GeolCarp_Vol70_No4_279

GEOLOGICA CARPATHICA

, AUGUST 2019, 70, 4, 279–297

doi: 10.2478/geoca-2019-0016

www.geologicacarpathica.com

Turbidite sedimentology, biostratigraphy and paleoecology:

A case study from the Oligocene Zuberec Fm.

(Liptov Basin, Central Western Carpathians)

DUŠAN STAREK



, VLADIMÍR ŠIMO, SILVIA ANTOLÍKOVÁ and TOMÁŠ FUKSI

Earth Science Institute of the Slovak Academy of Sciences, Dúbravská cesta 9, 840 05 Bratislava, Slovakia;



dusan.starek@savba.sk

(Manuscript received December 17, 2018; accepted in revised form June 4, 2019)

Abstract: Outcrops of a thick turbiditic succession are exposed on the northern bank of the Liptovská Mara reservoir

near Liptovská Ondrašová and Ráztoky. The section consists of rhythmic, predominantly thin- to medium-bedded

turbidites of the Rupelian age. Their biostratigraphy is based on the calcareous nannofossils. Facies associations of

these deposits represent different components of depositional lobe deposits in the turbidity fan system, including mainly

the lobe fringe and lobe distal fringe/inter-lobe facies associations and locally the medium bedded deposits of the lobe

off-axis facies association. This interpretation is supported by statistical analysis. The deep-sea turbiditic deposits contain

trace fossil associations, which include deep-tier fodinichnia and domichnia up to shallow-tier graphoglyptids. Paleo-

current measurements indicate that the majority of sedimentary material was transported from SW and W.

Keywords: Western Carpathians, Oligocene, turbidites, trace fossils, calcareous nannofossils.

Introduction

The Oligocene sand-rich turbiditic system represents an im-

portant component of the Central Carpathian Paleogene Basin

(CCPB). Turbidites form a large part of the Liptov Depression

infilling, which is located in the northern part of the CCPB,

but in contrast to the adjacent regions (e.g., Orava–Podhale or

Spišská Magura), deposit outcrops are poor in the Liptov

Depression and larger sedimentary profiles, suitable for sedi-

mentological, biostratigraphic or paleoecological studies are

scarce currently. We present the results of research on an un-

usual section of a turbidite series which is exposed on

the banks of the Liptovská Mara Reservoir near Liptovská

Ondrašová village (north-west edge of the Liptovský Mikuláš

town) (Fig. 1C, D). This turbidite succession offers more than

700 completely exposed beds and provides a unique opportu-

nity to study vertical variation in bed thickness and sedimen-

tary structures. Occurrence of turbidite facies, their frequency

and vertical relationships, the sandstone and mudstone ratio

are important features used for discrimination of facies asso-

ciations and interpretation of the depositional environment.

Measurements of numerous paleocurrent indicators allowed

determinations of the main paleotransport direction in this part

of the basin. Detailed biostratigraphic analysis of calcareous

nannofossils through the entire section allowed dating of these

turbidite series. Paleoenvironmental evidence from study of

trace fossils is beneficial within a section that lacks macro fos-

sils. Only sporadic attention has been paid to trace fossils

within the Liptov Depression of the CCPB (Plička 1983, 1984,

1987; Plička et al. 1990).

Geological settings

The CCPB lies inside the Western Carpathian Mountain

chain (Fig. 1A) and belongs to the basinal system of the Peri-

and Paratethyan seas. The CCPB opening and evolution is

probably related to crustal thinning, either as a result of sub-

crustal erosion (e.g., Kázmér et al. 2003), or due to the exten-

sional collapse of the overthickened Central Western

Carpathian crust and the pull of the External Western

Carpathian oceanic lithosphere retreating subduction

(Plašienka & Soták 2015; Kováč et al. 2016).

The basin covered a large part of the Central Western

Carpathian area (Fig. 1A, B) and is mainly filled up with

marine, predominantly turbidite deposits which overlap the

nappe units substrates and their thickness reach up to 1000 m.

Their age ranges from the Bartonian (e.g., Samuel & Fusán

1992; Gross et al. 1993) to the Late Oligocene (cf. Olszewska

& Wieczorek 1998; Gedl 2000; Soták et al. 2001, 2007;

Garecka 2005). The CCPB sediments are preserved in many

structural sub-basins (Fig. 1B), located in the Žilina, Rajec,

Turiec, Orava, Podhale, Liptov, Poprad, and Hornád regions

as well as in the Spišská Magura, Levočské vrchy and Šarišská

vrchovina Mts.

The study area is a part of the Liptov Depression which is

one of the largest inner-Carpathian depressions. The Liptov

Depression is formed predominantly by the CCPB sediments

overlain by Quaternary deposits of variable thickness. Paleo-

gene deposits are bounded by the Mesozoic Central Carpathian

units and their contact is transgressional in the south while

the northern boundary is mostly tectonic (Fig. 1C).

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The CCPB deposits (so-called the “Podtatranská skupina

Group” sensu Gross et al. 1984; Gross 2008) are divided com-

monly into the following formations (Fig. 2) (Gross et al.

1984): the lowermost Borové Formation consists of breccias,

conglomerates, lithic sandstones to siltstones, marlstones,

organodetrital and organogenic limestones. These represent

the basal terrestrial and shallow-marine transgressive deposits

(e.g., Marshalko 1970; Kulka 1985; Gross et al. 1993; Baráth

& Kováč 1995; Filo & Siráňová 1996, 1998; Šurka et al. 2012;

Jach et al. 2016). This formation is overlain by the Huty

Formation which includes various mud-rich deep marine

deposits mainly (e.g., Janočko & Jacko 1999; Soták et al. 2001;

Fig. 1. A — Location of study area within the Alpine-Carpathian orogen; B — the Central Carpathian Paleogene Basin system depicting

structural sub-basins, basement massifs and surrounding units; C — simplified geological sketch of the part of the Liptov region (after Biely

et al. 1996; modified) with situated locality studied; D — situational geological map of the wider area of the studied localities (Geological Map

of Slovakia M 1:50,000 [online] 2013); key: 1 — a) roads and railway, b) rivers, c) built-up area (cities and settlements); 2 — a) deluvial

deposits, landslides (Quaternary), b) fluvial deposits (Holocene); 3 — a) fluvial and b) glaciofluvial gravels (Quaternary); 4 — Banská Bystrica

Formation: sand, clayey sand, gravel (Neogene); 5 — Zuberec Formation: a) normal flysch: mudstones, siltstones and sandstones, b) flysch

with predominance of mudstones and mudstone sequences in flysch deposits (Paleogene); 6 — Huty Formation: mudstones in absolute pre-

dominance over sandstones and conglomerates (Paleogene). Location of studied sections (Liptovská Ondrašová outcrop: 49°05’52.56” N,

19°34’22.98” E; Ráztoky outcrop: 49°06’06.02” N, 19°33’56.51” E).

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Starek et al. 2004) with the occurrences of sandstone mega-

bed events (Golab 1959; Sliva 2005; Starek et al. 2013).

The Zuberec Formation and the Biely Potok Formation com-

pose the up-section, predominantly consisting of rhythmically

bedded turbidites and massive sandstones and represent

the various sand-rich submarine fan facies associations (e.g.,

Westwalewicz-Mogilska 1986; Wieczorek 1989; Soták 1998;

Starek et al. 2000; Sliva 2005; Starek & Fuksi 2017a, b).

The evaluated and interpreted deposits are part of the

Zuberec Formation (earlier known as “Flysch lithofacies” e.g.,

Gross et al. 1980) within which the above mentioned authors

allocated several lithofacies with respect to the sandstone and

mudstone proportions. They interpreted the age of this forma-

tion as the Priabonian–Lower Oligocene. The Oligocene age

of the Zuberec Formation has also been confirmed in other

parts of the CCPB (e.g., Olszewska & Wieczorek 1998; Gedl

2000; Soták et al. 2001; Garecka 2005; Filipek et al. 2017).

Methods

The research involved a standard sedimentological analysis

of the sections. Bed thicknesses measurement and facies ana-

lysis were a key for further statistical analysis. Determination

of the bed thickness becomes complicated if it is thinning out

laterally, contains preserved bedform morphology or the bed

has an uneven — erosive base. In these cases the average

thicknesses were used.

Paleocurrent analysis included scour mark measurements

and current ripple cross-laminations. Postdepositional tilt of

the directions was restored by simple rotation along the hori-

zontal axis.

Calcareous nannofossils

Thirty-nine samples were evaluated to study calcareous

nannofossils from the Liptovská Ondrašová locality. Six sam-

ples come from a non-profiled part of outcrop. Samples for

the calcareous nannofossils study were prepared from mud-

stones containing CaCO

by using the decantation method

(Haq & Lohmann 1976; Perch-Nielsen 1985). The smear

slides were studied under the light microscope ZEISS AXIO

SCOPE AI, at 1000× magnification and nannofossil species

documented by digital camera AXIOCAM 105 COLOR.

Calcareous nannofossil age determination was carried out

according to the zonation by Martini (1971), supplemented by

Perch-Nielsen (1985), Young (1998) and Nannotax websites

(Young et al. 2017). Preservation and abundance of calcareous

nannofossils was determined according to Roth & Thierstein

(1972).

Statistical analysis

Sandstone and mudstone thickness were used for statistical

analysis. Specifically, 725 beds from 2 profiles (Liptovská

Ondrašová 1 = 566; Liptovská Ondrašová 2 = 159 beds), in total

length of more than 77 m (unlike the total length of outcrop

92 m) could be measured. All beds were measured in step by

0.5 cm. No correction was made for compaction. Sandstone–

mudstone ratio, mean, median, minimum, maximum and stan-

dard deviation of sandstone and mudstone thickness were used

to identify differences between profiles. Boxplot and histo-

gram functions demonstrated variability within profiles and

expressed the frequency distribution of bed thicknesses.

Autocorrelation or serial correlation is a tool for identifying

repeating patterns (Priestley 1981). Autocorrelation shows

correlation between the lagged values of the time series. It can

be interpreted as periodicity. The autocorrelation coefficient

values close to zero show no periodicity (Pinheiro et al. 2018).

Coarse-division (sandstone) thicknesses of turbidite beds were

processed by Hurst statistics. Hurst exponent is related to

autocorrelation of series (Hurst 1951, 1956; Chen & Hiscott

1999). Recalculated K and D values from Hurst statistics can

be used to depositional environment interpretation (Chen &

Hiscott 1999). Coarse-division (sandstone) thicknesses were

used for computation of cumulative distribution also. Typi-

cally, this function shows a degree of variation from the power-

law (straight-line) distribution and is calculated and examined

on a log plot. 2D model simulates proximal vs. distal

(non-channelized) environment effect (Carlson & Grotzinger

2001). All analyses were processed by R-cran software

(R Core Team 2014) and package nlme (Pinheiro et al. 2018).

Fig. 2. Descriptive lithostratigraphy of the filling in the western part

of the Central-Carpathian Paleogene Basin. Nomenclature of the for-

mations according to Gross et al. (1984, adapted). Biostratigraphy is

based on the data from Olszewska &Wieczorek (1998), Gedl (2000),

Starek et al. (2000), Starek (2001), Garecka (2005) and Soták et al.

(2007).

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Description of outcrops

The outcrop studied near Liptovská Ondrašová shows a long

succession in which two continuously exposed sections

Liptovská Ondrašová 1 (LO 1) and Liptovská Ondrašová 2

(LO 2) were processed (Fig. 3A). LO 1 has a total length of

more than 68 m and LO 2 is more than 23 m long. Within the

studied profiles the sedimentary successions show relatively

monotonous lithology of alternating sandstones and mud-

stones. Between LO 1 and LO 2 sections there is an uncovered

or poorly outcropped part about 10–15 m long. Here the shor-

ter, non-continuously exposed portions indicate mudstone and

mainly thin-bedded sequences. However, because of this rela-

tively large interruption of the sedimentary sequence, we have

processed and evaluated the obtained dataset as two sepa rate

parts (LO 1 and LO 2). The LO 2 section ends at a pier on

the edge of the Ráztoky Bay. Further exposures appear on

the shore of the lake, on the other side of the bay, towards

the cadastral area of the Ráztoky village drowned by damming

(Fig. 1D). The following will be referred as the Ráztoky loca-

lity. The exposed sedimentary sequences at the Ráztoky

loca lity are tectonically fractured and are not suitable for

detailed profiling.

Results

Sedimentary facies

Since the sedimentary facies within the LO 1 and LO 2 sec-

tions with the Ráztoky locality as well, are very similar, they

are described together in the following description. This clas-

sification is based on lithology and primary sedimentary struc-

tures mostly. The following sedimentary facies were identified:

unstructured ungraded to normally graded medium- to fine-

grained sandstone; parallel-laminated medium- to fine-grai-

ned sandstone; sandstone with asymmetrical cross-lamination;

coarse-grained to fine-grained laminated siltstone; massive

mudstone and mudstone, parts of which reveal an increased

content of silt and very fine sand (graded and laminated mud-

stone). Sedimentary facies identified within deposits of

indi vi dual sections reflect deposition from sandy high- to low

density turbidity current (Bouma 1962; Mutti 1992). More

detailed hydrodynamic interpretation of individual facies as

well as possible identification of the same facies from other

authors is shown in Table 1. However, in the following text

the Bouma classification (Ta–Te divisions sensu Bouma 1962)

is used for better clarity of identified sedimentary facies.

Table 1: Sedimentary facies and their interpretation within the studied sections.

Facies

Interpretation

Unstructured ungraded to normally

graded medium- to fine-grained

sand stone (Fig. 4A)

A rapid accumulation of sand from dense sandy turbidity current which bypassing the zone of deposition of

the preceding gravelly flows — Ta division (sensu Bouma 1962) or F8 facies (after Mutti 1992)

Parallel-laminated medium- to fine-

grained sandstone (Fig. 4A–D)

The upper flow regime conditions; traction carpet that is driven by basal shearing of an overlying turbulent

flow — Tb division (sensu Bouma 1962) or F9 facies (after Mutti 1992)

Sandstone with asymmetrical cross-

lamination (Fig. 4E, F)

The lower flow regime; traction movement with fallout processes from waning turbidity currents (e.g., Jopling

& Walker 1968; Mulder & Alexander 2001; Zavala et al. 2011) — Tc division (sensu Bouma 1962), F9 facies

(after Mutti 1992)

Coarse-grained to fine-grained lami-

nated siltstone

Traction plus fallout processes associated with deposition from suspension during weak turbulent motion in

low-density turbidity currents (Arthur et al. 1984; Stow & Piper 1984) — Tb division (sensu Bouma 1962),

E1 interval (after Piper 1978) or F9 facies (after Mutti 1992)

Massive mudstone, some parts reveal

an increased contents of silt and very

fine sand (graded and laminated

mud stone) (Fig. 4G)

Suspension fall-out from static or slow-moving mud cloud; flnal deposition from a sediment gravity flow event

(e.g., Piper 1978) — Te division (sensu Bouma 1962), T6 and T7 divisions (after Stow & Shanmugam 1980

— graded and ungraded turbidite muds respectively)

Fig. 3. A — Sedimentary logs of rhythmical bedded, sand/mud-mixed turbidite succession of the Zuberec Fm. studied in an outcrop near

Liptovská Ondrášová. The chard depicts vertical distribution of sandstone- and mudstone thicknesses and their possible trends, the sedimentary

facies, the facies associations, and sampling for stratigraphy. B — Schematic model for the facies associations of the Liptovská Ondrášová

sections. Individual facies associations represent different components of distributive lobe deposits (model after Prelát et al. 2009, modified).

C — LO2 section; note the gradual transition between mudstone dominated sequence (FA4) in the bottom of the outcrop and rhythmically

bedded sandstone-mudstone sequence (FA3) towards the top of the profile. D — Thinning-upward trend of sandstone bed thickness from

medium- to thick beds with smaller ratio of mudstones (FA2) in the lower part of the picture to thin bedded sequence FA3 in middle part and

mudstone dominated FA4 in the upper part of the picture. E – Turbidite sequence characterized by FA3 and FA2. Thickening-upward trend of

sandstone beds is highlighted by white arrow. Note the erosive character of some beds in Fig. 3D, E (highlighted with small black arrows).

F — Rhythmically bedded turbidite sequences with relatively balanced sandstone–mudstone ratio in the middle and top of the outcrop (FA3).

The lowermost part of the outcrop with mudstone dominated unit corresponds to FA4. Note the relatively sharp transition between thin-bedded

part and medium-bedded upper part of succession. G — detailed view of very regular thin-bedded, mudstone dominated sequences typical for

lobe distal fringe/inter-lobe environment (FA4). The scale corresponds to 10 cm.

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Apart from minor exceptions, the whole evaluated sedimen-

tary succession comprises beds which are composed of

medium- to very fine-grained sandstone with a typical vertical

arrangement of divisions Ta, Tb and Tc. Here continuous tran-

sition to Td and Te divisions is common. Generally, the Ta

division usually forms the gradational interval in the turbidite

lowermost part, especially on thicker beds. Not all beds have

developed complete Ta–Te Bouma divisions (Fig. 4A). The beds

(especially thicker ones) are often characterized only by Ta

and Tb divisions with a rapid transition into siltstones and

mudstones (Td, Te). The lower bed interfaces are sharp and

plain mostly, rarely gently undulated (loading deformation).

Some beds show complex internal arrangement of individual

facies and they multiply repetitions within a single bed

(Fig. 4B, C). This type of complex bedding shows a symmetri-

cal arrangement of divisions (Tb–Ta–Tb) (Fig. 4D). On the

contrary, most of the thin beds (up to 3–5 cm) have developed

the ripple lamination only (Tc). These beds often show com-

pletely preserved bedform morphology (Fig. 4E, F). Mudstones

are layered with very thin laminae (in mm scale) of siltstone

and/or very fine-grained sandstone frequently. They are fine

horizontally laminated or small scale ripple laminated with

completely preserved bedform morphology (Fig. 4G). Some

ripple laminated beds show pinching out character, especially

the thinner of them. In very rare cases, the beds erosive

cha racter may be observed with development of shallow

scour structures as well (Fig. 4H, I). The erosive character of

some currents indicates the presence of floating mudstone

intraclasts (Fig. 5A) which are rarely embraced on the top

of the sandstone bed. The base of the beds is characterized

by relatively common small-size erosional current marks

(Fig. 5B–D) and trace fossils (see Ichnofossils chapter).

Loading and dilatation ridges are much rarer (Fig. 5E), as

well as coalified phytodetritus on separated bedding planes

(Fig. 5F).

Facies associations

Within the studied sections, in the sense Prélat et al. (2009),

the distinguished facies associations mostly correspond to the

lobe fringe and lobe distal fringe/inter-lobe facies associations

and to a small extent also lobe off-axis facies association

(Fig. 3B). For easier comparison we denote the related facies

associations as FA2–FA4 (identically as So et al. 2013).

The facies association corresponding to the lobe axis (FA1)

cannot be identified therefore, the following description

begins with FA2.

Locally occurring sequences from the middle to upper part

of the LO 1 section (Fig. 3A) may represent lobe off-axis

facies association (FA2). They are represented by medium-

thick sandstone beds and balanced to slightly predominant

ratio of sandstones. (Fig. 3D, E). In thicker sandstone beds

(>15 cm), massive bedding is the most common (ungraded to

normally graded sandstone — Ta division). The Ta division

within thick beds is commonly overlain by parallel-laminated

sandstones (Tb division) or may fining upwards with rela-

tively sharp transition to siltstone and mudstone facies.

The ripple cross-lamination (Tc division) is rather sparse in

thick sandstone beds and is poorly developed. They form only

thin intervals at the top of the beds, near the transitions to silt-

stones. The geometry of each bed is tabular or sheet-like and

generally the beds have a good lateral stability. Especially

within this facies association, beds occur with complex inter-

nal arrangement of individual facies in which multiple repeti-

tion is frequent (Fig. 4B–D), apart from the more frequent

Ta division and rare occurrence of shallow scour structures

(Fig. 3D, E).

The medium- to fine grain sizes of most sandstones, tabular

geometry of beds, occurrence of medium-bedded sandstone

with massive bedding, intercalation of thin- bedded turbidites

with abundant Tb, Tc, and Td divisions as well as absence of

both — some metres to tens metres thick bedseds of massive,

frequently amalgamated thick sandstones, and large scours or

evidence for channels suggest deposition in the lobe off-axis

environment (Prélat et al. 2009; Prélat & Hodgson 2013; So et

al. 2013).

In lobe fringe facies association (FA3) mudstone beds are

predominant (60–70 %). The main component of this facies is

rhythmic thin-bedded sequence with sandstone and mudstone

beds, generally ranged from several cm to tens cm in thickness

(Fig. 3C–F). Beds are tabular or sheet-like and generally they

have a good lateral stability. The lower bed interfaces are

sharp with common small-size erosional current marks

(Fig. 5B–C). Lobe fringe facies association comprises all

identified sedimentary facies and the beds often show com-

plete developed Bouma divisions (Ta–Te, sensu Bouma 1962).

However, unstructured ungraded- to normally graded sand-

stone facies is much rarer compared to others (Tb–Te divisions)

and usually builds the rare thicker beds (up to 15–20 cm) or

lowermost part of the thiner turbidites. The Ta division is less

common as in the FA2. Especially thin, very fine-grained, up

to 5 cm thick turbidites consist of Tc–Te divisions only.

A regularly thin-bedded, rhytmic, some metres thick

sequence with a high proportion of mudstone, thin-bedded

finely-structured sandstone with good lateral continuity sup-

ported interpretation of FA3 as lobe fringe deposits (Prélat &

Hodgson 2013; So et al. 2013).

Lobe distal fringe/inter-lobe facies association (FA4) is

dominated by thin-bedded fine to very fine-grained sand-

stones, siltstones, and medium- to thick-bedded mudstones

mainly. In this facies association, mudstones have a strong

dominance and often make up more than 70 % of the total

thickness of FA4. Tc–Te divisions are frequent, but the sand-

stone Ta and Tb divisions are very sporadic. This facies asso-

ciation forms shorter sequences in the whole sections but

reaches its maximum thickness in the lowermost part of

LO 2 where the mudstone thickness forms up to 120 cm

(Fig. 3A). A large part of the poorly uncovered succession

between LO 1 and LO 2 sections as well as succession at

the Ráztoky locality probably also belong to this facies

asso ciation. Regularly thin-bedded, fine- to very fine-grained

turbidites with good lateral continuity and height contents of

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mudstone facies support interpretation of FA4 as lobe distal

fringe and inter-lobe with the deposition of dilute low concen-

tration turbidity currents or slow hemipelagic deposition

(Stow & Piper 1984).

Paleocurrent analysis

The typical features of the thin- to medium-bedded, fine-

grained turbidity sequences are paleocurrent indicators such

as oriented erosive structures on the bed soles (e.g., frondes-

cent marks, flute marks, longitudinal furrows, ridges and

tool marks (Fig. 5B–D) and current ripple cross-lamination.

Paleocurrent data derived from the lower bedding plane struc-

tures, provide general flow orientation SW–NE with transport

in a NE direction (Fig. 6). These indicators show relatively

small variation and orientation remains constant throughout

the whole studied section. Paleocurrent data derived from rip-

ples shows a more significant variability with transport in

a SE–NE direction. Rarely, some current ripples show mea-

surements of contra-directional orientation with transport NW

direction. These contradictory ripple laminations occur within

separate beds (Fig. 4E) or oppositely oriented parts of lamina-

tions within cross-bedded layers where herringbone cross-

stratification has formed (Fig. 4F).

Fig. 5. Structures on bedding planes. A — Sandstone molds of weathered mudstone intraclasts; B — flute casts; C — small scale of tool marks,

a non-defined circular structure in the upper right part of the figure is probably of mechanical origin, similar to the impact or impress structure;

D — frondescent marks (black arrows on the pictures indicate the direction of paleoflows); E — loading and dilatation ridges on the lower

bedding plane; F — coalified plant detritus in sandstone. A black field on the scale corresponds to 1 cm.

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Bed thickness statistical analysis

The sections consist of rhythmic, predominantly thin- to

medium-bedded successions which differ mainly by ratio of

sandstone (LO 1: 44.5 %, LO 2: 24.2 %) and mudstone beds

(LO 1: 55.5 %, LO 2: 75.8 %). The vertical arrangement of all

beds from both sections, as well as the variability in sand-

stone–mudstone proportion, is depicted in Fig. 3.

Beds have variable thickness up to 50 cm (Figs. 3A, 7A).

Only a few mudstone beds reach greater thicknesses (60–

120 cm) in the lowermost part of the LO 2 section.

Boxplots and histograms show thickness distributions (both

sandstone and mudstone divisions) of the beds among indivi-

dual profiles (Fig. 7A, B). The average thicknesses of turbidite

sandstone facies are 5.4 cm (LO 1 section) and 3.6 cm (LO 2

section). In the LO 1 section sandstone beds with thicknesses

smaller than 5 cm are most frequent. 50 % of the beds range

between 2 and 6 cm. Mudstones from this profile are repre-

sented mostly by beds thinner than 6 cm. In contrast, the LO 2

section is characterized by thin rhythmically repeating sand-

stone beds of which 50 % are between 1.5 to 5 cm. Mudstone

variability is higher here and 50 % of mudstone thicknesses

range between 4 and 14 cm. Frequency distributions are right

skewed and show higher proportions of small beds and beds

thicker than 10 or 15 cm are rare.

Generally, beds show noncyclic vertical organization or

only low-expressive vertical organization into small-scale

series with upward thickening of sandstone beds. Bed thinning

tendency is less common. Autocorrelation of coarse grained

divisions also shows relatively weak periodicity on 16

, 18

and 27

beds in LO 1 section and on every 4

bed in LO 2

section (Fig. 7C). Other bed periodicity signals are

insignificant. However, vertical patterns in bed arrangement

of some few metres thick units show a clear upward thicken-

ing tendency (Fig. 3E, F).

The cumulative distribution of the complete coarse-division

thicknesses from both profiles has an almost linear shape

(Fig. 7D). Cumulative distributions on logarithmic scales y

and x axes correspond to frequent occurrence of well defined

thin turbidites in succession (Fig. 3A). Rare occurrence of

a few thicker beds within the profile affects the line and bends

its upper part slightly.

The Hurst coefficient was used to verify assumed interpreta-

tions of the depositional paleoe-nvironment (Chen & Hiscott

1999). The K (0.69–0.73) and D (1.9–3.8) values of coarse

division thicknesses and their percentage within the Liptovská

Ondra šová sections are located in a narrow field near the inter-

face of basin-floor sheet sand and lobe-interlobe deposits

(Fig. 7E).

Ichnofossils

Trace fossils found in the outcrops studied belong to 11

ichno species.

Arenicolites Salter, 1857

Arenicolites isp. (Fig. 8)

Arenicolites isp. was observed as a vertically oriented

U-shaped burrow without wall. Pairs of openings on the bed-

ding planes have the same diameters, but it also has sparsely

dimorphic morphology. Diameters of sectioned burrows attain

2.5 to 3.7 mm. Depth of U-shaped burrows is up to 13 mm.

Distances between pair opening vary between 7 to 14 mm.

Burrow is relatively shallow. Arms of U-shaped burrow are not

parallel but are slightly divergent. Arenicolites and Saerichnites

burrows have the same range of diameters, which may imply

that Arenicolites represents initial form of Saerichnites burrow

system. This trace fossil belongs to domichnion, producer is

thought to be suspension and/or deposits feeder polychaetes

(Bromley 1996) and amphipod crustaceans (Baucon et al.

2014) in marine environment.

Arthrophycus Hall, 1852

Arthrophycus cf. tenuis (Książkiewicz, 1977) (Fig. 9A)

A. cf. tenuis was observed as hypichnial tiny sickle-shaped

burrows with the tapered ends. Branching to bunch-shaped

burrows were rare. The most typical forms of this ichnogenus

are arranged into bundles but it is not typical of A. cf. tenuis at

this locality. The trace fossil occurs on sole of bedding plane

with occasionally occurrence of bioglyphes striae, which are

oriented transverse through the trace fossil (modified accor-

ding to Uchman 1998). A. cf tenuis has relatively high

abundance in the lower part of described succession at the

locality Liptovská Ondrašová. Arthrophycus is considered to

be fee ding burrows of arthropods and polychaetes (Seilacher

2007).

Fig. 6. Paleocurrent data derived from oriented erosive structures on

the lower sides of the beds (white: orientations, dark-grey: directions)

and current ripple cross-lamination (light-grey).

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Bergaueria Prantl, 1947

Bergaueria hemispherica Crimes et al. 1977 (Fig. 9B)

B. hemispherica is presented as a hypichnial knobby hemi-

spherical symmetrical to slightly asymmetrical trace fossil

without central depression. Height of observed Bergaueria

attains 14 mm and its diameter is up to 36 mm. B. hemisphe

rica surface is smooth, occasionally concentric patterns pro-

bably reflected boundaries of surrounding layers of mud or

sandstone. Producers of Bergaueria are thought to be sea

anemones (Bromley 1996).

Helminthopsis Heer, 1877

Helminthopsis tenuis Książkiewicz, 1968 (Fig. 9C)

Helminthopsis tenuis was observed as unbranched relatively

long hypichnial, horizontal, cylindrical, wide, shallow, mean-

der, 1 mm thick. This trace fossil occurs in shallow-marine to

deep-sea facies, commonly in turbiditic deposits. Systematic

revision of this ichnogenera (Wetzel & Bromley 1996; Uchman

1998) shows relatively wide variability within several ichno-

species. Producer of Helminthopsis probably belongs to poly-

chaetes or priapulids (Fillion & Pickeril 1990). H. tenuis is

relatively rare and it has been found at the Liptovská Ondrašová

locality only.

Laevicyclus Quenstedt 1881

Laevicyclus isp. (Fig. 9D)

Only one specimen of this structure has been found on

the sole bed. Provisionally without further samples it was

assigned to Laevicyclus isp. It is consisted of two concentric

circles. Outer circle attains diameter 6 mm and inner circle has

2.5 mm. Width of the circle strings is 0.3 mm. Central knob

0.9 mm in diameter with short string is situated inside the inner

circle. However circular structures can be reflected

Bathy siphon test scratch marks circular-shape mechanogly-

phes also (Uchman & Rattazzi 2013).

Paleodictyon Meneghini 1850

Paleodictyon minimum Sacco 1888 (Fig. 9E)

P. minimum is typical of tiny mesh size that attains 2–2.2 mm.

Measured string diameters are in the range 0.47 to 0.56 mm.

A poorly preserved fragment of one specimen was found on

the sole bed. Structure of ichnogenus Paleodictyon is charac-

terized as shafts which run up from the middle of tunnels

between the corners or from the point of corners of horizon-

tally oriented hexagonal mesh to the sea bottom (Rona et al.

2009, fig. 8; Seilacher 2007, plate 55). Paleodictyon ichnotaxo-

nomical summary revision has been provided by Uchman (1995).

Planolites Nicholson 1873

Planolites montanus Richter 1937 (Fig. 9F)

Planolites occurs as simple not branched burrows with

smooth surface which are elliptical or circular in cross section.

Diameter of observed burrows attains 0.9 to 1.2 mm and

30 mm length. This morphologically simple burrow is typical

of cross-facies trace fossils (Fillion & Pickeril 1990).

Saerichnites Billings 1866

Saerichnites isp. (Fig. 9G,H)

This trace fossil has frequently been found on the upper bed

surface as a view of sections of two rows of circular or semi-

circular weathered pits or positively weathered vertical or

oblique burrows. Diameter of sectioned burrows arranged in

the rows and it attain 2.4 to 3.2 mm in diameter. Morphology

of such sectioned burrow can be interpreted by two ways:

(i) horizontal burrow with branched shaft, or (ii) horizontally

spiralled burrow (Uchman 1995, 1998; Fürsich et al. 2006).

Fig. 8. Arenicolites isp. from the Ráztoky locality. Perpendicular section with weathered U-shaped burrow of Arenicolites isp. Several sectioned

burrows on the bedding surface are visible.

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This form of traces can be assigned into pearl string traces like

Hormosiroidea, Margaritichnus, Nereites, Parahaentzsche

linia and Ctenopholeus (Uchman 1995; Fürsich et al. 2006).

Scolicia De Quatrefages 1849

Scolicia strozzii (Savi & Meneghini 1850) (Fig. 9I)

At Liptovská Ondrašová relatively frequented trace fossils

occurring on sole beds. It has double parallel ridge morpho-

logy. Diameter of specimen is in the range 12 to 20 mm.

Diameter of the lobes is 3 to 6 mm. Lobes of ridges are

semi-circular in cross-section. Meandering, diameter of trace

fossil and lobe is often changing in the same specimen

(Uchman 1995). Abundance of S. strozzii is low but it occurs

on the Liptovská Ondrašová and Ráztoky localities. Scolicia is

produced by irregular echinoids with double drainage tube

assigned to the Spatangus group (Uchman 1995; Gibert &

Goldring 2008).

Strobilorhaphe Książkiewicz, 1968

Strobilorhaphe clavata Książkiewicz, 1968 (Fig. 9J)

Strobilorhaphe clavata has hypichnial branched burrow

with numerous laterally arranged cone shaped chambers.

Length of the chamber attains 7.2 mm and the width is from

3 to 3.3 mm. Diameter of the burrow is unclear because it is

covered by lateral clavate chambers. Książkiewicz (1977)

noted that the burrow is 2 mm wide. Common abundance of

S. clavata is registered only at the locality Ráztoky.

Thalassinoides Ehrenberg 1944

Thalassinoides suevicus (Rieth 1932) (Fig. 9K)

Thalassinoides burrows are visible with Y-shaped branching

on the lower bed surface. Burrows are elliptical to circular in

cross section, 12–18 mm wide. Thalassinoides are assigned

into groups of thalassinidean shrimp and part of callianassids

mostly, which construct open burrow (Bromley 1996). A lot

of fragments of Thalassinoides have been found at the

L. Ondrašová locality.

Meandered sinusoidal trace fossils (Fig. 9L)

Width of burrow is 0.9 to 1.8 mm. Wavelength attains

13.4 mm and amplitude is 3.1 mm. This form of trace is rare

and only one has been found on bedding sole at the Ráztoky

locality. This type of trace can be attributed to fragments of

meandered traces (e.g., Protopaleodictyon, Belorhaphe).

In addition to trace fossils and sole marks the rare body fos-

sils were also found on the sandstone surfaces (Fig. 10A–D).

Calcareous nannofossils

All samples (for sample distribution see Fig. 3A) were posi-

tive and rich in calcareous nannofossils. Calcareous nannofos-

sil preservation is moderate — mechanical damage, etching of

the specimens is weak. The abundance of the calcareous nan-

nofossils is moderate — about 10 specimens per field of view

of the microscope.

The majority of the assemblage is composed of allochtho-

nous species, Cretaceous and Eocene age.

Cretaceous species which were found: Arkhangelskiella

cymbiformis, Cyclagelosphaera reinhardtii, Chiastozygus cf.

trabalis, Eiffelithus eximius, Lucianorhabdus sp., Micula sp.,

Zeugrhabdotus embergeri, Watznaueria barnesae, Watz

naueria manivitae.

Species that occur only in Eocene strata were found:

Discoaster barbadensis, Discoaster multiradiatus, Discoaster

saipanensis, Chiasmolithus grandis, Neococcolithus dubius,

Tribrachiatus contortus.

A large part of the assemblage comprised species with their

first occurrence in the Eocene and also they occur in Oligocene

strata: Chiasmolithus altus, Chiasmolithus oamaruensis, Cycli

cargolithus floridanus, Dictyococcites bisectus, Discoaster

nodifer, Helicosphaera bramlettei, Helicosphaera compacta,

Isthmolithus recurvus, Lanternithus minutus, Pontosphaera

latelliptica, Reticulofenestra hillae, Reticulofenestra moorei,

Reticulofenestra umbilicus, Sphenolithus radians, Trans ver

sopontis pulcher (Fig. 11).

Biostratigraphically significant species with their first

occurrence in the Oligocene (see Fig. 11 and Table 2): Cycli

cargolithus abisectus, Helicosphaera recta, Reticulofenestra

lockeri, Reticulofenestra ornata, Sphenolithus dissimilis. They

formed the smallest part of the nanno-assemblage.

On the basis of the detected nano-assemblage the Lower

Oligocene age of the samples was determined. The NP23

Zone (Rupelian age) was determined by the species Reti

culofenestra lockeri, Reticulofenestra ornata, Helicosphaera

recta, Sphenolithus dissimilis, Chiasmolithus altus, Trans

versopontis pulcher and Cyclicargolithus abisectus.

Fig. 9. Trace fossil assemblage of the Liptovská Ondrašová and the Ráztoky localites. A — Sole bed with tiny scratchy like hypichnial lines of

Arthrophycus tenuis (L. Ondrašová); B — Bergaueria hemispherica presents natural casts of biologically originated depressions that are situa-

ted on the sole beds. Upper and side views (Ráztoky); C — slim (up to 1 mm in diameter) unbranched irregularly meandered Helminthopsis

tenuis occurs as a hyporelief (L. Ondrašová); D — rarely occurring hypichnial questionable specimen of Laevicyclus isp., this structure can be

interpreted as scratch circle-shaped marks also (sensu Uchman and Rattazzi, 2013), (Ráztoky); E — poorly preserved Paleodictyon minimum

on sole bed (Ráztoky); F — hypichnial, unbranched Planolites montanus is pointed by arrows. Trace in the right corner of the picture belongs

to Thalassinoides (L. Ondrašová); G, H — vertical to subvertical oriented burrows arranged in the double rows of Saerichnites isp. on upper

bedding surface (Ráztoky); I — hypichnial Scolicia strozzii double line traces produced by irregular sea urchins (L. Ondrašová); J — branched

hypichnial burrow of Strobilorhaphe clavata with magnified part of triangular shaped tiny chambers (Ráztoky); K — Thalassinoides suevicus

with Y-shaped branched burrows, swollen in area of branching, sole bed (L. Ondrašová); L — regularly meandered hypichnial fragmented trace

fossil rare occurs on the Ráztoky locality.

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Cycli cargolithus abisectus was found only in the sample

Lo-21 and first occurrence of this species is biostratigrafical

significant for the NP23/24 Zone boundary (Perch-Nielsen

1985; Young 1998).

In six samples from non-profiled exposures (Ráztoky

loca lity) Isthmolithus recurvus was indicated. It determines

the lower part of the NP 23 Zone. The species Isthmolithus

recurvus has the last occurrence in the Zone NP 23 (Perch-

Nielsen 1985; Young 1998) (see Table 2).

Discussion

Most of the beds studied have the character of deposition

from sandy high- to low density turbidity currents with typical

vertical development of Bouma divisions. However, some

beds show the repeated or symmetrical arrangement of indi-

vidual facies within a single bed which should be caused by:

hidden amalgamation in short successive turbidities or it is a

reflection of waxing vs. waning processes in pulsating flows.

The second case is more characteristic of turbulent hyper-

pycnal flows. However, frequent phytodetritic material as

a characteristic diagnostic feature of hyperpycnites (if present

in the source material, e.g., Zavala et al. 2012) was not

observed here. Although the presence of phytodetritus was

recorded in some sandstones (Fig. 5F) its occurrence is rather

rare compared to other localities of the Zuberec Formation (cf.

Starek & Fuksi 2017a,b; Kotulová et al. 2019).

The facies associations distinguished on the basis of the pre-

dominant sedimentary facies, sandstone bed thickness and

proportion of mudstone facies have a close affinity to different

components of distributive lobe deposits in a turbidity fan

system. The mud-dominant zone (including the lowermost

part of LO 2) may correspond to the interlobe environment in

the outer fan lobes but also may indicate either starvation of

the basin or reduction of the sediment input to the basin’s

deeper part, probably related to relative sea-level rise (Johnson

et al. 2001; Prélat et al. 2009; Grundvag et al. 2014). Frequent

alternation of individual facies associations can be interpreted

as a result of random shifting of lobe elements due to intra-

basinal factors such as depositional topography (autogenic

compensation processes), fan-channel switching, channel

bifurcation and avulsion of channel or lobe shifting. On the

basis of identified facies associations it is possible to interpret

the sedimentary record of the studied outcrops as distal lobe

deposits in an outer fan environment. This interpretation was

also supported by the results of Hurst statistics which show

that coarse division thickness and coarse division thickness

percentage values define the environment as basin-floor sheet

sand near the interface with lobe-interlobe deposits. Greater

dissipation of values of the LO 1 section located symmetri-

cally around the border between basin-floor sheet sand and

lobe interlobe deposits is caused by occurrence of a few

thicker beds in the dataset. Coarse division thickness percen-

tage represents harmonized data which minimize the effect of

these thicker beds occurrence. The almost linear shape of

cumulative distribution can also be correlated with the outer

fan environment, not affected by significantly thicker amalga-

mated beds of the lobe axis and channels (Carlson & Grotziger

2001).

The identified trace fossils Arthrophycus cf. tenuis, Scolicia

strozzii, Strobilorhaphe clavata, Thalassinoides suevicus from

the Liptovská Ondrášová sections can be interpreted as a typi-

cal association for a turbidite depositional system of

Fig. 10. Body fossils. A — Shark vertebra; B — circular fragment of a bone on the upper bed surface with shale rip-up clasts; C — fish scale;

D — rib bone fragment; B–D scale in millimetres.

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archety pal Cruziana ichnofacies (Seilacher 1967; Knaust &

Bromley 2012; MacEachern et al. 2007). This assemblage can

be situated in the area of the turbidite sedimentary system of

depo sitional lobes. Traces described within the Ráztoky loca-

lity section such as Arenicolites isp., Bergaueria hemisphe

rica, Saerichnites isp. and questionable finds of Paleodiction

minimum, fragments of sinusoidal graphoglyptids and

Laevicyclus isp. present significant change of the ichnoassem-

blage. This change can be summarized as a change from

an association of deposit feeders (e.g., Helminthopsis tenuis,

Planolites montanus, Scolicia strozzii, Thalassinoides suevi

cus) to an association of shallow domichnia (Arenicolites isp.,

Bergaueria hemispherica, Saerichnites isp. that occupy the

sub strate to depths of 13–14 mm) and form traces of bottom

surface association (Paleodictyon minimum and sinusoidal

fragments of graphoglyptids). With regard to the thin layered

lithology of the upper part of the studied section and occur-

rences of graphoglyptid fragments, this ichnoassemblage can

be approximately compared with fan-fringe facies of

Paleodictyon–Nereites subichnofacies (sensu Uchman 2007)

with unusual association of Arenicolites isp., Bergaueria

hemispherica and Saerichnites isp.

The predominantly thin-bedded development of turbidite

sequences identified at the Liptovská Ondrášová and Ráztoky

localities is characteristic rather for the facies association of

the distal parts of the sandy fan. However, the available data

from other parts of the CCPB point to a much greater varia -

bility of facies and facies associations within deposits of

the Zuberec Formation (cf. Soták 1998; Starek & Fuksi

2017a,b). This variability can also be observed within

the Liptov Depression itself. Especially in the middle to eas-

tern part of the depression (in a wider area near settlements of

Fig. 11. Calcareous nannofossils from Liptovská Ondrašová and Ráztoky locations. 1, 2 — Reticulofenestra lockeri, samples: Lo-11, Lo-31;

3, 4 — Chiasmolithus altus, sample: Lo-21; 5 — Dictyococcites bisectus , sample: Lo-21; 6 — Isthmolithus recurvus, sample: Ráztoky 3;

7 — Discoaster nodifer, sample: Lo-14; 8 — Sphenolithus dissimilis, sample: Lo-12; 9 — Cyclicargolithus floridanus, sample: Lo-12;

10 — Lanternithus minutus, sample: Lo-21; 11 — Helicosphaera recta, sample: Lo-24; 12 — Helicosphaera bramlettei, sample: Lo-33;

13 — Transversopontis pulcher, sample: Lo-31; 14, 15 — Reticulofenestra ornata, samples: Lo-21, Lo-29; 16 — Cyclicargolithus abisectus,

sample: Lo-15; 17 — Reticulofenestra moorei, sample: Lo-21; 18 — Reticulofenestra umbilicus, sample: Lo-21; 19 — Reticulofenestra hillae,

sample: Lo-21; 20 — Pontosphaera latelliptica, sample: Lo-7.

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the Gôto vany, Bodice, Bobrovček, Bobrovec, Pavlová Ves,

Liptovská Kokava and Liptovský Mikuláš town) there are tens

of metres thick turbidity sequences with a slight mudstone

predominance and similar sediment development to the out-

crops stu died. On the other hand, in other locations such as the

Likavka–Ružomberok area and in the area of the Liptovská

Mara Dam wall, the sequences of the Zuberec Formation have

the character of medium- to thick-bedded turbidites with up to

1m thick massive sandstones (Gross et al. 1980). On the

Liptovský Ondrej locality these turbidite sequences associate

with the conglomerates of incised submarine slump. The varia-

bility of facies and facies associations within the Zuberec

Formation is probably related to the position of the deposits

studied within the depositional fan architecture and their spa-

tial migration during the sequential-stratigraphic development

of the CCPB.

The paleoecological evaluation of the nannofossil assem-

bla

ge was done on the basis of autochthonous species.

The majo rity of the autochthonous assemblage was formed by

tem perate-water species like Cyclicargolithus, Reticulo

fenestra, Dictyococcites, Cocolithus. Warm water species

such as Discoasters, Sphenolithus, Helicosphaera are very

rare. Cold water species such as Reticulofenestra lockeri and

Reticulofenestra ornata also occurred in small numbers.

Reticulofenestra lockeri and Reticulofenestra ornata are

endemic species which tolerated hyposaline waters (Báldi-

Béke 1984; Nagymarosy & Voronina 1992). This paleoeco-

logical condition is typical for the NP23/24 Zone (Báldi-Béke

1984; Nagymarosy 1990; Soták 2010).

Paleocurrent measurements point to the main transport of

the material from SW and W which is generally consistent

with the measurements of paleocurrents in the Orava–Podhale

part of the CCPB (cf. Marschalko & Radomski 1960; Starek

2001; Starek & Fuksi 2017a). Uniform paleotransport mode

suggests that the Liptov and Orava–Podhale sub-basins for-

med one sedimentary area without distinctive segmentation

during the Oligocene. Rare opposite oriented paleocurrent

indicators could be dimensions which occur in confined basins

bounded by tectonic slopes or which would indicate feeding of

depositional lobes from several sources. However, the scarcity

of these results, as well as the fact that these paleocurrent data

were derived from ripples, point rather to the combined flows

and possible reworking of sandy fine-grained turbidites

through bottom currents (e.g., Shanmungam et al. 1993;

Martín-Chivelet et al. 2008).

Conclusions

The facies associations we have distinguished represent dif-

ferent components of distributive lobe deposits in a turbidite

fan system. They correspond mainly to the lobe fringe and

lobe distal fringe/inter-lobe facies associations with the local

occurrence of medium bedded sequences corresponding to the

lobe off-axis facies association. The interpretation as outer fan

environment with basin-floor sheet sand near the interface

with lobe–interlobe deposits was also supported by Hurst sta-

tistics and the shape of cumulative distribution. Relatively

frequent alternation of individual facies associations within

the evaluated sedimentary sections could be interpreted as

a result of random shifting of depositional lobe elements and

sedimentary facies.

An environment with turbidite deposition also generally

corresponds to the identified trace fossil association of

deep-tiering fodinichnia and domichnia up to shallow-tiering

graphoglyptid traces.

The Rupelian age of the sedimentary sections near the

Liptovská Ondrašová and Ráztoky localities was determined

on the basis of the nanoassemblage detected.

Measurement of paleocurrents shows transport of material

mainly from the SW and W. It is generally consistent with

the paleotransport in Orava and Podhale, pointing to one sedi-

mentation area without distinctive segmentation during

the Oligocene.

Table 2: Distribution of nannofossils in the Liptovská Ondrašová and

Ráztoky outcrops with indications of important index species for

biostratigraphic classification of the Oligocene formations.

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Acknowledgements: This work was supported by the scien-

tific grant agency of the Slovak Republic (Vega 2/0014/18)

and Slovak Research and Development Agency under the con-

tract No. APVV-14-0118. The authors are grateful to Ivana

Koubová (Earth Science Institute of the SAS, Bratislava) for

language correction. Thanks are also extended to Jozef

Michalík (Earth Science Institute of the SAS, Bratislava),

Alfred Uchman (Jagiellonian University, Kraków), Ľubomír

Sliva (Nafta a.s., Bratislava) and an anonymous reviewer for

the detailed review of the manuscript and constructive com-

ments.

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Appendix

Checklist of taxa mentioned in the text in alphabetic order:

Nannoplankton species

Arkhangelskiella cymbiformis Vekshina, 1959

Chiasmolithus altus Bukry & Percival, 1971

Chiasmolithus grandis (Bramlette & Riedel, 1954) Radomski, 1968

Chiasmolithus oamaruensis (Deflandre, 1954) Hay et al., 1966

Cyclagelosphaera reinhardtii (Perch-Nielsen, 1968) Romein, 1977

Cyclicargolithus abisectus (Muller, 1970) Wise, 1973

Cyclicargolithus floridanus (Roth & Hay, in Hay et al., 1967) Bukry,

1971

Dictyococcites bisectus (Hay, Mohler, & Wade, 1966) Bukry &

Percival, 1971

Discoaster barbadensis Tan, 1927

Discoaster nodifer (Bramlette & Riedel, 1954) Bukry, 1973

Discoaster multiradiatus Bramlette & Riedel, 1954

Discoaster saipanensis Bramlette & Riedel, 1954

Eiffelithus eximius (Stover, 1966) Perch-Nielsen, 1968

Helicosphaera bramlettei (Müller, 1970) Jafar & Martini, 1975

Helicosphaera compacta Bramlette & Wilcoxon, 1967

Helicosphaera recta (Haq, 1966) Jafar & Martini, 1975

Isthmolithus recurvus Deflandre in Deflandre & Fert, 1954

Lanternithus minutus Stradner, 1962

Neococcolithus dubius (Deflandre in Deflandre & Fert, 1954) Black,

1967

Pontosphaera latelliptica (Báldi-Beke & Baldi, 1974) Perch-

Nielsen, 1974

Reticulofenestra hillae Bukry & Percival, 1971

Reticulofenestra lockeri Müller, 1970

Reticulofenestra moorei Bown & Dunkley Jones, 2012

Reticulofenestra ornata Müller, 1970

Reticulofenestra umbilicus (Levin, 1965) Martini & Ritzkowski,1968

Sphenolithus dissimilis Bukry & Percival, 1971

Sphenolithus radians Deflandre in Grassé, 1952

Transversopontis pulcher (Deflandre in Deflandre & Fert, 1954)

Perch-Nielsen, 1967

Tribrachiatus contortus (Stradner, 1958) Bukry, 1972

Zeugrhabdotus embergeri (Noël 1959) Perch-Nielsen, 1984

Watznaueria barnesae (Black in Black & Barnes, 1959) Perch-

Nielsen, 1968

Watznaueria manivitae Bukry, 1973