GeolCarp_Vol69_No5_498

GEOLOGICA CARPATHICA

, OCTOBER 2018, 69, 5, 498–511

doi: 10.1515/geoca-2018-0029

www.geologicacarpathica.com

Integrated stratigraphy of the Upper Barremian–Aptian

sediments from the south-eastern Crimea

MARIA S. KARPUK



, EKATERINA A. SHCHERBININA

, EKATERINA A. BROVINA

GALINA N. ALEKSANDROVA

, ANDREY YU. GUZHIKOV

ELENA V. SHCHEPETOVA

and EKATERINA M. TESAKOVA

1,3

Geological Institute of RAS, Pyzhevski Lane 7, Moscow, 119017, Russia,



maria.s.karpuk@gmail.com

Saratov State University, Department of General Geology and Mineral Resources, Astrakhanskaya st. 83, Saratov, 410012, Russia

Moscow State University, geological department, Vorobiovy Gory 1, Moscow, 123103, Russia

(Manuscript received February 7, 2018; accepted in revised form October 4, 2018)

Abstract: Previous studies made in different parts of the world have shown that Barremian–Aptian times imply many

difficulties in deciphering the biostratigraphy, microfossil evolution and correlation of bioevents. In an attempt to improve

our knowledge of this period in a particular area of the Tethyan realm, we present the first integrated study of microbiota

(including planktonic foraminifera, calcareous nannofossils, ostracods and palynomorphs) and magnetostratigraphy of

the upper Barremian–Aptian sediments from south-eastern Crimea. The nannofossils display the classical Tethyan chain

of bioevents in this interval, while the planktonic foraminifera demonstrate an incomplete succession of stratigraphically

important taxa. Our study enabled the recognition of a series of biostratigraphic units by means of four groups of

microfossils correlated to polarity chrons. The detailed analysis of the microfossil distribution led to a biostratigraphic

characterization of the Barremian/Aptian transition and brought to light an interval, which may correspond to the OAE1a.

Keywords: Crimea, Barremian, Aptian, biostratigraphy, planktonic foraminifera, calcareous nannofossils, ostracods,

palynomorphs, magnetostratigraphy.

Introduction

Thick Lower Cretaceous sediments are widely exposed in

south-eastern Crimea southward of the city of Feodosia, where

they form the eastern margin of the First Range of the Crimean

Mountains. The Berriasian–Valanginian succession, made up

of limestones, marlstones and mudstones, gets younger going

from the sea-shore cliffs toward the hinterland; these deposits

are succeeded by Hauterivian–Aptian non-calcareous and cal-

careous siliciclastics mostly devoid of or very poor in macro-

fossils. The Lower Cretaceous sediments of different intervals

are studied in this area in varying degrees by different methods,

including biostratigraphical, paleomagnetic, sedimentological

and geochemical analyses. The main recent studies were focu-

sed on the Jurassic/Cretaceous transition (e.g., Arkadiev 2004,

2011; Guzhikov et al. 2012; Arkadiev et al. 2018) and on

the upper Berriasian to Valanginian sediments (Arkadiev 2007;

Guzhikov et al. 2014; Arkadiev et al. 2017, a.o.). However,

during the last half-century the Hauterivian to Aptian sedi-

ments of this area were rarely studied (e.g., Salman &

Dobrovolskaya 1968; Baraboshkin 2016). In fact, in this area

the Hauterivian and most of the Barremian sediments have

been disturbed by anthropogenic impact during the last deca-

des and thus are now barely exposed. As a result, we had to

limit our study to the upper Barremian–Aptian sediments,

which crop out in the Feodosia suburban area.

Recent bio-, magneto- and chemostratigraphic studies dea-

ling with the Barremian–Aptian interval improved calibration

of this time period (e.g., Erba et al. 1996; Moullade et al.

1998 a, b, 2011; Aguado et al. 1999; Erba et al. 1999;

Channell et al. 2000; Ropolo et al. 2008; Coccioni et al. 2012;

Savian et al. 2016, a.o.). The base (GSSP) of the Aptian

stage is not yet formally ratified, however, the base of M0

Magnetochron has been considered by many authors to

define the Barremian/Aptian boundary since the proposition

of the Aptian Working Group in 1996 (Erba et al. 1996).

The classical biostratigraphy of this interval in the Tethyan

realm includes ammonite and planktonic foraminifera (PF)

zonations, which are still in progress mainly because of

problems of correlation between the Tethyan and Boreal

Realms, and standard nannofossil zonations codified with

CC (Sissingh 1977) and NC (Roth 1978; Bralower et al. 1995)

labels. Ammonites are scarce or absent from the upper

Barremian to Aptian of the Crimea and thus could not be

used in the biostratigraphy of this interval in the studied

area.

A developed micropaleontological study of the Lower

Cretaceous sediments in Crimea began in the second half of

the last century. The occurrence of abundant and diverse cal-

careous nannofossils in the Crimean Lower Cretaceous was

shown by Vishnevsky & Menaylenko (1963) and Shumenko

(1974), but they did not consider the possibility of their strati-

graphic application. The study of the Barremian–Aptian strati-

graphic division based on PF was pioneered by T.N. Gorbachik

(Gorbachik 1959, 1964, 1969, 1986; Gorbachik & Krechmar

1969). This author proposed the zonal subdivision of

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the Barremian–Aptian sediments on the basis of PF study in

the south-western Crimean sections (Fig. 1).

Recently, new research has been carried out towards a more

detailed subdivision and correlation of the Lower Cretaceous

sediments from south-western and central Crimea. Calcareous

nannofossil studies processed on several Lower Cretaceous

sections in south-western Crimea enabled their detailed sub-

division following the CC and NC standard zonations (Shcher-

binina & Loginov 2012). The classical sections described by

T.N. Gorbachik were revisited and PF assemblages were

restudied (see Brovina 2017 and discussion herein; Brovina

et al. 2017) to improve the correlation of the Crimean upper

Barremian–Aptian subdivisions with the Tethyan PF

zonation.

The Crimean Barremian–Aptian ostracods were first found

and described by T.N. Nemirovskaya (1972), but without

stratigraphical analysis. Several decades later, Karpuk (Karpuk

& Tesakova 2010, 2013, 2014; Karpuk 2016 a, b) studied

the species composition, stratigraphical distribution and

paleoecological affinities of the Barremian–Aptian ostracods

of the Crimean Mts. The succession of four ostracod zones was

established in this interval and correlated to the PF and cal-

careous nannofossil zonation (Brovina et al. 2017). The pre-

liminary study of dinocysts in SW Crimea led to the iden tification

of two dinocyst assemblages in the uppermost Barremian and

lowermost Aptian (Shurekova 2016). In the 2000s, paleomag-

netic studies of the Lower Cretaceous defined the position of

the M0 Chron in SW Crimea (Baraboshkin et al. 2004;

Yampolskaya et al. 2006), but magnetostratigraphy of this

interval from E Crimea was not initiated up to now.

This paper presents the first study of the upper Barremian to

Aptian sediments of the Zavodskaya Balka section, south-

eastern Crimea. This work includes the stratigraphic distribu-

tion of planktonic foraminifera, calcareous nannofossils,

ostra cods, palynomorphs and magnetostratigraphy. The obtai-

ned results enabled the first stratigraphic subdivision of

the succession and correlation of the bioevents recognized

among the different groups of microfossils.

Material and methods

Material

The outcrop of Zavodskaya Balka was studied and sampled

in the upper SE part of the ravine crossing the eastern wall of

the abandoned quarry located 1 km eastward from the city of

Feodosia, on the left side of Feodosia – Ordzhonikidze road

(GPS data: 45°1’56” N, 35°20’14” E; Fig. 2). The 33.5 m-thick

mid-Cretaceous muddy succession (dip azimuth — 50°, dip

angle — 20°) with decimetre-scale intercalations of carbonate

and hard ferruginous beds was first sampled using nearly

equal intervals (1.3–1.5 m). 23 samples were collected and on

the basis of a preliminary study, a few additional samples were

taken during a recent field trip from two particular intervals:

one which was suggested to include the OAE1a (between 15.0

and 19.0 m) and another — the Barremian/Aptian boundary

(between 5.3 and 9.0 m). The Barremian–Aptian succession in

the Zavodskaya Balka section consists of light grey mudstones

and contains irregularly intercalated reddish layers. The cal-

cium carbonate content varies throughout the section from

3.92 to 42.85 %. The CaCO

mainly comes from coccoliths,

foraminiferal tests, ostracod valves and carapaces and rare

fragments of macrofossils. The sediment is intensively biotur-

bated mostly by small burrows (up to 0.5 mm in diameter and

few mm in length). The harder intercalations consist of diage-

netic limestone and marlstone concretions made of microcrys-

talline calcite aggregates. Some of these beds can be interpreted

as hardgrounds formed during a process of non-deposition.

They contain manganocalcite, siderite and phosphatic matter

(apatite) (Fig. 3). The TOC content is very low in the whole

succession and irregularly varies between 0.5 and 1.2 %.

Methods

All the samples obtained were processed for paleomagnetic

and micropaleontological analyses using the following

methods.

Calcareous nannofossils: Smear-slides for nannofossil

study were prepared from raw sediment with Norland Optical

Adhesive 61 using standard techniques (Bown & Young

1998). Nannofossils were examined at 1250x magnification

under light microscope Olympus BX41 and their pictures

were made using an Unfinity X video-camera.

Planktonic foraminifera and ostracods: The sample prepa-

ration evolved from the technique described by Sohn (1961).

All ostracod specimens from the 0.1–1 mm fraction were

picked. All PF specimens were picked up from the samples

with rare PF and only the first hundred specimens from

the samples rich in PF. Ostracods and PF images were made

using the CamScan Electron Microscope of the Paleontological

Institute of the Russian Academy of Sciences.

Palynomorphs were studied from 12 samples (23, 19, 17,

15, 14, 13, 1504, 10, 8, 6, 3, 1). Chemical preparation of sam-

ples for palynological study followed the method developed

by the research team of the Geological Institute of the RAS

(see, for example, Shcherbinina et al. 2016). Spores, pollen

and microphytoplankton (dinoflagilates, algae) were exami-

ned at 400–600× magnification under a light microscope Carl

Zeiss Axioplan and their pictures were made using a Canon

PowerShot A640 camera and an Axiovision visualization pro-

gramme. Two hundred specimens were counted from samples

with abundant palynomophs and all specimens from the sam-

ples with less rich palynomophs.

Magnetostratigraphy: The field and laboratory rock-mag-

netism and paleomagnetic studies and data processing were

carried out by standard procedures (Khramov 1982). Oriented

samples were sawn up into 3 to 4 cubes with 2 cm-long sides.

They were treated with magnetic cleaning by variable field

using LDA-3 AF С outfit under the temperature obtained

using the kiln designed by V.P. Aparin. The Lab Petromagnetic

and magneto-mineralogical analysis includes: magnetic

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heating, magnetite becomes the only magnetic mineral left

(Fig. 4A-II).

The effect of Fe hydroxides, such as hydrogoethite (peak

around 100–150 ºC on the second derivative), on thermomag-

netic curves is negligible (Fig. 4A-I). However, the magnetic

saturation curves demonstrate a magnetically rigid phase,

featured for ferric oxides, in the red sediments of sample 8.

This is proved by non-saturation in the high fields (up to

700 mT; Fig. 4B-I). In all other samples (Fig. 4B-II), mainly

the magnetically soft phase, featured for the fine magnetite, is

detected.

The average values of K and J

in the grey mudstones are

66*10

−5

of SI units and 23*10

−3

A/m, respectively, which

indicates high concentrations of magnetite (Fig. 3). The sam-

ples rich in siderite are characterized by abnormally high

values of J

— 179–1080*10

−3

A/m (Fig. 3) and nearly

reversed magnetic fabric with the long axes projections of

the magnetic ellipsoids (K1) approaching the centre of stereo-

projection (Fig. 4C-I). The AMS in the grey mudstones tends

towards classic sedimentary magnetic fabric, where short axes

(K3) are vertical and K1 projections lie along the stereogram

margin (Fig. 4C-II). The ranking of the long axes of the mag-

netic ellipsoids along the NW–SE direction (Fig. 4C-II) is

similar to the arrangement of K1 in the studied earlier

Berriassian mudstones that outcrop 1 km east of the studied

section (Guzhikov et al. 2014; Fig. 4C-III). The similarity

of this parameter throughout the whole territory of

the Crimean Mts. is likely to be caused by large-scale tectonic

compression (Bagaeva & Guzhikov 2014). The shape of

the magnetic particles is defined from the Flinn diagram (Flinn

1965; Fig. 4C). Both elongated and flattened forms of the mag-

netic ellipsoids are characteristic for samples containing side-

rite (Fig. 4C-I); the flattened form of the magnetic ellipsoids

dominates in other mudstones (Fig. 4C-II). This is likely to be

related to the aggregation of sub-micrometer sized ferromag-

netic grains on the flakes of clay minerals.

The age determination of magnetization components, asso-

ciated with siderite or iron hydroxides, is difficult or invalid

because the components are more likely to be of the chemical

genesis. The samples containing these minerals, marked by

anomalously high J

values (> 100*10

−3

A/m; Fig. 3), should

be excluded from consideration. This does not imply signi fi-

cant variations in the structure of the paleomagnetic column.

Paleomagnetic study: All magnetization components are

defined with high accuracy (maximal angle of deviation

(MAD) is less than 10°). Only one magnetization component

is determined in some samples (Fig. 5A-I). Both low-coer-

civity or low-temperature component (C

) and high-coercivity

or high-temperature characteristic component magnetization

(ChRM) are recognized in most of the samples (Fig. 5A-II).

The projections of all components (C

, C

and ChRM) are loca-

ted in the northern rhumbs of the lower hemisphere (Fig. 5B)

that characterizes the magnetization of normal polarity.

A different pattern of the paleomagnetic vectors is observed

during magnetic cleanings of sediments sampled between

the levels 3129-3 and 3129-9: the J

projections displace along

the arcs of the great circles (GC; Fig. 5C). Not less than 4

(mainly 5–8) points were used for the approximation of the

tracks of the changing J

directions during the magnetic clea-

nings (the MAD is less than 10°).

Dating of paleomagnetic components: In the single-compo-

nent samples, the mean C

vector has normal polarity direc-

tion and corresponds to the magnetic inclination near the city

of Feodosia (I = 63.4°; Fig. 5-I). More likely, the sediments

of these intervals were completely remagnetized by the pre-

sent-day geomagnetic field, and C

is a viscuous remanent

magnetization (VRM). In the two-component samples, the mean

and C

vectors statistically coincide (Fig. 5B-I, II, IV),

while the mean direction of ChRM and C

(and ChRM and

) significantly differ (Fig. 5B-I–IV). This pattern is in good

accordance with the hypothesis of the secondary (viscous)

nature of the C

and C

components, related to the modern

magnetic field, and primary nature of the ChRM component.

The regular displacement of the J

projections along

the arcs of GC from lower to upper hemisphere is featured

for reversely magnetized deposits, which were partially

remagnetized by the modern magnetic field. The recognition

of the zones of reverse polarity in the paleomagnetic column

of the section (Fig. 3) is based on the suggestion that the pre-

sence of the ancient reverse polarity component caused

the displacement of the paleomagnetic vectors along the arcs

of great circles.

Since the primary J

components were not reliably identi-

fied, their orientational and/or chemical genesis is still poorly

Fig. 2. Location of the studied section in the general geography (A)

and the sketch-map of the vicinity of the city of Feodosia (B).

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gradually increases from two species in the lower part of the

section (0–7.0 m, samples 23–19) to 9 species in the middle of

the section (17.0–18.3 m, samples 1503–1505), with a small

decrease between 14.0 and 16.5 m (samples 15–13). The inter-

val between samples 10 and 6 (20.2–26.3 m) is characterized

by the occurrence of abundant H. infracretacea, together with

rare H. trocoidea (Gandolfi, 1942) in the restricted interval of

21.8–23 m. Poor and low-diversity PF assemblages are found

in the uppermost part of the section.

We identified six PF zones in the studied succession. The

Blowiella blowi Zone is defined in the lower part of the section

(samples 23–18) by the occurrence of the index species (Fig. 6).

We should emphasize that we accept the view suggesting

the differentiation of two genera: Blowiella Kretchmar and

Gorbachik, 1971 and Globigerinelloides Cushman and ten Dam,

1948. According to this concept, Blowiella specimens have

smooth planispiral tests mainly with few chambers (up to 5),

while Globigerinelloides usually have more chambers (˃ 6)

and coarser sculpture (for more detailed taxonomic discussion

see Brovina 2017).

The successive FOs of Hedbergella ruka (Banner, Copestake

and White, 1993) and Hedbergella excelsa Longoria, 1974 (in

samples 18 and 17, respectively) are very characteristic in

many Crimean sections (Brovina 2017). This enabled us to

establish the H. ruka Bed

in the lowermost Aptian. The FO of

H. excelsa marks the base of an overlying zone (Coccioni et al.

2007). It should be mentioned that the stratigraphic range of

this zone in the studied section differs from the H. excelsa

Zone of Coccioni et al. (2007), where it ranges from the latest

Barremian to the earliest Aptian, while the FO of the marker is

shown in the Deshayesites weissi ammonite Zone (=Des.

forbesi Zone according to Reboulet et al. 2014), which means

Fig. 5. The results of the magnetic component analysis: A and C (from left to right) — stereographic presentation of J

changes in the process

of magnetic cleaning, Ziderweld diagrams, sample demagnetization plots (I — single-component sample, II — two-component sample);

B — stereographic projection of J

components before (left) and after (right) tectonic correction: C

(VRM) (I), C

(VRM) (II), ChRM (III)

, I

— average paleomagnetic declination and inclination, respectively, n — number of samples in a set, k — interbedded paleomagnetic

precision parameter, α

— radius of the vector confidence circle); D — angles formed by mean directions of ChRM, C

, C

. The angles

between paleomagnetic vectors are given with inaccuracy (±) determined by the statistics of these vectors according to Debiche & Watson

1995. If the angle is greater than the inaccuracy, the vectors differ greatly. If the angle is smaller than the inaccuracy, the vectors statistically

match (Debiche & Watson 1995). Legend: 1, 2 — J

projections on the lower semisphere and the upper semisphere, respectively; 3 — line

segments corresponding to the J

components; 4 — great circles; 5 — MAD for each component, 6 — average direction of J

components with

confidence circle, 7 — direction determined by GC intersection with confidence circle.

According to the Russian Stratigraphic Сode, a faunistic Layer or Bed is

an informal biostratigraphic unit, which is characterized by a specific fossil

assemblage, but is inconsistent with any type of biozone, because its boundaries

cannot be clearly defined by any reasons.

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based on the well-known Globigerinelloides phyletic lineage

(Gl. ferreolensis heptacameratus Moullade et al., 2008, Gl.

ferreolensis ferreolensis (Moullade, 1961), Gl. barri (Bolli,

Loeblich and Tappan, 1957), Gl. algerianus Cushman and ten

Dam, 1948) used in the zonation of Moullade et al. (2015)

cannot be applied here due to the absence of these species in

the studied succession. The absence of these multichambered

species, assumed to be deeper water dwellers (Leckie 1987)

might be caused by the low paleodepth of the SE Crimean

basin.

Despite the diachroneity in the FO of H. trocoidea in many

areas (Spain: in Gl. ferreolensis Zone (Coccioni et al. 2007);

South France: in Gl. algerianus Zone (Moullade 1966);

Bavarian calcareous Alps: uppermost Aptian (Risch 1971)

a.o.), this bioevent seems to be the useful regional zonal

marker for the Crimea, as was already shown by previous

studies (Gorbachik 1986; Brovina 2017).

The specimens with few (5–6) chambers in the last whorl,

coalesced perforation cones and cover-plates (Supplementary

Fig. S1:19–22) found in Zavodskaya Balka section can be

attributed to Paraticinella rohri according to the species defi-

nition given by Premoli Silva et al. (2009): “umbilical area is

covered by large flaps from the ultimate and penultimate

chambers that form a cover-plate”, while the inner whorl of

Hedbergella is always exposed. We consider these tests as

Pt. rohri juveniles, as there are only 5–6 chambers, while

adult Pt. rohri have 9 chambers in the last whorl. The FO

of these specimens in sample 6 (25.3 m) is considered

here as the base of the eponym zone. The rare adult

specimens of Pt. rohri are found at the higher level (sample 4,

29.0 m).

In the uppermost part of the outcrop (samples 3–1, 30.8–

33.2 m), PF are very rare and agglutinated benthics widely

dominate the foraminiferal assemblage. Based on a previous

study (Gorbachik 1986), such an assemblage likely corre-

sponds to the lower Albian interval; however, we have no

other indication for an Albian age of this part of the section.

Calcareous nannofossils

The calcareous nannofossils of the Zavodskaya Balka

section show moderate to good preservation and significant

fluctuations in both total abundance and species diversity.

Different species of Watznaueria largely dominate the assem-

blages in the whole studied interval. The warm-water

Rhagodiscus are common, showing minor variations in rela-

tive abundance. In addition, generally rare specimens of

Zeugrhabdotus, Flabellites oblongus and cool-water Assipetra

permanently occur in most of the succession (Supplementary

Figs. S2, S3, Table S2).

The more abundant and diverse nannofossil assemblage is

found in the lower part of the succession (0–14 m, samples

23–15), where it includes Micrantholithus obtusus Stradner,

1963, M. hoschulzii (Reinhardt, 1966), Conusphaera rothii

(Thierstein, 1971), Hayesites irregularis (Thierstein in Roth &

Thierstein, 1972) and common nannoconids. Nannofossils

dramatically reduce their abundance and species diversity at

the level of 15.0 m (sample 14) and disappear in the short

interval comprising samples 1501–1502 (15.5–16.0 m). Above

this interval, nannofossil abundance and species diversity pro-

gressively increase again, but without attaining their former

representativity. The upper part of the section contains only

rare nannofossil specimens, which dramatically decline at

29.0 m (sample 4), but then slightly recover at 33.2 m.

Several nannofossil bioevents were identified in the studied

succession. The occurrence of Hayesites irregularis at the very

base of the section suggests that this interval belongs to

the NC6A Subzone (Fig. 6). In many areas worldwide, the FO

of H. irregularis is documented prior to the base of magnetic

Chron M0 (e.g., Channell et al. 2000; Ogg & Hinnov 2012;

Patruno et al. 2015, a.o.). In the Zavodskaya Balka section,

this species occurs at least at 7.0 m below the Chron M0.

The nannofossil assemblage of NC6A Subzone is distin-

guished by common and diverse nannoconids, which dramati-

cally decline at the top of this subzone interval (sample 16,

12.2 m, Fig. 7). Such nannoconid decline evidently corre-

sponds to widely known events named “nannoconid crises”,

preceding the global Oceanic Anoxic Event 1a (OAE1a; Erba

1994; Aguado et al. 1999; Erba et al. 1999; Habermann &

Fig. 7. Upper Barremian to Aptian nannofossil bioevents in

the Zavodskaya Balka section.

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Mutterlose 1999; Erba & Tremolada 2004; Luciani et al. 2006;

Bottini et al. 2015).

The LO of Conusphaera rothii in the sample 15 (14.0 m)

marks the base of the NC6B Subzone (Roth 1978; Bralower et

al. 1995). The nannofossil abundance tends to impoverish

toward the middle of this subzone and the interval 15.5–16.0 m

(samples 1501–1502) is even nannofossil-free. This interval is

made up of non-calcareous mudstone and might correspond to

OAE1a. However, this assumption needs much more evidence

(e.g., stable isotope analyses) because of low contents of both

TOC and CaCO

at this level. The FO of Eprolithus floralis

(Stradner, 1962) is found above this interval at the level

17.0 m (sample 1503); this event corresponds to the base of

the NC7 Zone (Roth 1978; Bralower et al. 1995). The division

of this interval into subzones is quite difficult, since the LO of

M. hoschulzii, which defines the base of the NC7B Subzone,

is documented much earlier in the Crimea — in the NC6A

Subzone (E. Shcherbinina, personal observations). Although

few specimens of this species are found in sample 1504

(~17.5 m, bottom of NC7 Zone) in the Zavodskaya Balka

section, the inconsistent occurrence of M. hoschulzii in

the section and the diachronicity of its LO in the area make

the location of this boundary rather tentative. The short-time

re-occurrence of rare nannoconids at the level of 17.5 m (sam-

ple 1504) likely corresponds to the episode of “nannoconid

abundance pulse” documented in Italy (Patruno et al. 2015).

The FO of typical Rhagodiscus achlyostaurion (Hill, 1976)

(small Rhagodiscus with bright birefringent spine filling

the central area) is found at the level of 21.5 m (sample 9),

which can suggest the base of the NC7C Subzone. However,

similar specimens with smaller spine occur earlier in some

sections of the Crimea (Brovina et al. 2017), in the lower part

of NC7 Zone, and equivocation of problems in the definition

of this species also leads to some uncertainty on the recogni-

tion of its FO.

Ostracoda

Ostracod assemblages show an uneven distribution through-

out the section. Their total abundance and species diversity are

relatively high in the lower part of the succession (0–12.5 m,

sample 23–16). Their abundance progressively decreases at

the level 14.2 m (sample 15) up to a total elimination in

the interval 15.2–16.0 m (samples 14–1502). Above this inter-

val, the ostracod amount is restored between 16.0–21.5 m

(samples 1503–9), but it never reaches its former abundance

and finally declines in the interval 30.5–33.5 m (samples 3–1)

(Supplementary Fig. S4, Table S3). The species composition

of Lower Cretaceous ostracod assemblages of Crimea appears

to be affected by a marked endemism and thus none of

the proposed zonations (Neale 1978; Wilkinson & Morter

1981; Damotte et al. 1981; Babinot et al. 1985; Lott et al.

1985, 1986; Wilkinson 1988, 2008; Vivers et al. 2000; Woods

et al. 2001; Coimbra et al. 2002; Bachmann et al. 2003) can be

applied in this area. Nevertheless, the recent study of ostracod

stratigraphic distribution in the upper Barremian–Aptian

sediments of the SW Crimea enabled the recognition of several

correlative ostracod Zones (Karpuk 2016 b; Brovina et al.

2017), which were also found in the Zavodskaya Balka

section.

The diverse assemblage of the lower part of section (sam-

ples 23 to 15) includes up to 35 species. The co-occurrence

Loxoella variealveolata Kuznetsova, 1956 and Robsoniella

minima Kuznetsova, 1961 allows the identification in this sec-

tion of the L. variealveolata – R. minima Zone of Karpuk

(2016 b) (Fig. 6).

Several eurybiontic species, such as different cytherellas,

Bairdia projecta, Bythocypris sp., Cytheropteron ventriosum,

reappear at the level of sample 1503, but with few specimens.

Monoceratina bicuspidata (Gründel, 1964) and Dorsocythere

stafeevi Karpuk et Tesakova, 2013 show their FOs at this level

and they gradually tend to dominate the assemblage along

with R. minima, which disappears above sample 9 (16.5 m).

The FO of M. bicuspidata corresponds to the base of

the M. bicuspidata – R. minima Zone, which is defined by

the co-occurrence of these two species. The FO of Saxocythere

omnivaga (Lyubimova, 1965) in sample 10 (~ 20.5 m)

marks the base of the S. omnivaga Zone, where this species

represents its most characteristic feature. Protocythere sp. is

an additional marker of this zone, because it becomes common

in this interval and co-occurs with S. omni

vaga in many sec-

tions studied in Crimea (Karpuk 2016 b). Above the level

~ 24.5 m (sample 7), many ostracod species become extinct

and only a few cytherellas, D. stafeevi, C. ventriosum and

some other species persist but in small amounts. Further

upsection, in the interval 27.5–29.0 m (samples 5–4) only

a few specimens of the genus Cytherella (C. ovata (Roemer,

1841), C. dilatata Donze, 1964, C. infrequens Kuznetsova,

1961) and one valve of Dolocythere rara Mertens, 1956 were

found. The uppermost part of the section (above ~ 30.5m,

sample 3) is ostracod free.

Palynomorphs

All the samples studied contain a high amount of fragments

from plant tissue and coal particles. The palynomorph assem-

blages are dominated by spores and pollen grains, while the

dino cysts percentage is relatively low (at most 10 % of the total

of palynomorphs; Supplementary Table S4). The total abun-

dance of palynomorphs is highest in the middle part of the sec-

tion (16.0–20.2 m, samples 15–10) and progressively decreases

toward the top of the section.

On the basis of the changes in taxonomical composition and

taxa proportions, two spore-pollen assemblages (PA) are dis-

tinguished (Fig. 6). PA1 corresponds to the lower part of

the section (samples 23 and 19). It is dominated by pollen of

the genus Classopollis (60 to 80 %), while fern and bryophyte

spores are scarce.

The PA2 is defined in the interval from 10.7 m (sample 17)

to the top of the studied succession. It is dominated by bisac-

cate pollens of gymnosperms and spores of Gleicheniaceae,

while Classopollis become scarce. The level 16.5 m

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, 2018, 69, 5, 498–511

(sample 13) is the unique episode of relatively increased

Classopollis abundance (45 %) in this interval. Among

the spores, species diversity and abundance of Schizaeaceae

decreases, but several new taxa of Gleicheniaceae appear.

The latter are repre

sented by Gleicheniidites, Clavifera,

Ornamentifera granulata and gradually tend to dominate

the spore assemblage.

The dinocyst assemblages are characterized by low abun-

dance but high species diversity (>80 taxa) (Supplementary

Table S5). They are mostly badly preserved possibly as

a result of unfavourable habitat and/or burial. Three dinocyst

assemblages have been recognized.

The D1 assemblage is identified in the lowermost part of

the section (0–7 m, samples 23, 19; Fig. 6). It is characterized

by the occurrence of Surculosphaeridium sp. III sensu Davey,

1982, Taleisphaera hydra subsp. elongata (late Barremian of

Germany, Heilmann-Clausen & Thomsen, 1995) (Supple-

mentary Fig. S5, Table S5) and Prolixosphaeridium parvi

spinum, which has its FO in the late Barremian in both Boreal

and Tethyan realms (Oosting et al. 2006). In the Zavodskaya

Balka section, the D1 assemblage corresponds to the upper-

most part of the B. blowi Zone and H. ruka Bed, and the greater

part of the NC6A nannofossil Subzone.

The D2 assemblage was recognized in the interval 10.5–

23.0 m (samples 17–8) and can be correlated to the dinocyst

assemblage of the Bedoulian (Lower Aptian) of the Aptian strato-

type sections in southern France (Davey & Verdier 1974). This

D2 assemblage includes Pseudoceratium polymorphum,

which has its FO in the lowermost part of the Aptian, and

Pseudoceratium securigerum and Palaeoperidinium cretaceum,

which show their FOs in the uppermost part of the Barremian

(Heimhofer et al. 2007). The LO of Muderongia cf. staurota

sensu Davey, Verdier, 1974 is found in the lower part of the early

Aptian (Bedoulian) in the stratotype area. In the Zavodskaya

Balka section, it occurs up to the level 10.8 m (sample 17).

This assemblage ranges from the upper part of NC6A to

the lower part of NC7C and the upper part of H. excelsa to

the lower part of H. trocoidea Zones.

The D3 assemblage is found in the upper part of the section

from 23.0 m (samples 6, 3 and 1) and is characterized by

a decline of the majority of the species, which occurred in

the lower part of the section. Only Protoellipsodinium spino

cristatum, Subtilisphaera perlucida, Pterospermella sp.,

several acritarchs and green algae phytomata persist in this

interval. The D3 assemblage correlates to the upper part of

the NC7C Subzone and to the interval including the upper part

of the H. trocoidea Zone and the P. rohri Zone.

Discussion and conclusion

The study of the upper Barremian–Aptian planktonic fora-

minifera, calcareous nannofossils, ostracods and palyno-

morphs of the Zavodskaya Balka showed similar trends in

the distribution of these microfossil groups throughout

the succession: the most abundant and diverse assemblages

are found in the lower part of the section, all microfossils are

progressively eliminated in the interval likely corresponding

to OAE1a, recover part of their initial abundance above this

event and decline again in the upper part of the section. Our

results show the specificity of the occurrence of the late

Barremian–Aptian microfossil markers of south-eastern Crimea

and the correlation between the most important markers of

different microfossil groups. The calcareous nannofossil assem-

blage of the Zavodskaya Balka section is typical for the Tethyan

Barremian–Aptian interval, while PF, ostracods and dinocysts

present some regional specificity. The succession of standard

nannofossil zones and subzones was identified in the section,

although subzonal boundaries within NC7 Zone are not certain

due to scarcity or unreliable species definition of the markers

(M. hoschulzii and R. achlyostaurion, respectively). The absence

from our samples of several stratigraphically important PF

species, such as L. cabri, G. ferreolensis and G. algerianus,

caused a discontinuity in the recognition of several standard

PF zones and thus prevented the direct correlation of the mid-

dle part of the section with the Tethyan PF zonations. The bio-

horizon characterized by the occurrence of H. ruka, recently

established in the Lower Aptian of several sections from

south-western Crimea, has been identified in the Zavodskaya

Balka section in the upper half of the NC6A Subzone.

The H. excelsa Zone, defined by the FO of the zonal marker,

shows a larger stratigraphic range in the studied section than in

the Tethyan area. It roughly corresponds to the upper part

of NC6A and the greater part of NC6B and thus, covers

the part of L. cabri Zone (Coccioni et al. 2007). The FOs of

H. trocoidea and P. rohri are useful bioevents for subdivision

of the late Aptian interval. The succession of ostracod bio-

events in the Zavodskaya Balka section led to identification of

three ostracod zones (R. minima – L. variealveolata, M. bicus

pidata – R. minima and S. omnivaga), recently established in

south-western Crimea. The dinocyst distribution throughout

the section showed the succession of three assemblages deter-

mined by the FOs of the marker species and dominance of

different taxa.

The base of the Aptian in the section is based on the position

of the magnetic reversal assumed to be the base of Chron M0.

The upper Barremian part of the section corresponds to

the lower half of the nannofossil NC6A Subzone, the greater

part of the foraminiferal B. blowi Zone and the D1 dinocyst

assemblage. The ostracod L. variealveolata – R. minima Zone

approximately embraces the upper Barremian–lower Aptian

part of the section.

The lower Aptian is characterized by the highest resolution

in the stratigraphic subdivision based on nannofossil and

ostracod study. Biostratigraphic subdivision of the series is

made still more difficult and uncertain in the upper part of

the section (upper upper Aptian) because of the scarcity of

the microfossils.

One interesting result of this study is the recognition of

an interval likely corresponding to the OAE1a, which has never

been documented in the Aptian sedimentary record of the Crimea

until now. It is preceded by a “nannoconid crisis” and

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, 2018, 69, 5, 498–511

characterized by dramatically reduced productivity of micro-

biota. The specificity of this global event in the Crimea is the

very low TOC content which makes its repercussion distinc-

tive compared to many other world areas, where this event is

featured by sediments rich in TOC (e.g., Jenkyns 1980; Arthur

et al. 1990; Bralower et al. 1994; Föllmi 2012; Giorgioni 2015,

a.o.). Our further study will be focused on the paleoecological

reconstruction of the south-western Crimean basin in the late

Barremian–Aptian with special emphasis on the OAE1a.

Acknowledgements: The authors are grateful to A.G. Manikin

and M.I. Bagaeva, the Saratov State University and to

I.M. Byakin for helping with the collection of samples for paleo-

magnetic study. We appreciate Prof. Michel Moullade,

Dr. Milan Kohut and two anonymous reviewers a lot for their

careful reading of the manuscript, many useful remarks and ad-

vice given to improve the paper. This study was made following

the plans of the scientific research of the Geological Institute

of RAS (for M. Karpuk, E. Brovina, E. Shcherbinina and

E. Tesakova, project no. 0135-2018-0036). Field works were

supported by RFBR projects nos. 16-35-00468 and 16-05-

00363 (M. Karpuk and E. Brovina). Analytical data were deri-

ved with partial support of the RAS presidium program (for

E. Shcherbinina and E. Shchepetova no. 0135-2018-0050).

References

Aguado R., Castro J.M., Company M. & De Gea G.A. 1999: Aptian

bio-events—an integrated biostratigraphic analysis of the Alma-

dich Formation, Inner Prebetic Domain, SE Spain. Cretaceous

Res. 20, 663–683.

Arkadiev V.V. 2004: The first record of a late Tithonian ammonite in

the Feodosiya section of Eastern Crimea. Paleontol. J. 38, 3,

265–267.

Arkadiev V.V. 2007: Zonation of the Berriasian sediments of the

Mountain Crimea. Vestnik of Saint Petersburg University, Earth

sciences, ser. 7, 2, 27–43 (in Russian).

Arkadiev V.V. 2011: New data on ammonoids of the genus Paraula

cosphinctes from the upper Tithonian of the Mountainous

Crimea. Stratigraphy and Geological Correlation, 19, 2,

238–242.

Arkadiev V.V., Grishchenko V.A., Guzhikov A.Yu., Manikin A.G.,

Savelieva Yu.N., Feodorova A.A. & Shurekova O.V. 2017:

Ammonites and magnetostratigraphy of the Berriasian–

Valanginian boundary deposits from eastern Crimea: Geol.

Carpath., 68, 6, 505–516.

Arkadiev V., Guzhikov A., Baraboshkin E., Savelieva J., Feodorova A.,

Shurekova O., Platonov E. & Manikin A. 2018: Biostratigraphy

and magnetostratigraphy of the upper Tithonian–Berriasian of

the Crimean Mountains: Cretaceous Res. 87, 5–41.

Arthur M.A., Jenkyns H.C., Brumsack H.J. & Schlanger S.O. 1990:

Stratigraphy, geochemistry, and paleoceanography of organic

carbon–rich Cretaceous sequences. In: Ginsburg R.N. &

Beaudoin B. (Eds.): Cretaceous Resources, Events and Rhythms:

Background and Plans for Research, NATO ASI Series, C 304,

75–119.

Babinot J.-F., Damotte R., Donze P., Grosdidier E., Oertli, H.J. &

Scarenzi-Carboni G. 1985: Cretace Inferieur, In Oertli H.J.

(Ed.), Atlas des ostracodes de France (Paléozoïque-Actuel):

Bull. Centres Rech. Explor. Prod. ElfAquitaine, 9, 163–210.

Bachmann M., Bassiouni M. A. A., & Kuss J. 2003: Timing of

mid-Cretaceous carbonate platform depositional cycles, northern

Sinai, Egypt. Palaeogeogr. Palaeoclimatol. Palaeoecol. 200,

131–162.

Bagaeva M.I. & Guzhikov A.Yu. 2014: Magnetic textures as indica-

tors of formation of Tithonian-Berriasian rocks of the Mountain

Crimea. Izvestiya of Saratov University. New Series. Series:

Earth Sciences 14, 1, 41–47 (in Russian).

Baraboshkin E.Yu. 2016: Geological history of the Crimea. Precam-

brian–Early Cretaceous. In: Baraboshkin E.Yu. & Yaseneva E.V.

(Eds.): Ecological and resource potential of the Crimea. History

of formation and prospects of development: VVM 1, 38–84 (in

Russian).

Baraboshkin E.Yu., Guzhikov A.Yu., Mutterlose J., Yampolskaya

O.B., Pimenov M.V. & Gavrilov S.S. 2004: New data on strati-

graphy of the Barremian-Aptian of the Mountain Crimea in

accordance to finding of the analogue of the magnetochron M0

in the Verkhorechie section. Vestnik of the Moscow State Univer

sity, Geology series 1, 10–20 (in Russian).

Bolii H. 1959: Planktonic foraminifera from the Cretaceous of

Trinidad. Bull. Amer. Paleontol., 257–277.

Bolli H. 1966: Zonation of cretaceous to pliocene marine sediments

based on planktonic foraminifera. Bol. Inform. Asoc. Venez.

Geol., Miner., Petrol. 9, 1, 3–32.

Bottini C., Erba E., Tiraboschi D., Jenkyns H.C., Schouten S. &

Sinninghe Damsté J. S., 2015: Climate variability and ocean

fertility during the Aptian Stage. Climate of the Past, 11,

383–402.

Bown P.R. & Young J.R. 1998: Techniques. In Bown P.R. (Ed.). Cal-

careous Nannofossil Btostratigraphy: Kluwer Academic Press,

Dordrecht, 16–28.

Bown P.R., Rutledge D.C., Crux J.A. & Gallagher L.T., 1998:

Lower Cretaceous. In: Bown P.R. (Ed.): Calcareous Nanno-

fossil Biostratigraphy: Kluwer Academic Press, Dordrecht,

86–131.

Bralower T.J., Arthur M.A., Leckie R.M., Sliter W.V., Allard D.J. &

Schlanger S.O. 1994: Timing and palaeoceanography of oceanic

dysoxia/anoxia in the late Barremian to early Aptian (early Cre-

taceous). Palaios 9, 335–369.

Bralower T.J., Leckie R.M., Sliter W.V. & Therstein H. R. 1995.

An intergrated Cretaceous microfossil biostratigraphy. In: Berggren

W.A., Kent D.V. & Hardenbol, J. (Eds.), Geochronology, Time

Scales and Global Stratigraphic Correlations: SEPM Spec. Publ.

54, 65–79.

Brovina E.A. 2017: Problems in stratigraphy of the upper Barremian

– Aptian of the Cremia using planktonic foraminifera. Strati

graphy and Geological Correlation, 25, 5, 41–57 (in Russian).

Brovina E.A., Karpuk M.S., Shcherbinina E.A. & Tesakova E.M.

2017: Stratigraphy of r. Alma basin Aptian deposits based on

new micropaleontological data. Bulleten MOIP. Otd. Geologii,

92, 6, 26–42 (in Russian).

Channell J.E.T., Erba E., Muttoni G. & Tremolada F. 2000: Early

Cretaceous magnetic stratigraphy in the APTICORE drill core

and adjacent outcrop at Cismon (Southern Alps, Italy), and cor-

relation to the proposed Barremian–Aptian boundary stratotype.

GSA Bulletin 112, 9, 1430–1443.

Coccioni R., Premoli Silva I., Marsili A. & Verga D. 2007: First

radiation of Cretaceous planktonic foraminifera with radially

elongate chambers at Angles (Southeastern France) and bio-

stratigraphic implications. Revue de micropaleontologie 50,

215–224.

Coccioni R., Jovane L., Bancalà G., Bucci C., Fauth G., Frontalini F.,

Janikian L., Savian J., Paes De Almeida P., Mathias G.L. &

Da Trindade R.I.F. 2012: Umbria-Marche Basin, Central Italy:

A Reference Section for the Aptian-Albian Interval at Low Lati-

tudes. Scientific Drilling 13, 42–46.

510

KARPUK, SHCHERBININA, BROVINA, ALEKSANDROVA, GUZHIKOV, SHCHEPETOVA and TESAKOVA

GEOLOGICA CARPATHICA

, 2018, 69, 5, 498–511

Coimbra J.C., Arai M. & Carreno A. L. 2002: Biostratigraphy of

Lower Cretaceous microfossils from the Araripe basin, north-

eastern Brazil. Geobios 35, 687–698.

Damotte R., Babinot J.-F. & Colin J-P. 1981: Les Ostracodes du

Cretace Moyen Europeen. Cretaceous Res. 2, 287–306.

Davey R. J. & Verdier J. P. 1974: Dinoflagellate cysts from the Aptian

type sections at Gargas and La Bédoule, France. Palaeontology

17, 3, 623–653.

Debiche M.G. & Watson G.S. 1995: Confidence limits and bias cor-

rection for estimating angles between directions with applica-

tions to paleomagnetism. Journal of Geophysical Research, 100,

B12, 24405–24430.

Erba E. 1994: Nannofossils and superplumes: The early Aptian

“nannoconid crisis”. Paleoceanography 9, 3, 483–501.

Erba E., & Tremolada F. 2004: Nannofossil carbonate fl uxes during

the Early Cretaceous: Phytoplankton response to nutrifi cation

episodes, atmospheric CO2 and anoxia. Paleoceanography 19,

PA1008.

Erba E., Aguado R., Avram E., Baraboschkin E.J., Bergen J.A.,

Bralower T.J., Cecca F., Channell J.E.T., Coccioni R.,

Company M., Delanoy G., Erbacher J., Herbert T.D.,

Hoedemaeker P., Kakabadze M., Leereveld H., Lini A.,

Mikhailova I.A., Mutterlose J., Ogg J.G., Premoli Silva I.,

Rawson P.F., Von Salis K. & Weissert H. 1996: The Aptian

stage: Bulletin de l’institut Royal des sciences naturelles

de Belgique. Proceedings “Second International Symposium on

Cretaceous Stage Boundaries”. Brussels 8 16 September 1995,

31–43.

Erba E., Channell J.E.T., Claps M., Jones C., Larson R., Opdyke B.,

Premoli Silva I., Riva A., Salvini G., & Torricelli S. 1999:

Integrated stratigraphy of the Cismon Apticore (southern Alps,

Italy); a “reference section” for the Barremian-Aptian interval

at low latitudes. J. Foram. Res. 29, 4, 371–391.

Flinn D., 1965: Оn the symmetry principle and the defоrmatiоn

ellipsоid. Geоl. Mag. 102, 36–45.

Föllmi K.B. 2012: Early Cretaceous life, climate and anoxia.

Cretaceous Res. 35, 230–257.

Gorbachik T.N. 1959: New foraminifera species from the lower

Cretaceous deposits of the Crimea and SW Caucasus. Paleonto

logical Journal 1, 78–83 (in Russian).

Gorbachik T.N. 1964: Variability and mircosturcture of the test wall

of the Globigerinelloides algerianus Cushman et Dam.

Paleontological Journal 4, 32–37 (in Russian).

Gorbachik T.N. 1969: Peculiarity of foraminifer distribution of in the

Berriassian and Valanginian sediments of the Crimea. Vestnik

MSU, ser. 4, Geology 4, 56–67 (in Russian).

Gorbachik T.N. 1986: Jurassic and Early Cretaceous planktonic

foraminifera of the south of USSR. Nauka, Moskva, 1–239

(in Russian).

Gorbachik T.N. & Krechmar V. 1969: Stratigraphical subdivision of

the Aptian and Albian sediments of the Crimea using planktonic

foraminifera. Vest. MSU, Ser. 4, Geology 3, 46–56 (in Russian).

Giorgioni M., Keller C.E., Weissert H., Hochuli P.A. & Bernasconi S.M.

2015: Black shales — from coolhouse to greenhouse (early

Aptian). Cretaceous Res. 56, 716–731.

Guzhikov A.Yu., Arkadiev V.V., Baraboshkin E.Yu., Bagaeva M.I.,

Piskunov V.K., Rudko S.V., Perminov V.A. & Manikin A.G.

2012: New sedimentological, bio-, and magnetostratigraphic

data on the Jurassic–Cretaceous Boundary Interval of Eastern

Crimea (Feodosiya). Stratigraphy and Geological Correlation,

20, 3, 261–294.

Guzhikov A., Bagayeva M. & Arkadiev V. 2014: Magnetostrati-

graphy of the Upper Berriasian “Zavodskaya Balka” section

(East Crimea, Feodosiya). Volumina Jurassica XII, 1, 175–184.

Habermann A. & Mutterlose J. 1998. Early Aptian blackshales from

NW Germany: calcareous nannofossils andtheir palaeoceano-

graphic implications. Neues Jahrb. Geol. Paläontol. 212, 1–3,

379–400.

Heilmann-Clausen C. & Thomsen E. 1995: Barremian-Aptian dino-

flagellates and calcareous nannofossils in the Ahlum 1 borehole

and the Otto Gott clay pit, Sarstedt, Lower Saxony Basin,

Germany. In Kemper E. (Ed.): The Barremian-Aptian Boundary.

A Study of profiles from the Boreal Cretaceous. Geologisches

Jahrbuch Reihe A, 141, 257–365.

Heimhofer U., Hochuli P.A., Burla S. & Weissert H. 2007: New

records of Early Cretaceous angiosperm pollen from Portuguese

coastal deposits: Implications for the timing of the early angio-

sperm radiation. Review of Palaeobotany and Palynology, 144,

39–76.

Jenkyns H.C. 1980: Cretaceous anoxic events: from continents to

oceans: J. Geol. Soc. 137, 171–188.

Karpuk M.S. 2016a: New Protocytherines (Ostracods) from the Low-

er Cretaceous sequences of the Crimean Peninsula. Revue de

micropaléontologie 59, 180–187.

Karpuk M.S. 2016b: Biostratigraphy of the upper Barremian–Aptian

of the Mountain Crimea based on Ostracodes. In: Baraboshkin

E.Yu. (Ed.): Proceedings of 8-th All-Russian Symposium on the

Cretaceous system, Simferopol, 142–145 (in Russian).

Karpuk M.S. & Tesakova E.M. 2010: Lower Cretaceous ostracodes

of the Verkhorechie section (SW Crimea). In: Baraboshkin E.Yu.

(Ed.): Proceedings of 5-th All-Russian Symposium on the Creta-

ceous system, Ulianovsk, 188–191 (in Russian).

Karpuk M.S. & Tesakova E.M. 2013: New ostracods of the Family

Cytheruridae G. Mueller from the Barremian-Albian of the

Southwestern Crimea. Paleontological Journal (Moscow), 47,

6, 588–596.

Karpuk M.S. & Tesakova E.M. 2014: New ostracods of the families

Loxoconchidae and Trachyleberididae from the Barremian-Al-

bian of southwestern Crimea. Paleontological Journal 48, 2,

177–181.

Khramov A.N. (Ed.) 1982: Paleomagnetology: Nedra, St. Petersburg,

1–312 (in Russian).

Leckie R.M. 1987: Paleoecology of mid-Cretaceous planktonic fora-

minifera: A comparison of open ocean and Epicontinental Sea

assemblages. Micropaleontology 33, 2, 164–176.

Lott G.K., Ball K.C. & Wilkinson I.P. 1985: Mid-Cretaceous strati-

graphy of a cored borehole in the western part of the Central

North Sea Basin. Proceedings of the Yorkshire Geological

Society 45, 4, 235–248.

Lott G.K., Fletcher B. N. & Wilkinson I.P. 1986: The stratigraphy of

the Lower Cretaceous Speeton Clay Formation in a cored bore-

hole off the coast of north-east England. Proceedings of the

Yorkshire Geological Society 46, 1, 39–56.

Luciani V., Cobianchi M. & Lupi C. 2006: Regional record of

a global oceanic anoxic event: OAE1a on the Apulia Platform

margin, Gargano Promontory, southern Italy. Cretaceous Res.

27, 754–772.

Moullade M. 1966. Etude stratigraphique et micropaléontologique du

créetacé inférieur de la “fosse vocontienne”. Stratigraphy.

Université de Lyon, 1–369.

Moullade M. 1974: Zones de foraminiferes du cretace inferieur

mesogeen. Comptes Rendus Hebdomadaires des Séances de

l’Académie des Sciences de Paris D278, 1813–1816.

Moullade M., Tronchetti G., Busnardo R. & Masse J.-P. 1998a.

Description lithologique des coupes types du stratotype his-

torique de l’Aptien inférieur dans la région de Cassis-La Bédoule

(SE France). Géologie Méditerranéenne 25, 15–29.

Moullade M., Masse J.-P., Tronchetti G., Kuhnt W., Ropolo P., Bergen

J.A., Masure E. & Renard M. 1998b. Le stratotype historique de

l’Aptien inférieur dans la région de Cassis-La Bédoule (SE

France): Synthèse stratigraphique. Géologie Méditerranéenne

25, 289–298.

511

STRATIGRAPHY OF THE UPPER BARREMIAN–APTIAN SEDIMENTS FROM THE SOUTH-EASTERN CRIMEA

GEOLOGICA CARPATHICA

, 2018, 69, 5, 498–511

Moullade M., Tronchetti G. & Bellier J.-P. 2005: The Gargasian

(Middle Aptian) strata from Cassis-La Bédoule (Lower Aptian

historical stratotype, SE France): Planktonic and benthic fora-

miniferal assemblages and biostratigraphy. Carnets de Géologie,

Article 2005/02, 1–20.

Moullade M., Granier B. & Tronchetti G. 2011: The Aptian Stage:

Back to fundamentals. Episodes 34, 3, 148–156.

Moullade M., Tronchetti G., Granier B., Bornemann A., Kuhnt W. &

Lorenzen J. 2015: High-resolution integrated stratigraphy of the

OAE1a and enclosing strata from core drillings in the Bedoulian

stratotype (Roquefort-La Bedoule, SE France). Cretaceous Res.

56, 119–140.

Neale J.W. 1978: A stratigraphycal index of British Ostracoda. In:

Bate R. & Robinson E. (Eds.): Geol. J. Spec. Iss. 8, 325–384.

Nemirovskaya T.N. 1972: About the Barremian and Aptian ostracods

of the South-Western Crimea. In: Questions about the geology

of the sedimentary basins of the Ukraine. Kiev, 15–20 (in Rus-

sian).

Ogg J.G. & Hinnov L.A. 2012: Cretaceous. In: Gradstein F.M.,

Ogg J.G., Schmitz M.D. & Ogg G.M. (Eds.): Geological Time

Scale. Elsevier, 793–853.

Ogg J.G., Ogg G.M. & Gradstein F.M. 2016: A Concise Geologic

Time Scale, Elsevier, Amsterdam, 1–230.

Oosting A.M., Leereveld H., Dickens G.R., Henderson R.A. &

Brinkhuis H. 2006. Correlation of Barremian-Aptian (mid-

Cretaceous) dinoflagellate cyst assemblages between the Tethyan

and Austral realms. Cretaceous Res. 27, 6, 792–813.

Opdyke N.D. & Channell J.E.T. 1996: Magnetic Stratigraphy.

Academic pr

ess. N.Y., 1–344.

Patruno S., Triantaphyllou M.V., Erba E., Dimiza M.D., Bottini C. &

Kaminski M.A. 2015. The Barremian and Aptian stepwise

development of the ‘Oceanic Anoxic Event 1a’ (OAE 1a) crisis:

Integrated benthic and planktic high-resolution palaeoecology

along the Gorgo a Cerbara stratotype section (Umbria–Marche

Basin, Italy). Palaeogeogr. Palaeoclimatol. Palaeoecol. 424,

147–182.

Premoli Silva I., Caron M., Leckie R.M., Petrizzo M.R., Soldan D. &

Verga D. 2009. Paraticinella n. gen. and taxonomic revision of

Ticinella bejaouaensis Sigal, 1966. The Journal of Foraminiferal

Research 39, 2, 126–137.

Reboulet S., Szives O., Aguirre-Urreta B., Barragán R., Company M.,

Idakieva V., Ivanov M., Kakabadze M.V., Moreno-Bedmar J.A,

Sandoval J., Baraboshkin E.J., Çaglar M.K., Fozy I.,

González-Arreola C., Kenjo S., Lukeneder A., Raisossadat S.N.,

Rawson P.F. & Tavera J.M. 2014: Report on the 5th International

Meeting of the IUGS Lower Cretaceous Ammonite Working

Group, the Kilian Group (Ankara, Turkey, 31st August 2013).

Cretaceous Res. 50, 126–137.

Risch H. 1971: Stratigraphie der höheren Unterkreide der bayerischen

Kalkalpen mit Hilfe von Mikrofossilien. Palaeontographica

Abteilung A138, 1–80.

Roth P.H. 1978: Cretaceous nannoplankton biostratigraphy and

oceanography of the northwestern Atlantic Ocean. In: Benson W.E.,

Sheridan R.E. et al. (Eds.): Init. Repts. DSDP 44, Washington

(U.S. Govt. Printing Office), 731–759.

Salman G.B. & Dobrovolskaya T.I. 1968: The Valanginian–Barremian

conglomerates of the eastern Crimea. Proceedings of the Aca

demy of Sciences of USSR, 133, 6, 1432–1434 (in Russian).

Savian J., Trindade R., Janikian L., Jovane L., Paes de Almeida P.,

Coccioni R., Frontalini F., Sideri M., Figueiredo M., Tedeschi L.R.

& Jenkins J. 2016: The Barremian-Aptian boundary in the

Poggio le Guaine core (central Italy): Evidence for magnetic

polarity Chron M0r and oceanic anoxic event 1a. The Geological

Society of America Special Paper 524, 57–78.

Shcherbinina E.A. & Loginov M.A. 2012: Lower Cretaceous nanno-

fossilstratigraphy of the Sw Crimea. In: Vishnevskaya V.S.,

Goreva N.V. & Filimonova T.V. (Eds.): Proceedings of XVth

Allrussian micropaleontological symposium, Gelendzhik,

324–327 (in Russian).

Shcherbinina E., Gavrilov Yu., Iakovleva A., Pokrovsky B.,

Golovanova O. & Aleksandrova G., 2016. Environmental dyna-

mics during the Paleocene–Eocene thermal maximum (PETM)

in the northeastern Peri-Tethys revealed by high-resolution

micropalaeontological and geochemical studies of a Caucasian

key section. Palaeogeogr. Palaeoclimatol. Palaeoecol. 456,

60–81.

Shumenko S.I. 1974: Lower Cretaceous calcareous nannofossils of

the Crimea. Bulletin of the High Scools, Geology and Explora

tion Series N9, 52–60 (in Russian).

Shurekova O.V. 2016: Stratigraphical scale based on dinocysts for

lower Cretaceous of the Crimea. In: Tolmacheva T.Yu. (Ed.)

: Proceedings of the workshop: Stratigraphical scale and metho-

dical problems in regional Russian stratigraphical scales deve-

lopment, 188–190.

Sigal J. 1977: Essai de zonation du cretace mediterranean a l’aide des

foraminiferes planctoniques. Géologie méditerranéenne 4,

49–108.

Sissingh W. 1977: Biostratigraphy of Cretaceous calcareous nanno-

plankton. Geol. Mijnbouwn, 56, 37–50.

Sohn I.G. 1961: Techniques for preparation and study of fossil ostra-

cods. In: Treatise on Invertebrate Paleontology. Part Q, Arthro-

poda 3, Crustacea, Ostracoda, 64–70.

Szives O., Fodor L., Fogarasi A. & Kövér Sz. 2018: Integrated calca-

reous nannofossil and ammonite data from the upper Barremian

– lower Albian of the northeastern Transdanubian Range

(central Hungary): Stratigraphical implications and conse-

quences for dating tectonic events. Cretaceous Research 91,

229–250.

Van Der Voo R. 1993: Palaeomagnetism of the Atlantic, Tethys,

and Iapetus oceans, Cambridge. Cambridge University Press,

1–412 .

Vishnevsky A.V. & Menaylenko P.A. 1963: Coccolithoforids of

the lower Cretaceous (Aptian) clays of the Bakhchisaray area.

Bulletin of the High Scools, Geology and Exploration Series 11,

47–53 (in Russian).

Viviers M.C., Koutsoukos E.A.M., da Silva-Telles A.C. Jr. &

Bengtson P. 2000: Stratigraphy and biogeographic affinities of

the late Aptian–Campanian ostracods of the Potiguar and

Sergipe basins in northeastern Brazil. Cretaceous Res. 21,

407–455.

Wilkinson I.P. 1988: Ostracoda across the Albian/Cenomanian

Boundary in Cambredgeshire and Western Suffolk, Eastern

England. Evolutionary Biology of Ostracoda its fundamentals

and applications. In: Hanai T., Ikeya N. & Ishizaki K. (Eds.):

Developments in Palaeontology and Stratigraphy, 11,

1229–1244.

Wilkinson I.P. 2008: The effect of environmental change on early

Aptian ostracods faunas in the Wessex Basin, southern England.

Revue de micropaleontology 51, 259–272.

Wilkinson I.P. & Morter A.A. 1981: The biostratigraphical zonation

of the East Anglian Gault by Ostracoda. In: Neale J.W. &

Brasier M.D. (Eds.): Microfossils from Recent and Fossil Sherf-

Seas. Ellis Horwood, Ltd., Chichester. 163–176.

Woods M.A., Wilkinson I. P., Dunn J. & Ridingl J. B. 2001: The bio-

stratigraphy of the Gault and Upper Greensand formations

(Middle and Upper Albian) in the BGS Selborne boreholes,

Hampshire. In: BGS Selborne boreholes, Hampshire. Proceed

ings of the Geologists’ Association 112, 211–222.

Yampolskaya O.B., Baraboshkin E.Yu., Guzhikov A.Yu., Pimenov M.V.

& Nikulshin A.S. 2006: Paleomagnetic column of the Lower

Cretaceous of the South-Western Crimea. Vestnik of the Moscow

State University, Geology series 1, 3–15.

STRATIGRAPHY OF THE UPPER BARREMIAN–APTIAN SEDIMENTS FROM THE SOUTH-EASTERN CRIMEA

GEOLOGICA CARPATHICA

, 2018, 69, 5, 498–511

1501

1502

1503

1504

1505

Hedber

gella infracr

etacea

Blowiella blowi Hedber

gella ruka

Hedber

gella excelsa

Hedber

gella sigali

Hedber

gella aptiana

Hedber

gella similis

Hedber

gella primar

Hedber

gella luterbacheri

Hedber

gella r

oblesae

Hedber

gella kuhryi

Leupoldina r

eiche

Hedber

gella tr

ocoidea

Planomalina cheniour

ensis

Paraticinella r

ohri

Sample nos.

U. Barremian

Lower

Aptian

Upper

Aptian

Substages

Species

f
f
f
f
f

a
a
a
a
a
a
c
c

f
f
f
f
f
f
f f

f r

r r

f f f

c c

r r

r
r
r
r

f
r
r

f
f
f f

r f

B. blowi

H. excelsa

trocoidea

P. r

ohri

Foraminifera zones

- H. luterbacheri

- H. ruka Bed

Table S1. The PF range chart of Zavodskaya Balka section. Symbols: a – abundant (20 specimens in the picked up material, p.m.), с – common (10–20

specimens in the p.m.), r – rare (3–10 specimens in the p.m.), f – few (1–2 specimens in the p.m.).

Table S1: The PF range chart of Zavodskaya Balka section. Symbols: a — abundant (20 specimens in the picked up material, p.m.), с — com-

mon (10–20 specimens in the p.m.), r — rare (3–10 specimens in the p.m.), f — few (1–2 specimens in the p.m.).

vii

KARPUK, SHCHERBININA, BROVINA, ALEKSANDROVA, GUZHIKOV, SHCHEPETOVA and TESAKOVA

GEOLOGICA CARPATHICA

, 2018, 69, 5, 498–511

1501

1502

1503

1504

1505

Sample nos.

U. Barremian

Lower Aptian

Upper Aptian

Substages

Nannofossils species

Assipetra terebr

odentarius terebr

odentarius

Conusphaera rothii

Flabellites oblongus

Hayesites irregularis

Lithraphidites carniolensis

Micrantolithus hoschulzii

Micrantolithus obtusus

Nannoconus bonetii

Nannoconus circularis

Nannoconus inornatus

Nannoconus kamptneri

Nannoconus steinmannii

Nannoconus truittii

Percivalia fenestrata

Retecapsa angusiphorata

Retecapsa crenulata

Rhagodiscus asper

Rotelapillus laﬃttei

Watznauria barnesae/fossacincta

Zeugrhabdotus diplogrammus

Zeugrhabdotus ember

geri

Zeugrhabdotus er

ectus

Zeugrhabdotus howei

Zeugrhabdotus xenotus

Haquis circumradiatus

Watznaueria britannica

Axopodorhabdus diettzmannii

Tubodiscus burnettiae

Assipetra terebr

odentarius youngii

Nannoconus vocontiensis

Rhagodiscus amplus

Watznaueria manivitae

Manivitella pemmatoidea

Cretar

habdus striatus

Nannoconus elongatus

Staurolithites mutterlosii

Zygrhabdotus noeliae

Biscutum constans

Nannoconus globulus

Cretar

habdus conicus

Crucibiscutum bosunensis

Tegumentum stradneri

Grantarhabdus cor

onadventis

Repagulum parvidentatum

Staurolithites sciesseri

Zeugrhabdotus str

eetiae

Eiﬀellithus hankockii

Stoverius acutus

Watznaueria biporta

Eprolithus ﬂoralis

Radiolithus planus

Rhagodiscus achlyostaurion

f r

Nannofossils zones

NC6A

NC6B

NC7A

NC7B

NC7C

Nannoconus wassalii

Nannoconus bucheri

Chiastozygus litterarius

Farhania var

olii

Nannoconus donatensis

Nannoconus quadricanalis

Calcicalathina erbae

Pickelhaube furtiva

Nannofossils are absent

TABLE S2. – The nannofossil range chart of Zavodskaya Balka sec

tion. Symbols: a - abundant ( 5 specimens per field of view, f

.v.), с - common (1-4 specimens per

f.v.), r - rare (several specimens per the row of the smear-sli

de), f - few (several specimens in the smear-slide).

Table S2:

The

nannofossil

range

chart

Zavodskaya

Balka

section.

Symbols:

—

abundant

( 5

specimens

per

field

view

, f.v

.),

—

common

(1–4

specimens

per

f.v

.),

r —

rare

(several

specimens

per the row of the smear

-slide), f — few (several specimens in the smear

-slide).

viii

STRATIGRAPHY OF THE UPPER BARREMIAN–APTIAN SEDIMENTS FROM THE SOUTH-EASTERN CRIMEA

GEOLOGICA CARPATHICA

, 2018, 69, 5, 498–511

1501

1502

1503

1504

1505

Cyther

ella ovata

Cyther

ella dilatata

Gen. 21 sp. Eucytherura miriﬁca

1
1

5 1

Bair

dia pr

ojecta

Cyther

opter

on latebr

osum

Robsoniella minima Robsoniella obovata Bythocypris

sp.

Exophthalmocyther

e poster

opilosa

Bair

dia

sp. 2

Eucytherura

sp. 15

Paracypris acuta

Loxoella variealveolata

2
1

29
33
25

8
2

1
2
2
1
3

90
78

6
4

40
32
26
15
19

1
1

10 1

7
2
5

1
1 1

2 4

2 1

3
2

47
27

2
2 1

3
3
4

2
2
4
1

"Macr

ocypris

" sp. 2

Pontocypris explorata

Gen. 6 sp.

Eucytherura

sp. 7

Loxoconcha

sp. 1

Gen. 23 sp. Gen. 9 sp. Gen. 25 sp. Monoceratina tricuspidata

2 2

4 2 1 2 1 1

Sigillium pr

ocerum

Gen. 40 sp. Gen. 39 sp. Paracypris

cf.

alta

Gen. 2 sp. Loxoella ? macr

ofoveata

Pedicyther

e longispina

Pleur

ocyther

e costaﬂexuosa

Bair

dia

sp. 4

Pseudocyther

e sp. 1

3 2

1 1

1
1

1 9

Gen. 3 sp.

3
6

Pontocypris

sp.

ocytherura

sp. 5

Gen. 13 sp. Pedicyther

e sp. 2

Gen. 28 sp.

Gen. 27 sp. Gen. 45 sp. Gen. 31 sp. Cyther

opter

on ventriosum

Cyther

ella infr

equens

Gen. 8 sp.

1 8

2
1

4
1
6

1 1

ocyther

opter

sp. 1

ocytherura

sp. 7

Cyther

opter

sp. 3

ocytherura

sp. 6

ocyther

opter

sp. 2

Cyther

ella

cf.

eosulcata

1 1

ocytherura

sp. 2

Cyther

ella lubimovae

Gen. 42 sp.

ocytherura

aﬀ.

beerae

Aratr

ocypris

sp.

1 4

Sample nos.

U. Barremian

Lower

Aptian

Upper

Aptian

Substages

Ostracod species

R. minima - L. variealveolata

M. bicuspidata - R. minima

S. omnivaga

Ostracoda zones

1501

1502

1503

1504

1505

Eucytherura

sp. 16

1 1

Amphicytherura

cf.

roemeri

Gen. 17 sp.

Gen. 1 sp. 1 Pontocypr

ella

rara

Asciocyther

e poster

otunda

Eucytherura

sp. 1

Gen. 1

1 sp.

Shuleridea der

ooi

1
1

1
4 1

1 3 2 2

1
1

Eucytherura

sp. 13

ocytherura

sp. 4

Gen. 30 sp. Gen. 10 sp. Gen. 12 sp.

Gen. 35 sp.

Cyther

ella exquisita

Gen. 44 sp. Pseudocytherura

sp. 2

Gen. 24 sp. "Macr

ocypris

" sp. 1

2 2

1 1 2 7 2

1 1

6 2

4 3

Pseudocyther

e sp. 3

Eucytherura

sp. 8

Ovocytheridea

sp.

Robsoniella longa Pontocypr

ella maynci

ocyther

opter

sp. 3

ocytherura

sp. 1

Eucytherura

sp. 1

Eucytherura monstrata Dolocytheridea vinculum Gen. 51 sp. Eocyther

opter

sp.

Par

exophthalmocyther

e r

odewaldensis

1 4 4 2

1 1 1

Neocyther

e (Physocyther

e) vir

ginea

Neocyther

e vanveeni

Gen. 41 sp. Monoceratina bicuspidata Dorsocyther

e stafeevi

Loxoella? micr

ofoveata

Paraphysocyther

sensu

Babinot et al.

1 1

2 1

1 1

Gen. 5 sp. Eucytherura

sp. 20

Paranotacyther

e sp.

Eucytherura

sp. 10

Eucytherura

aﬀ.

kotelensis

Saxocyther

e omnivaga

otocyther

sp.

Pontocypr

ella harrisiana

Cyther

ella gigantosulcata

Dolocyther

e rara

Cyther

ella

cf.

pilicae

Gen. 32 sp.

Eucytherura

sp. 4

1 2 1

15 15

5
4

8 1

1 1 1

Sample nos.

Ostracod species

U. Barremian

Lower

Aptian

Upper

Aptian

Substages

R. minima - L. variealveolata

M. bicuspidata - R. minima

S. omnivaga

Ostracoda zones

Ostracods are absent

TABLE S3. – The ostracod range chart of Zavodskaya Balka section. Numbers are the abundance of

specimens found in the sample.

Table S3: The ostracod range chart of Zavodskaya Balka section. Numbers are the abundance of specimens found in the sample.

KARPUK, SHCHERBININA, BROVINA, ALEKSANDROVA, GUZHIKOV, SHCHEPETOVA and TESAKOVA

GEOLOGICA CARPATHICA

, 2018, 69, 5, 498–511

1501

1502

1503

1504

1505

Sample nos.

Substages

U. Barremian

Lower

Aptian

Upper

Aptian

Substages

Dictyophyllidites harrisii

Deltoidospora

sp.

Bir

etisporites potoniaei

Tripartina variabilis

Leiotriletes

sp.

Cyathidites australis

Gleicheniidites

sp.

Gleicheniidites senonicus

Gleicheniidites laetus

Ornamentifera echinata

Ster

eisporites antiquasporites

Concavissimosporites

sp.

Concavisporites dubia Concavissimosporites penolaensis

Baculatisporites / Osmundacidites

Contignisporites

sp.

Duplexisporites anagrammensis

Lycopodiumsporites mar

ginatus

Lycopodiumsporites

sp.

Cicatricosisporites

sp.

Cicatricosisporites tersus

Cicatricosisporites mediostriatus

Cicatricosisporites minutaestriatus Cicatricosisporites

sp. cf.

C. venustus

Cicatricosisporites hughesi

Appendicisporites pr

oblematicus

Appendicisporites baconicus

Appendicisporites

sp.

Klukisporites

sp.

Cor

onatispora valdensis

Foraminisporites wonthaggiensis

Leptolepidites

verrucosus

Leptolepidites tumulosus

Taur

ocusporites

sp.

Antulisporites distalverrucosus

Polycingulatisporites

sp.

Deltoidospora juncta

Triplanosporis

sp.

Todisporites

sp.

Cyathidites minor

Gleicheniidites carinatus

Clavifera triplex

Clavifera

sp.

Ornamentifera

sp.

Cyathidites punctatus

Matonisporites

sp. cf.

M. phlebopter

oides

Stoverisporites lunaris

Distaltriangulisporites

sp.

Cicatricosisporites imbricatus

Pilosisporites trichopapillosus

Sestr

osporites pseudoalveolatus

Foraminisporites asymmetricus

Undulatisporites

sp.

1 1

1 1 1

1 1 1 1

1 1 1

1 1

1 1 1 1 1 1

1 1

1
1 1

1 1 1

1 1

1 1 1

1 1

1 1 1 1

1 1

1 1 1 1

1 1

1 1 1 1 1

1 1 1 1 1 1 1

1 1

5 5

1 1 1 1 1

1 3 1

1 10

1 15

1 1

1 10

1
1

1 1 1

1 1

1
1

1
1 1

1 1

1 1 1

1 1

Fern and bryophytes spores

1501

1502

1503

1504

1505

Sample nos.

Substages

U. Barremian

Lower

Aptian

Upper

Aptian

Substages

Dictyophyllidites

sp.

Deltoidospora hallii

Cyathidites

sp.

Clavifera tuber

osa

Clavifera rudis

Ornamentifera granulata

Mur

ospor

oides chlonovae

Lycopodiacidites

sp.

Tigrisporites r

eticulatus

Cicatricosisporites

angustus

Cicatricosisporites pseudotripartitus

Costatoperfor

osporites foveolatus

Trilobosporites

cf.

hannonicus

Micr

eticulatisporites

sp. cf.

M. uniformis

Densoisporites velatus Hoegisporites

sp.

Converr

cucosisporites

cf.

exguisitus

sp.

Classopollis

spp.

Sciadopityspollenites multiverrucosus

Cer

ebr

opollenites mesozoicus

Piceaepollenites

spp.

Vitr

eisporites pallidus

Alisporites

spp.

Parvisaccites radiatus

Podocarpidites

spp.

Cedripites

sp.

Micr

ocar

hydites

sp.

Rugubivesiculites

sp.

Phyllocladidites

sp.

Pinuspollenites

sp.

Disaccites

Inaperturpollenites

sp.

Taxodiaceaepollenites hiatus

Araucariacites sp.

Araucariacites australis

Perinopollenites elatoides

Callaiosporites dampieri

Calliaiosporites trilobatus Callaiosporites segmentatus

Eucomiidites

sp.

Cycadopites

Clavatipollenites

sp.

Retimonocolpites

sp.

Tricolpites

sp.

Dinocysts (% of all palynomorpha)

Gymnospermae pollen

(

of all spores and pollen

)

Angiospermae pollen

(

of all spores and pollen

)

Total of palynomorpha

Spores (

of all spores and pollen

)

1 1

1 1 1 1

1 1

1 1 1 1 1 1

1 1

1 1 1

20 56 5 5

42 45 5

28 35 5 1 1 1 1

4018 5 5

1 1 1 1

30 15 5 10 1

1 5 5

1 5

40 15 1 5 1 1

5 1

1 1 1

1 5

1 31 5 1

1 1 1

1 1

1
1

10 35

1 1

1 13

1 1

1 5 1

1 1 5 1

1 1 1 1

1 1 1 1 1

1 1

2 163

5 171

9 231

23 239

25 346

30 370

5 318

10
18

267

265

259

325

25 249

28 72

27 73

22 78

24 75

45 53

47 53
26 74

7 93

20 80

30 69

Fern and bryophytes spores

Gymnospermae pollen

Angiospermae pollen

TABLE S4. – The spores and pollens range chart of Zavodskaya balka section. Percentage of

the amount spores and pollen.

Table S4: The spores and pollens range chart of Zavodskaya balka section. Percentage of the amount spores and pollen.

STRATIGRAPHY OF THE UPPER BARREMIAN–APTIAN SEDIMENTS FROM THE SOUTH-EASTERN CRIMEA

GEOLOGICA CARPATHICA

, 2018, 69, 5, 498–511

1501

1502

1503

1504

1505

Achomosphaera sp.

Batiacasphaera sp.

Apteodinium sp.

Coronifera oceanica

Fromea

sp.

Pterospermella

sp.

Tasmanites

sp.

phycomata green algae

Cribroperidinium

cf. conjunctum

Ctenidodinium elegantulum

Cometodinium sp.

Cleistosphaeridium spp.

Circulodinium

cf. deflandr

Circulodinium br

evispinatum

Spiniferites dentatus

Subtilisphaera ventriosa

acritarchs

Pseudoceratium polymorphum

Oligosphaeridium albertense

Rhynchodiniopsis cf.

cladophora

Subtilisphaera perlucida

Spiniferites spp.

Rhombodella paucispina

Rhynchodiniopsis fimbriata

Surculosphaeridium

sp. III

Surculosphaeridium sp.

Taleisphaera

hydra

subsp. elongata

Tanyosphaeridium boletus

Tehamadinium tenuiceras

Trichodinium

sp.

aff.

Valensiella r

eticulata

aff.

Wallodinium

sp.

Muderongia

sp.

Canningia colliveri

Cassiculosphaeridia sarstedtensis

M. cf.

staurota

sensu

Dav., V

erd., 1974

Pareodinia

sp.

Palaeoperidinium cretaceum

Meiourogonyaulax stoveri

Pervosphaeridium cf.

truncatum

Cribroperidinium?

cf. edwar

dsii

Cribroperidinium? tenuiceras

Cyclonephelium cf.

intonsum

Cribroperidinium?

cf. cornutum

Florentinia cooksoniae

Exochosphaeridium phragmites

Cerbia tabulata

Cribroperidinium sepimentum

Cyclonephelium sp.

Dingodinium? albertii

Dingodinium? cf.

spinosum

Protoellipsodinium spinocristatum

Pterodinium

spp.

Pseudoceratium cf.

retusum

Pseudoceratium pelliferum

Impagidinium sp.

? Kalyptea

sp.

? Kallosphaeridium

sp.

Kleithriasphaeridium eoinodes

Cribroperidinium bor

eas

Circulodinium

distinctum

Cribroperidinium?

cf. muder

ogense

Callaiosphaeridium trycherium

Cribroperidinium

sp.

Pseudoceratium securigerum

Pseudoceratium sp.

indetermined fragment

chorate cysts

Pilosidinium sp.

Prolixosphaeridium parvispinum

Florentinia

sp.

Florentinia mantellii

Protoellipsodinium

cf. clavulus

Gardodinium eisenackii

Protoellipsodinium spinosum

Odontochitina operculata

Heslertonia heslertonensis

Hystrichosphaerina schindewolfii

Impagidinium alectrolophum

Impagidinium verrucosum

Chytroesphaeridia

sp.

Chlamydophorella

sp.

Circulodinium

cf. attadalicum

Oligosphaeridium prolixispinosum

Ovoidinium incomptum

Oligosphaeridium? asterigerum

Oligosphaeridium complex

Oligosphaeridium sp.

Cymatiosphaera sp.

Sample nos.

Dinoﬂagellates species

D 1

D 2

Substages

U. Barremian

Lower Aptian

Upper Aptian

Substages

D 3

TABLE S5. – The dinocyst range chart of Zavodskaya Balka secti

on. Numbers are specimen abundance in the sample.

Table S5:

The dinocyst range chart of Zavodskaya Balka section. Numbers are specimen abundance in the sample.