Benthic foraminiferal biostratigraphy of the lower and middle Campanian of the Polish Lowlands and its application for interregional correlation

Cretaceous Research 56 (2015) 491e503

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Benthic foraminiferal biostratigraphy of the lower and middle Campanian of the Polish Lowlands and its application for interregional correlation Zofia Dubicka* _ University of Warsaw, Faculty of Geology, Zwirki i Wigury 93, 02-089 Warsaw, Poland

a r t i c l e i n f o

a b s t r a c t

Article history: Received 22 January 2015 Received in revised form 10 June 2015 Accepted in revised form 20 June 2015 Available online 5 July 2015

This paper presents the benthic foraminiferal biostratigraphy of the lower and middle Campanian of the wka and Rzezu _ snia sections in the WolbromPolish Lowlands based on the study of Wierzchowisko, Jez_ o  w area (southern Poland) and the Mielnik section (eastern Poland). Miecho The ranges of twenty two selected stratigraphically useful taxa of the genera Gavelinella, Bolivinoides, Cibicidoides, Globorotalites and Stensioeina are presented in relation to macrofossil zonation, previously established in the same successions. The evolutionary changes within selected lineages of the studied genera and major foraminiferal bioevents are discussed. The taxa ranges recorded in the Polish Cretaceous are compared with the ranges described from western Europe. Most of the studied events seem to be readily applicable for stratigraphic correlation all over Europe. © 2015 Elsevier Ltd. All rights reserved.

Keywords: Benthic foraminifera Campanian Poland Biostratigraphy

1. Introduction The Campanian is the longest stage of the Upper Cretaceous system, spanning around 11 myr. Yet there are still many deficiencies in the standard and global Campanian strata selection criteria (Ogg and Hinnov, 2012). The base of the Campanian has not yet been formally ratified. A provisional and commonly used boundary marker for the base of the Campanian Stage is the extinction of the crinoid Marsupites testudinarius although the occurrence of this taxon is restricted to certain environments and thus is not found everywhere in the world (Hancock and Gale, 1996). The Waxahachie dam spillway section (central Texas) is regarded as a potential Global Stratotype Section for the base of the Campanian Stage, where the boundary is also marked by a d13C excursion (Gale et al., 2008). The base of the Campanian lies also at or within the lower portion of reversed-polarity Chron C33r (e.g., Montgomery et al., 1998); if this definition would be applied as the primary boundary definition for the base of the Campanian then the Gubbio section, in Italy, could be proposed as its stratotype (e.g., Alvarez et al., 1977). The Campanian Stage is generally subdivided into lower, middle and upper substages of approximately equal

* Corresponding author. E-mail address: [email protected]. http://dx.doi.org/10.1016/j.cretres.2015.06.012 0195-6671/© 2015 Elsevier Ltd. All rights reserved.

duration; although no formal recommendation for any of these boundaries were proposed (Ogg and Hinnov, 2012). Informally, definitions of these boundaries follow the North American Western Interior concepts, with the lower/middle and middle/upper Campanian boundaries defined with the lowest occurrences of ammonoids Baculites obtusus and Didymoceras nebrascense, respectively (Cobban, 1993; Cobban et al., 2006). Traditionally, in Europe it is the two-fold subdivision of the Campanian stage (lower/upper), which is commonly used; the three-fold subdivision is used additionally. The base of the upper Campanian is placed at the first appearance of the belemnite Belemnitella mucronata (Schlotheim), the level which is correlated slightly below the lower/middle Campanian boundary as defined in the US Western Interior (Ogg and Hinnov, 2012). The correlation between tripartite US and two-fold traditional European subdivisions was mainly established using inoceramid fauna (Walaszczyk, 1997; Walaszczyk et al., 2001, 2008). Benthic foraminifera have been used for a long time to recognize lower and upper Campanian in European epicontinental facies (e.g. Hofker, 1957; Vasilenko, 1961; Hiltermann and Koch, 1962; Koch, €nfeld, 1990; 1977; Bailey et al., 1983; Hart et al., 1989; Scho Gawor-Biedowa, 1992; Dubicka and Peryt, 2014; Peryt and Dubicka, in press). The distribution of benthic foraminifera is also important in the definitions of the lower and upper boundaries of the Campanian stage as well as for the lower/upper Campanian boundary in European chalky facies (Hampton et al., 2007;

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Peryt and Dubicka, in press). The first or last appearance datums (FAD and LAD) of some of the benthic taxa were even discussed as potential markers for the boundary levels in the North Temperate Zone. For instance, the LAD of Bolivinoides strigillatus, which coincides with the top of the Marsupites testudinarius Zone, and the FAD of Bolivinoides culverensis, which occurs within the basal part of the Offaster pilula Zone, were proposed as foraminiferal proxies for the base of the Campanian Stage (Hampton et al., 2007). The FAD of Neoflabellina reticulata was discussed as an important foraminiferal proxy for the base of the Maastrichtian in Europe (Odin, 1996; Peryt and Dubicka, in press). However, more recent studies of the Campanian benthic foraminiferal stratigraphy correlated with well-established macrofaunal biostratigraphy were €nfeld, conducted mostly in western Europe (Hart et al., 1989; Scho 1990). There is very little data about species ranges correlated with other stratigraphic indicators in the Campanian of central and eastern Europe. The present paper combines the stratigraphic range data of the lower and middle Campanian benthic foraminifera of the two distinct regions of Poland. The species ranges are presented in relation to macrofossil zonations (Jagt et al., 2004; Olszewska Nejbert and Swierczewska-Gładysz, 2011; Jurkowska et al., 2015), including inoceramids which are extremely important for correlating the European and US Western Interior Campanian (Walaszczyk et al., 2001; Walaszczyk, 2004; Jurkowska, in press). It allowed the comparison of the foraminiferal ranges recorded within the studied successions with those of other European regions and thus discussion of their correlation potential over much of Europe. The probable phylogenetic relationships of selected species are presented. Also discussed are new phylogenies of some of the presented species (transitional forms) which are critical in their proper biostratigraphic interpretation.

Fig. 1. Simplified tectonic sketch-map of Poland (without the Cenozoic cover) _ zniewicz et al., 2011; simplified) showing _ (geological units after Pozaryski, 1974; Zela the location of the studied successions.

2. Geological settings The present study is based on the material from four sections _ snia, Jez_ o  wka) and located in southern (Wierzchowisko, Rzezu eastern (Mielnik) extra-Carpathian Poland (Fig. 1). During the Late Cretaceous, the entire extra-Carpathian Poland was a part of an _ extensive European epicontinental sea (Pozaryski, 1960;  ski, 1997, 2012), dominated by the monotonous carbonLeszczyn ate sedimentation, represented today by chalks, opokas (siliceous _ limestones), marly limestones and marls (Pozaryski, 1960; Rutkowski, 1965). _ snia and Jez_ o wka sections are located The Wierzchowisko, Rzezu  w) Trough, the southern segment of the in the Nida (¼Miecho  d w synclinorium (see Pozaryski, _ Szczecin-Ło z-Miecho 1974). The Cretaceous of the unit, with total thickness up to 800 m, spans the upper Albian through to lower Maastrichtian; the lack of the upper Maastrichtian is a result of the Laramide uplift (Voigt et al., 2008). The Cretaceous overlies disconformably the upper Jurassic and, in its central and southern parts, is partially covered by the Miocene of _ the Carpathian Foreland Basin (Pozaryski, 1977). Two major discontinuities mark the Campanian-Maastrichtian part of the Upper Cretaceous succession of the area; the lower one at the lower/upper Campanian boundary and the upper one within the lower Maastrichtian (Rutkowski, 1965; Jurkowska, 2014; Jurkowska et al., wka sec2015). The lower discontinuity is well visible in the Jez_ o tion and represents the equivalent of (portion of) the gracilis mucronata and conica/mucronata zones (see Jagt et al., 2004). The stratigraphy of the studied successions is based on macrofauna (ammonites, belemnites, inoceramids and echinoids) (Jagt et al., 2004). Accordingly, the strata exposed in Wierzchowisko represent the lower Campanian pilula, pilula/senonensis and possibly also senonensis zones (the zones as defined in northern Germany; Schulz et al., 1984; Niebuhr et al., 1997). No inoceramids were found at this site (Jagt et al., 2004). The lower part of the stratigraphically wka section (below the hardground) yielded the late younger Jez_ o early Campanian inoceramids (Jagt et al., 2004) which document the Sphaeroceramus sarumensis-Cataceramus dariensis Zone (as defined by Walaszczyk, 1997). In terms of echinoid zonation the succession represents the conica/papilosa and papilosa zones acwka section cording to the German usage. The upper part of the Jez_ o (above the hardground), represents the upper part of the Cataceramus beckumensis Zone (see Jagt et al., 2004; Jurkowska et al., _ snia sec2015). The middle portion of the succession of the Rzezu tion yielded a very rich inoceramid fauna, which documents the “Inoceramus” azerbaydjanensis e “Inoceramus” vorhlemensis Zone (sensu Walaszczyk, 1997) of the lower, but not lowermost, upper Campanian in European sense (Jagt et al., 2004), corresponding to the middle Campanian in tripartite Campanian subdivision (Walaszczyk et al., 2008). This inoceramid assemblage corresponds (Walaszczyk, 1997) to the stobaei/basiplana (¼spiniger/basiplana) and vulgaris/basiplana echnoid zones of northern Germany (Ernst, 1963; Ernst et al., 1979; Schulz et al., 1984). The section of Mielnik is located in the SE part of the MazuryPodlasie Homocline of eastern Poland (for structural details see _  Narkiewicz and Dadlez, 2008; Zela zniewicz et al., 2011). The total thickness of the Upper Cretaceous in the area is about 200 m  ski and Jaskowiak, 1973). The succession is exposed in the (Cieslin working quarry in Mielnik and comprises c. 30 m of Campanian and Maastrichtian white chalk (see also Ga zdzicka, 1981; Peryt, 1981;  Olszewska, 1990; Olszewska-Nejbert and Swierczewska-Gładysz, 2011; Jurkowska et al., 2015). The Campanian is capped by the hardground, with which the stratigraphical gap, comprising a large portion of the upper Campanian and almost entire lower Maastrichtian is associated. Below the hardground, there are two welldeveloped flint horizons. The sediment just below the

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hardground is highly bioturbated and filled with glauconitic chalk. Based on belemnite fauna, Campanian chalk of Mielnik represents the upper part of ‘boreal’ lower Campanian (undivided belemnite zones Goniotheutis gracilis þ Belemnellocamax mammillatus) and the upper Campanian, B. mucronata Zone (Olszewska, 1990;  Olszewska-Nejbert and Swierczewska-Gładysz, 2011). 3. Material and methods The succession of the Mielnik section is divided into three parts labelled I to III due to the needs of this paper. The Campanian chalk of the Mielnik section is labelled herein as Mielnik I, the sediment which fills the burrows just below the hardground is labelled as Mielnik II, whereas the Maastrichtian part of the succession, which is not studied in this work, is named as Mielnik III (Fig. 2). Fifty three sediment samples from four outcrops Wierzcho_ snia, Jez_ o wka and Mielnik I and II were studied wisko, Rzezu micropaleontologically. The samples of about 300 g weight were collected from freshly dug walls. Samples from the burrows and from encompassing sediments were collected separately. All samples were disaggregated with use of liquid nitrogen (Remin et al., 2012), cleaned in an ultrasonic bath, dried and sieved into the same fraction (63 mme700 mm). The specimens were initially studied under a standard optical binocular microscope and scanning electron microscope at the Institute of Paleobiology, Polish Academy of Sciences. The ranges of selected benthic foraminifera were studied accurately; whole residues (obtained from minimum 300 g bulk samples) were examined from selected foraminifera. The species selected for inclusion were based on their stratigraphical usefulness and most of them were described in stratigraphic context by earlier workers from the other parts of Europe. It allowed for the discussion of the species correlative potential and utility in biostratigraphy over much of Europe. A ‘common occurrences of taxa’ in samples are understood herein as an occurrence of dozens of specimens in the studied 300 g samples. A ‘rare occurrences of taxa’ are understood herein as an occurrence of a single record or a few specimens in minimum 300 g samples. The material is stored in the S.J. Thugutt Geological Museum, Faculty of Geology, University of Warsaw. 4. The benthic foraminifera record in the lower and middle Campanian of southern and eastern Poland The species discussed herein are stratigraphically useful and most of them have a good record in other parts of Europe, which enables the discussion of their correlative potential and utility in biostratigraphy of the lower and middle Campanian of Europe. The succession of the Wierzchowisko section, which comprises the pilula, pilula/senonensis and possibly also the senonensis echinoid zones (Jagt et al., 2004), yielded a few important benthic foraminifera, including Bolivinoides culverensis, Bolivinoides granulatus, Cibicidoides sp. 1 (Cibicidoides ex. gr. voltzianus), Gavelinella ex. gr. clementiana, Gavelinella costulata, Gavelinella stelligera morphotype A, Gavelinella monterelensis, Globorotalites michelinianus, and Stensioeina pommerana (Fig. 2). All of these taxa, which range through the entire Wierzchowisko succession, are also recoded wka section (below the hardground), from the basal part of the Jez_ o which corresponds to the conica/papilosa papilosa Zone (Jagt et al., wka section 2004). The samples examined from this part of the Jez_ o (sample -3, -2, -1) also contain examples of a transitional form between Bolivinoides culverensis and Bolivinoides decoratus. This form also occurs in the Mielnik section (Fig. 3), where it has a continuous record from sample 1 through sample 4. Its highest

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common occurrence in sample 4, approximately 1 m above the lower flint horizon, coincides with the lowest common occurrence of B. decoratus. In general, the Mielnik section is characterized by the series of FADs and LADs of stratigraphically important benthic foraminifera. The LAD of Bolivinoides granulatus is recorded in sample 22, however its highest consistent record is in sample 5. Worthy of note is that in sample 5 first appears Bolivinoides laevigatus, and right below, in sample 4, disappears Stensioeina gracilis. B. laevigatus sporadically occurs through the lower and middle part of the section, between sample 5 and 20, and its major abundance increase starts with sample 21. In the Mielnik section, the FAD of Cibicidoides voltzianus morphotype A is noted in sample 13, approximately 1 m below the higher flint horizon. The FAD of C. voltzianus morphotype B is recorded in sample 19 whereas the FAD of G. monterelensis is recorded in sample 17, c. 2 and 4 m above the higher flint horizon respectively. Both these events coincide with the lowereupper  Campanian boundary (Olszewska-Nejbert and SwierczewskaGładysz, 2011). The highest record of G. costulata is in sample 13, however, its rare occurrence is recorded in sample 26. Gavelinella sp. 1 occurs in the upper part of the Mielnik section between sample 21 and 26. The LAD of this taxon in sample 21 coincides with the last common occurrence of Gavelinella stelligera group, represented by the planispiral Gavelinella stelligera morphotype D. Evolutionary older forms of this group, G. stelligera morphotype A and G. stelligera morphotype C, almost disappear in sample 9 and 15 respectively; rare occurrences of G. stelligera morphotype A is recorded in samples 21, 22 and 23. Globorotalites sp. 1, a transitional form between G. michelinianus and Globorotalites emdyensis, first appears in sample 24 and ranges to the top of the Mielnik section. Globorotalites michelinianus, the ascendant of the lineage, occurs throughout the Mielnik succession. The youngest sample of the Mielnik section (sample 30) contains some taxa, not recorded in the main Campanian part of the succession (Mielnik 1) (Fig. 3). These are G. emdyensis and a transitional form between B. decoratus and Bolivinoides sidestrandensis refereed openly to herein as Bolivinoides sp. 1. wka section (above hardground), The upper part of the Jez_ o which corresponds to the Cataceramus beckumensis inoceramid Zone, is characterized by B. decoratus, B. laevigatus, Cibicidoides sp. 1, Cibicidoides voltzianus morphotype A, Cibicidoides voltzianus morphotype B, Gavelinella annae, G. ex. gr. clementiana, G. monterelensis, Gavelinella stelligera morphotype D, Gavelinella sp. 1 and G. michelinianus. The records of Gavelinella sp. 1 and Gavelinella wka section (above hardground) stelligera morphotype D in the Jez_ o  w area are the last records of these taxa within the studied Miecho succession, whereas Gavelinella monterelensis, Gavelinella stelligera morphotype D and transitional form between B. culverensis to B. decoratus occur in this section for the first time. _ snia section, represented by the “Inoceramus” azerThe Rzezu baydjanensis- “Inoceramus” vorhlemensis inoceramid zone, yielded the following stratigraphically significant benthic foraminifera: B. decoratus, B. laevigatus, Cibicidoides sp.1, Cibicidoides voltzianus morphotype A, Cibicidoides voltzianus morphotype B, Gavelinella annae, G. ex. gr. clementiana, G. monterelensis, G. michelinianus and _ snia Globorotalites sp. 1. The record of the latter taxon in the Rzezu section is its oldest record within the examined sections of the w area. Miecho 5. Discussion Stensioeina gracilis is a very common species in the late Santonian and early Campanian all over Europe (e.g. Koch, 1977; GaworBiedowa, 1992; Hart et al., 1989; Dubicka and Peryt, 2014). Its FAD is close to the middle/upper Santonian boundary (Hart et al., 1989;

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 Fig. 2. Stratigraphical ranges of selected benthic foraminifera in Mielnik succession. Biostratigraphic zonation after Olszewska-Nejbert and Swierczewska-Gładysz, 2011.

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 w Trough. Biostratigraphic zonation after Jagt et al., 2004 and Jurkowska et al., Fig. 3. Stratigraphical ranges of selected benthic foraminifera within studied successions of Miecho 2015; modified.

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Koch, 1977; Niebuhr et al., 1997; Dubicka and Peryt, 2014), defined at the base of the Uintacrinus socialis Zone. In the studied area wka (below S. gracilis is noted in the Wierzchowisko and Jez_ o hardground) sections, and its LAD is noted in sample 12 of the Mielnik section, slightly below the lower/upper Campanian belemnite boundary (Olszewska, 1990; Olszewska-Nejbert and  Swierczewska-Gładysz, 2011). In NW Germany and southern England the species ranges slightly higher, up to the lower boundary of the B. mucronata Zone (Hiltermann and Koch, 1962; Koch, 1977; Hart et al., 1989), i.e., to the base of the upper Campanian in a European sense (Ernst, 1963; Schulz et al., 1984). Accordingly, the LAD of S. gracilis is potentially a good proxy of the ‘boreal’ lowereupper Campanian boundary in Europe. The genus Bolivinoides is an important biostratigraphical marker in Europe and, in some cases, in worldwide correlations of the Santonian through to Maastrichtian (Hiltermann and Koch, 1950, € nfeld, 1990; Petters, 1977; 1962; Barr, 1966; Koch, 1977; Scho Hampton et al., 2007; El-Nady, 2006; Dubicka and Peryt, in press). Several bolivinacean species (Fig. 4), with high stratigraphical potential, are recognized: Bolivinoides granulatus, B. culverensis, transitional form between B. culverensis and B. decoratus, B. decoratus, B. laevigats and an early form of B. sidestrandensis labelled herein as Bolivinoides sp. 1. B. granulatus occurs abundantly (several dozen of specimens in examined samples) in Wierzchowisko and in the lower part of the wka section. According to Jagt et al. (2004) this interval repJez_ o resents the middle and upper parts of the lower Campanian (in the European two-fold subdivision) corresponding to the pilula, pilula/ senonensis, senonensis, conica/papilosa and papilosa echinoid zones, as commonly recognized in northern Germany (see Ernst, 1963; Schulz et al., 1984; Niebuhr et al., 1997). In northern Germany, € rf section, B. granulatus first appears in the including the Lagerdo €nfeld, 1990), and at similar level it senonensis Zone (Koch, 1977; Scho appears also in England (see Hart et al., 1989; FAD in the middle Gonioteuthis quadrata Zone, i.e., above the O. pilula Zone). Consequently, B. granulatus could have either appeared slightly earlier in Poland than in western Europe, or the succession of the Wierzchowisko section does not range stratigraphically down to the

pilula and pilula/senonensis zones. The latter view seems to be supported by another foraminiferal species, Cibicidoides ex. gr. voltziana (Cibicidoides sp. 1), which ranges through the entire Wierzchowisko succession, and the FAD of which is in the Gonioteuthis quadrata Zone (above the Offaster pilula Zone) as documented in southern England (Bailey et al., 1983). In the studied area, the LAD of B. granulatus is recorded in the lowermost upper Campanian of the Mielnik section (Olszewska Nejbert and Swierczewska-Gładysz, 2011), where it occurs much rarer than in stratigraphically older intervals. The position of the event in Poland is very close to that, which was recorded at €gerdorf (see Scho €nfeld, 1990), namely in the middle part of the La conica/senior Zone. The next important foraminiferal bioevent observed in the studied successions, is the FAD of B. laevigatus. The event is recorded in the Mielnik section in sample 5, which is placed in the upper lower Campanian. This foraminiferal event was noticed stratgraphically slightly higher in the nortwestern Germany, including €gerdorf, since the taxon appears in the lower part of the conica/ La € nfeld, senior Zone (Hiltermann and Koch, 1962; Koch, 1977; Scho 1990). However, the common occurrence of the species in Poland is also present in the lowermost upper Campanian in B. mucronata  Zone (Olszewska-Nejbert and Swierczewska-Gładysz, 2011). In the English Cretaceous, the stratigraphic range of B. laevigatus is more comparable to its range recorded in the studied area. Namely, Hart et al. (1989) recognized the first appearance of B. laevigatus in the topmost lower Campanian (uppermost part of G. quadrata Zone), however in the G. quadrata Zone the species is very rare and intermittent. The persistent and common occurrence of B. laevigatus begins directly above the base of Belemnella mucronata Zone (Hart et al., 1989), thus same as at Mielnik. B. decoratus is another very common Campanian bolivinacean species (Hart et al., 1989). In the studied areas it is common shortly above the lower flint bed in Mielnik, thus slightly below the “boreal” lower/upper Campanian boundary. Similarly, in the Cretaceous of southern England (Bailey et al., 1983; Hart et al., 1989) its common occurrence is placed in the uppermost G. quadrata Zone. The event is marked stratigraphically much lower in western

Fig. 4. Ranges of stratigraphically important benthic foraminifera of the sections studied in relation to macrofossil zonations. A - substage subdivision according to standard definition (three-fold subdivision); B- substage subdivision according to 'boreal' definition; C- inocermid zonation after Walaszczyk, 2004 and Jagt et al., 2004; D e echinoid/ belemnite zonation after Jagt et al., 2004, modified; E  ammonite division after Błaszkiewicz, 1980; F- geological columns and preliminary correlations of sections studied in w area with Mielnik succession; Jez_ o  wka (*) e the Jez_ o  wka section below hardground, Jez_ o  wka (^) e the Jez_ o  wka section abowe hardground; G - stratigraphical ranges of Miecho rna (Middle Vistula River section, central Poland) are selected foraminiferal species in Polish Lowlands, foraminiferal distribution in Dorotka, Kolonia Ciszyca and Ciszyca Go published in Peryt and Dubicka, in press.

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€ nfeld, 1990), namely, close Germany (Seitz, 1952; Koch, 1977; Scho to the lower part of the senonensis Zone. This difference is probably related to the fact that the German authors did not distinguish B. culverensis within the B. strigillatus-B. decoratus lineage. The major evolutionary changes recorded in the lineage include increase in test size, gradual broadening of test and increase in a number of ornamental lobes (Edgell, 1954; Barr, 1966; Hiltermann, 1963; Petters, 1977; Dubicka and Peryt, in press) (Fig. 5). Accordingly, these forms which are labelled herein as transitional between B. culverensis and B. decoratus, are probably regarded in the latest studies as B. decoratus. The last common occurrence of these transitional forms appears in Mielnik, at nearly the same position as the FO of B. decoratus. They are characterized by four lobes and a relatively narrow test and being smaller size than true B. decoratus (Fig. 6). Bolivinoides miliaris, a descendant of B. decoratus, from which differs in having tubercled ornamentation of the initial part of the test, has not been recorded in the studied successions. This taxon is a very distinctive and stratigraphically useful bolivinacean species in the European Cretaceous and its FAD defines the base of the Bolivinoides miliaris Interval Zone (Hiltermann and Koch, 1950; Hart et al., 1989). In the Polish Lowlands the taxon appears in the Cataceramus subcompressus inoceramid Zone and in the Bostrychoceras polyplocum ammonite Zone (Peryt and Dubicka, in press), similarly _ as in northwestern and the rest of central Europe (Pozaryska, 1954; €nfeld, 1990). AddiBarr, 1966; Koch, 1977; Hart et al., 1989; Scho tionally, the first record of B. miliaris was recognized in the uppermost Campanian in Asia Minor (Reiss, 1954), British Isles (Barr, 1966), Atlantic Coastal Plain (Petters, 1977), Trinidad (South America) and even Australia (Edgell, 1954). The next important foraminiferal bioevent is the FAD of Cibicidoides voltzianus, the species commonly used for stratigraphy in western Europe. The event defines the base of the voltziana Partial € nfeld, 1990), established in the La €gerdorf Range Zone (sensu Scho section, spanning the upper part of the gracilis/senior Zone and the lowermost conica/senior Zone. The FAD of Cibicidoides voltzianus was described from around the boundary between Gonioteuthis

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quadrata and Belemnitella mucronata zones (at the ‘boreal’ lower/ upper Campanian boundary) of the Anglo-Paris Basin (Bailey et al., 1983; Hart et al., 1989), i.e., slightly higher than those in western Germany. This difference is probably related to different taxonomic determination of distinctive morphotypes of C. voltzianus. In the studied succession there are two clearly distinguishable morphotypes of the species: C. voltzianus morphotype A and C. voltzianus morphotype B. These two morphotypes also differ in stratigraphical ranges. C. voltzianus morphotype A, which possesses a rounded periphery situated on the equatorial position (Fig. 7), appears in sample 13 of the Mielnik section, whereas C. voltzianus morphotype B, which has a sub-acute periphery in a more spiral position, appears in sample 19. C. voltzianus was described and illustrated by Hart et al. (1989), who marked its FAD in England at the base of the upper Campanian, parallel to C. voltzianus morphotype B which appears in Poland also at the base of the B. mucronata Zone  (Olszewska-Nejbert and Swierczewska-Gładysz, 2011). Additionally the event co-occurs close to the level of the appearance of G. monterelensis in both discussed regions. Therefore, the FAD of C. voltzianus morphotype B seem to be a good proxy of the lower/ upper Campanian boundary. The older and more primitive form of C. ex. gr. voltzianus appears much lower in the succession, namely at Wierzchowisko which could represent the pilula, pilula/senonensis and senonensis zones (Jagt et al., 2004). They are characterized by a slightly convex ventral side, a bluntly rounded periphery and lack of bosses on both test sides (evolutionary older forms) or possess a small boss on the spiral test side only, and are named herein as Cibicidoides sp. 1. According to Bailey et al. (1983), the FAD of Cibicidoides ex. gr. voltzianus in England is placed in the Gonioteuthis quadrata Zone, within the range of Galeola. Therefore, the Wierzchowisko section may represent a slightly lower position i.e. the senonensis Zone, a proposal supported by the co-occurrence of € nfeld, 1990). Moreover, more recent studies B. granulatus (see Scho of echinoids (Smith and Wright, 2003; Jagt et al., 2004), suggest that Galeola senonensis, which is a an index of the pilula/senonensis and senonensis zones in the German scheme (Ernst, 1963; Ernst et al., 1979; Schulz et al., 1984) is synonymized with O. pilula, and

Fig. 5. Evolutionary interpretation of selected lineages of the genera Bolivinoides, Cibicidoides, Gavelinella and Globorotalites. Biostratigraphic zonation after Jagt et al., 2004 and Walaszczyk, 2004.

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can slightly dismiss the role of echinoids as precise stratigraphical index fossils in this interval. Gavelinella stelligera is another taxon with stratigraphical potential in the Cretaceous successions (Hart et al., 1989). Its FAD seems to be a useful marker for the middle-upper Santonian boundary in Europe (Edwards, 1981; Hart et al., 1989; Dubicka and Peryt, 2014). In the Cretaceous of extra-Carpathian Poland, representatives of G. stelligera group occur commonly in the upper Santonian and lower Campanian. The last abundant occurrence of typical morphotypes of the species (G. stelligera morphotype A) is recorded at Mielnik in sample 9; a few single specimens were found _ snia. Within the in samples 21 and 23 of this section and in Rzezu lower part of the succession, trochospiral G. stelligera morphotype

A gradually transforms into planispiral morphotype D (Dubicka et al., 2015). In the middle part of the section, the assemblages of G. stelligera group are dominated by G. stelligera morphotype C (transitional between morphotype A and D), which finally disappears in the uppermost lower Campanian. Higher in the succession, in the substage boundary interval as well as in the basal upper  Campanian (Olszewska-Nejbert and Swierczewska-Gładysz, 2011), the G. stelligera group is dominated by planispiral morphotype D. The occurrence of Gavelinella stelligera morphotype D accompanied by the lack of Gavelinella stelligera morphotype A is also noted in the wka section (above hardground). Gavelinella monterelensis and Jez_ o C. voltzianus, which seem to be useful markers deciphering the upper Campanian, are also recorded in the section. According to

Fig. 6. Selection of stratigraphically significant benthic foraminifera from the studied interval. Aa-Ac, Gavelinella stelligera (Marie) morphotype A, Mielnik, sample 5, MWGUW ZI/ 67/16.45.Ba-Bb, Gavelinella stelligera (Marie) morphotype A, Mielnik, sample 3, MWGUW ZI/67/08.30. Ca-Cc, Gavelinella stelligera (Marie) morphotype D, Mielnik, sample 12, _ MWGUW ZI/67/13.14.Da-Db, Gavelinella stelligera (Marie) morphotype D, Mielnik, sample 7, MWGUW ZI/67/07.23. E, Gavelinella annae (Pozaryska), Mielnik, sample 28, MWGUW ZI/ _ 67/12.45. F, Bolivinoides culverensis Barr transitional to B. decoratus (Jones), Mielnik, sample 2, MWGUW ZI/67/12.23. Ga-Gc, Gavelinella annae (Pozaryska), Mielnik, sample 28, MWGUW ZI/67/11.13. H, transitional form between Bolivinoides decoratus and Bolivinoides sidestrandensis Barr, Mielnik, sample 28, MWGUW ZI/67/12.53.

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wka seems to correspond to the interval exposed at these data, Jez_ o Mielnik a few metres above the upper flint horizon, which based on the belemnite fauna represents the lowermost “boreal” upper Campanian. This agrees with Jagt et al. (2004), who recognized the wka. This correlation can also be conica/mucronata Zone in Jez_ o supported by a record of Gavelinella sp. 1 (newly described herein) in the lower upper Campanian of the Mielnik section as well as in wka. This taxon evolved probably from G. costulata, since they Jez_ o possess the umbilical area typical for the G. ammonoidesG. lorneiana-G. costulata lineage (Dubicka and Peryt, 2014), however differ from other representatives of the group by having a much lower test and acute periphery (Fig. 8). Hart et al. (1989) marked the discontinuous and doubtful range of G. stelligera up to the lower/upper Campanian boundary in European sense, thus

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approximately in near stratigraphic position, which was recorded in the studied area. Higher in the succession, i.e. in the lower part of the upper Campanian, G. stelligera group occurs very rarely and intermittently, and completely disappears in the middle part of B. mucronata Zone. Accordingly, the range of the G. stelligera group in southern England by Hart et al. (1989) is roughly similar to its range in Poland. The stratigraphically useful, distinctive, and common taxon in the European Campanian is Gavelinella monterelensis. The G. monterelensis Range Zone is commonly used in England (Bailey et al., 1983; Hart et al., 1989). The base of the zone corresponds nearly to the lower boundary of the B. mucronata Zone, regarded as the lower/upper Campanian “boreal” boundary, and to the common appearance of true C. voltzianus (Bailey et al., 1983). The zone of

Fig. 7. Selection of stratigraphically significant benthic foraminifera from the studied interval. Aa-Ac, Cibicidoides voltzianus (d'Orbigny) morphotype B, Mielnik, sample 19, MWGUW ZI/67/13.27. Ba-Bb, Cibicidoides voltzianus (d'Orbigny) morphotype A, Mielnik, sample 15, MWGUW ZI/67/05.08. Ca-Cc, Cibicidoides voltzianus (d'Orbigny) morphotype B,  wka, sample 1, MWGUW ZI/67/05.18. Da-Dc, Cibicidoides voltzianus (d'Orbigny) morphotype A, Mielnik, sample 13, MWGUW ZI/67/05.24. Ea-Eb, Cibicidoides sp., Wierzchowisko, Jez_ o sample8, MWGUW ZI/67/05.12. Fa-Fc, Cibicidoides sp., Mielnik, sample 10, MWGUW ZI/67/5.10. Scale bars e 200 mm.

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G. monterelensis is also distinguished on the East European Platform (Olfer'ev et al., 2007). In the studied area, G. monterelensis first appears in sample 19 of the Mielnik section, approximately at the level of common appearance of C. voltzianus morphotype B; at the same position it was described from southern England (Bailey et al., 1983). Accordingly, the foraminiferal lower/upper Campanian “boreal” boundary seems to occur in the Mielnik section about 3 m above the upper flint horizon. This agrees with the belemnite data, on which the substage boundary was also placed about a few (3e4) metres above the flint horizon. Accordingly, the FO of C. voltzianus morphotype B, and the FO of G. monterelensis seem to be a good proxies for the European lower/upper “boreal” boundary all over Europe.

In sample 24 of the Mielnik section, there is the last common occurrence of Gavelinella costulata belonging to the Gavelinella lorneiana (d'Orbigny) group (Dubicka and Peryt, 2014). This event was first described from the North Norfolk coast (East England) by Hart et al., 1989, where it is placed in the lower part of Belemnella mucronata Zone; the same as it is recorded in Poland. Moreover, in England, the event is placed slightly above the first occurrence of G. monterelensis thus in the same foraminiferal succession as it is recorded in Mielnik. Another foraminiferal event is the FAD of Gavelinella annae, which evolved from G. ex. gr. clementiana and from which it can be distinguished by the disappearance of spiral side ornamentation (rows and tubercles). Since the taxon is not distinguished in

Fig. 8. Selection of stratigraphically significant benthic foraminifera from the studied interval. Aa-Ac, Gavelinella clementiana (d'Orbigny), Mielnik, sample 7, MWGUW ZI/67/13.6. BBolivinoides laevigatus Marie, Mielnik, sample 23, MWGUW ZI/67/17.11. Ca-Cc, Gavelinella costulata (Marie), Mielnik, sample 2, MWGUW ZI/67/13.4. D- Bolivinoides laevigatus Marie, Mielnik, sample 26, MWGUW ZI/67/5.21. Ea-Ec, Gavelinella sp., Mielnik, sample 12, MWGUW ZI/67/13.16. F, Bolivinoides decoratus (Jones), Mielnik, sample 15, MWGUW ZI/67/5.35. Ga-c Stensioeina gracilis Brotzen, 1945, Wierzchowisko, sample 10, MWGUW ZI/67/13.1. H Bolivinoides decoratus (Jones), Mielnik, sample 17, MWGUW ZI/67/5.17. Scale bars e 200 mm.

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western Europe, further studies are needed to estimate its correlative potential. In Polish Lowlands its LAD is recorded in the Cataceramus subcompressus inoceramid Zone of Dorotka, in the Middle Vistula River section (Peryt and Dubicka, in press). Globorotalites michelinianus is a very common species within the whole European lower and middle Campanian. In the upper Campanian it evolves into G. emdyensis (Vasilenko, 1961; Goel, 1965). The latter species is a senior synonym of Globorotalites hiltermanni Kaever, 1961, and its FAD seems to be a very important correlative €nfeld, 1990; Hart and Swiecicki, marker (Hart et al., 1989; Scho 2003; Peryt and Dubicka, in press). In the Mielnik section, G. emdyensis occurs only in the burrow fills just below the

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hardground (Mielnik II). Based on foraminiferal data (see Peryt and Dubicka, in press), these sediments represent probably the upper part of the Bostrychoceras polycplocum ammonite Zone and the Cataceramus subcompressus inoceramid zone. The transitional form _ snia between G. michelinianus and G. emdyensis is recorded in Rzezu and in the uppermost part of the Mielnik I section. The major evolutionary changes involved in the transition from G. michelinianus to G. emdyensis include a formation of more tight spiral test and an appearance of convexity of spiral side (Fig. 9). These transitional forms are labelled herein as Globorotalites sp. 1. It differs from G. michelinianus in possessing a more convex spiral side and less convex umbilical side, and from G. emdyensis in having a

Fig. 9. Selection of stratigraphically significant benthic foraminifera from the studied interval. Aa-Ac, Gavelinella monterelensis (Marie), Mielnik, sample 21, MWGUW ZI/67/13.09. Ba-Bb, Gavelinella monterelensis (Marie), Mielnik, sample 26, MWGUW ZI/67/07.01. Ca-Cc, Globorotalites emdyensis Vasilenko, Mielnik, sample 28, MWGUW ZI/67/13.13. Da-Dc, Globorotalites michelinianus (d'Orbigny), Mielnik, sample 12, MWGUW ZI/67/13.21. E, Bolivinoides granulatus Hofker, Wierzchowisko, sample 16, MWGUW ZI/67/12.32. Fa-Fc, transitional form between Globorotalites michelinianus (d'Orbigny) and Globorotalites emdyensis Vasilenko, Mielnik, sample 28, MWGUW ZI/67/13.12. G, Bolivinoides granulatus Hofker, Wierzchowisko, sample 10, MWGUW ZI/67/12.02. Scale bars e 200 mm.

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less tight spiral test and thus still open umbilicus. The taxon seems to be good marker of the lower part of the middle Campanian in its tripartite subdivision. 6. Conclusions The stratigraphic ranges of selected benthic foraminiferal species within the lower and middle Campanian successions of wka, Rzezu _ snia sections) and southern (Wierzchowisko, Jez_ o eastern Poland (Mielnik section) were investigated. A series of conspicuous and stratigraphically important foraminiferal bioevents were recognized. Some of them, including LAD of Stensioeina gracilis, FAD of Bolivinoides decoratus, FAD of Cibicidoides voltzianus morphotype B, LAD of Gavelinella costulata (G. ex gr. lorneiana), were previously noted from equivalent levels of southern England (e.g. Bailey et al., 1983; Hart et al., 1989) and/or € nfeld, 1990), and can serve western Germany (e.g. Koch, 1977; Scho as important bio-markers for stratigraphic correlation across Europe. Also recognized are few less conspicuous and less evident foraminiferal bioevents, however, their record in the studied area provides an important link with the north-western European sections. Among them are: the LAD of Bolivinoides granulatus, the consistently common occurrence of B. laevigatus and the last common and consistent occurrence of G. stelligera morphotype A. The FAD of Gavelinella monterelensis and FAD of Cibicidoides voltzianus morphotype B (possessing plano-convex test with a subacute periphery in more spiral position) are placed close to the lower/upper Campanian belemnite boundary and seem to be good proxies of this substage boundary. The LAD of Stensioeina gracilis and LAD of Bolivinoides decoratus, the events postulated earlier as foraminiferal proxies for this boundary (Koch, 1977; Bailey et al., 1983; Hart et al., 1989), are slightly older. Gavelinella stelligera morphotype D (planispiral morphotype) seems to be a good marker of the gracilis/mucronata and conica/ mucronata zones. The transitional form between the Globorotalites michelinianus and G. emdyensis lineages, referred herein to as Globorotalites sp. 1., seems to be a good marker of the lower middle Campanian in its tripartite subdivision. The major evolutionary changes involved in this evolutionary transition include the formation of a more tight spiral test and the appearance of convexity of the spiral side. Acknowledgements This work was funded by a grant number UMO-2013/09/D/ST10/ 04059 from the National Science Centre (NCN). I warmly thank Danuta Peryt (Polish Academy of Sciences) and Irek Walaszczyk (University of Warsaw) for their valuable comments and suggestions which helped improve and clarify this manuscript. References Alvarez, W., Arthur, M.A., Fischer, A.G., Lowrie, W., Napoleone, G., Premoli Silva, I., Roggenthen, M.W., 1977. Upper Cretaceous-Palaeocene magnetic stratigraphy at Gubbio, Italy- V. Type section for the late Cretaceous-Palaeocene geomagnetic reversal time scale. Geological Soc. Am. Bull. 88, 383e389. Bailey, H.W., Gale, A.S., Mortimore, R.N., Swiecicki, A., Wood, C.J., 1983. The Coniacian e Maastrichtian stages of the United Kingdom, with particular reference to southern England. Newsletters Stratigr. 12, 19e42. Barr, F.T., 1966. The foraminiferal genus Bolivinoides from the upper cretaceous of the British Isles. Palaeontology 9, 34e38. Błaszkiewicz, A., 1980. Campanian and Maastrichtian ammonites of the Middle Vistula River Valley, Poland: a stratigraphic-paleontological study. Pr. Inst. Geol. 92, 1e63.  ski, S., Jaskowiak, M., 1973. Niecka brzezna. _  rna. In: Słowian  ska, B., Cieslin Kreda go Bartys-Pelc, M. (Eds.), Budowa Geologiczna Polski. Stratygrafia, tom.1, cze˛ s c 2, Mezozoik. Wydawnictwa Geologiczne, Warszawa, pp. 603e609.

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Appendix. Alphabetical list of taxa cited and taxonomic notes A full descriptions of most of the foraminiferid taxa discussed herein are published elsewhere. They are indicated by specific symbols respectively: Dubicka and Peryt (in press) e indicated by (*), Peryt and Dubicka (in press) e (#), Dubicka and _ Peryt, 2014 e (**), Dubicka et al., 2015 e (^), Hart et al., 1989 e (##), Pozaryska, 1954 e (!). A description of new distinguished taxa are presented below (see Taxonomic notes). Bolivinoides culverensis Barr, 1967* Bolivinoides decoratus (Jones, 1875)* Bolivinoides granulatus Hofker, 1952* Bolivinoides laevigatus Marie, 1941* Bolivinoides miliaris Hiltermann and Koch, 1950* Bolivinoides sidestrandensis Barr, 1966*, ^ Cibicidoides sp. 1. Cibicidoides voltzianus (d'Orbigny, 1840) morphotype A. Cibicidoides voltzianus (d'Orbigny, 1840) morphotype B ## _ Gavelinella annae (Pozaryska, 1954)! Gavelinella clementiana (d'Orbigny, 1840)# Gavelinella costulata (Marie, 1941)** Gavelinella monterelensis (Marie, 1941)# Gavelinella stelligera (Marie, 1941) morphotype A**, ^ Gavelinella stelligera (Marie, 1941) morphotype C, ^ Gavelinella stelligera (Marie, 1941) morphotype D, ^ Gavelinella sp. 1. Globorotalites emdyensis Vasilenko, 1961# Globorotalites michelinianus (d'Orbigny, 1840)# Globorotalites sp.1. Stensioeina gracilis Brotzen, 1945** Taxonomic notes. Cibicidoides sp. 1 (Fig. 7: Da-Dc, Ea-Eb) Description and remarks: Test low trochospiral, involute, with flat umbilical side and slightly convex ventral side, central part of ventral side is also flat, bluntly rounded periphery. There are lack of bosses on both test sides (evolutionary older forms) or small boss occur on the only spiral test side. Cibicidoides sp.1. differs from Cibicidoides voltzianu in possessing flat central part of ventral side and lack of boss in the central part of dorsal part of the test. Occurrence: Cibicidoides sp.1. was recorded in from the Sphaeroceramus sarumensi-Cataceramus dariensis Zone up to “Inoceramus” tenuilineatus Zone. _ Gavelinella annae (Pozaryska, 1954) (Fig. 6: E, Ga-Gc) Description and remarks: Test low trochospiral, large, plano-convex with convex umbilical side and flattened spiral side, with a flush margin outline and a broad and bluntly rounded periphery. Test surface smooth with coarse pores on the umbilical side. G. annae differs from the other representatives of the G. clementiana lineage by lacking or possessing very poorly visible spiral-side ribs and tubercles. Occurrence: G. annae was recorded from Cataceramus beckumensis Zone up to Cataceramus subcompressus Zone. Gavelinella sp. 1. (Fig. 8: Ea-Ec) Description and remarks: Test very low trochospiral, compressed, symmetrically biconvex. A sharply angular periphery, which constitute the “keel-like structure; umbilicus open. Sutures on the umbilical and spiral side are curved and depressed. Prominent septa-ridges elements on the umbilical side project into the relatively large and open umbilicus. Gavelinella sp.1 differs from the G. costulata by having a much thinner test and acute periphery and from G. stelligera in possessing possess elevated septa-ridges elements on the umbilical area.  wka section Occurrence: Gavelinella sp. 1 was recorded in the upper part of Jez_ o (Cataceramus beckumensis Zone) and in the Belemnitella mucronata Zone of the Mielnik succession. Globorotalites sp. 1. (Fig. 9: Fa-Fc) Description and remarks: Test trochospiral, slightly convex spiral side and much more convex umbilical side; umbilicus narrow, deep and open; 7 to 9 chambers enlarging gradually in the last whorl; sutures oblique, limbate and elevated on the spiral side; radial, curved and slightly depressed on the umbilical side; surface smooth. Globorotalites sp. 1 differs from G. michelinianus in possessing a more convex spiral side and less convex umbilical side and from G. emdyensis in having a less tight spiral test and thus still open umbilicus. Occurrence: Globorotalites sp. 1 was recorded in “Inoceramus” azerbaydjanensis e “Inoceramu” vorhlemensis and Cataceramus subcompressus zones.