GEOLOGIJA 50/2, 293–322, Ljubljana 2007
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko (Eastern Slovenia)
Najpogostejše srednjemiocenske rotaliine (podred Rotaliina, Foraminifera) Kozjanskega (vzhodna Slovenija)
Katarina OBLAK
Naravoslovnotehni{ka fakulteta, Univerza v Ljubljani, Oddelek za geologijo, Privoz 11, SI - 1000 Ljubljana, Slovenija, katarina.oblak@ntf.uni-lj.si
nija
Key words: Benthic foraminifera, Rotaliina, Middle Miocene, Kozjansko, Slovenia Klju~ne besede: bento{ke foraminifere, Rotaliina, srednji miocen, Kozjansko, Slove-
Abstract
This research presents the most numerous Middle Miocene foraminifera of the suborder Rotaliina from the Planina syncline in Kozjansko. 85 species and 2 subspecies have been identified. The species that show abundance in samples are: Angulogerina angulo-sa, Trifarina bradyi, Sphaeroidina bulloides, Cibicidoides ungerianus, Nonion commune, Melonis pompilioides, Pullenia bulloides, Heterolepa dutemplei, Hansenisca soldanii and Hanzawaia boueana.
Izvle~ek
V nalogi so predstavljene najpogostej{e srednjemiocenske foraminifere podreda Rotaliina iz Planinske sinklinale na Kozjanskem. Izmed 85 dolo~enih rotaliinskih vrst in 2 podvrst so po {tevilu vzorcev, v katerih se pojavljajo, in po deležu hi{ic znotraj ve~ine teh vzorcev naj{tevil~nej{e naslednje vrste: Angulogerina angulosa, Trifarina bradyi, Sphae-roidina bulloides, Cibicidoides ungerianus, Nonion commune, Melonis pompilioides, Pul-lenia bulloides, Heterolepa dutemplei, Hansenisca soldanii in Hanzawaia boueana.
Introduction
The foraminiferal suborder Rotaliina was established in 1896 by Delage & Herou-ard as the suborder Rotalidae (renamed in Rotaliina in 1961 by Loeblich and Tappan) (Loeblich & Tappan, 1987). It represents the second largest foraminiferal suborder, comprising 628 genera according to Loeblich & Tappan (1987). The suborder includes bent-hic foraminifera with multilocular tests that have a perforated hyaline calcite wall of a lamellar structure. Other test characteristics show great variety; test is typically spiral or may be reduced to triserial, bise-rial and uniserial growth. Chambers can be simple or subdivided by septulae. The surfa-
ce can be smooth, costate, striate, cancellate or papillate. The aperture can be simple or contain internal toothplate or other structures (Loeblich & Tappan, 1987). A simple to very complex internal canal system may be developed (Billman et al., 1980).
Rotaliinas show a wide tolerance to environment parameters: substrates, water depth, temperature, salinity and availability of food. They also show great variety in their mode of life, being either infaunal, semi-infaunal or epifaunal. In the case of an epifaunal mode they are either sessile attaching to hard substrates or completely mobile on the substrates surface. The strength of the wave action being important, in high-energy environments there is a preference
294
Katarina Oblak
for attachment to hard substrates. Their depth habitat has been shown to range from the shelf (< 180 m) to the abyssal plane (> 4000 m). They are found in water with temperatures ranging from cold to warm. They are euryhaline with specimens being found in brackish (< 32‰), marine (32-37‰) or hypersaline (> 37‰). They exhibit a range of trophic mechanisms: passive suspension feeding, herbivore, detritivore and rarely parasitic (Murray, 1991), in shallow nutrient poor waters symbiosis with diatoms has also been identified (Billman et al., 1980; Murray, 1991).
Foraminifera of the suborder Rotaliina have existed from the Triassic (Loeblich & Tappan, 1987). Due to the great diversity, fossil and recent species are recognized globally.
In this research, rotaliinas were studied from six sections; Imenska Gorca, Plohov breg, Javor{ica, Sveta Ana, Trobni Dol and Drensko Rebro (Fig. 1). The investigated area is located mostly on the northern flank of the Planina syncline, only the Drensko Rebro section lies on its southern flank (Buser, 1977, 1979; Ani~i} & Juri{a, 1984, 1985; Ani~i} & Ogorelec, 1994/95, 1996; Ani~i} et al.; 2002, 2004). Results show that rotaliinas have great diversity and abundance in the Planina sync-line. Previous researches have shown that rotaliinas are numerous also in other Slovenian Middle Miocene sedimentary sequences. Although they represent a significant
proportion of foraminiferal assemblages, they have not been described and mostly not imaged in the Slovenian literature previously.
Methods
Six sections within the Planina syncline were selected for the micropalaeontological research: Imenska Gorca, Plohov breg, Ja-vor{ica, Sveta Ana, Trobni Dol and Drensko Rebro (Fig. 1). One hundred and fifty nine samples, consisting of marly calcarenite and marl, were taken. The samples range from the Early Lower Badenian to Early Sarmatian. According to Oblak (2006), the following foraminiferal biozones are involved in this stratigraphic range: the Lower Badenian Lower Lagenidae and Upper La-genidae Zones, the Middle Badenian Pseu-dotriplasia robusta Zone and Uvigerina cf. pygmea Zone, the Upper Badenian Bolivina dilatata Zone and Virgulinella pertusa Zone and the Sarmatian Anomalinoides divi-dens Zone and Elphidium hauerinum Zone (Tab. 1). The younger Sarmatian Elphidi-um hauerinum Zone lacks rotaliinas. One hundred and sixteen benthic species were described and classified according to Loe-blich & Tappan foraminiferal classification (1987). Electron images of spiral, umbilical and side views were taken using the Jeol T330A scanning electron microscope at the Ivan Rakovec Institute of Palaeontology, ZRC SAZU.
Figure 1. Location map of studied sections in the Planina syncline
(modified after Geological Map of Kozjansko (Slovenia), 1:50 000,
Anici} et al., 2004): Td (Trobni Dol), Sa (Sveta Ana), J (Javor{ica),
Pb (Plohov breg), Ig (Imenska Gorca) and Dr (Drensko Rebro).
Slika 1. Položaj obravnavanih profilov v Planinski sinkinali
(prirejeno po Geolo{ki karti Kozjanskega (Slovenija), 1:50 000,
Anici} et al., 2004): Td (Trobni Dol), Sa (Sveta Ana), J (Javor{ica),
Pb (Plohov breg), Ig (Imenska Gorca) and Dr (Drensko Rebro).
LaSko
.Šentrupert
^   '   n. n   i 'n   n
3 km
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              295
Age (Ma)
5,33
10
15
213
23,03
25
3D
Epoch
CD
<D O
O
(D
C <D
o o
0)
C 0)
o o
O)
Standard Stages
GELASIAN
PIACENZ1AN
ZANCLEAN
MESSIN1AN
TORTONIAN
SERRAVALLIAN
LANGHIAN
BURDIGALIAN
AQU I TAN I AN
CHATTIAN
RUPELIAN
Central Paratethys Stages
ROMANIAN
DACIAN
PONT IAN
PANNONIAN
SAR M ATI AN
BADENIAN
KARPATIAN
OTTNANGIAN
EGGENBURGIAN
EGERIAN
KISCELLIAN
Tabla 1. Correlation time scale
(modified after Loubens et al., 2004
and Piller et al., 2004). Foraminiferal
biozones are not chronologically equal.
Tabela 1. Korelacijska ~asovna skala
(prirejeno po Loubens et al., 2004 in Piller et al., 2004). Foraminiferne biocone niso v ~asovnem sorazmerju.
Foraminiferal Biozones (OBLAK, 2006)
/	Si E rt	d) o _i	Anomalinoides dividens
	z < z UJ D <	0) Q. O.	Virgulinetla pertusa
			Bolivina d tla tat a
		-a •a	Uvigerina cf. pygmea
			Pseudotriplasia robusta
1 L \ \ \ 1		O _l	Upper Lagenidae Zone
			Lower Lagenidae Zone
Results
Rotaliinas of the investigated area
From 159 Middle Miocene samples taken from all sections, eighty five species and two subspecies of the foraminiferal suborder Rotaliina have been determined:
Bolivina antiqua d’Orbigny, Bolivina crenulata Cushman Bolivina dilatata dilatata Reuss Bolivina dilatata maxima Cicha & Zapleta-lová
Bolivina hebes Macfadyen
Bolivina pokornyi Cicha & Zapletalová
Bolivina viennensis Marks
296
Lapugyina schmidi Popescu Loxostomoides zsigmondyi (Hantken) Cassidulina laevigata d’Orbigny Globocassidulina oblonga (Reuss) Globocassidulina subglobosa (Brady) Ehrenbergina serrata Reuss Hopkinsina bononiensis (Fornasini) Bitubulogenerina reticulata Cushman Bulimina buchiana d’Orbigny Globobulimina pupoides (d’Orbigny) Globobulimina pyrula (d’Orbigny) Pappina neudorfensis (Toula) Uvigerina aculeata d’Orbigny Uvigerina acuminata Hosius Uvigerina bellicostata Luczkowska Uvigerina brunnensis Karrer Uvigerina macrocarinata Papp & Turnovsky Uvigerina cf. pygmea d’Orbigny Uvigerina pygmoides Papp & Turnovsky Uvigerina semiornata d’Orbigny Uvigerina venusta Franzenau Angulogerina angulosa (Williamson) Trifarina bradyi Cushman Reussella spinulosa (Reuss) Coryphostoma digitalis (d’Orbigny) Fursenkoina acuta (d’Orbigny) Sigmavirgulina tortuosa (Brady) Virgulinella pertusa (Reuss) Caucasina elongata (d’Orbigny) Caucasina gutsulica (Livental) Caucasina subulata (Cushman & Parker) Nodosarella rotundata (d’Orbigny) Pleurostomella alternans Schwager Myllostomella recta (Palmer & Bermúdez) Neugeborina longiscata (d’Orbigny) Orthomorphina dina (Venglinski) Orthomorphina pupoides (Silvestri) Siphonodosaria consobrina (d’Orbigny) Siphonodosaria scripta (d’Orbigny) Siphonodosaria verneuilii (d’Orbigny) Stilostomella adolphina (d’Orbigny) Baggina dentata Hagn Cancris auriculus (Fichtel & Moll) Valvulineria complanata (d’Orbigny) Neoeponides schreibersii (d’Orbigny) Rosalina obtusa d’Orbigny Sphaeroidina bulloides d’Orbigny Conorbella patelliformis (Brady) Heronallenia sp.
Schackoinella imperatoria (d’Orbigny) Siphonina reticulata (Czjzek) Cibicidoides pseudoungerianus (Cushman) Cibicidoides ungerianus (d’Orbigny) Fontbotia wuellerstorfi (Schwager) Lobatula lobatula (Walker & Jacob) Planorbulina mediterranensis d’Orbigny Nonion commune (d’Orbigny)
Katarina Oblak
Nonionella turgida (Williamson) Astrononion stelligerum (d’Orbigny) Melonis pompilioides (Fichtel & Moll) Pullenia bulloides (d’Orbigny) Pullenia quinqueloba (Reuss) Allomorphina trigona Reuss Chilostomella oolina Schwager Chilostomella ovoidea Reuss Quadrimorphina petrolei (Andreae) Oridorsalis umbonatus (Reuss) Anomalinoides badenensis (d’Orbigny) Heterolepa dutemplei (d’Orbigny) Hansenisca soldanii (d’Orbigny) Hanzawaia boueana (d’Orbigny) Riminopsis boueanus (d’Orbigny) Pararotalia aculeata (d’Orbigny) Ammonia beccarii (Linnaeus) Elphidiella sp.
Elphidium aculeatum (d’Orbigny) Elphidium crispum (Linnaeus) Elphidium fichtellianum (d’Orbigny) Elphidium hauerinum (d’Orbigny) Elphidium josephinum (d’Orbigny) Elphidium reginum (d’Orbigny) Porosononion granosum (d’Orbigny)
The following ten species were recognized to be particularly abundant through the sections: Angulogerina angulosa, Trifarina bradyi, Sphaeroidina bulloides, Cibicidoi-des ungerianus, Nonion commune, Melonis pompilioides, Pullenia bulloides, Hetero-lepa dutemplei, Hansenisca soldanii and Hanzawaia boueana. They occur in samples of the Lower Badenian Lower Lagenidae Zone to the Upper Badenian Virgulinella pertusa Zone, a few range up to the Lower Sarmatian Anomalinoides dividens Zone (Oblak, 2006). Beside a great stratigraphic range, these species show high abundance inside particular samples (Tab. 2).
Taxonomy of most abundant rotaliinas of the investigated area
Ordo Foraminiferida Eichwald, 1830 Subordo Rotaliina Delage & Herouard,
1896
Superfamilia Buliminacea Jones, 1875
Familia Uvigerinidae Haeckel, 1894
Subfamilia Angulogerininae Galloway,
1933
Genus Angulogerina Cushman, 1927
Angulogerina angulosa (Williamson, 1858) (Pl. 1, figs. 1a–b)
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              297
1858 Uvigerina angulosa – Williamson, 67, pl. 5, fig. 140.
1960 Angulogerina angulosa (Williamson) – Barker, 154, pl. 74, figs. 15–16.
1979 Trifarina angulosa (Williamson) – Po-pescu, 36, pl. XXI, fig. 6.
1982 Trifarina angulosa (Williamson) – Dondi & Barbieri, tav. XXXVII, fig. 3.
1986  Trifarina angulosa (Williamson) – Belanger & Berggren, 336, pl. 3, fig. 4.
1987  Angulogerina angulosa (Williamson) – Loeblich & Tappan, pl. 574, figs. 5-9.
1987 Trifarina   angulosa   (Williamson)   –
Wenger, 282, Taf. 9, Fig. 21-22. 1991 Angulogerina angulosa (Williamson)
– Cimerman & Langer, 63, pl. 66, figs.
3–4. 1993 Angulogerina angulosa (Williamson)
– Hottinger et al., 100, pl. 126, figs.
1–7. 1993 Angulogerina angulosa (Williamson)
– Sgarrella & Moncharmont Zei, 215,
pl. 16, fig. 8.
1996 Trifarina angulosa (Williamson) – Vio-lanti, 46, pl. 9, figs. 11–12.
1998 Angulogerina angulosa (Williamson) – Cicha et al., 80, pl. 54, figs. 5–6.
1998 Angulogerina angulosa (Williamson) – Rögl, 137, Taf. 4, Fig. 8.
2003 Trifarina angulosa (Williamson) – Murray, 26, pl. 51, fig. 1–6.
2003 Angulogerina angulosa (Williamson) – Rögl & Spezzaferri, pl. 6, fig. 2.
Material: Numerous tests in samples from six sections (Tab. 2).
Description: Small elongated test is trise-rial in its early part but later a tendency toward uniserial growth appears. Transverse section is circular in an initial tri-serial stage, and triangular in the main later stage. Test is thickest at the half of the length. It is about 2–2.5 times as long as thick. Chambers are slightly inflated and enlarge gradually as added. They are arranged in about five whorls. Sides of the test are convex due to chamber inflated-ness. The three angles of the test are cari-nate, more intensively toward the aperture. Sutures are curved and depressed. Wall is calcareous and optically radial. It is finely perforated. The surface is ornamented by fine longitudinal costae that are usually not continuous over the sutures. Aperture is terminal; it is developed at the end of a short neck and it is bordered by a lip. It is provided with a toothplate.
Remark: In this study, specimens show a variety of ornamentation and flatness of angels. Specimens with more carina-te angels are usually less ornamented; such tests are in literature cited also as Angulogerina carinata Cushman (Barker, 1960). Specimens of this study show intermediate forms therefore they are all determined as the species Angulogerina angulosa.
Size: Test length is 0.26 mm and thickness about 0.1 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to Early Upper Ba-denian (Bolivina dilatata Zone).
Occurrence: The species was first described on recent specimens from Great Britain. In Australia, it is known from the Upper Oligocene to Lower Miocene (Li & McGowran, 2000), in Italy from the Oligocene (Poignant, 1983) to Pleistocene (Dondi & Barbieri, 1982: Langhian to Pleistocene, Dieci, 1959: Miocene to Pleistocene, Giannini & Tavani, 1960: Miocene, Pliocene), in the North Atlantic from the Miocene and Pliocene (Belanger & Berggren, 1986), and in Germany and Scandinavian from Pleistocene (Wie-gank, 1972).
The species is extant; it is known from the North and South Atlantic, Indian Ocean, North and South Pacific (Longi-nelli, 1956; Wiegank, 1972; Dieci, 1959: Pacific, Barker, 1960: South Pacific, Loe-blich & Tappan, 1987; Debenay & Konate, 1987; Debenay et al., 1987; Murray, 2003: North Atlantic), it is common from the Antarctica and Sub Antarctica (Violan-ti, 1996). It is noted also from the Mediterranean Sea (Parisi, 1981; Debenay et al., 1987; Sgarrella & Moncharmont Zei, 1993) and the Adriatic Sea (Cimerman & Langer, 1991).
In the Central Paratethys, it exists from the Lower Kiscellian to the end of the Badenian (Cicha et al., 1998). In Bavaria, it is noted from the Kiscellian to Ottnangian (Reiser, 1987: Lower Ru-pelian – Lower Egerian, Wenger, 1987: Upper Egerian – Middle Ottnangian), in Austria from the Karpatian (Rögl, 1998) and Early Lower Badenian (Rögl & Spez-zaferri, 2003), and in Romania from the Upper Badenian (Popescu, 1979).
In Slovenia, the fossil specimens of the species have not been determined yet. The species is described and imaged only
298
on recent specimens of the Adriatic Sea (Cimerman & Langer, 1991). Ecology and palaeoecology: Miocene specimens from Romania are recorded from the pelitic facies (Popescu, 1979). The extant species prefers sandy sediments of the outer shelf and uppermost bathyal (continental slope), influenced by strong bottom currents (Violanti, 1996; after Mackensen et al., 1990). The species is reported from 18 to 3000 m (inner sublittoral to bathyal), of temperature range from 0 to 16°C (sub-arctic to temperate-cold) (Wiegank, 1972). It is a euhaline species (Wiegank, 1972: salinity above 34‰, Rögl, 1998). In the North Atlantic, the species is reported from the shore down to 2900 m, in the South Atlantic from 180 to 1800 m, in the India Ocean down to 2000 m, in the North Pacific down to 720 m and in the South Pacific from 15 to 2450 m (Dieci, 1959). In the Mediterranean, the species is extant in the circalittoral and particularly in the bathyal, in the Northern Adriatic Sea also in the infralitoral. The deepest occurrence is noted at 2860 m in the Tyrrhenian Sea (Sgarrella & Moncharmont
Zei, 1993). In the Adriatic Sea, it was noticed also in detritus from cliff face at 35 m (Cimerman & Langer, 1991).
Genus Trifarina Cushman, 1923
Trifarina bradyi Cushman, 1923 (Pl. 1, figs. 2a–b)
1923 Trifarina bradyi – Cushman, U. S. Nat. Mus., Bull., 104(4), 99, pl. 22, figs. 3a– 9b (Ellis & Messina, 1940).
1959  Trifarina bradyi Cushman – Dieci, 75, tav. VI, fig. 16.
1960  Trifarina bradyi Cushman – Premoli Silva, 569, tav. LVI, fig. 2.
1975 Trifarina bradyi Cushman – Popescu,
79, pl. LXXX, figs. 1a, b. 1982 Trifarina bradyi Cushman – Dondi &
Barbieri, tav. XXXVII, fig. 5. 1987 Trifarina bradyi Cushman – Loeblich
& Tappan, pl. 574, figs. 10–13. 1987 Trifarina bradyi Cushman – Wenger,
283, Taf. 9, Fig. 25–26. 1994 Trifarina bradyi Cushman – Bolli et
al., 358, fig. 80.32. 1998 Trifarina bradyi Cushman – Cicha et
al., 132, pl. 54, figs. 13–15.
Katarina Oblak
Material: Numerous tests in samples from five sections (Tab. 2).
Description: Test is small, elongated and regularly triangular in transverse section. It is thickest in the upper third of the length. It is about twice times as long as thick. Sides of the test are flush or slightly concave. The early stage is triserial; later the test becomes uniserial and usually slightly twisted. Up to seven chambers that enlarge gradually are visible on each side. The three angles of the test are distinctly carinate in the whole length; from the initial part of the test up to the end of the neck. Sutures are thickened, curved and flush or depressed. Wall is calcareous, optically radial and finely perforated. The surface is smooth. Terminal aperture is developed at the end of a short neck. It is bordered by a lip and provided with a toothplate.
Size: Test length is 0.28 mm and thickness 0.12 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to Late Middle Ba-denian (Uvigerina cf. pygmea Zone).
Occurrence: The species was first described on recent specimens from the Caribbean Sea. It appears for the first time in the Oligocene (Giannini & Tavani, 1960). In Australia, it is known from the Upper Oligocene to the end of Miocene (Li & McGowran, 2000), in Italy from the Aquitanian to Pleistocene, it is numerous particularly in the Pliocene (Dondi & Barbieri, 1982, Premoli Silva, 1960: Langhian, Dieci, 1959: Tortonian to Pleistocene, Giannini & Tavani, 1960: Miocene, Pliocene), in South America from the Lower and Middle Miocene (Bolli et al. 1994), and in Algeria from the Messinian (Poignant & Moissette, 1992).
The species is extant. It is known from the North and South Atlantic, Pacific (Longinelli, 1956; Barker, 1960: Pacific) and according to Dieci (1959), also from the Mediterranean. In view of Sgarrel-la & Moncharmont Zei (1993), the tests found on the Mediterranean bottom are most likely reworked from the Pliocene and Pleistocene sediments; the species is not extent any more in the Mediterranean.
In the Central Paratethys, it is known from the Upper Eocene to the end of the Badenian (Cicha et al., 1998); e.g. in Bavaria from the Kiscellian to Ottnangian
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              299
(Reiser, 1987: Lower Rupelian – Lower Egerian, Wenger, 1987: Eggenburgian – Middle Ottnangian), and in Romania from the Lower and Middle Miocene (Po-pescu, 1975).
In Slovenia, the fossil species has not been determined yet. Ecology and palaeoecology: The genus Trifarina is infaunal and characteristically found in temperate to cold marine environments of depths ranging from 0 to 400 m; from the shelf to upper bathy-al (Murray, 1991). Karpatian specimens from the Central Paratethys are reported mostly from the euhaline assemblages (Cicha & Zapletalová, 1967). Extant specimens occur in the depth-range from 700 to 2450 m in the North Atlantic, from 630 to 1210 m in the South Atlantic (Dieci, 1959), and from 22 to 500 m in the South Pacific (Longinelli, 1956).
Superfamilia Discorbacea Ehrenberg, 1838
Familia Sphaeroidinidae Cushman, 1927
Genus Sphaeroidina d’Orbigny, 1826
Sphaeroidina bulloides d’Orbigny, 1826 (Pl. 2, figs. 1a–b)
1826 Sphaeroidina bulloides – d’Orbigny,
101. 1956 Sphaeroidina  bulloides   d’Orbigny  –
Longinelli, 175, tav. X, fig. 1.
1959  Sphaeroidina bulloides d’Orbigny – Dieci, 87, tav. VII, figg. 18–19.
1960  Sphaeroidina bulloides d’Orbigny – Premoli Silva, 560, tav. LVI, figg. 1a–b.
1975 Sphaeroidina bulloides d’Orbigny – Popescu, 72, pl. XLIX, figs. 10a–b.
1985  Sphaeroidina bulloides d’Orbigny – Papp & Schmid, 96, Taf. 90, Fig. 7–12.
1986  Sphaeroidina bulloides d’Orbigny – Belanger & Berggren, 332, pl. 1, fig. 18.
1987  Sphaeroidina bulloides d’Orbigny – Wenger, 302, Taf. 14, Fig. 11–12.
1993 Sphaeroidina     bulloides     d’Orbigny
– hottinger et al., 113, pl. 147, figs.
4–11. 1995 Sphaeroidina  bulloides   d’Orbigny  –
Yassini & Jones, 160, figs. 936–937. 1998 Sphaeroidina     bulloides     d’Orbigny
– Cicha et al., 127, pl. 60, fig. 4. 1998 Sphaeroidina     bulloides     d’Orbigny
– Robertson, 196, pl. 74, figs. 4a–c.
2003 Sphaeroidina  bulloides   d’Orbigny  – Rögl & Spezzaferri, pl. 6, Fig. 24.
Material: Numerous tests in samples from all six sections (Tab. 2).
Description: Test is subglobular and involute. It is built of tightly embracing hemispherical chambers that enlarge rapidly in size. There are four chambers in the last whorl. Periphery is broadly rounded. Sutures are flush or slightly depressed and hardly visible. Wall is calcareous and optically radial. Surface is smooth and very finely perforate. Inter-iomarginal narrow crescentic aperture is developed near the junction of last three chambers. It is bordered by a lip and it is provided with an apertural plate.
Remark: In this study, tests are mostly subglobular, although rare more lobed forms may be present. Similar lobed tests are classified in the species Sphaeroidina bulloides also in the literature (Wenger, 1987).
Size: Test height is 0.35 mm and thickness 0.3 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to Late Upper Badenian (Virgulinella pertusa Zone). Rare reworked tests were found also in the Lower Sarmatian samples (Anomali-noides dividens Zone).
Occurrence: Recent specimens from the Adriatic Sea (Italy) and fossil specimens from Sienna (Italy) are noted by the first description of the species (d’Orbig-ny, 1826). According to Papp and Schmid (1985), the species first appeared in the Eocene; while Bartolini (1966) gives an earlier first occurrence, placing it in the Cretaceous. In Middle America, the species is noted from the Lower Oligocene to Lower Pliocene (Robertson, 1998), in Italy from the Lower Oligocene to Pleistocene (Dondi & Barbieri, 1982; Barbieri & d’Onofrio, 1984: Middle Miocene, Gia-nnini & Tavani, 1960: Miocene, Pliocene), in Australia from the Upper Oligocene to the end of Miocene (Li & McGowran, 2000), in the North Atlantic from the Middle Miocene to Pliocene (Belanger & Berggren, 1986), in Algeria from the Mes-sinian (Poignant & Moissette, 1992), in South America from the Miocene (Hasson & Fischer, 1986), in Spain and California from the Pliocene (Longinelli, 1956), in the Indian Ocean from the Pliocene and
300
Katarina Oblak
Pleistocene (Basov & Krasheninnikov, 1995), and in the Arabian Sea from the Quaternary (den Dulk et al., 1998).
The species is extant and is cosmopolitan (Papp & Schmid, 1985; Robertson, 1998; Barker, 1960: North Atlantic and Pacific; Hottinger et al. 1993: Red Sea). It is noted also from the Mediterranean Sea
(Sgarrella & Moncharmont Zei, 1993).
In the Central Paratethys, it appears from the Lower Kiscellian to the end of the Badenian (Cicha et al., 1998) and it is numerous in the Badenian (Cicha & Za-pletalová, 1967). In Romania, it is known from the Oligocene to Middle Miocene (Popescu, 1975), in Croatia (Šiki}, 1985) and Hungary (Sztrŕkos, 1979) from the Upper Kiscellian, in Bavaria from the Kiscellian to Ottnangian (Reiser, 1987: Lower Rupelian – Lower Egerian, Wen-ger, 1987: Upper Egerian – Middle Ot-tnangian), in Austria from the Karpatian (Rögl, 1998) and Early Lower Badenian (Rögl & Spezzaferri, 2003), and in Poland from the Badenian (Szczechura, 2000)
In Slovenia, the species has not been described and imaged yet. It is only noted from Lower Egerian to Upper Badenian sediments. It is mentioned from Lower Egerian of the La{ko syncline (Petrica et al., 1995; Dozet et al., 1999; Rijavec, 1976a, 1984) and Planina syncline (Rija-vec, 1977), from the Upper Egerian of the La{ko syncline (Rijavec, 1984; Dozet & Ri-javec, 1994; Dozet et al., 1996; 1999) and Planina syncline (Rijavec, 1977; Rijavec & Dozet, 1996), from the Eggenburgian of the La{ko syncline (Rijavec, 1984), from the Lower Badenian of the Celje syncline (Rijavec, 1978a), La{ko syncline (Rijavec, 1976a, 1984; Dozet & Rijavec, 1994; Do-zet et al., 1999), Planina syncline between Trobni Dol and Rudnica mountain (Rija-vec & Dozet, 1996) and by Vir{tanj (Rija-vec, 1977), and of the Bizeljsko syncline (Dozet et al., 1998). It is known also from the Middle Badenian of the Celje syncline (Rijavec, 1975, 1978a), La{ko syncline (Ri-javec, 1976a, 1984), Planina syncline by Planina pri Sevnici (Rijavec, 1977), and of the Bizeljsko syncline (Dozet et al., 1998). From the Upper Badenian, it appears in Slovenske gorice (Rijavec, 1974), La{ko syncline (Rijavec, 1976a, 1984) and Senovo syncline (Dozet et al., 1998). Ecology and palaeoecology: Fossil specimens from the Central Paratethys are
characteristically found in sediments from the outer shelf (deepest neritic) to bathyal (Cicha & Zapletalová, 1967). Extant specimens prefer cool bottom waters (Rögl & Spezzaferri, 2003) and is a subo-xic indicator (den Dulk et al., 1998). They occur deeper than 100 m (Wenger, 1987: after Phleger 1960). In the North Atlantic, it occurs in the depth-range from 160 to 3100 m, in the South Atlantic from 760 to 4200, in the North Pacific from 180 to 3700 m, and in the South Pacific from 70 to 2500 (Dieci, 1959). On the Australian coast, it is reported from the outer shelf and bathyal (continental slope) (Yassini & Jones, 1995). In the Mediterranean, it is characteristic for muds of the circa-littoral and bathyal; it appears down to
1300 m (Sgarrella & Moncharmont Zei,
1993).
Superfamilia Discorbinellacea Sigal, 1952 Familia Parrelloididae Hofker, 1956 Genus Cibicidoides Thalmann, 1939
Cibicidoides ungerianus (d’Orbigny, 1846) (Pl. 2, figs. 2a–c)
1846 Rotalina ungeriana – d’Orbigny, 157, Tab. VIII, fig. 16–18.
1959  Cibicides   ungerianus   (d’Orbigny)   – Dieci, 102, tav. VIII, fig. 17.
1960  Cibicides   ungerianus   (d’Orbigny)   – Giannini & Tavani, 56, tav. IX, fig. 2–4.
1967 Cibicides     ungerianus     (d’Orbigny)
– Cicha & Zapletalová, 142, Taf. 13A,
Fig. 1a–c. 1975 Cibicidoides  ungerianus  (d’Orbigny)
– Popescu, 104, pl. LXXXV, figs. 1a–c. 1979 Cibicidoides  ungerianus  (d’Orbigny)
– Sztrŕkos, pl. 30, figs. 4a–b. 1985 Cibicides   ungerianus   (d’Orbigny)   –
Papp & Schmid, 60, Taf. 51, Fig. 7–11. 1998 Cibicidoides  ungerianus  ungerianus
(d’Orbigny) – Cicha et al., 91, pl. 61,
figs. 15–17. 2003 Cibicidoides ungerianus (d’Orbigny) –
Rögl & Spezzaferri, pl. 6, figs. 26–29.
Material: Numerous tests in samples from all six sections (Tab. 2).
Description: Biconvex biumbonate test is very low trochospiral. Spiral side is evolute and umbilical side involute. Test is nearly circular in equatorial section. There are two and a half to three whorls
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              301
that enlarge rapidly in size. Last whorl consists of 10–13 chambers. Chambers are low, crescentic in shape and enlarge gradually. Sutures of both sides are curved backward; more distinctly on the spiral side. Whorl suture is flush but hardly visible due to granular ornamentation. Periphery is angular and very slightly lobate in outline. Wall is calcareous and optically radial. It is coarsely perforated on the spiral side and finely perforated on the umbilical side. Surface is smooth apart for typical granular ornamentation, which is developed around the umbo of the spiral side. Narrow arched aperture is interiomarginal and equatorial; it is bordered by a thin lip.
Remark: Reiser (1987) and Cicha et al. (1998) divide the species Cibicidoides ungerianus into subspecies C. ungerianus ungerianus (d’Orbigny) with weaker ornamentation and C. ungerianus filicosta (Hagn) with stronger ornamentation. Specimens from this study correspond to the subspecies C. ungerianus ungerianus (d’Orbigny).
Size: Test diameter is 0.58 – 0.6 mm and thickness 0.2 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to Early Upper Badenian (Bolivina dilatata Zone). Rare reworked tests were found also in the Lower Sarmatian samples (Anomalinoides dividens Zone).
Occurrence: The species was first described from the Late Lower Badenian. There is no data about the type locality by the first description (d’Orbigny, 1846). The species appeared in the Oligocene according to Giannini & Tavani (1960), or in the Upper Eocene according to Asco-li (1956) and Gohrbandt (1961). In Italy, it is known from the Upper Eocene (As-coli, 1956) to Pleistocene (Dondi & Bar-bieri, 1982: Serravallian to Pleistocene, Dieci, 1959: Miocene, Pliocene), but becomes the most abundant in the Torto-nian (Dondi & Barbieri, 1982: Po Valley). In Middle America, it is noted from the Middle Oligocene (Bolli et al., 1994), in the Mediterranean from the Oligocene, and in the Arabian Sea from the Quaternary (den Dulk et al., 1998).
The species is extant (Giannini & Ta-vani, 1960). It is noted from the Arabian Sea (den Dulk et al., 1998).
In the Central Paratethys, it is known from the Upper Eocene to the Lower Sar-
matian (Cicha et al., 1998). In Austria, it is noted from the Upper Eocene (Gohr-bandt, 1961) and Early Lower Badenian (Rögl & Spezzaferri, 2003); in the Vienna Basin, it is especially abundant in the whole Lower Badenian (Papp & Schmid, 1985). In Hungary, it is known from the Upper Kiscellian (Sztrŕkos, 1979), in Bavaria from the Kiscellian and Lower Egerian (Reiser, 1987: Lower Rupelian – Lower Egerian), in Croatia from the Kis-cellian (Šiki}, 1985) and Upper Badenian (Bajraktarevi}, 1979, Pikija et al., 1984), in Romania from the Lower and Middle Miocene (Popescu, 1975), and in Poland from the Badenian (Szczechura, 2000)
In Slovenia, the species has not been described yet. It was only imaged from the Upper Eocene (Priabonian) of Socka –Dobrna area (northern of Celje; Cimer-man et al., 2006). It is also noted from the Kiscellian to Middle Badenian sediments. It is mentioned from the Kiscel-lian of Zasavje (Kolar, 1978), from the Lower Egerian of the La{ko syncline (Rijavec, 1984; Dozet & Rijavec, 1994; Petrica et al., 1995; Dozet et al., 1999), Planina syncline (Rijavec, 1977; Rijavec & Dozet, 1996) and Senovo syncline (Do-zet et al., 1998), from the Upper Egerian of the Celje syncline (Rijavec, 1984), La-{ko syncline (Rijavec, 1977, 1984; Dozet & Rijavec, 1994; Dozet et al., 1996, 1999) and Planina syncline (Rijavec & Dozet, 1996), from the Lower Badenian of Slovenske gorice (Rijavec, 1976b), Dravinjske gorice (Rijavec, 1975), Celje syncline (Rijavec, 1978a), La{ko syncline (Rijavec, 1976a, 1977, 1984; Dozet & Rijavec, 1994; Dozet et al., 1999), Planina syncline between Trobni Dol and Rudnica mountain (Rijavec & Dozet, 1996), by Vir{tanj and Plohov breg (Rijavec, 1977), and of the Bizeljsko syncline (Dozet et al., 1998). It is noted also from the Middle Badenian of Dravinjske gorice (Rijavec, 1975), Celje syncline (Rijavec, 1978a), La{ko syncline (Rijavec, 1976a, 1984; Dozet & Rijavec, 1994), Planina syncline by Trobni Dol (Petrica et al., 1995), between Trobni Dol and Rudnica mountain (Rijavec & Dozet, 1996) and by Planina pri Sevnici (Rijavec, 1977), and of the Bizeljsko syncline (Do-zet et al., 1998). Ecology and palaeoecology: The genus Cibicidoides is epifaunal and is believed to attach itself to hard substrates. It is
302
characteristic for cold marine environments of the shelf and bathyal (Murray, 1991). It is an oxic indicator (Rögl & Spezzaferri, 2003). Fossil Badenian specimens of the species C. ungerianus from the Central Paratethys are reported from sediments of the shelf (sublittoral to shallow neritic) (Cicha & Zapletalová, 1967).
Superfamilia Nonionacea Schultze, 1854
Familia Nonionidae Schultze, 1854
Subfamilia Nonioninae Schultze, 1854
Genus Nonion de Montfort, 1808
Nonion commune (d’Orbigny, 1846) (Pl. 3, figs. 1a–b)
1846 Nonionina communis – d’Orbigny, 106, Tab. V, fig. 7–8.
1959 Nonion commune (d’Orbigny) – Dieci, 53, tav. IV, fig. 25a–b.
1967 Florilus communis (d’Orbigny) – Cicha & Zapletalová, 136.
1979 Florilus communis (d’Orbigny) – Po-pescu, 46, pl. XXVII, figs. 8a–b.
1985 Nonion commune (d’Orbigny) – Papp & Schmid, 45, Taf. 34, Fig. 1–5.
1987 Florilus communis (d’Orbigny) – Wen-ger, 298, Taf. 13, Fig. 15, 19.
1997  Nonion commune (d’Orbigny) – Fili-pescu & Girbacea, pl. VI, fig. 4.
1998  Nonion commune (d’Orbigny) – Cicha et al., 113, pl. 66, figs. 1–2.
2003 Nonion commune (d’Orbigny) – Rögl & Spezzaferri, pl. 6, fig. 35.
2007 Nonion commune (d’Orbigny) – Schütz et al., 457, Taf. 5, Fig. 3a-b.
Material: Numerous tests in samples from all six sections (Tab. 2).
Description: Planispirally enrolled test is involute. It is ovate in outline. Whorls enlarge rapidly in size. There are 9–12 low triangular low chambers in the last whorl. Sutures of both sides are curved backward. Umbilicus is narrow. Periphery is slightly compressed and smooth in outline. Calcareous optically granular wall is very finely perforated. The surface is smooth; except for the umbilical, su-tural and apertural regions where numerous distinct pustules are developed. Sutures are curved and depressed. Narrow slitlike aperture is interiomarginal and equatorial. Triangular apertural face is typically well developed.
Katarina Oblak
Size: Test length is 0.4–0.6 mm, width 0.3– 0.4 mm and thickness 0.25–0.3 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to Early Upper Ba-denian (Bolivina dilatata Zone).
Occurrence: The species was first described from the Tertiary of the Vienna basin. In Algeria, it is known from the Messini-an (Poignant & Moissette, 1992).
The species is extant; it is known from the Atlantic (Dieci, 1959; Debenay & Ko-nate, 1987), also from the Adriatic Sea (Dieci, 1959).
In the Central Paratethys, it appears from the Upper Eocene to the end of the Sarmatian (Cicha et al., 1998); e.g. in Hungary, it is known from the Upper Kiscellian (Sztrŕkos, 1979), in Bavaria from the Kiscellian to Ottnangian (Reiser, 1987: Lower Rupelian – Lower Egerian, Wenger, 1987: Upper Egerian – Middle Ottnangian), in Austria from the Karpatian, Badenian (Papp & Schmid, 1985; Rögl & Spezzaferri, 2003: Early Lower Badenian) and Lower Sarmatian (Schütz et al., 2007), in Romania from the Late Lower Badenian (Filipescu & Gir-bacea, 1997) and Upper Badenian (Pope-scu, 1979), and in Croatia from the Upper Badenian (Bajraktarevi}, 1978).
In Slovenia, the species hasn’t been described yet; it was only imaged from the Badenian of the Celje syncline (Rijavec, 1978a). It is also noted from Kiscellian to Middle Badenian sediments. It is mentioned as Nonion communis from the Kiscel-lian of Zasavje (Kolar, 1978). As Florilus communis, it is noted from the Upper Egerian of the Celje syncline (Rijavec, 1984), from the Eggenburgian of the La-{ko syncline (Petrica et al., 1995; Rijavec & Dozet, 1996), from the Lower Badeni-an of Dravinjske gorice (Rijavec, 1975), of the Celje syncline (Rijavec, 1978a), La{ko syncline (Rijavec, 1976a, 1977, 1984; Dozet & Rijavec, 1994; Dozet et al., 1999), Planina syncline between Trobni Dol and Rud-nica mountain (Rijavec & Dozet, 1996), by Vir{tanj and Plohov breg (Rijavec, 1977), and of the Bizeljsko syncline (Dozet et al., 1998). It appears in the Middle Badenian of the Celje syncline (Rijavec, 1978a), La-{ko syncline (Rijavec, 1976a, 1977, 1984; Dozet et al., 1996), Planina syncline by Planina pri Sevnici and Plohov breg (Ri-javec, 1977), and of the Bizeljsko syncline (Dozet et al., 1998).
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              303
Ecology and palaeoecology: The genus Nonion is infaunal and characteristic for muddy and silty sediments. It occurs in cold to warm waters of the shelf zone from 10 to 180 m (Murray, 1991). Fossil specimens of the species N. commune from the Central Paratethys are recorded from sediments of the shelf (deep sublit-toral) to bathyal; they are most frequent in sediments of the neritic (Cicha & Za-pletalová, 1967). The extant species is characteristic for the shelf of a depth-range from 0 to 180 m (Rögl & Spezza-ferri, 2003). It may occur also in brackish waters (Wenger 1987).
Subfamilia Pulleniinae Schwager, 1877 Genus Melonis de Montfort, 1808
Melonis pompilioides (Fichtel & Moll,
1798)
(Pl. 3, figs. 2a–b)
1798 Nautilus pompilioides – Fichtel & Moll, Test. Micro. Arg. Naut., 31, pl. 2, figs. a–c (Ellis & Messina, 1940).
1956 Nonion pompilioides (Fichtel & Moll) – Longinelli, 143, tav. XI, figg. 12a–b.
1959  Nonion pompilioides (Fichtel & Moll) – Dieci, 55, tav. I V, figg. 27a–b.
1960  Nonion pompilioides (Fichtel & Moll) – Giannini & Tavani, 23, tav. VI, fig. 5.
1969 Nonion pompilioides (Fichtel & Moll)
– Rögl, 101, Taf. 4, Fig. 11a–b. 1979 Melonis    pompilioides    (Fichtel    &
Moll) – Popescu, 48, pl. XXVIII, fig.
7a–b. 1985 Melonis    pompilioides    (Fichtel    &
Moll) – Papp & Schmid, 46, Taf. 36,
Fig. 1–5. 1987 Melonis    pompilioides    (Fichtel    &
Moll) – Wenger, 300, Taf. 13, Fig.
23–24. 1991 Melonis    pompilioides    (Fichtel    &
Moll) – Cimerman & Langer, 74, pl.
85, figs. 1–4. 1998 Melonis    pompilioides    (Fichtel    &
Moll) – Cicha et al., 111, pl. 66, figs.
14–15. 1998 Melonis    pompilioides    (Fichtel    &
Moll) – Robertson, 228, pl. 91, figs.
4a–b. 2003 Melonis    pompilioides    (Fichtel    &
Moll) – Rögl & Spezzaferri, pl. 7, fig.
9–10.
Material: Numerous tests in samples from all six sections (Tab. 2).
Description: Planispiral test is involute and biumbilicate. It is circular in outline. Last whorl consists of 9–10, rarely of 11 chambers that enlarge gradually as added. Chambers are low and triangular in a side view. Sutures are radial, flush and straight to slightly curved backward; they are hardly visible. In the earlier part of the last whorl they may be thickened. Umbilici of both sides are wide and deep. Periphery is broadly rounded and smooth in outline. Toward the earliest part of the last whorl it can become slightly compressed. Wall is calcareous and optically granular. It is coarsely perforate. Surface is smooth. Apertural face is broad and smooth. Interiomarginal equatorial aperture extends laterally toward the umbilici. It is boarded by a lip.
Size: Test diameter is 0.4 mm and thickness 0.25 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to Early Upper Ba-denian (Bolivina dilatata Zone).
Occurrence: There is no data about the type locality and type level in the catalogue (Ellis & Messina, 1940). In South America, it occurs from the Oligocene to Miocene (Robertson, 1998), in Middle America, in the Lower Miocene (Bolli et al., 1994) and Pliocene (Hasson & Fischer, 1986), in Italy from the Tortonian to Pleistocene (Dieci, 1959; Barbieri & d’Onof-rio, 1984: Middle Miocene), in Egypt in the Middle Miocene (Cherif et al., 1994), in Algeria in the Messinian (Poignant & Moissette, 1992), and in the Atlantic in the Pleistocene (Lévy et al., 1998).
The species is extant; it is known from the Pacific and Atlantic (Robertson, 1998; Barker, 1960: Eastern Atlantic). It is noted also from the Mediterranean and Adriatic Sea (Cimerman & Langer, 1991). In the Central Paratethys, it is known from the Upper Eocene to the end of the Badenian (Cicha et al., 1998), according to Papp & Schmid (1985) to the Sarmati-an. In Bavaria, it appears from the Kis-cellian to Ottnangian (Reiser, 1987: Upper Rupelian – Lower Egerian, Wenger, 1987: Upper Egerian – Middle Ottnangi-an), in Austria in the Karpatian (Rögl, 1969) and Early Lower Badenian (Rögl & Spezzaferri, 2003), in Romania in the Upper Badenian (Popescu, 1979), and in Poland in the Badenian (Szczechura, 2000).
304
Katarina Oblak
In Slovenia, the species has not been described and imaged yet. It is only noted from the Karpatian of Slovenske gorice (Jelen & Rifelj, 2003), and from the Lower Badenian of the Celje syncli-ne (Rijavec, 1984) and Bizeljsko syncline (Dozet et al., 1998). Ecology and palaeoecology: The genus Melonis is infaunal and occurs on the muddy and silty bottom of the shelf and bathyal zones. It is characteristic for cold marine waters (temperature below 10°C) (Murray, 1991). Fossil specimens of the species Melonis pompilioides from Upper Egerian to Ottnangian of Bavaria are most frequent recorded above the shelf/ bathyal boundary (neritic/bathyal, Wen-ger, 1987). The extant species occurs in the depth-range from 50 to 4000 m (Rögl & Spezzaferri, 2003), and is typical in the range from 1000 to 3000 m (Wenger, 1987). According to older literature, the maximum depth of occurrence has moved downward; in the Atlantic down to 4900 m (Longinelli, 1956), in the North Pacific down to 5000 m and in the South Pacific down to 4400 m (Dieci, 1959). In the Tyrrhenian Sea, the tests were found in soft sediments at 130 m, and in the Adriatic Sea in detrital sands at 55 m (Cimerman & Langer, 1991).
Genus Pullenia Parker & Jones, 1862
Pullenia bulloides (d’Orbigny, 1846) (Pl. 4, figs. 1a–b)
1846 Nonionina bulloides – d’Orbigny, 107, Tab. V, fig. 9–10.
1956 Pullenia sphaeroides d’Orbigny – Lon-ginelli, 174, tav. X, figg. 2–3.
1959 Pullenia bulloides (d’Orbigny) – Dieci, 87, tav. VII, figg. 16a–b.
1967 Pullenia bulloides (d’Orbigny) – Cic-ha & Zapletalová, 137, Taf. 6A, Fig. 8a–b.
1971 Pullenia bulloides (d’Orbigny) – Cicha et al., 281–282, Taf. 11, Fig. 2-3.
1975 Pullenia bulloides (d’Orbigny) – Po-pescu, 101, pl. LXXXIII, figs. 1a–b.
1982 Pullenia bulloides (d’Orbigny) – Dondi & Barbieri, tav. XLIV, fig. 8.
1985  Pullenia bulloides (d’Orbigny) – Papp & Schmid, 45, Taf. 34, Fig. 6–9.
1986  Pullenia bulloides (d’Orbigny) – Belanger & Berggren, 342, pl. 5, figs. 1a–b.
1987 Pullenia bulloides (d’Orbigny) – Miller & Katz, 136, pl. 4, figs. 4a–b.
1987 Pullenia bulloides (d’Orbigny) – Wen-ger, 299, Taf. 13, Fig. 17–18.
1993 Pullenia bulloides (d’Orbigny) – Sgar-rella & Moncharmont Zei, 240, pl. 24, figs. 12–13.
1995 Pullenia bulloides (d’Orbigny) – Yassi-ni & Jones, 181, figs. 966–967.
1998 Pullenia bulloides (d’Orbigny) – Cicha et al., 121, pl. 66, figs. 12–13.
1998 Pullenia bulloides (d’Orbigny) – Robertson, 230, pl. 92, figs. 1a–b.
2003 Pullenia bulloides (d’Orbigny) – Rögl & Spezzaferri, pl. 7, figs. 11–12.
2005 Pullenia bulloides (d’Orbigny) – VÉ-NEC-PEYRÉ, 214–215, Pl. 35, Fig. 2.
2007 Pullenia bulloides (d’Orbigny) – Schütz et al., 457, Taf. 5, Fig. 6a–b.
Material: Numerous tests in samples from all six sections (Tab. 2).
Description: Globular test is planispiral by growth. It is involute. Whorls enlarge slowly in size. Last whorl consists of four, rarely of four and a half chambers that are triangular in a side view. They are as long as high and they enlarge slowly as added. Radial sutures are straight and flush. Periphery is rounded and smooth in outline. Umbilicus is very narrow and flush. Wall is calcareous and optically granular; it is very finely perforated. Surface is smooth. Apertural face is very low and broad. Slitlike aperture is inte-riomarginal and equatorial, extending laterally to the umbilici.
Size: Test diameter is 0.28–0.35 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to Early Upper Ba-denian (Bolivina dilatata Zone). Reworked tests were found also in the Lower Sarmatian samples (Anomalinoides divi-dens Zone).
Occurrence: The species was first described from the Late Upper Badenian of the Vienna basin. In the Middle America, it is known from the Upper Eocene to Pleistocene (Robertson, 1998), in South America from the Upper Eocene to Pliocene (Robertson, 1998; Emiliani, 1954: Miocene, Pliocene; Hasson & Fischer, 1986: Miocene, Pliocene), in Italy from the Middle Eocene to Pleistocene, it is numerous in the Pliocene (Dondi & Barbieri, 1982: Po Valley, Emiliani, 1954: Oligocene; Giannini & Tavani, 1960: Mi-
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              305
ocene, Pliocene, Dieci, 1959: Miocene to Pleistocene). In New Zealand, it appears in the Oligocene, in North Africa and Australia in the Miocene and Pliocene (Emiliani, 1954), in Australia in the Lower Miocene (Li & McGowran, 2000), in the Mediterranean in the Middle Miocene (Cherif et al., 1994), in Algeria in the Messinian (Poignant & Moissette, 1992), and in the Atlantic in the Miocene, Pliocene (Belanger & Berggren, 1986) and Pleistocene (Lévy et al., 1998).
The species is extant and is cosmopolitan (Longinelli, 1956; Dieci, 1959). It is noted from the South Atlantic, North Pacific (Barker, 1960; Robertson, 1998) and South Pacific (Yassini & Jones, 1995). It is noted also from the Mediterranean where appears scarcely (Sgarrella & Monchar-mont Zei, 1993).
In the Central Paratethys, it exists from the Upper Eocene to the end of the Badenian (Cicha et al., 1998), Schütz et al. (2007) determined it also from the Lower Sarmatian. In Bavaria, it is noted from the Kiscellian to Ottnangian (Reiser, 1987: Upper Rupelian – Lower Egerian, Wenger, 1987: Upper Egerian – Middle Ottnangian), in Croatia from the Kiscellian (Šiki}, 1985) and Upper Badenian (Bajraktarevi}, 1979; Pikija et al., 1984), in Austria from the Karpatian (Rögl, 1969, 1998) and Early Lower Ba-denian (Rögl & Spezzaferri, 2003), in Romania from the Lower and Middle Miocene (Popescu, 1975), and in Poland from the Badenian (Szczechura, 2000)
In Slovenia, the species has not been described yet, it is only imaged from the Upper Eocene (Priabonian) of Socka-Do-brna area (northern of Celje; Cimerman et al., 2006) and from the Middle Miocene of Slovenske Gorice (Rijavec, 1978b). It is also noted from the Lower Egerian to Upper Badenian sediments. It is mentioned from the Lower Egerian of the Celje syncline (Rijavec, 1984) and La{ko sync-line (Rijavec, 1976a, 1984; Dozet et al., 1999), from the Upper Egerian of the La-{ko syncline (Rijavec, 1977, 1984; Dozet et al., 1996, 1999) and Planina syncline between Trobni Dol and Rudnica mountain (Rijavec & Dozet, 1996), from the Eggenburgian of the Celje syncline (Rija-vec, 1984), from the Karpatian of Slovenske gorice (Jelen & Rifelj, 2003), from the Lower Badenian of the La{ko syncli-
ne (Rijavec, 1977, 1984; Dozet & Rijavec, 1994; Dozet et al., 1999), Planina sync-line between Trobni Dol and Rudnica mountain (Rijavec & Dozet, 1996), and of Bizeljsko syncline (Dozet et al., 1998). It is known also from the Middle Badenian of Slovenske gorice (Rijavec, 1974), Dravinjske gorice (Rijavec, 1975), Celje sync-line (Rijavec, 1978a), La{ko syncline (Ri-javec, 1976a, 1984), Planina syncline by Planina pri Sevnici (Rijavec, 1977), and Bizeljsko syncline (Dozet et al., 1998). It appears in the Upper Badenian of the La{ko syncline (Rijavec, 1984). Ecology and palaeoecology: The genus Pullenia is infaunal and typical for cold marine waters of the outer shelf and bathyal (Murray, 1991). Fossil specimens from the Central Paratethys are reported from sediments of the shelf to bathy-al (shallow neritic to bathyal) (Cicha & Zapletalová, 1967). The extant species occurs down to 5000 m and is more frequent deeper than 550 m (Dieci, 1959). At the Australian coast, it is recorded from the outer shelf and bathyal (outer shelf and continental slope) (Yassini & Jones, 1995). In the Mediterranean, it appears in muddy bottom from the shelf to bat-hyal (circalittoral to bathyal) (Sgarrella & Moncharmont Zei, 1993).
Superfamilia Chilostomellacea Brady, 1881
Familia Heterolepidae Gonzáles-Donoso,
1969
Genus Heterolepa Franzenau, 1884
Heterolepa dutemplei (d’Orbigny, 1846) (Pl. 4, figs. 2a–c)
1846 Rotalina dutemplei – d’Orbigny, 157,
Tab. VIII, fig. 19–21. 1967 Heterolepa    dutemplei    (d’Orbigny)
– Cicha & Zapletalová, 144, Taf. 21A,
Fig. 1. 1969 Heterolepa dutemplei (d’Orb.) – Rögl,
103, Taf. 5, Fig. 13a–c. 1971 Heterolepa dutemplei (d’Orbigny) –
Cicha et al., 285, Taf. 25, Fig. 1–3. 1975 Heterolepa dutemplei (d’Orbigny) –
Popescu, 104, pl. LXXXVI, figs. 1a–2c,
pl. LXXXVIII, figs. 2a–c, pl. LXXXIX,
figs. 1a–3c. 1985 Heterolepa    dutemplei    (d’Orbigny)
– Papp & Schmid, 59, 61, Taf. 50, Fig.
1–3, Taf. 52, Fig. 1–6.
306
1987 Heterolepa    dutemplei    (d’Orbigny)
– Loeblich & Tappan, pl. 709, figs. 1–8. 1987 Heterolepa    dutemplei    (d’Orbigny)
– Wenger, 327, Taf. 22, Fig. 6–8. 1998 Heterolepa    dutemplei    (d’Orbigny)
– Cicha et al., 107, pl. 71, figs. 1–3. 2003 Heterolepa dutemplei  (d’Orbigny) –
Rögl & Spezzaferri, pl. 7, figs. 23–25.
Material: Numerous tests in samples from all six sections (Tab. 2).
Description: Biconvex test is trochospi-rally enrolled and circular in outline. Spiral side is evolute and weakly convex, rarely high convex; with three to four visible whorls. Umbilical side is involute and highly convex. The last whorl is built of rarely 6 and more frequently of 7–9 chambers that increase slowly in size. They are parallelogram to trapezoidal in shape on the spiral side and triangular on the umbilical side. Sutures are oblique and flush on the spiral side, and straight to curved backward and slightly depressed on the umbilical side. Whorl suture is flush to slightly depressed toward the end of the last whorl. Periphery is subangular and smooth to very slightly lobate in outline toward the latest part of the test. Wall is calcareous, optically granular and coarsely perforate. Surface is smooth. Slitlike interiomarginal aperture is developed on the upper half of the apertural face and extends in a short distance on the spiral side. It is bordered by a lip.
Remark: Specimens of this study show a great variety in convexity of the spiral side. Tests with different degree of convexity were originally described as separate species; Rotalina kalembergensis d’Orbigny, Heterolepa dutemplei d’Or-bigny (low convexity) and Rotalina hai-dingerii d’Orbigny (high convexity). Papp & Schmid (1985) placed all these forms into a single species, Heterolepa dutem-plei (d’Orbigny).
Size: Test diameter is 0.53–0.6 mm and thickness 0.4 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to ? Early Upper Badenian (Bolivina dilatata Zone). Tests (reworked?) were found also in the Lower Sarmatian samples (Anomalinoides divi-dens Zone) of two sections.
Occurrence: The species was first described from the Late Lower Badenian of
Katarina Oblak
the Vienna basin. According to Popescu (1975) its first occurrence is in the Oli-gocene. In Tunisia, it is known from the Serravallian (Salaj, 1992), in Sardinia (Italy) from the Middle Miocene (Barbieri & d’Onofrio, 1984) and in Algeria from the Messinian (Poignant & Moissette, 1992).
In the Central Paratethys, it is known from the Upper Kiscellian to the end of the Badenian (Cicha et al., 1998); it is most common in Late Early Badenian (Papp & Schmid, 1985). In Bavaria, it is noted from the Kiscellian to Middle Ot-tnangian (Reiser, 1987: Lower Rupelian – Lower Egerian; Wenger, 1987: Upper Egerian – Middle Ottnangian), in Romania from the Oligocene to Middle Miocene (Popescu, 1975), in Hungary from the Egerian (Sztrŕkos, 1979), and in Austria from the Karpatian (Rögl, 1969, 1998) and Early Lower Badenian (Rögl & Spez-zaferri, 2003).
In Slovenia, the species has not been described and imaged yet. It is only noted from Kiscellian to Upper Badenian sediments. It is mentioned from the Kis-cellian of Zasavje (Kolar, 1978), from the Upper Egerian of the La{ko syncline (Dozet et al., 1999), from the Eggenbur-gian of the Celje syncline (Rijavec, 1984), from the Karpatian of Slovenske gorice (Jelen & Rifelj, 2003), from the Lower Badenian of the Celje syncline (Rijavec, 1978a), La{ko syncline (Rijavec, 1984), Planina syncline by Plohov breg (Rijavec, 1977), and of Bizeljsko syncline (Dozet et al., 1998). It is noted also from the Middle Badenian of Celje syncline (Rijavec, 1978a), La{ko syncline (Rijavec, 1984), Planina syncline by Planina pri Sevnici (Rijavec, 1977), and of Bizeljsko syncline (Dozet et al., 1998). From the Upper Ba-denian, it is known of the La{ko syncline (Rijavec, 1984) and Planina syncline by Dobje (Rijavec, 1977). Ecology: The genus Heterolepa is epi-faunal and is probably attached to hard substrates. It occurs in temperate to cold marine waters from the shelf to bathyal (Murray, 1991). It is an oxic indicator (Rögl & Spezzaferri, 2003). The fossil species Heterolepa dutemplei from the Central Paratethys shows wide depth-range, with an optimum in the sublitto-ral. It is euryhaline but within euhaline limits (Cicha & Zapletalová, 1967).
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              307
Familia Gavelinellidae Hofker, 1956
Subfamilia Gavelinellinae Hofker, 1956
Genus Hansenisca Loeblich & Tappan, 1987
Hansenisca soldanii (d’Orbigny, 1826) (Pl. 5, figs. 1a–c)
1826 Gyroidina soldanii – d’Orbigny, 112.
1956 Gyroidina soldanii d’Orbigny – Longi-nelli, 71, tav. XIV, figg. 16a–b.
1960 Gyroidina soldanii d’Orbigny – Gian-nini & Tavani, 42, tav. VII, figg. 15–16.
1975 Gyroidinoides soldanii (d’Orbigny) – Popescu, 103, pl. LXXXIV, figs. 2a–c.
1979 Gyroidinoides soldanii (d’Orbigny) – Popescu, 47, pl. XXVIII, figs. 6a–c.
1982 Gyroidina soldanii d’Orbigny – Dondi & Barbieri, tav. XL, fig. 1.
1985  Gyroidina soldanii d’Orbigny – Papp & Schmid, 60, Taf. 50, Fig. 4–9.
1986  Gyroidinoides soldanii (d’Orbigny) – Belanger & Berggren, 344, pl. 6, figs. 3a–c.
1987  Hansenisca soldanii (d’Orbigny) – Lo-eblich & Tappan, pl. 719, figs. 5–9.
1987 Gyroidina soldanii d’Orbigny – Reiser, 101, Taf. 12, Fig. 7, 10–11.
1991 Gyroidinoides soldanii (d’Orbigny) – Cimerman & Langer, 75, pl. 85, figs. 5–6.
1998 Hansenisca soldanii (d’Orbigny) – Cic-ha et al., 105, pl. 72, figs. 6–8.
2003 Gyroidinoides soldanii (d’Orbigny) – Rögl & Spezzaferri, pl. 8, fig. 4.
Material: Numerous tests in samples from all six sections (Tab. 2).
Description: Test is trochospirally enrolled, composed of three to four whorls. Whorls enlarge gradually in size. Spiral side is evolute and slightly convex, umbilical side is involute and highly convex. On the spiral side, the last whorl stands above the level of earlier stage. Equatorial section of the test is circular while the transverse section is conical. Last whorl is built of 9–10 chambers that appear trapezoidal on the spiral side, and triangular on the umbilical side. They enlarge slowly as added. Sutures are straight, oblique and depressed on the spiral side. On the umbilical side, they are straight, radial and flush; toward the umbilicus they may get incised. Whorl suture is depressed. Umbilicus is wide and deep. Periphery is angular; it is smooth in outline in the early part of the last whorl
and slightly lobate in the late part. Wall is calcareous and optically granular. It is finely perforate. Surface is smooth. Short slitlike aperture is interiomarginal and equatorial. It is bordered by a weak lip.
Remark: Hansenisca soldanii has been established as the type species of the genus Hansenisca Loeblich & Tappan, 1987. The main characteristic of the genus is having an open umbilicus which is surrounded by small umbilical chamber folia. Tests observed in this study show open umbilicus therefore they are classified in the genus Hansenisca.
Size: Test diameter is 0.32–0.35 mm and thickness 0.2 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to Late Upper Badenian (Virgulinella pertusa Zone). Reworked tests were found also in the Lower Sarmatian samples (Anomalinoi-des dividens Zone).
Occurrence: The species was first described on recent specimens from the Adriatic Sea (Italy). The species has existed from the Cretaceous (Ogniben, 1958). In Italy, it is known from the Upper Eocene (Ascoli, 1956) to Pleistocene (Dondi & Barbieri, 1982: ?Upper Oligocene to Pleistocene; Ogniben, 1958: Oligocene, Aqui-tanian; Giannini & Tavani, 1960: Miocene, Pliocene; Dieci, 1959: Tortonian to Pleistocene), and in Algeria from the Messi-nian (Poignant & Moissette, 1992).
The species is extant; it is known from the Atlantic, Pacific and Antarctica (Longinelli, 1956; Dieci, 1959: Atlantic, Pacific). It is noted also from the Mediterranean (Cimerman & Langer, 1991; Lo-eblich & Tappan, 1987) and Adriatic Sea (Dieci, 1959).
In the Central Paratethys, it appears from the Egerian to the end of the Badeni-an (Cicha et al., 1998) although some authors report about its earlier appearance; from the Kiscellian in Croatia (Šiki}, 1985) and Hungary (Sztrŕkos, 1979: Upper Kis-cellian), and from the whole Oligocene in Bavaria (Reiser, 1987: Lower Rupelian – Lower Egerian). The species becomes abundant in the Karpatian (Cicha et al., 1998). In Croatia, it is noted also from the Middle Badenian (Bajraktarevi}, 1982), in Austria from the Karpatian (Rögl, 1998) and Early Lower Badenian (Rögl & Spez-zaferri, 2003), and in Romania from the Upper Badenian (Popescu, 1979).
308
Katarina Oblak
In Slovenia, the species has not been described and imaged yet. It is only noted from Lower Egerian to Upper Ba-denian sediments. It is mentioned from the Lower Egerian of the Celje syncline (Rijavec, 1984), La{ko syncline (Rijavec, 1976a, 1984, Dozet & Rijavec, 1994) and Planina syncline (Rijavec, 1977; Rijavec & Dozet, 1996), from the Upper Egerian of the Celje syncline (Rijavec, 1984; Dozet & Rijavec, 1994), La{ko syncline (Rijavec, 1977: subspecies G. soldanii girardana; Dozet et al., 1996, 1999) and Planina syncline (Rijavec & Dozet, 1996), from the Lower Badenian of the Celje syncline (Rijavec, 1978a), from the Karpatian of Slovenske gorice (Jelen & Rifelj, 2003), from the Middle Badenian of Slovenske gorice (Rijavec, 1974), Dravinjske gorice (Rijavec, 1975), La{ko syncline (Rija-vec, 1976a, 1984; Dozet & Rijavec, 1994), Planina syncline at Planina pri Sevnici (Rijavec, 1977) and Bizeljsko syncline (Dozet et al., 1998), and from the Upper Badenian of Slovenske gorice (Rijavec, 1974) and the La{ko syncline (Rijavec, 1984). Ecology: The species is characteristic for the deep bathyal and abyssal zones (Wenger, 1987). It occurs down to 1800 m and it is more common deeper than 550 m (Dieci, 1959). In the Tyrrhenian Sea, it is reported from the soft sediment at 210 m (Cimerman & Langer, 1991).
Genus Hanzawaia Asano, 1944
Hanzawaia boueana (d’Orbigny, 1846) (Pl. 5, figs. 2a–c)
1846 Truncatulina boueana – d’Orbigny, 169, Tab. IX, fig. 24–26.
1967 Hanzawaia boueana (d’Orbigny) – Cic-ha & Zapletalová, 145, Taf. 10, Fig. 1a–c.
1975 Hanzawaia boueana (d’Orbigny) – Cic-ha et al., 242, Taf. 2, Fig. 4a–c.
1975 Hanzawaia boueana (d’Orbigny) – Po-pescu, 79, pl. LXXXVII, figs. 3a–c, pl. LXXXVIII, figs. 1a–c.
1985 Cibicides boueanus (d’Orbigny) – Papp & Schmid, 64, Taf. 56, Fig. 6–9.
1998 Hanzawaia boueana (d’Orbigny) – Cic-ha et al., 106, pl. 72, figs. 9–11.
2007 Hanzawaia boueana (d’Orbigny) – Schütz et al., 457, Taf. 6, Fig. 1a–c.
Material: Numerous tests in samples from all six sections (Tab. 1).
Description: Flattened test is very low trochospiral. It is circular in outline. Spiral side is flat or slightly concave and convolute, while the umbilical side is convex and involute. Whorls enlarge rapidly in size. The last whorl comprises 8–10 chambers that are crescentic in shape. They gradually increase in size. Sutures are strongly curved backward and weakly depressed on both sides. Periphery is angulate. It is smooth in outline, or may be slightly lobate toward the end of the last whorl. Wall is calcareous, optically granular and moderately perforate. Surface is smooth. Aperture is interio-marginal and equatorial, and continues on the spiral side.
Size: Test diameter is 0.3–0.35 mm and thickness 0.1 mm.
Age: From the Early Lower Badenian (Lower Lagenidae Zone) to Late Upper Badenian (Virgulinella pertusa Zone). Reworked tests were found also in the Lower Sarmatian samples (Anomalinoi-des dividens Zone).
Occurrence: The species was first described from Late Lower Badenian of the Vienna basin. Its first appearance was placed in the Eocene (Ogniben, 1958). In Australia, it is noted from the Lower Miocene (Li & McGowran, 2000), in Italy from the Tortonian to Pleistocene (Dieci, 1959; Ogniben, 1958: Langhian to Quaternary; Giannini & Tavani, 1960: Miocene, Pliocene), and in Algeria from the Messinian (Poignant & Moissette, 1992). In the Central Paratethys, it is known from the Egerian to the end of the Bade-nian (Cicha et al., 1975, 1998); it is numerous particularly in the Upper Lage-nidae Zone (Papp & Schmid, 1985: Vienna basin). In Romania, it is noted from the Lower Miocene (Popescu, 1975), and in Croatia from the Upper Badenian (Pikija et al., 1984). Schütz et al. (2007) determined the species in Lower Sarmatian sediments where could be reworked from older sediments.
In Slovenia, the species has not been described and imaged yet. It is only noted as Hanzawaia boueana or Cibicides boueanus from Lower Egerian to Upper Badenian sediments. It is mentioned from the Lower Egerian of the La{ko syncline (Rijavec, 1984; Dozet et al., 1999), from
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              309
the Upper Egerian of the Celje syncline (Rijavec, 1984), from the Lower Badeni-an of the La{ko syncline (Rijavec, 1976a, 1984; Dozet et al., 1999), from the Middle Badenian of Dravinjske gorice (Rijavec, 1975), the Celje syncline (Rijavec, 1975, 1978a), La{ko syncline (Rijavec, 1976a, 1984, Dozet et al., 1996, 1999), Planina syncline by Trobni Dol (Petrica et al., 1995) and Planina pri Sevnici (Rijavec, 1977), and of the Kr{ko-Brežice plain (Dozet et al., 1998). It is known also from the Upper Badenian of Slovenske gorice (Rijavec, 1974), the La{ko syncline (Rija-vec, 1976a, 1984, Dozet et al., 1996) and Planina syncline by Trobni Dol (Petrica et al., 1995) and Škarnice (Rijavec, 1977). Ecology: Extant specimens of the genus Hanzawaia are epifaunal and attached to hard substrates. They are found in temperate to warm marine waters of the inner shelf (Murray, 1991).
Conclusions
In the Middle Miocene sediments of the Planina syncline, 85 species and 2 subspecies of the foraminiferal suborder Rotaliina have been determined. The following species show particular high abundance in all sections: Angulogerina angulosa, Trifarina bradyi, Sphaeroidina bulloides, Cibicidoi-des ungerianus, Nonion commune, Melonis pompilioides, Pullenia bulloides, Hetero-lepa dutemplei, Hansenisca soldanii and Hanzawaia boueana (Tab. 2). In the studied area, they are present already in the lowest Badenian biozone, the Lower Lagenidae Zone. The shortest stratigraphic range is seen for Trifarina bradyi, which ranges up to the Late Middle Badenian Uvigerina cf. pygmea Zone. Most of other abundant ro-taliins, Angulogerina angulosa, Cibicidoides ungerianus, Nonion commune, Melonis pom-pilioides and Pullenia bulloides occur up to the Early Upper Badenian Bolivina dilatata Zone, and species Sphaeroidina bulloides, Hansenisca soldanii and Hanzawaia bouea-na up to the Late Upper Badenian Virguli-nella pertusa Zone. The longest stratigrap-hic range is shown by the species Heterole-pa dutemplei which is found in the Trobni Dol section also in the Lower Sarmatian Anomalinoides dividens Zone. In Sarmati-an samples of the Imenska Gorca section, some other species are found (Sphaeroidina bulloides, Cibicidoides ungerianus, Pulle-
nia bulloides, Heterolepa dutemplei, Han-senisca soldanii and Hanzawaia boueana); but are considered to be reworked Badenian specimens.
All species, which are presented in this work, appear in the Central Paratethys from the beginning to the end of the Bade-nian. Few of them: Cibicidoides ungerianus, Nonion commune (Papp & Schmid, 1998), Pullenia bulloides and maybe also Han-zawaia boueana, if not reworked (Schütz, 2007) range further into the Sarmatian. In this view, the results of this study are comparable with findings of previous studies of the Central Paratethys. More interesting is the presence of Heterolepa dutemplei tests in the Lower Sarmatian sample of the Trob-ni Dol section. If they are not reworked this could be an evidence for an increased biostratigraphic range for the species within the region.
From Middle Miocene sediments of Slovenia, the species Angulogerina angulosa and Trifarina bradyi are identified for the first time. Longer stratigraphic ranges are seen for: Melonis pompilioides (extending into the Middle and Upper Badenian), Cibi-cidoides ungerianus and Nonion commune (extending into the Upper Badenian), and possibly for Heterolepa dutemplei (extending into the Sarmatian).
All foraminifera show high abundance from the Lower Badenian Lower Lageni-dae Zone up to the Early Upper Badenian Bolivina dilatata Zone. Abundance reduces in the following Late Upper Badenian V. pertusa Zone. Most species are indicators for deeper environments, from the shelf to bathyal or even abyssal zone: A. angulosa, T. bradyi, S. bulloides, C. ungerianus, M. pompilioides, P. bulloides, H. dutemplei and H. soldanii. The species A. angulosa, T. bra-dyi, C. ungerianus, M. pompilioides, P. bul-loides, H. dutemplei and H. boueana are known to be euhaline so indicate full marine conditions. The pattern of abundance of the investigated species can be interpreted as evidence of environmental change that occurred towards the end of the Middle Miocene; when shoaling within the sea occurred and brackish conditions developed (Ková~ et al., 2004, Oblak, 2006). The frequent epi-faunal high-oxygen indicators C. ungeria-nus and H. dutemplei show that the bottom waters were well oxygenated from the beginning of the Badenian at least up to the Early Upper Badenian (B. dilatata Zone).
Tabla 2. Distribution of rotaliinas in the studied sections (after Oblak, 2006). Columns represent a percentage of positive samples
(samples where the particular species is present).
AGE
B   A   D   E   N   I   A   N
SAR MAT IAN
LOWER
MIDDLE
UPPER
LOWER
BIOZONE FORAMINI FERA
Lower Lagenidae Z.
Upper Lagen Z
P. robusta
U. cf. pygmea
B dilatata
V. pertusa
A. dividens
rf*
«f
LJU
I
D
™ 0     n
JU
D
0    0         0    0
,(-'
sf
1
0
XL!
o   nö °.
ft             (h   0    D    0
ao       od
J?
,6s"'
DIL
una
1
1
Bi
JL
¦¦*¦
I
fal
O             0    0
^
J*'
nvC
nH
1
ICO
1
1'Ti                        ICO
D
I
D i
!¦¦<:-
1
<t?
P
\<K VK \<K                  IEQ
100                         100
100                  ICO
M
1
I
0   0         0   0
Tabela 2. Pojavljanje rotaliin v obravnavanih profilih (po Oblak, 2006). Stolpci predstavljajo odstotek pozitivnih vzorcev
(vzorcev, kjer je posamezna foraminifema vrsta prisotna).
BIOZONE FORAMINI FERA
Lower Lagenidae Z.
Upper Lagen. Z.
P. robusta
U cf. pygmea
B. dilatata
V. pertusa
A. dividens
Jfi
fr
*'
100               WO        HO
ICD K»               HO
100        ID               KD
1
0   0        0   0
,tf*
SP*
«r
!-.i.        :.¦-¦       \-. 100
ffll
UUJ
?Dil
ICO ICO                 W
II
100                                 1C0
a   ° ° ° I
*
9»
¦^
rfff
W
ICQ
W®         ¦
ill
I
ID
1CP
¦   Doli
I
in
Vi
fal
J?
&
100                                 :¦¦'.
KD       ICO       W (00
aT
105
.,- i
Jn
KD
ü
BD                 KO HO
1C0        HC 100 ICO KD
I
? Imenska Gorca ? Ftohov breg D Javorsica B Sveta Ana HTTobni Dol ¦ Drensko Ftebro
312
Katarina Oblak
In this paper, all species, except for the recent Angulogerina angulosa from the Adriatic Sea (Cimerman & Langer, 1991), are described for the first time in Slovenia.
Najpogostej{e srednjemiocenske rotaliine (podred Rotaliina, Foraminifera) Kozjanskega (vzhodna Slovenija)
Povzetek
Podred Rotaliina je bil dolo~en leta 1896 kot podred Rotalidae s strani avtorjev Delage & Herouard (v Rotaliina sta ga preimenovala Loeblich in Tappan leta 1961) (Loeblich & Tappan, 1987). Z ve~ kot 600 rodovi predstavlja drugi najve~ji foramini-ferni podred. Vklju~uje bento{ke foramini-fere ve~kamri~nih hi{ic s porozno steklasto lamelarno kalcitno steno. Glede na na~in rasti, predeljenost kamric, ornamentiranost povr{ine, prisotnost kanalnega sistema in izoblikovanost ustja so rotaliine zelo heterogene. Zaradi velike tolerance do okoljskih parametrov, kot so substrat, globina, temperatura, slanost in hrana, se pojavljajo v zelo razli~nih okoljih (Billman et al., 1980, Murray, 1991). Najstarej{e rotaliine so na-{li v triasnih plasteh, podred živi {e danes in je kozmopolitsko raz{irjen (Loeblich & Tappan, 1987).
V nalogi so obravnavane srednjemiocen-ske foraminifere podreda Rotaliina iz Planinske sinklinale na Kozjanskem (vzhodna Slovenija, sl. 1.). Vzor~ene so bile badenij-ske in sarmatijske plasti {estih profilov: Imenska Gorca, Plohov breg, Javor{ica, Sveta Ana, Trobni Dol in Drensko Rebro (sl. 1). Pobranih je bilo 159 vzorcev, ki segajo od spodnjebadenijskih spodnje lagenidne in zgornje lagenidne biocone, preko srednjeba-denijskih Pseudotriplasia robusta in Uvige-rina cf. pygmea biocon, zgornjebadenijskih Bolivina dilatata in Virgulinella pertusa biocon do spodnjesarmatijskih Anomalino-ides dividens in Elphidium hauerinum bio-
con (tab. 1.). Rotaliine se v mlaj{i sarmatij-ski bioconi Elphidium hauerinum ne pojavljajo ve~, zato biocona v nadaljevanju ni ve~ obravnavana. Iz podreda Rotaliina je bilo dolo~enih 85 vrst in 2 podvrsti. Najpogoste-j{e vzdolž vseh profilov so naslednje vrste: Angulogerina angulosa, Trifarina bradyi, Sphaeroidina bulloides, Cibicidoides unge-rianus, Nonion commune, Melonis pompi-lioides, Pullenia bulloides, Heterolepa du-templei, Hansenisca soldanii in Hanzawaia boueana. Vse omenjene vrste se pojavljajo na preiskanem obmo~ju od najnižje badenij-ske spodnje lagenidne biocone dalje (tab. 2). Med njimi kaže najkraj{i stratigrafski razpon vrsta Trifarina bradyi, ki je prisotna do mlaj{e srednjebadenijske Uvigerina cf. pyg-mea biocone. Ve~ina ostalih rotaliin, Angu-logerina angulosa, Cibicidoides ungerianus, Nonion commune, Melonis pompilioides in Pullenia bulloides, se pojavlja do starej{e zgornjebadenijske Bolivina dilatata biocone in vrste Sphaeroidina bulloides, Hansenis-ca soldanii in Hanzawaia boueana dalje do mlaj{e zgornjebadenijske Virgulinella per-tusa biocone. Najdalj{i stratigrafski razpon je razviden pri vrsti Heterolepa dutemplei, ki je bila najdena {e v starej{i spodnjesar-matijski Anomalinoides dividens bioconi. V sarmatijskih vzorcih profila Imenska Gorca so bile sicer najdene {e nekatere druge rota-liine: Sphaeroidina bulloides, Cibicidoides ungerianus, Pullenia bulloides, Heterolepa dutemplei, Hansenisca soldanii in Hanza-waia boueana, ki pa so bile glede na sprem-ljajo~o mikrofavno po vsej verjetnosti pre-ne{ene iz starej{ih, badenijskih plasti.
Vse vrste, ki so obravnavane v tej nalogi, se pojavljajo na obmo~ju Centralne Parate-tide od za~etka do konca badenija, vrsti Ci-bicidoides ungerianus in Nonion commune {e naprej v sarmatij (Papp & Schmid, 1998). V tem pogledu so rezultati te raziskave primerljivi z ugotovitvami predhodnih raziskav Centralne Paratetide. Zanimivej{a pa je prisotnost hi{ic vrste Heterolepa dutemplei v
Plate 1 – Tabla 1
1. Angulogerina angulosa (Williamson); a. side view (Ig 4), b. enlarged aperture with a toothplate (Ig 4).
1.  Angulogerina angulosa (Williamson); a. stranski pogled (Ig 4), b. pove~ano ustje z zobno plo{~ico (Ig 4).
2.  Trifarina bradyi Cushman; a. side view (Ig 4), b. enlarged aperture with a toothplate (Ig 4). 2. Trifarina bradyi Cushman; a. stranski pogled (Ig 4), b. pove~ano ustje z zobno plo{~ico (Ig 4).
Scale bar = 100 µm. Merilce = 100 µm.
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              313
Plate 1 – Tabla 1
314
Katarina Oblak
spodnjesarmatijskih plasteh profila Trobni Dol. ^e hi{ice niso prene{ene, bi bil s tem lahko dokazan dalj{i stratigrafski razpon vrste.
V srednjemiocenskih sedimentih Slovenije sta vrsti Angulogerina angulosa and Trifarina bradyi dolo~eni prvi~. Dalj{i stra-tigrafski razpon je dokazan za vrste: Me-lonis pompilioides (raz{irjen v srednji in zgornji badenij), Cibicidoides ungerianus in Nonion commune (raz{irjen v zgornji bade-nij) in morda tudi vrste Heterolepa dutem-plei (raz{irjen v sarmatij).
Predstavljene foraminifere so zelo {tevil-~ne od spodnjebadenijske spodnje lagenidne biocone vse do starej{e zgornjebadenijske biocone Bolivina dilatata, in skoraj izginejo v naslednji, mlaj{i zgornjebadenijski bio-coni V. pertusa. Ve~ina teh vrst je zna~ilnih za globlja okolja, od {elfa do globine bati-ala ali celo abisala: A. angulosa, T. bradyi, S. bulloides, C. ungerianus, M. pompilioides, P. bulloides, H. dutemplei in H. soldanii. Vrste A. angulosa, T. bradyi, C. ungerianus, M. pompilioides, P. bulloides, H. dutemplei in H. boueana so evhaline in kažejo na morsko okolje. Vzorec njihovega pojavljanja je verjetno posledica spremembe okolja, do katere je pri{lo proti koncu srednjega miocena; ko je za~elo morje plitveti in se oslajevati (Ková~ et al., 2004, Oblak, 2006). Pogosta epifavnisti~na indikatorja oksi~nega okolja, C. ungerianus in H. dutemplei, kažeta, da je bila voda pri dnu dobro prezra~ena od za-~etka badenija vsaj do starej{ega zgornjega badenija (B. dilatata biocona).
Vse vrste, razen recentne Angulogerina angulosa iz Jadranskega morja (Cimerman & Langer, 1991), so v Sloveniji opisane prvi~.
Acknowledgements
I am grateful to Ivan Rakovec Institute of Palaeontology, ZRC SAZU for allowing me to take SEM images. I wish to thank to M.Sc. Bogoljub Ani~i} for his help by the field work, to M.Sc. Franci Cimerman for checking my determination of benthic fo-raminifera, and to Dr. Katica Drobne for her constructive review of the manuscript. Special thanks are due also to Dr. Kevin R. Brown for English corrections of the text.
References – Literatura
Ani~i}, B. & Juri{a, M. 1984: Osnovna geo-lo{ka karta SFRJ 1: 100 000, list Rogatec L 33–68, Zvezni geolo{ki zavod, Beograd.
Ani~i}, B. & Juri{a, M. 1985: Tolma~ k Osnovni geolo{ki karti SFRJ 1: 100 000, list Rogatec L 33–68, 76 str., Zvezni geolo{ki zavod, Beograd.
Ani~i}, B. & Ogorelec, B. 1996: Badenij-ski rodolit na Kozjanskem. – Geologija, 37/38, (1994/95), 225–249, Ljubljana
Ani~i}, B., Ogorelec, B., Kralj, P. & Mi-{i~, M. 2002: Litolo{ke zna~ilnosti terciarnih plasti na Kozjanskem. Geologija, 45/1, 213–246
Ani~i}, B., Ogorelec, B. & Dozet, S. 2004: Geolo{ka karta Kozjanskega, 1 : 50 000, Geolo{ki zavod Slovenije, Mladinska knjiga, Ljubljana.
Ascoli, P. 1956: Microfaune della serie eo-cenica di Rio Repregoso e della serie oligoceni-ca superiore di Mombisaggio – Mongariolo (Tor-tona – Alessandria). – Riv. Ital. Paleont. Strat., LXII(3), 153–196, Milano.
Bajraktarevi}, Z. 1978: Gornjetortonska starost sedimenata Zapre{i}-brijega kod Samo-bora. – Geol. Vjesnik, 30(1), 63–67, Zagreb.
Bajraktarevi}, Z. 1979: Mikropaleontolo-{ka i biostratigrafska istraživanja tortona (bade-na) nekih lokaliteta Samoborskog gorja, Ple{ivi-ce i Marija – Gori~kih brda. – Geol. Vjesnik, 31, 37–47, Zagreb.
Bajraktarevi}, Z. 1982: Mikrofosili i na-nofosili sedimenata badena (»tortona«) podru~ja Sokolovac u Pože{koj gori. – Geol. Vjesnik, 35, 43–46, Zagreb.
Barbieri, R. & d’Onofrio, S. 1984: Bent-hic Foraminifera of the Fangario Formation (Ca-
Plate 2 – Tabla 2
1. Sphaeroidina bulloides d’Orbigny; a. umbilical side (J 28), b. side view (Pb 23).
1.  Sphaeroidina bulloides d’Orbigny; a. umbilikalna stran (J 28), b. stranski pogled (Pb 23).
2.  Cibicidoides ungerianus (d’Orbigny); a. spiral side (Pb 23), b. umbilical side (Pb 23), c. side view (Pb 23).
2. Cibicidoides ungerianus (d’Orbigny); a. spiralna stran (Pb 23), b. umbilikalna stran (Pb 23), c. stranski pogled (Pb 23).
Scale bar = 100 µm. Merilce = 100 µm.
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              315
Plate 2 – Tabla 2
316
Katarina Oblak
gliari, Sardinia). – Boll. Soc. Paleont. Ital., 23(2), 439–447, Modena.
Barker, R. W. 1960: Taxonomic notes on the species figured by H. B. Brady in his report on the Foraminifera dredged by H.M.S. challenger during the years 1873–1876. Accompanied by a reproduction of Brady’s plates. – Soc. Econom. Paleont. Miner., Spec. Publ., 9, 238 pp., Tulsa, Oklahoma.
Basov, I. A. & Krasheninnikov, V. A. 1995: Stratigraphy and Foraminifers of the Pliocene and Quaternary Deposits of the Timor Trough (the Indian Ocean). – 112 pp., Nau~nii mir, Moskva.
Belanger, P. E. & Berggren, W. A. 1986: Neogene benthic foraminifera of the Hatton-Roc-kall Basin. – Micropaleontology, 32(4), 324–356, New York.
Billman, H., Hottinger, L. & Oester-le, H. 1980: Neogene to Recent Foraminifera from the Indopacific Ocean; their Canal System, their Classification and their Stratigraphic Use. In: Hottinger, L. (ed.), Rotaliid Foramini-fera, Schweizerische Paläontologische Abhandlungen, 101, 71–113, 39 pls., Birkhäuser Verlag, Basel.
Bolli, H. M., Beckmann, J.-P. & Saun-ders, J. B. 1994: Benthic foraminiferal biostra-tigraphy of the south Caribbean region. – Cambridge University Press, 408 pp., Cambridge.
Buser, S. 1977: Osnovna geolo{ka karta SFRJ 1: 100 000, list Celje L 33–67, Zvezni geolo{ki zavod, Beograd.
Buser, S. 1979: Tolma~ k Osnovni geolo{ki karti SFRJ 1: 100 000, list Celje, 72 str., Zvezni geolo{ki zavod, Beograd.
Cherif, O. H., El-Sheikh, H. A. & Mohamed, S. I. 1994: Paleoecology of the Oligo-Miocene in the subsurface of the northeastern reaches of the Nile Delta, Egypt. – N. Jb. Geol. Paläont. Mh., 12, 703–725, Stuttgart.
Cicha, I. & Zapletalová, I. 1967: Die Fo-raminiferen der Karpatischen Serie. In: Cicha, I., Sene{, J. & Tejkal, J. (Eds.), Chronostratigraphie und Neostratotypen, Miozän der Zentralen Para-tethys, Bd.I, Karpatien, 104–148, VEDA, Bratislava.
Cicha, I., ^tyroká, J. & Horváth, M. 1975: Die Foraminiferen des Egerien. In: Bresten-ska, E. (Ed.), Chronostratigraphie und Neostrato-typen, Miozän der Zentralen Paratethys, Bd. V, Egerien, 233–277, VEDA, Bratislava.
Cicha, I., Rögl, F. , Rupp, C. & ^tyroká, J. 1998: Oligocene – Miocene foraminifera of the Central Paratethys. – Abh. Senckenberg. Naturforsch. Ges., 549, 1–325, Frankfurt am Main.
Cicha, I., Zapletalová, I., Papp, A., ^tyroká, J. & Lehotayova, R. 1971: Die Fo-raminiferen der Eggenburger Schichten-gruppe (incl. Arcellinida). In: Steininger, F. & Sene{, J. (Eds.), Chronostratigraphie und Neostratotypen, Miozän der Zentralen Paratethys, Bd. II, Eggen-burgien, 234–355, VEDA, Bratislava.
Cimerman, F. & Langer, M. R. 1991: Mediterranean Foraminifera. – Opera IV. classis: Hi-storia Naturalis, Slovenska akademija znanosti in umetnosti, 30, 118 pp., 93 pls., Ljubljana.
Cimerman, F., Jelen, B. & Skaberne, D. 2006: Late Eocene benthic foraminiferal fauna from clastic sequence of the Socka – Dobrna area and its chronostratigraphic importance (Slovenia). – Geologija, 49(1), 7–44, Ljubljana.
Debenay, J.-P & Konate, S. 1987: Les Foraminifčres actuels des îles de Los (Guinée). Premier inventaire, comparaison avec les microfaunes voisines. – Rev. Paléobiol., 6(2), 213–227, Geneve.
Debenay, J.-P., Ba, M., Ly, A. & Sy, I. 1987: Les écosystčmes paraliques du Sénegal. Description, répartition des peuplements de foraminifčres bentiques. – Rev. Paléobiol., 6(2), 229–255, Geneve.
Dieci, G. 1959: I foraminiferi tortoniani di Montegibbio e Castel Vetro. – Palaeontographia Italica, LIV (n. ser. vol. XXIV), 1–113, Pisa.
Dondi, L. & Barbieri, R. 1982: Foramini-feri Padani, Atlante iconografico e distribuzione stratigrafica (Terziario e Quaternario ). – AGIP S.p.A., 52 pls., Milano.
Dozet, S. & Rijavec, L. 1994: On the geological relations of the Šentjur – Planina – Trob-ni Dol – Loka at Žusem area (Eastern Slovenia). – Rudarsko metalur{ki zbornik, 41, 27–41, Ljubljana.
Dozet, S., Rijavec, L. & Grad, K. 1999: Western Kozje Area Tertiary (Eastern Slovenia). – Rudarsko metalur{ki zbornik, 46(3), 475–489, Ljubljana.
Dozet, S., Rijavec, L. & Stojanovi~, B. 1996: Geological Relations in the La{ko Syncli-norium Area between Lahomno and Grahov{e. – Rudarsko metalur{ki zbornik, 43(1–2), 37–53, Ljubljana.
Dozet, S., Rijavec, L., Ani~i}, B., Škerlj, Ž. & Stojanovi~, B. 1998: Neogene Beds of the Kr{ko – Brežice Plain and its Borderland (Southern Slovenia). – Materiali in okolje, 45(3–4), 375–404, Ljubljana.
den Dulk, M., Reichart, G. J., Memon, G. M., Roelofs, E. M. P. , Zachariasse, W. J. & Van der Zwaan, G. J. 1998: Bent-hic foraminiferal response to variations in surface
Plate 3 – Tabla 3
1. Nonion commune (d’Orbigny); a. side view (Ig 4), b. front view (Ig 4).
1.  Nonion commune (d’Orbigny); a. stranski pogled (Ig 4), b. pogled od spredaj (Ig 4).
2.  Melonis pompilioides (Fichtel & Moll); a. side view (Pb 23), b. front view (Pb 23). 2. Melonis pompilioides (Fichtel & Moll); a. stranski pogled (Pb 23), b. pogled od spredaj (Pb 23).
Scale bar = 100 µm. Merilce = 100 µm.
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              317
Plate 3 – Tabla 3
318
Katarina Oblak
water productivity and oxygenation in the northern Arabian Sea. – Mar. Micropal., 35, 43–66, Amsterdam.
Ellis, B. F. & Messina, A. R. 1940: Catalogue of Foraminifera. Am. Mus. Nat. Hist., Spec. Publ., New York.
Emiliani, C. 1954: The Oligocene microfa-unas of the Central part of the Northern Apennines. – Palaeontographia Italica, X LVIII (n. ser. vol. XVIII), 77–184, Pisa.
Filipescu, S. & Girbacea, R. 1997: Lower Badenian sea-level drop on the Western border of the Transylvanian basin: Foraminiferal pale-obathymetry and stratigraphy. – Geol. Carpat., 48(5), 325–334, Bratislava.
Giannini, E. & Tavani, G. 1960: Fora-miniferi miocenici e pliocenici di un sondaggio effettuato in Val di Trossa (Toscana). – Palaeon-tographia Italica, LV (n. ser. vol. XXV), 21–90, Pisa.
Gohrbandt, K. 1961: Die Kleinforaminife-renfauna des obereozänen Anteils der Reigruber Serie bei Bruderndorf (Bezirk Korneuburg, Niederösterreich). – Mitt. Geol. Ges., 54, 55–145, Wien.
Lourens, L., Hilgen, F., Shackleton, N. J., Laskar, J. Wilson, D. 2004: The Neogene period. – In: Gradstein, F. M., Ogg, J. G. & Smith, A.G. (Eds.), A Geologic Time Scale 2004, Part III, Geologic Periods, 409–440, Cambridge University Press, Cambridge.
Hasson, P. F. & Fischer, A. G. 1986: Observations on the Neogene of northwestern Ecuador. – Micropaleontology, 32(1), 32–42, New York.
Hottinger, L., Halicz, E. & Reiss, Z. 1993: Recent Foraminiferida from the Gulf of Aqaba, Red Sea. – Dela IV. razreda SAZU, 33, 179 pp., Ljubljana.
Jelen, B. & Rifelj, H. 2003: The Karpatian in Slovenia. – In: Brzobohaty, R., Cicha, I., Ková~, M. & Rögl, F. (Eds.), The Karpatian – a Lower Miocene Stage of the Central Paratethys, Masaryk University Brno, 133–139, Brno.
Kolar, T. 1978: Oligocenska mikrofavna iz Hrastnika. – Rudarsko metalur{ki zbornik, 4, 407–415, Ljubljana.
Ková~, M., Baráth, I., Harzhauser, M., Hlavatý, I. & Hudá~ková, N. 2004: Miocene depositional systems and sequence stratigraphy of the Vienna Basin. - Courier Forschungsinstitut Senckenberg, 246, 187-212, Frankfurt am Main.
Lévy, A., Mathieu, R., Poignant, A. & Rosset-Moulinier, M. 1998: 44. Data Report:
Distribution of Pleistocene Benthic Foraminifers from the Eastern Equatorial Atlantic Ocean. – In: Mascle, J., Lohmann, G.P. & Moullade, M. (Eds), Proceedings of the Ocean Drilling Program, Scientific Results, Vol. 159, 605–610, Texas.
Li, Q. & McGowran, B. 2000.: Miocene foraminifera from Lakes Entrance Oil Shaft, Gippsland, southeastern Australia. – Memoir of the Association of Australasian Palaeontologists, 22, 1–142, Canberra.
Loeblich, A. R. Jr. & Tappan, H. 1987: Foraminiferal Genera and their Classification. – Vol. 1–2, 970 pp., 847 pls., Van Nostrand Reinhold, New York.
Longinelli, A. 1956: Foraminiferi del Cala-briano e Piacenziano di Rosignano Marittimo e della Val di Cecina. – Palaeontographia Italica, XLIX (n. ser. vol. XIX), 99–214, Pisa.
Miller, K. G. & Katz, M. E. 1987: Oligoce-ne to Miocene benthic foraminiferal and abyssal circulation changes in the North Atlantic. – Mi-cropaleontology, 33(2), 97–149, New York.
Murray, J. W. 1991: Ecology and palaeoeco-logy of benthic foraminifera. – Longman Scientific and Technical, John Wiley & Sons Inc., 397 pp., New York.
Murray, J. W. 2003: An illustrated guide to the benthic foraminifera of the Hebride-an Shelf, West of Scotland, with notes on their mode of life. – Palaentologia Electronica, 5(1), 31 pp, 1.4MB; http://palaeo-electronica.org/pa-leo/2002_2/guide/issue2_02.htm (read in May, 2006).
Oblak, K. 2006: Foraminiferna taksonomija, biostratigrafija in paleoekologija badenija v Planinski sinklinali (vzhodna Slovenija, Centralna Paratetida). Ph.D. Thesis. Ljubljana: University of Ljubljana, 310 pp. 60 pls.
Ogniben, L. 1958: Stratigrafia e microfaune del terziario della zona di Caiazzo (Caserta). – Riv. Ital. Paleont., LXIV/3, 199-286, Milano.
D’Orbigny, A. 1826: Tableau Méthodique de la Classe des Céphalopodes. Ann. Sci. D’Hist. Nat., Ser. 7, 7–150, Paris.
D’Orbigny, A. 1846: Foraminifčres fossiles du Bassin Tertiaire de Vienne (Autriche). – 312 pp., Gide et Comp, Paris.
Papp, A. & Schmid, M. E. 1985: Die Fossilen Foraminiferen des Tertiären Beckens von Wien. Revision der Monographie von Alcide d’Orbigny (1846). – Abh. Geol. Bundesanst., 37, 311 pp., Wien.
Parisi, E. 1981: Distribuzione dei forami-niferi bentonici nelle zone batiali del Tirreno e
Plate 4 – Tabla 4
1. Pullenia bulloides (d’Orbigny); a. side view (Pb 23), b. front view (Pb 23).
1.  Pullenia bulloides (d’Orbigny); a. stranski pogled (Pb 23), b. pogled od spredaj (Pb 23).
2.  Heterolepa dutemplei (d’Orbigny); a. spiral side (Pb 23), b. umbilical side (Pb 23), c. side view (Pb 23).
2. Heterolepa dutemplei (d’Orbigny); a. spiralna stran (Pb 23), b. umbilikalna stran (Pb 23), c. stranski pogled (Pb 23).
Scale bar = 100 µm. Merilce = 100 µm.
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              319
Plate 4 – Tabla 4
320
Katarina Oblak
del Canale di Sicilia. – Riv. Ital. Paleont., 87(2), 293–328, Milano.
Petrica, R., Rijavec, L. & Dozet, S. 1995: Stratigraphy of the Upper Oligocene and Miocene beds in the Trobni Dol area (Kozjansko). – Rudarsko metalur{ki zbornik, 42(3–4), 127–141, Ljubljana.
Pikija, M., Šiki}, K. & Šiki}, L. 1984: Miocen na lokalitetima Ba~uga i Jurjev~ani (sre-di{nja Hrvatska). – Geol. Vjesnik, 37, 65–80, Zagreb.
Piller, W. E., Egger, H., Erhart, C. W. , Gross, M., Harzhauser, M., Hubmann, B., van Husen, D., Krenmayr, H.-G., Kry-styn, L., Lein, R., Lukeneder, A., Mandl, G. W. , Rögl, F. , Roetzel, R., Rupp, C., Schnabel, W., Schönlaub, H. P. , Summes-berger, H., Wagreich, M. & Wessely, G. 2004: Die stratigraphische Tabelle von Österreich 2004 (sedimentäre Schichtfolgen), Gerin, Wolkersdorf.
Poignant, A. 1983: The Case Cocuzza Section, Benthonic Foraminifera. In search of the Palaeogene/Neogene boundary stratotype. – Riv. Ital. Paleont. Strat., 89(4), 465, Milano.
Poignant, A. & Moissette, P. 1992: Fora-miniferes bentiques des intercalations marneuses d’une serie diatomitique du Messinien d’Algerie. – N. Jb. Geol. Paläont. Mh., 11, 657–674, Stuttgart.
Popescu, G. 1975: Études des foraminifčres du miocčne inférieur et moyen du nord-ouest de la Transylvanie. – Mémoires Inst. Géol. Géophys., XXIII, 5–121, Bucarest.
Popescu, G. 1979: Kossovian foraminifera in Romania (IUGS-IGCP Project 25: Stratigraphic correlation of the Tethys-Paratethys Neogene). – Mémoires Inst. Géol. Géophys., XXIX, 5–64, Buchurest.
Premoli Silva, I., 1960: Le Buliminidae del Langhiano delle Langhe (1). – Riv. Ital. Paleont., LXVI(4), 551–589, Milano.
Reiser, H. 1987: Die Foraminiferen der bayerischen Oligozän – Molasse; Systematik, Stra-tigraphie und Paläobathymetrie. – Zitteliana, 16, 3–131, München.
Rijavec, L. 1974: Korelacija miocenskih plasti v vzhodni Sloveniji, I. faza. Arhiv geolo{kega zavoda Slovenije, 55 str., Ljubljana.
Rijavec, L. 1975: Korelacija miocenskih plasti v vzhodni Sloveniji, II. faza. Arhiv geolo{kega zavoda Slovenije, 63 str., Ljubljana.
Rijavec, L. 1976a: Korelacija miocenskih plasti v vzhodni Sloveniji, III. faza. Arhiv geolo-{kega zavoda Slovenije, 52 str., Ljubljana.
Plate 5 –
1. Hansenisca soldanii (d’Orbigny); a. spiral side (Pb
1.  Hansenisca soldanii (d’Orbigny); a. spiralna stran pogled (Pb 23).
2.  Hanzawaia boueana (d’Orbigny); a. spiral side (Pb
2. Hanzawaia boueana (d’Orbigny); a. spiralna stran pogled (J 32).
Scale bar = 100 µm. Merilce = 100 µm.
Rijavec, L. 1976b: Biostratigrafija miocena v Slovenskih goricah. – Geologija, 19: 53–82, Ljubljana.
Rijavec, L. 1977: Korelacija miocenskih plasti v vzhodni Sloveniji, I V. faza. Arhiv geolo{kega zavoda Slovenije, 56 str., Ljubljana.
Rijavec, L. 1978a: Korelacija miocenskih plasti v vzhodni Sloveniji, V. faza. Arhiv geolo-{kega zavoda Slovenije, 39 str., Ljubljana.
Rijavec, L. 1978b: Tortonska in sarmatska mikrofavna v zahodnem delu Slovenskih goric. – Geologija, 21, 209–238, Ljubljana.
Rijavec, L. 1984: Oligocen i miocen podru~-ja izmedju Rudnice i Bo~a (isto~na Slovenija) na osnovi mikrofosila. – Sveu~ili{te u Zagrebu, Pri-rodoslovno-matemati~ki fakultet Zagreb, disertacija, 141 pp., Zagreb.
Rijavec, L. & Dozet, S. 1996: Lithostra-tigraphy and biostratigraphy of the Upper Oli-gocene and Miocene beds from the Central Sava Folds (Slovenia). – Rudarsko metalur{ki zbornik, 43(1–2), 11–22, Ljubljana.
Robertson, B. E. 1998: Systematics and pa-leoecology of the benthic Foraminiferida from the Buff Bay section, Miocene of Jamaica. – Micro-paleontology, 44(2), 266 pp., New York.
Rögl, F. 1969: Die miozäne Foraminiferen-fauna von Laa an der Thaya in der Molassezone von Niederösterreich. – Mitt. Geol. Ges., 61, 63–123, Wien.
Rögl, F. 1998: Foraminiferenfauna aus dem Karpat (Unter-Miozän) des Korneuburger Beckens. – Beitr. Paläont., 23, 123–173, Wien.
Rögl, F. & Spezzaferri, S. 2003: Forami-niferal paleoecology and biostratigraphy of the Mühlbach section (Gaindorf Formation, Lower Badenian), Lower Austria. – Ann. Naturhist. Mus. Wien, 104 (A), 23–75, Wien.
Salaj, J. 1992: The Foredeep Miocene of Bou Sefra in Northern Tunisia. – Geol. Carpath., 43(5), 295–304, Bratislava.
Schütz, K., Harzhauser, M., Rögl, F. , ]ori}, S. & Galovi}, I. 2007: Foraminiferen und Phytoplankton aus dem unteren Sarmatium des südlichen Wiener Beckens (Petronell, Niederösterreich). – Jahrb. Geol. Bundesanst., 147(1+2), 449–488, Wien.
Sgarrella, F. & Moncharmont Zei, M. 1993: Benthic foraminifera of the Gulf of Naples (Italy): systematics and autoecology. – Boll. Soc. Paleont. Ital., 32(2), 145–264, Modena.
Szczechura, J. 2000: Age and evolution of depositional environments of the supra-evapo-ritic deposits in the northern, marginal part of the Carpathian Foredeep: micropalaeontological
Tabla 5
23), b. umbilical side (Pb 23), c. side view (Pb 23). (Pb 23), b. umbilikalna stran (Pb 23), c. stranski
23), b. umbilical side (Pb 23), c. side view (J 32). (Pb 23), b. umbilikalna stran (Pb 23), c. stranski
Most abundant Middle Miocene rotaliinas (suborder Rotaliina, Foraminifera) of Kozjansko ...              321
Plate 5 – Tabla 5
evidence. – Geological Quarterly, 44(1), 81–100, Warszawa.
Sztrŕkos, K. 1979: La stratigraphie, paléoé-cologie, paléogéographie et les Foraminifčres de l’Oligocčne du nord-est de la Hongrie. – Cahiers Micropaléontologie, 3, 95 pp., Paris.
Šiki}, L. 1967: Torton i sarmat jugozapadnog dijela Medvednice na osnovu favne foraminifera. – Geol. vjesnik, 20, 127–135, Zagreb.
Šiki}, L. 1985: The Rupelian in the area of Ravna Gora (northwestern Croatia) based on fo-raminiferous fauna. – Geol. vjesnik, 38, 73–80, Zagreb.
Vénec-Peyré, M.-T. 2005: Les Planches inédites de Foraminifčres d’Alcide d’Orbig-ny, Publ. Scient. Mus. Paris, MNHN, 302 pp., Paris.
Violanti, D. 1996: Taxonomy and distribution of recent benthic foraminifers from Terra Nova Bay (Ross Sea, Antarctica), Oceanographic
Campaign 1987/1988. – Palaeontographia Italica, 83, 25–71, Pisa.
Wenger, W. F. 1987: Die Foraminiferen des Miozäns der bayerischen Molasse und ihre stra-tigraphische sowie paläogeographische Auswertung. – Zitteliana, 16, 173–340, München.
Wiegank, F. 1972: Ökologische Analyse quartärer Foraminiferen (Beitrag zur Quartär-stratigraphie in der nördlichen Deutschen Demokratischen Republik). – Geologie, Zeitsch. Ge-sam. Geol. Wiss., 77, 1–111, Berlin.
Williamson, W. C. 1858: On the Recent Fo-raminifera of Great Britain. – Ray Society, I–XX, 107 pp., 6 pls., London.
Yassini I. & Jones, B. G. 1995: Recent Fo-raminiferida and Ostracoda from estuarine and shelf environments on the southeastern coast of Australia. – 484 pp., The University of Wollon-gong Press, Wollongong.