012).
The stra tig ra phy of the Berriasian in the Lower SubTatric suc ces sion of the Tatra Mts. is well es tab lished, ow -ing to micropalaeontological (Lefeld, 1974; Pszczó³kowski, 1996) and magnetostratigraphic stud ies (Grabowski and Pszczó³kowski, 2006). The Ju ras sic/Cre ta ceous (Tithonian/ Berriasian) bound ary is sit u ated close to the bot tom of Osnica Fm (Michalík et al., 1990) which is seen as well bed -ded grey ish micritic lime stones with abun dant calpionellids. The Osnica Fm in the Tatra Mts. at tains a thick ness of up to 25–37 m (Pszczó³kowski, 1996). It is over lain by the Koœcieliska Marl Fm (Lefeld et al., 1985). The bound ary be -tween the two for ma tions is diachronous and ranges from the Remaniella cadischiana Subzone in the G³adkie Up³a-ziañskie sec tion to the Calpionellopsis oblonga Subzone in the Gêsia Szyja sec tion (Pszczó³kowski, 1996, 2003). In the Bobrowiec Unit in the West ern Tatra Mts., the bound ary is sit u ated in the up per part of the Calpionellopsis sim plex Subzone, in the lower part of the magnetozone M16n (Gra-bowski and Pszczó³kowski, 2006).
An es ti ma tion of the sed i men ta tion rate re vealed a mar-ked con trast be tween the two for ma tions: 10–17 m/My in the Osnica Fm and at least 18–23 m/My in the Koœcieliska Marl Fm (Up per Berriasian) (Grabowski and Pszczó³kow-ski, 2006).
An at tempt at palaeoenvironmental in ter pre ta tion of the Tithonian–Berriasian suc ces sion was per formed by Gra-bowski et al. (2013) for the Poœrednie III sec tion. Abrupt
Fig. 1. Tec tonic sketch map of the Tatra Mts. and lo cal iza tion of the sec tions stud ied: PS – Poœrednie III, RO – Rówienka, GU – G³adkie Up³aziañskie, GS – Gêsia Szyja.
MS vari a tions ap par ently cor re late well with rel a tive sea-level changes and in di cate re gres sive in ter vals (MS highs) in the Up per Tithonian/low er most Berriasian (mag netozo-nes M20r to M19n2n) and Up per Berriasian (M16n) and a transgressive in ter val (MS low) in the Lower Berriasian (M18r to M17r). Long-term MS vari a tions might be linked to en hanced con ti nen tal run-off, con trolled by palaeocli-mate. Geo chem i cal data (P, Th/U, Mn, Cd, Ni, Mo and TOC con tent) in di cate an in crease in bi o log i cal pro duc tiv ity and a slight ox y gen de fi ciency in the Lower Berriasian, which cor re spond to MS low val ues and typ i cal nannofossil-cal-pionellid lime stone sed i men ta tion. The tim ing of ma jor palaeoenvironmental changes might be cor re lated also with gen eral palaeoclimatic trends in the West ern Tethys and West ern Eu rope: cool ing in the late Tithonian fol lowed by a tem per a ture in crease through out the Berriasian and an im -por tant hu mid ity in crease in the up per part of the Lower Berriasian (M17n; Grabowski et al., 2013).
MA TE RIAL
The G³adkie Up³aziañskie (GU) sec tion (Up³aziañska Kopa in Jach et al., 2014) is lo cated within a sep a rate small tec tonic slice (Kotañski, 1965), on the south ern slope of the G³adkie Up³aziañskie hill (GPS co or di nates: N 49°14'22.1", E 19°53'22.7"). It is al most 85 m thick and cov ers a large part of the Lower and Up per Berriasian from the Alpina up to the Murgeanui subzones (Fig. 2). The sec tion pre sented in the Fig. 2 is a com pos ite sec tion, based on the data of Pszczó³kowski (1996, 2003). The bound ary of the Osnica/ Koœcieliska for ma tions oc curs in the Lower Berriasian, in the Cadischiana Subzone.
The Gêsia Szyja (GS) sec tion, 46 m thick, is sit u ated on the tour ist trail lead ing from the Rusinowa Polana (Rusi-nowa Glade) to Gêsia Szyja Hill (GPS co or di nates: N49° 15'32.4", E20°04'49.86") in the east ern part of the Tatra Mts. (Pszczó³kowski, 1996). It be longs to a tec tonic slice, called the Gêsia Szyja Cre ta ceous Slab (Lefeld, 1999) or the Gêsia Szyja Par tial Nappe (Soko³owski, 1978; Birkenmajer, 2000). It cov ers the up per part of the Lower Berriasian (the up per part of the Alpina Subzone) up to the Oblonga Sub-zone of the Up per Berriasian. The con tact be tween the Osnica and Koœcieliska Marl for ma tions is sit u ated in the up -per most part of the sec tion, in the up -per part of the Oblonga Subzone (Fig. 3).
The Poœrednie III and Rówienka sec tions (Grabowski and Pszczó³kowski, 2006) are sit u ated in the Bobrowiec Unit (Bac, 1971; Bac-Moszaszwili, 1998) in the West ern Tatra Mts.
The Rówienka (RO) sec tion (Grabowski and Pszczó³-kowski, 2006) lies in the lower part of the Lejowa Val ley, in a gully on its south-east ern slopes (be gin ning of the sec tion: N49°16'14.0", E19°50'51.8"; end of the sec tion: N49°16' 11.8", E19°50'54.3"). The sec tion, 37 m thick, com prises con tin u ous ex po sure from the up per most Lower Ber-riasian (Elliptica Subzone, M16r) up to the up per part of the Up per Berriasian (up per part of the Calpionellopsis Zone, M16n). A con tin u ous tran si tion be tween the Osnica and Koœcieliska Marl fms is well ex posed there (Fig. 4).
The Poœrednie III (PS) sec tion is lo cal ized to the west of the Chocho³owska Val ley, on the ridge be tween the Kryta and D³uga val leys (be gin ning of the sec tion: N49°15'37.1", E19°48'05.5"; end of the sec tion: N49°15'38.5", E19°48' 05.8"). The en tire sec tion cov ers in ter val from the up per -most part of the Lower Tithonian up to the Up per Ber-riasian (Grabowski and Pszczó³kowski 2006; Grabowski et
al., 2013). In this study, only the up per part of the sec tion is
con sid ered and com prises the up per part of the Lower Ber-riasian (top most part of the Calpionella alpina Subzone; M17r) up to the Up per Berriasian (Calpionellopsis oblonga Subzone, M16n), about 22.5 m in thick ness (see Fig. 5). Un -for tu nately, the con tact be tween the Osnica and Koœcieliska Marl fms is cov ered in that sec tion and most prob a bly is tec -tonic in char ac ter (Grabowski et al., 2013).
Fig. 2. G³adkie Up³aziañskie sec tion: li thol ogy and biostratigraphy (slightly mod i fied af ter Pszczó³kowski, 1996, 2003), mag netic sus cep ti bil ity (MS), iso ther mal remanent mag ne ti za tion ac -quired in the field of 1 T (IRM1T), and S-ra tio.
SAM PLING AND METH ODS
In the pres ent study, the au thors used the ar chi val sam -ples of Pszczó³kowski (1996) from the G³adkie Up³aziañskie and Gêsia Szyja sec tions. The au thors also used the ar -chi val sam ples of Grabowski and Pszczó³kowski (2006) for the Rówienka sec tion. Ad di tion ally, the re sults were com -pared with the data from the Poœrednie III sec tion, pub lished by Grabowski et al. (2013). Bulk mag netic sus cep ti bil ity (MS) was mea sured in three po si tions for 162 sam ples us ing a KLY-2 kappabridge (AGICO, Brno, sen si tiv ity 10-8 SI), in the Paleomagnetic Lab o ra tory of the Pol ish Geo log i cal In sti tute – Na tional Re search In sti tute in War saw. Iso ther -mal remanent mag ne ti za tion (IRM) was ac quired us ing a MMPM pulse mag ne tizer, in the fields of 1T (IRM1T) and
then anti-par al lel in the field of 100mT (IRM100mT). The S
pa ram e ter (S-ra tio), cal cu lated as a ra tio of IRM in ten si ties ap plied in both fields (IRM100mT/IRM1T), was in dic a tive
for pro por tions of low- and high-coercivity min er als. All magnetic mea sure ments were nor mal ized for mass. The quan ti ties of sam ples from par tic u lar sec tions were as fol -lows: 64 from the G³adkie Up³aziañskie, 36 sam ples from the Gêsia Szyja and 62 sam ples from the Rówienka sec -tions. All sam ples pre vi ously had been in ves ti gated bio-stratigraphically (Pszczó³kowski, 1996, 2003; Grabowski and Pszczó³kowski, 2006). The Poœrednie III and Rówienka sec tions were cal i brated with the magnetostratigraphy (Grabowski and Pszczó³kowski, 2006). Chem i cal anal y ses of 114 whole-rock sam ples (RO – 42, PS – 32, GU – 19, GS – 21) were per formed at the Acme An a lyt i cal Lab o ra to ries, Van cou ver, Brit ish Co lum bia. The con cen tra tions of ma jor and trace el e ments were mea sured by in duc tively cou pled plasma mass spec trom e try (ICPMS). Mea sure ment pre ci -sion was as fol lows: 0.02% for Al, Ca, K, and Fe; 0.001% for Ti, 0.1 ppm for Sc, Rb, Th, Ni, and U; 0.02 ppm for Ga;
Fig. 3. Gêsia Szyja sec tion: li thol ogy and biostratigraphy (slightly mod i fied af ter Pszczó³kowski, 1996), mag netic sus cep ti -bil ity (MS), iso ther mal remanent mag ne ti za tion ac quired in the field of 1 T (IRM1T), and S-ra tio. Ab bre vi a tions: fer. – ferasini; ellip. – elliptica; cad. – cadischiana.
Fig. 4. Rówienka sec tion: li thol ogy, biostratigraphy, mag netic sus cep ti bil ity (MS), iso ther mal remanent mag ne ti za tion ac quired in the field of 1 T (IRM1T), and S-ra tio (slightly mod i fied af ter Grabowski and Pszczó³kowski, 2006). Ab bre vi a tions: CAL. – Calpionella; ell. – elliptica; cad. – cadischiana.
Fig. 5. Poœrednie III sec tion: li thol ogy, biostratigraphy, mag netic sus cep ti bil ity (MS), iso ther mal remanent mag ne ti za tion ac -quired in the field of 1 T (IRM1T), and S-ra tio (slightly mod i fied af ter Grabowski et al., 2013). Ab bre vi a tions: alp. – alpina; ell. – elliptica; sim. – sim plex; KMF – Koœcieliska Marl For ma tion.
0.001 ppm for P; 0.2 ppm for Co, Zr, and Zn; and 1 ppm for Cr. In this pa per, only el e ments re lated to the de tri tal in put are dis cussed. Alu minium con tent was se lected as a nor mal -iz ing fac tor, on the as sump tion that it is hosted solely in the lithogenous sed i ment frac tion (e.g., Calvert and Pedersen, 1993; Brumsack, 2006; Tribovillard et al., 2006; see also Grabowski et al., 2013).
RE SULTS
Mag netic sus cep ti bil ity
MS in the G³adkie Up³aziañskie sec tion (Fig. 2) re -vealed a de creas ing pat tern in the lower part, from 30 × 10-9 m3/kg in the Alpina Subzone to 10 × 10-9 m3/kg in the Re-maniella ferasini Subzone, the C. elliptica Subzone and the lower part of the R. cadischiana Subzone. A grad ual in -crease to 20–25 × 10-9 m3/kg was ob served in the up per part of the Cadischiana Subzone and the lower part of the Sim -plex Subzone. A no tice able in crease to 60–70 × 10-9 m3/kg oc curs in the up per most part of the Sim plex Subzone and these val ues, with mi nor vari a tions, are pre served up to the top of the sec tion (Murgeanui Subzone).
In the Gêsia Szyja sec tion (Fig. 3), the Ferasini, Elli-ptica and Cadischiana subzones are re duced in thick ness (about 10 m) by com par i son with the G³adkie Up³aziañskie sec tion (al most 30 m). Nev er the less, sim i lar MS trends were ob served. A sub tle MS de crease was ob served be tween the Alpina and Elliptica subzones (be tween 20 and 15 × 10-9 m3/kg). Through out the Cadischiana Subzone and the lower part of the Sim plex Subzone the MS re turns to val ues of 20 × 10-9 m3/kg and in the mid dle part of the Sim plex Subzone it rises sharply to 45–50 × 10-9 m3/kg. Even higher val ues of MS were ob served in the up per part of the Oblonga Sub-zone (up to 70 × 10-9 m3/kg).
In the Rówienka sec tion (Fig. 4), the MS rises gently from 10 to about 20 × 10-9 m3/kg be tween the Elliptica Sub- zone and the lower part of the Sim plex Subzone and then rather sharply to 40 × 10-9 m3/kg in the up per part of the
Sim plex Subzone. Also in this sec tion, the high est MS val -ues oc cur in the up per part of the Oblonga Subzone. In the
Poœrednie III sec tion (Fig. 5), MS fluc tu ated be tween 10
and 20 × 10-9 m3/kg in the Elliptica and Cadischiana sub-zones. A con tin u ous tran si tion to wards the Sim plex Sub-zone is not ex posed; how ever, in the Oblonga SubSub-zone MS val ues amount al ready to 40–50 × 10-9 m3/kg.
Mag netic min er al ogy and geo chem is try
The pre vi ous rock mag netic in ves ti ga tions, per formed for the Poœrednie III and Rówienka sec tions (Grabowski and Pszczó³kowski, 2006), proved that mag ne tite is the main mag netic min eral in the Osnica and Koœcieliska Marl fms. The sub or di nate pres ence of he ma tite was noted only in the lower part of the Osnica Fm.
The pre dom i nance of low-coercivity min er als also was con firmed in the pres ent study. The S-ra tio re vealed al most ex clu sively low neg a tive val ues, which con firmed the presence of mag ne tite. The only ho ri zon with a slightly pos i tive value of Sra tio (highercoercivity min er als, pos si bly he -ma tite?) is rep re sented by sam ple GU 73 in the G³adkie Up³a- ziañskie sec tion (lower part of the Oblonga Subzone; Fig. 2). Mag ne tite con trib utes to the MS, which is ev i denced in a generally good cor re la tion be tween MS and IRM1T (Fig.
6A). An MS in crease from 10 to 50 × 10-9 m3/kg is ac com -pa nied by only a slight pos i tive shift of the IRM1T. For sam
-ples with MS val ues higher than 50 x 10-9 m3/kg, the slope of cor re la tion is much steeper, so that even a slight in crease in MS re sults in a large in crease in IRM1T. This is es pe cially
well dem on strated in the G³adkie Up³aziañskie and Rówienka sec tions (Fig. 6A). This in di cates that in those sam -ples (mostly in the Koœcieliska Marl Fm) the fer ro mag netic con tri bu tion to the MS might be more sig nif i cant.
An ex cel lent pos i tive cor re la tion is ob served be tween MS and Al, as well as the other de tri tal el e ments (Ti, Zr, Th, and other; see Ta ble 1 and Fig. 6B). There is also a good neg a tive cor re la tion be tween MS and Ca (Fig. 6C). This is proof that MS might be re garded as a good proxy for
Fig. 6. Cor re la tion be tween mag netic sus cep ti bil ity (MS) and: (A) iso ther mal remanent mag ne ti za tion ac quired in the field of 1 T (IRM1T), (B) alu minium, and (C) cal cium. Black and white sym bols: data be fore (up to the last MS low value = lower end of the ar rows in Fig. 7) and af ter MS in crease in Sim plex Subzone (see Fig. 7). GU – crosses, GS – di a monds, RO – cir cles, PS – tri an gles.
lithogenic in put in all four sec tions, in de pend ently of the rel a tive para and fer ro mag netic con tri bu tion. Pre vi ous in -ves ti ga tions re vealed that de tri tal ma te rial is abun dant in both the Osnica and Koœcieliska Marl fms of the PS sec tion (Grabowski et al., 2013). It com prises quartz, chlorite, al bite, mus co vite, ap a tite, rutile and in places also bi o tite. Ti -ta nium ox ides are ap par ently more com mon in the Koœcieliska Marl Fm than in the Osnica Fm, which might in di -cate that also de tri tal magnetites and/or titanomagnetites are more abun dant in the for mer.
DIS CUS SION
The four stud ied sec tions re veal quite sim i lar pat tern of MS vari a tion. Gen eral low MS pre dom i nates from the up per part of the Alpina, through the Ferasini, Elliptica and Ca-dischiana subzones, up to the lower part of the Sim plex Subzone (lower part of M16n). Higher up in the lat ter subzone, a ma jor in crease in MS oc curs, which is per sis tent with some small-scale vari a tions also in the Oblonga and Murgeanui subzones. An in ter val of MS in crease is lo cated in the up per part of Sim plex Subzone (lower part of M16n) in the Rówienka and Gêsia Szyja sec tions, and at the bound -ary be tween the Sim plex and Oblonga subzones in the G³adkie Up³aziañskie sec tion. Un for tu nately, de tailed dat -ing of this in ter val is im pos si ble in the Poœrednie III sec tion, be cause it is lo cated in a gap in the sec tion (be tween the lower part of the Sim plex and the Oblonga subzones). As the MS in creases, a rel a tively higher amount of fer ro mag -netic par ti cles is pres ent in the sed i ment.
A con trast in terrigenous in put be tween the Osnica and Koœcieliska fms was well known and quite ob vi ous (Lefeld, 1974; Lefeld et al., 1985). The pres ent study proves that the ma jor in crease in terrigenous in put be tween the Sim plex and Oblonga subzones might be a syn chro nous event within the Zliechov Ba sin and the for ma tion bound aries do not al -ways cor re late with it. In the G³adkie Up³aziañskie sec tion, it oc curs in the Koœcieliska Marl Fm (about 17 m above the base), while in the Gêsia Szyja sec tion, still in the Osnica Fm (about 24 m be low the top). This ob ser va tion in di cates that cor re la tion of clastic events on the ba sis of field ob ser -va tions might be mis lead ing. There fore, the au thors re gard MS as an ap pro pri ate tool for the quan ti fi ca tion of fine clastic in put in such pe lagic and hemipelagic sed i ments. An in crease in clastic in put in the Lower Sub-Tatric suc ces sion in the Tatra Mts. (based on MS log ging and gamma-ray spec trom e try in the Poœrednie III sec tion) be tween the
Lower and Up per Berriasian was al ready doc u mented by Grabowski et al. (2013).
The re sults ob tained in sec tions from the Lower Sub-Tatric suc ces sion in the pres ent study might be com pared to magnetostratigraphic and MS data from the Barlya sec tion in Bul garia (West ern Bal kans, Grabowski et al., 2014b). It is ev i dent that there too, an in crease in marly sed i men ta tion is ob served be tween the up per part of the Sim plex Subzone and the lower part of the Oblonga Subzone (the tran si tion be tween Glozhene and Salash fms; see Lakova et al., 2007; Lakova and Petrova, 2013), in the lower part of mag neto-zone M16n. The MS in crease is not as sharp as in the sec tions of the Lower Sub-Tatric suc ces sion and its mag ni tude is lower. Nev er the less, the MS in crease in Barlya, be tween 110 and 114 m in the lower part of M16n, cor re sponds ex actly to the pos i tive MS shift in the Rówienka sec tion (Fig. 7). It is note wor thy that the range of the Sim plex Subzone in the Rówienka and Barlya sec tions is slightly dif fer ent. The bot -tom of the Sim plex Subzone falls in the up per most part of M16r in the Rówienka and in the mid dle part of M16r in the Barlya sec tions.
The in creased sup ply of fine clastic ma te rial in the Late Berriasian might be in ter preted as a re sult of the in ter play be tween at least three fac tors:
1 – gen eral re gres sion in the Tethyan do main (Har-denbol et al., 1998; Pszczó³kowski and Myczyñski, 2010);
2 – an in crease in cli mate hu mid ity at the north west -ern mar gin of the Tethys and the sur round ing ar eas of the Eu ro pean plat form (Abbink et al., 2001; Schnyder et al., 2006; Mo rales et al., 2013);
3 – re gional tec tonic phe nom ena, re lated to rift ing pro -cesses in the Vahic-Magura Ocean (Golonka and Krobicki, 2001; Golonka et al., 2003; Plašienka, 2003b; Krobicki et al., 2010).
De tri tal sup ply as a re sult of re gres sion
Grabowski et al. (2013) noted sim i lar i ties be tween T-R cy cles in the Tethyan realm and the long-term MS pat tern in the Poœrednie III sec tion. The MS in crease in the Up per Berriasian would rep re sent a max i mum re gres sion in the up per most part of magnetozone M16n (Fig. 8). The in flu -ence of eustatic events on sed i men tary and bi otic changes in the West ern Carpathians was sug gested by Reháková (2000) and Michalík (2007). An in crease in fine clastic in -put and a shallowing ten dency in the Up per Berriasian of the West ern Tethys seems to be a re gional phe nom e non. In the West ern Carpathians, marly sed i men ta tion started at the
Ta ble 1
Cross-cor re la tions be tween Al and se lected el e ments
K Rb Ti Th Ga Zr V Sc Fe U P Co Ni Cr Zn Ca
GU 0.99 0.99 0.99 0.99 0.99 0.99 0.99 0.99 0.99 0.98 0.91 0.86 0.86 0.89 0.55 -0.98
GS 0.98 0.94 0.99 0.99 0.99 0.99 0.99 0.99 0.97 0.93 0.94 0.95 0.92 0.98 0.96 -0.98
RO 0.99 0.99 0.99 0.99 1.00 0.99 0.99 0.99 0.97 0.95 0.94 0.82 0.93 0.91 0.97 -0.83
PS 0.98 0.98 0.97 0.99 0.99 0.98 0.99 0.98 0.98 0.91 0.87 0.88 -0.09 0.58 0.89 -0.45
. 7 . gi F i ks w o ba r G re tf a , ai ra gl u B , na kl a B nr et se W( n oi t ce s a yl ra B e ht hti w n oi ss e c c us ci rt a T-b u S re w o L e ht ni de i d ut s s n oi t ce s e ht f o n oi t a l e r r o C .l a t e a r gi t art s-ot e n ga m , -oi b g n i s u ) b 4 1 0 2 , -– . re f : s n oi t ai ve r b b A . ) n 6 1 M f o t ra p re w ol ( e n oz b u S a g n ol b O f o t ra p re w ol d na e n oz b u S xe l p mi S e ht ni hti w es ae r c ni S M f o l e ve l e ht et a c i d ni s w o r r A . yt i li bi t pe cs us c it e n ga m d na y h p ;i ni sa re f – . pil le – . da c ; ac it pil le – . L A C ; a na i hc si da c – . ll e ; all e n oi pl a C – . pl a ; ac it pil le – . mi s ; a ni pl a – F M K ; xe l p mi s œ o K – L S-L G ; n oi t a mr o F l ra M a ks il ei c hs al a S d na e ne hz ol G ne e w t e b n oi t i s na rt e ht .s mf
Sim plex/Oblonga subzonal bound ary, as in the Hlboèa sec -tion in the Male Karpaty (Hlboè Fm – Grabowski et al., 2010) and in the lower part of the Calpionellopsis Zone in the Strážovce sec tion in the Strážov Mts. (Mráznica Fm – Michalík et al., 1995a).
An on set of marly sed i men ta tion in the early Late Ber-riasian, man i fested in the tran si tion be tween the Oberalm and Schrambach fms, is well known also in the North ern Calcareous Alps (e.g., Faupl et al., 1997; Rasser et al., 2003; Krische et al., 2013). In West ern Cuba, an im por tant lith o logic change takes place in the Up per Berriasian in the Guaniguanico suc ces sions, where radiolarian lime stones of the Artemisa Fm are over lain by clastic-rich sed i ments of the Polier Fm in the North ern Rosario suc ces sion (Pszczó³-kowski and Myczyñski, 2010). Pale red pe lagic biomicrites of Tumbitas Mem ber rest on the dark lime stones of Tum-badero Mem ber in the Los Organos suc ces sion. The au thors cor re lated this sed i men tary change with a sig nif i cant sea-level fall in the scheme of Haq et al. (1987).
De tri tal sup ply as a re sult of cli mate hu mid ity in crease
Re cently, the tim ing of a cli mate hu mid ity change in the Up per Berriasian was doc u mented in the Vocontian Ba sin (SE France, Montclus sec tion). Its on set (first kaolinite oc -cur rences) falls in the calpionellid D1 (Sim plex) Subzone, but kaolinite be comes more abun dant in the calpionellid D3 Subzone (Mo rales et al., 2013). Also in the Mount SalÀve sec tion (E France), the cli ma tic change oc curred in the calpionellid D2 Subzone (Bover-Arnal and Strasser, 2013). The MS event in the Sim plex Subzone broadly co in -cided in time with the hu mid ity change in the Late Ber-riasian. How ever, data on clay min er als (kaolinite con tent), which are of cru cial im por tance in pos tu lat ing the cli ma tic na ture of this event, are not avail able from the Lower Sub-Tatric suc ces sion. It is well known that clay min er als in the Me so zoic rocks of the Tatra Mts. were sig nif i cantly trans formed dur ing deep tec tonic burial, ow ing to the Late Cre ta ceous thrust ing, and pres er va tion of pri mary kaolinite was hardly pos si ble. Al most all data re vealed the pres ence of less than 15% of smectite (Œrodoñ et al., 2006), while un -pub lished data from the Tithonian–Berriasian strata in the area of the Kryta sec tion (West ern Tatra Mts., Lower Sub-Tatric suc ces sion – P. Brañski, pers. comm., 2013) in dica-ted the pres ence of illite (56–64%) and chlorite (36–44%).
De tri tal sup ply as an ef fect of re gional tec ton ics
Krobicki et al. (2010) point to the im por tance of tecto-nic phe nom ena as the main fac tors con trol ling de tri tal in put into the Carpathian bas ins. The idea was es pe cially well do-cumented in the Czorsztyn suc ces sion of the Pieniny Klip-pen Belt. The Walentowa Brec cia Mem ber (Birkenmajer, 1977), in ter preted as a prod uct of synsedimentary mass movements along sub ma rine scarps (Birkenmajer, 1958, 1975), is dated as Up per Berriasian (Calpionellopsis Zone; see Wierzbowski and Remane, 1992).
The shallowing-up ward trend in var i ous parts of the Czorsztyn suc ces sion of the Pieniny Klippen Belt was proved through out the Berriasian (from the Ju ras sic/Cre ta
-ceous bound ary to the up per part of the Calpionellopsis Zone) by anal y sis of brachi o pod as sem blages (Krobicki, 1994, 1996). These phe nom ena were in ter preted as an ef fect of “Neo-Cim mer ian” events, which in fact were re lated to ex ten sion and rift ing in the Magura Ocean, on the north ern side of the Czorsztyn Ridge (Walentowa Phase of Plašienka, 2003b). In crease of marly sed i men ta tion in the Up -per Berriasian (at the sim plex/oblonga subzonal bound ary) is ob served in the Branisko suc ces sion of the PKB (£ysonka Marl Bed; Pszczó³kowski and Myczyñski, 2004).
It is not easy to de cide to what ex tent each of the fac tors men tioned ex erted an in flu ence on the in creased terrigenous in flux into the Zliechov Ba sin in the Late Berriasian, doc u mented in this pa per. Both cli ma tic changes and eustatic re -gres sion in the Late Berriasian are well doc u mented and their ef fects might have been superposed, con trib ut ing to a wide re gional sed i men tary change. The se quence of events pre sented in Fig ure 8 does not ap pear to be syn chro nous, al though a con cen tra tion of events in the lower part of the Up per Berriasian is ev i dent. It must be kept in mind that in te -grated magnetostratigraphic, MS and calpionellid stud ies were per formed only in the Tatra Mts. and West ern Bal -kans. How ever, in these lo cal i ties the be gin ning of marly sed i men ta tion co in cides very clearly (see Fig. 7). The MS event is sit u ated in the re gres sive in ter val of both ref er ence sea level curves (Fig. 8), but it does not cor re late with the max i mum re gres sion in the Hardenbol et al. (1998) scheme. The sit u a tion is ad di tion ally com pli cated by lo cal and re -gional tec tonic ac tiv ity in the Late Berriasian: rift ing phases and ver ti cal tec tonic move ments man i fested by brec cias in the Cen tral West ern Carpathians and the Pieniny Klippen Belt (see Michalík et al., 1995a; Reháková, 2000; Golonka and Krobicki, 2001; Golonka et al., 2003: Nozdrovice and Walentowa brec cias).
In the opin ion of the au thors, how ever, the Czorsztyn Ridge and sur round ing ar eas def i nitely could not be the source of the fine siliciclastic ma te rial sup plied to the Zlie-chov Ba sin. The MS val ues in the Berriasian and Valangi-nian of the Pieniny Lime stone Fm are an or der of mag ni tude lower than in the co eval de pos its of the Lower Sub-Tatric suc ces sion (the Osnica Fm and the Koœcieliska Marl Fm; see Grabowski et al., 2014a). This in di cates that the source area must have been sit u ated south of the Zliechov Ba sin, most prob a bly in the area of the Meliata-Hallstatt su ture zone (see also Œwierczewska and Pszczó³kowski, 1997; Faupl et al., 1997; Jablonský et al., 2001; Michalík, 2007). The tec tonic phe nom ena re spon si ble for the for ma tion of the car bon ate brec cias were most prob a bly superposed on the eustatic and/or cli ma tic trends.
CON CLU SIONS
Four Berriasian sec tions in the Lower SubTatric suc ces -sion in the Pol ish part of the Tatra Mts. were cor re lated by means of mag netic sus cep ti bil ity. MS re flects the amount of in flux of clay par ti cles and de tri tal mag ne tite into the ba sin. This is ev i denced by very good pos i tive cor re la tion with lithogenic el e ments (Al, Th, Zr and oth ers) and a neg a tive cor re la tion with Ca. A sharp in crease in MS was ob served be
-tween the Calpionellopsis sim plex and the Calpionellopsis oblonga subzones, in the lower part of the Up per Berriasian magnetozone M16n.
The in crease in MS does not cor re spond ev ery where to the lithostratigraphical bound ary be tween the Osnica Fm and the Koœcieliska Marl Fm.
An in crease in marl sed i men ta tion in the early Late Ber- riasian was doc u mented and magnetostratigraphically dated also in the West ern Bal kans (Barlya sec tion). It seems that an in crease in clastic in put might have been a re gional phe -nom e non, at least in the West ern Tethys (e.g., in the Austro- Al pine do main and in west ern Cuba).
The palaeoenvironmental in ter pre ta tion of this late Ber- riasian MS event is not clear. It might have been con trolled ei ther by re gional re gres sion in the West ern Tethyan do -main and by cli ma tic change (in crease in hu mid ity). A joint
con tri bu tion of both of these fac tors (eustatic and cli ma tic) also is likely.
Ac knowl edge ments
The au thors are deeply grate ful to Andrzej Pszczó³kowski for ac cess to his ar chi val sam ple col lec tions as well as for nu mer ous com ments and dis cus sion of an ear lier ver sion of the manu script. The manu script ben e fit ted from the com ments from jour nal re -view ers: Renata Jach and Laurent Riquier. The in ves ti ga tions were fi nan cially sup ported by Pro ject DEC-2011/03B/ST10/ 05256 of the Na tional Sci ence Cen tre, Po land. This is a con tri bu tion to the IGCP Pro ject 609 “Cli mateen vi ron men tal de te ri o ra -tions dur ing green house phases: Causes and con se quences of short-term Cre ta ceous sea-level changes”. Thanks are due to Beata D¹browska (War saw Uni ver sity) for car ry ing out rock mag netic mea sure ments.
Fig. 8. In te grated Late Berriasian bio- and magnetostratigraphical scheme, its cor re la tion with eustatic sea level changes af ter Haq (2014) and Hardenbol et al. (1998, only T-R cy cles in Tethyan do main) and Berriasian clastic and cli ma tic events dis cussed in this study. Strati graphic po si tions of events af ter Mo rales et al. (2013; SE France), Pszczó³kowski and Myczyñski (2010; W Cuba), Wierzbowski and Remane (1992; Walentowa Brec cia), Golonka and Krobicki (2001; Czorsztyn Ridge), Pszczó³kowski and Myczyñski (2004; £ysonka Marl Bed), Krische et al. (2013; North ern Cal car e ous Alps), Grabowski et al. (2010; Hlboè Fm) and Michalík et al. (1995a; Mráznica Fm).
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