GEOLOGICA CARPATHICA
, APRIL 2019, 70, 2, 153–182
doi: 10.2478/geoca-2019-0009
www.geologicacarpathica.com
The Jurassic/Cretaceous boundary and high
resolution biostratigraphy of the pelagic sequences
of the Kurovice section (Outer Western Carpathians,
the northern Tethyan margin)
ANDREA SVOBODOVÁ
1,
, LILIAN ŠVÁBENICKÁ
2
, DANIELA REHÁKOVÁ
3
,
MARCELA SVOBODOVÁ
1
, PETR SKUPIEN
4
, TIIU ELBRA
1
and PETR SCHNABL
1
1
The
Czech Academy of Sciences, Institute of Geology, Rozvojová 269, 165 00 Prague, Czech Republic;
asvobodova@gli.cas.cz,
msvobodova@gli.cas.cz, elbra@gli.cas.cz, schnabl@gli.cas.cz
2
Czech Geological Survey, Klárov 131/3, 118 21 Prague, Czech Republic; lilian.svabenicka@geology.cz
3
Comenius University, Faculty of Natural Sciences, Department of Geology and Paleontology, Mlynská dolina G. Ilkovičova 6,
842 15 Bratislava, Slovakia; daniela.rehakova@uniba.sk
4
Institute of Geological Engineering, VŠB — Technical University of Ostrava, 17. listopadu 15,
708 33 Ostrava-Poruba, Czech Republic; petr.skupien@vsb.cz
(Manuscript received September 27, 2018; accepted in revised form March 12, 2019)
Abstract: Microfacies and high resolution studies at the Kurovice quarry (Czech Republic, Outer Western Carpathians)
on calpionellids, calcareous and non-calcareous dinoflagellate cysts, sporomorphs and calcareous nannofossils, aligned
with paleomagnetism, allow construction of a detailed stratigraphy and paleoenvironmental interpretation across
the Jurassic/Cretaceous (J/K) boundary. The Kurovice section consists of allodapic and micrite limestones and marlstones.
Identified standard microfacies types SMF 2, SMF 3 and SMF 4 indicate that sediments were deposited on a deep shelf
margin (FZ 3), with a change, later, into distal basin conditions and sediments (FZ 1). The sequence spans a stratigraphic
range from the Early Tithonian calcareous dinoflagellate Malmica Zone, nannoplankton zone NJT 15 and magnetozone
M 21r to the late Early Berriasian calpionellid Elliptica Subzone of the Calpionella Zone, nannoplankton NK-1 Zone and
M 17r magnetozone. The J/K boundary is marked by
a
quantitative increase of small forms of Calpionella alpina, the base
of the Alpina Subzone (that corresponds to NJT 17b and M 19n.2n) and by the rare occurrence of Nannoconus wintereri.
Palynomorphs include Early Berriasian terrestrial elements — non-calcareous dinoflagellate cysts Achomo sphaera
neptunii, Prolixosphaeridium sp. A and Tehamadinium evittii. The depositional area for Kurovice was situated at
the margin of the NW Tethys. The influence of cold waters from northern latitudes and potential upwellings is highlighted
by: 1) the high proportion of radiolarians and sponge spicules, 2) rare calpionellids represented mostly by hyaline forms,
3) the absence of microgranular calpionellids — chitinoidellids, 4) the small percentage of the genera Nannoconus,
Polycostella and Conusphaera in nannofossil assemblages, as
compared to other sites in Tethys, 5) scarce Nannoconus
compressus, which has otherwise been mentioned from the Atlantic area.
Keywords: Tithonian, Berriasian, calcareous and non-calcareous microfossils
,
calcareous nannofossils, palynomorphs,
magnetostratigraphy.
Introduction
Determining the Global Boundary Stratotype Section and
Point (GSSP) for the Berriasian Stage in the Tethys has been
the objective of elaborate research and discussions of the Ber-
riasian Working Group during the past several years. Tethys
was the largest depositional area during Tithonian and Berria-
sian times that is available for study by diverse stratigraphic
methods, namely lithostratigraphy, biostratigraphy (based on
calpionellids, nannofossils, dinoflagellates, radiolarians, fora-
minifers, ammonites and belemnites), as well as by magne-
tostratigraphy, geochemistry and sequence stratigraphy
(Andreini et al. 2007; Houša et al. 2007; Michalík et al. 2009,
2016; Casellato 2010; Lukeneder et al. 2010; Pruner et al.
2010; Grabowski et al. 2010a, b; Grabowski 2011; Michalík
& Reháková 2011; Wimbledon et al. 2011, 2013; Petrova
et al. 2012; Guzhikov et al. 2012; Lakova & Petrova 2013;
López-Martínez et al. 2013, 2015; Schnabl et al. 2015;
Svobodová & Košťák 2016; Hoedemaeker et al. 2016;
Grabowski et al. 2017; Kietzmann 2017; Lakova et al. 2017;
Wimbledon 2017; Elbra et al. 2018a, b, Kowal-Kasprzyk &
Reháková 2019).
Much research has been focused on the Jurassic/Cretaceous
(J/K) boundary of the Western Carpathians (Grabowski &
Pszczółkowski 2006; Grabowski et al. 2010b, 2013; Michalík
et al. 2016; Skupien et al. 2016); and the Brodno section in
Slovakia was chosen as a regional stratotype (Michalík et
al. 1990, 2009; Houša et al. 1996, 1999). Marine strata at
the locality of Kurovice were suggested as another possible
J/K profile for multidisciplinary research. Reháková (in
Eliáš et al. 1996) noted calpionellid zones ranging from
the Late Tithonian Crassicollaria Zone to the Late Berriasian
154
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Calpionellopsis Zone. However, the J/K boundary could not
then be strictly determined. Recent bed-by-bed study confir-
med a similar calpionellid distribution, with a biozonation,
and the J/K boundary to be precisely located (Svobodová et al.
2017; Švábenická et al. 2017; Elbra et al. 2018a).
This work follows the Elbra et al. (2018a) paper, which pre-
sented the magnetostratigraphy of the Kurovice sequence,
beds 1–148, compared to concise biostratigraphic data. The aim
of this study is to provide detailed documentation of the biota
in an extended succession (beds −29 to 148) and to compare
the distribution of calpionellids, calcareous dinoflagellates,
palynomorphs and calcareous nannofossils, with a focus on
the biostratigraphic and paleoenvironmental interpretations.
In addition, the work also includes the magnetostratigraphy of
the lower part of the sequence (beds −1 to −29), which was not
mentioned by Elbra et al. (2018a).
Geological setting
The Kurovice Quarry (49°16’25.0” N, 17°31’19.0” E; 260–
269 m a.s.l.) is located in the south-eastern part of the Czech
Republic, 9 km NW from Zlín (Fig. 1). It is situated in
the front of the Magura Group of nappes (Fig. 2) that represent
a sig nificant regional unit of the Outer Western Carpathians
(Švábenická et al. 1997; Pícha et al. 2006). In Tithonian
and Berriasian times, this depositional area was situated on
the nor thern margin of Tethys and was confined to the south
by the Czorsztyn Ridge and the Silesian Cordillera (Golonka
et al. 2006).
Limestone quarrying started in Kurovice during the first
half of the 18
th
century, and continued until 1997. In 1999,
the area of the abandoned quarry was declared as a nature
reserve due to its geological and paleontological significance,
and for the protection of rare biota. The geological age of
the quarry’s rocks described as the Kurovice Limestone
(Glöckner 1841) has always been a subject of discussion.
On the basis of finds of aptychi, a Jurassic age was assigned.
Andrusov (1933, 1945) documented both a Jurassic and a Lower
Cretaceous age for the deposits.
The Kurovice Limestone is a sequence consisting of centi-
metre- to decimetre-scale micrite limestones alternating with
whitish-grey allodapic limestones, silty limestones and marl-
stones, deposited on a deep shelf margin passing into deposi-
tion in distal basinal conditions (Vašíček & Reháková 1994).
The formation’s thickness is estimated to be approximately
120–150 m.
Material and methods
Samples from the Kurovice section were taken in 2016 and
2017. An almost 77 m thick sequence was recorded, numbered
from −29 to 148 and sampled for paleomagnetic and geo-
chemical research (Fig. 3). The paleomagnetic methods emp-
loyed here have already been described in Elbra et al. (2018a).
Calcareous nannofossils
Calcareous nannofossils have been analy-
zed in 114 smear slides. These came from
the size fraction of 1–30 µm, separated by
a pro cess of decantation using 7 % solution of
H
2
O
2
(e.g., Švábenická 2012). In order to
obtain the relative nannofossil abundances and
semiquantitative data, 500 specimens were
counted on each slide. Some samples did not
provide many specimens, so the number of all
nannofossils found on such slides was used
as the basis for interpretation. Slides were
observed under an Olympus BX51 and Nikon
Microphot-FXA transmitting light micro-
scopes with immersion objectives of ×100
magnifications. The identifications of species
follow Bralower et al. (1989), Bown & Cooper
(1989, 1998), Bown et al. (1998), Casellato
(2010), and Nannotax website (Young et al.
2013); and biostratigraphic data were inter-
preted with reference to the nannofossil zona-
tion of Casellato (2010). The smear slides are
stored at the Institute of Geology of the Czech
Academy of Sciences, v.v.i. (Department
of Paleobiology and Paleoecology) and at
the Czech Geological Survey in Prague.
Fig. 1. Simplified geological map of the Outer Western Carpathians. The Kurovice
section is marked with an arrow. 1 — Bohemian Massif, 2 — Carpathian Foredeep,
3 — Vienna Basin, 4 — Žďánice-Subsilesian Unit, 5 — Silesian Unit, 6 — Fore magura
Unit, 7 — Magura Group of Nappes, 8 — Outer Klippen Belt, 9 — Inner Klippen Belt.
Simplified after Švábenická (2012).
155
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Microfacies, calcareous dinoflagellates and calpionellids
Microfacies and calcareous microfossils — calpionellids and
calcareous dinoflagellates were studied in 220 thin sections
under a Leica DM 2500 transmitting light microscope and
documented by the Axiocam ERc 5s camera in the Depart-
ment of Geology and Paleontology, Comenius University in
Bratislava. The standard calpionellid zones of Remane et al.
(1986) and Reháková & Michalík (1997) and calcareous dino-
flagellate succession of Nowak (1968) and Reháková (2000)
were applied. Carbonate rocks were classified according to
the Folk (1959) and Dunham (1962) schemes. Standard micro-
facies types (SMFs) and facies zones (FZs) were determined
following Wilson (1975) and Flügel (2004).
Palynomorphs
A total of 24 samples were processed to concentrate
the resistant palynological component using standard macera-
tion techniques, including treatment with hydrochloric (HCl)
and hydrofluoric (HF) acids to remove carbonates and sili-
cates. The remaining inorganic fraction was removed by ace-
tolysis and HNO
3.
Due to the rare appearance of palynomorphs,
sieving was not used. The palynofacies analysis and photo-
documentation were carried out using Leica DM 2500 optical
microscope (software Leica IM 50) with magnifications of
200 –1000× (MS), and by Olympus BX60 optical microscope,
SW NIS-Elements 3.1. The formalized non-calcareous dino-
flagellate taxa are fully referenced in Fensome & Williams
(2004) and Fensome et al. (2009). The paly-
nological slides are stored in the Department
of Paleobiology and Paleoecology of the Insti-
tute of Geology of the Czech Academy of
Sciences, and Institute of Geological Engi-
neering VŠB — Technical University Ostrava.
Results
Calcareous nannofossils
In samples from Kurovice, calcareous nan-
nofossils are usually poorly preserved. Over-
growth and etching are extensive, making
identification of some specimens difficult.
Generally, nannofossil assemblages are cha-
racterized by the dominance of ellipsagelo-
sphae rids, making up more than 90 % of
spe cimens. The genera Conusphaera, Nanno
conus and Polycostella are found in small
numbers (Fig. 4). Other nannoliths and pla-
coiths are rare, fragmented and often cannot
be identified.
Fig. 2. Probable paleogeographic position of the depositional area (Kurovice section
marked by the red dot). After Michalík 2011, modified. Legend: white — dry land; light
gray — epicontinental sea; gray — marine basins; bricks — carbonate platforms and
basins; dark gray — oceanic bottom).
Fig. 3. The profile in the Kurovice quarry. A — location of the J–K boundary marked with black line. B — a detailed view of the middle part
of the section.
156
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 4. Percentage share of selected nannofossil genera in the assemblages across the Kurovice section. Lithology after M. Bubík in Košťák
et al. (2018), nannofossil zones (CNZ) by Casellato (2010).
157
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Calcarenites contain extremely poor nannofossil associa-
tions (Fig. 5A). Scarce nannofossil fragments (1–3 specimens
per 10 fields of view of the microscope, FOM) are represented
almost exclusively by ellipsagelosphaerids. Watznaueria div.
spec. may total up to 80 % and Cyclagelosphaera margerelii
up to 11 % of nannofossil assemblage. Micrite limestones con-
tain poorly preserved nannofossils with abundance ±1 up to 10
specimens per 1 FOM (Fig. 5B). The associations comprise
numerous specimens of the genera Watznaueria (Fig. 6S–AB)
and Cyclagelosphaera (Fig. 6AC–AH) accompanied by rare
specimens of Conusphaera (C. mexicana mexicana, C. mexi
cana minor, Conusphaera sp. 1), Polycostella beckmannii,
Nannoconus spp., Zeugrhabdotus (Z. embergeri, Z. cooperi),
and fragments of outer rims of the genera Retecapsa and
Helenea. Specimens of W. barnesiae may comprise 70 % and
C. margerelii up to 13 %. Marlstone interbeds contain highly
abundant (10–20 up to ±50 specimens per FOM and more)
diversified nannofossil assemblages (Fig. 5C). Although
ellipsagelosphaerids still predominate quantitatively, abun-
dances of Watznaueria species (W. manivitiae, W. fossacincta,
W. britannica, W. communis, W. cynthae, W. ovata) and Cycla
gelosphaera (C. deflandrei, C. argoensis) increase. Specimens
of genera Conusphaera (Fig. 7I–P), Nannoconus (Fig. 7S–AJ),
Polycostella (Fig. 7Q, R), Retecapsa (Fig. 6O, P), Helenea
(Fig. 6A–D), Diazomatolithus (Fig. 7B), Zeugrhabdotus
(Fig. 6I–L), Hexalithus (Fig. 7E, F) are present in higher quan-
tities than in calcarenites and micrite limestones. Generally,
the composition of calcareous nannofossil assemblage in
the studied material corresponds to the Tithonian and Early
Berriasian age, compared with the previous studies (e.g.,
Michalík et al. 2009; Casellato 2010; Lukeneder et al. 2010;
Svobodová & Košťák 2016). Selected calcareous nannofossil
taxa are presented in Figs. 6 and 7. The distribution of all nan-
nofossil species is shown in Table 1, and a list of calca reous
nannofossil taxa is given in Appendix.
Microfacies, calcareous dinoflagellates and calpionellids
The deposits contain selected bioclasts and allochems, such
as calpionellids, radiolarians, globochaetes, saccocomids, fila-
ments, fragments of benthic organisms, quartz and lithoclasts.
Calpionellids are generally rare and hyaline forms dominate.
Calpionellids are not well preserved. Gradually in the over-
lying beds, they exhibit loricae with thinned walls, which are
often damaged or have poorly preserved collars. Through
the section, calcified radiolarians and sponge spicules deter-
mine the prevailing type of spiculite-radiolarian and radiola-
rian–spiculite microfacies. In the lowermost part of the section,
cysts of dinoflagellates and crinoid fragments are locally
a significant part of fossil assemblages. Microgranular chiti-
noidellid loricae were not found. On the basis of microfacies,
calcareous dinoflagellate and calpionellid development,
the Kuro vice succession is divided into several intervals (from
the bottom to the top):
Beds −29 to −7 (~0 –7.7 m): Marly and slightly laminated,
locally bioturbated limestones (mudstones), in some places
with thin layers and laminae rich in a silt admixture and
silt-sized fragments of litho- and bioclasts, locally also silt-
stones. Further, biomicritic slightly bioturbated limestone of
Fig. 5. Kurovice section, abundance of nannofossils in the particular
types of rock. Fields of views in the microscope. A — calcarenite;
B — micrite limestone; C — marlstone.
158
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 6. Kurovice section, calcareous nannofossils, Heterococcoliths. Photographs in cross polarized light, figures E, G, AE and AG in plane
polarized light. A, B — Helenea staurolithina: A — sample 1t, B — sample 5b; C, D — Helenea chiastia, C — sample 142s, D — sample 107;
E, F — Rhagodiscus nebulosus, sample 145; G, H — Umbria granulosa minor (fragment), sample 100 marlstone; I, J – Zeugrhabdotus fluxus,
sample −6; K — Zeugrhabdotus cooperi, sample 1t; L — Zeugrhabdotus embergerii, sample 142s; M — Pickelhaube furtiva, sample 8/9;
N — Biscutum ellipticum, sample 133/134; O — Retacapsa surirella, sample 132; P — Retacapsa cf. octofenestrata, sample 133/134;
Q, R — Speetonia colligata (specimen in 0
o
and 30
o
), sample 133/134; S — Watznaueria barnesiae, sample 1t; T — Watznaueria communis,
sample 94; U — Watznaueria fossacincta, sample 105b; V, W — Watznaueria britannica: V — sample 1t, W — sample 144s; X — Watznaueria
ovata, sample 111/112; Y — Watznaueria biporta, sample 30; Z, AA — Watznaueria cynthae: Z — sample 46, AA — sample 142s;
AB — Watznaueria manivitiae, sample 132; AC, AD — Cyclagelosphaera margerelii: AC — sample 9, AD — sample 1t, small specimen;
AE, AF — Cyclagelosphaera deflandrei, sample 9; AG, AH — Cyclagelosphaera argoensis, sample 1t; AI — Parhabdolithus cf. robustus,
sample 5b, reworked specimen from the older Jurassic strata; AJ — Parhabdolithus marthae, sample 89, reworked specimen from the older
Jurassic strata.
159
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 7. Kurovice section, calcareous nannofossils, Nannoliths including Eoconusphaeraceae, Nannoconaceae and uncertain “polycycloliths”.
Photographs in cross polarized light, D, E, G, I, J, Q, S, U, W, X, Z, AA, AC, AF and AG in plane polarized light. A — Lithraphidites carnio
lensis, sample 142 s; B — Diazomatolithus lehmanii, sample 1t; C — Rotelapillus crenulatus, sample 133/134; D — pentalith, sample 8/9;
E, F — Hexalithus noeliae, sample 100 limestone; G, H — Assipetra infracretacea, sample 138; I–L — Conusphaera sp.: I–K — sample 103
(specimen in 0
o
and 30
o
), L — sample 1a; M, N — Conusphaera mexicana mexicana, sample 69 (specimen in 0
o
and 30
o
); O — Conusphaera
mexicana minor, sample 1t (specimen in 0
o
); P — Conusphaera mexicana minor, sample 1t (specimen exceeding the size of 4 µ), cf.;
Q, R — Polycostella beckmanii, sample 5b; S, T — Nannoconus sp., sample 1t; U, V — Nannoconus puer, sample 5b; W — Nannoconus
compressus, sample 133/134, reworked specimen; X — Nannoconus globulus minor, sample 75; Y, Z — Nannoconus globulus globulus,
sample 132; AA, AB — Nannoconus wintereri, sample 100 limestone; AC, AD — Nannoconus wintereri, sample 100 limestone (probably
early form of N. wintereri), cf.; AE, AF — Nannoconus steinmannii minor, sample 145; AG, AH — Nannoconus kamptneri minor, sample
133/134; AI, AJ — Nannoconus kamptneri kamptneri, sample 124.
160
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Chr
onostratigraphy
Zonation (Casellato 2010)
Sample No.
Nannofossil abundance
Nannofossil preservation
Assipetra infracr
etacea
Biscutum ellipticum
Conusphaera mexicana mexicana
Conusphaera mexicana minor
Conusphaera
sp. 1
Cr
etar
habdus
sp.
Cruciellipcis cuvillieri
Cyclagelosphaera ar
goensis
Cyclagelosphaera deflandr
ei
Cyclagelosphaera mar
ger
eli
Cyclagelosphaera r
einhar
dtii
Diazomatolithus lehmanii
Discor
habdus
cf.
ignotus
Ethmor
habdus gallicus
Ethmor
habdus hauterivianus
Favioconus multicolumnatus
Helenea chiastia
Helenea staur
olithina
Hexalithus noeliae
Hexalithus strictus
Lithraphidites carniolensis
Lotharingius hauffii
Lotharingius sigillatus
Manivitella pemmatoidea
Micrantholithus
sp.
Miravestina favula
Nannoconus colomi
Nannoconus compr
essus
Nannoconus erbae
Nannoconus globulus globulus
Nannoconus globulus minor
Nannoconus infans
Nannoconus kamptneri kamptneri
Nannoconus kamptneri minor
Nannoconus puer
Nannoconus steinmannii minor
Nannoconus st. steinmannii
B e r
r
i a s i a n
NK-1
148
VL EP
VR
R F
ER
ER ER
147 b
VL EP
?
ER
VR VR VR
?
VR
ER
ER
145
L
VP
?
VR ER ER
VR R R-F
VR
ER
ER
ER
ER
ER
144 s
VL VP
ER
VR R
ER
ER
ER
? ER
143 b
VL EP
VR
ER
ER R R-F
VR
142 s
L-M P
R VR ER
VR VR R
?
f
? VR
140
EL VP
VR
VR R
VR
?ER
?r ?r ?f
ER
ER
138
L-M VP ER
R VR ER
ER R R
ER
ER
136
EL EP
ER
?f fER ER VR
?f
?F
135
L
VP
R VR
VR VR R-F
VR
133/134 VL VP
ER VR ER
ER ?f ER VR VR ? VR
ER
ER
ER
ER ER
ER ER
132
M
P
ER ER
VR R R
ER
ER
?f
ER
131
VL EP
R ER ER
R R-F
?ER
ER
130 t
L-M VP
VR ER
fVR VR R
ER ER
?f
ER ER
129
VL EP
R VR VR
ER R R
ER
?ER ER
ER
128
EL EP ?ER
VR VR VR
R R-F
ER
ER
?ER
ER
?ER
127
VL VP
VR ER
ER VR R
?r
ER
126
L
P
R ER ER
ER VR R
?
124
VL VP ?ER
VR VR ER
?f
VR R
ER
ER ER
ER
ER
NKT
ZONE
122
VL EP
VR ER ER
ER R F
ER
?ER
120
M
P
R VR ER
R F
ER ER
?ER
118
M
P ?ER
R VR VR
R F
ER
ER ER
?ER ER
116
VL VP
VR ER ER
R F
ER ER
114
L-M VP
R ER
?ER R F
?ER
ER
112
L
VP
R VR
ER R R-F
ER
ER
111/112 M
P
R
?
R R-F
ER
f?
110
VL EP
R VR VR
ER R F
ER
r
ER
109
L
VP
VR ER ER
R R
ER
ER
107
VL VP
ER
ER
ER
106 t
VL VP
R VR ER
ER R F
ER
ER
106 b
L
VP
VR VR
R F
VR
ER
ER
105 s
EL VP
VR ER
ER R R
ER
ER
105 b
L
VP
ER
R R
ER ER
ER
f
103
L
VP
VR
VR
VR R
ER
ER
102
VL VP
R VR ER
ER R R
ER
ER
ER ER
101 t
L
VP
R VR
R R-F
ER
VR
ER ER
101 y
VL VP
R VR
R R
ER
ER
?ER
ER
101 x
L
VP
R VR ER
VR R R-F
ER
ER
?ER
101 b
L
VP
R VR ER
VR R C
VR
ER ER
100 lime EL EP ER
ER
VR
ER
ER
f
100 marl L
P
ER
ER
VR R-F
f? ER
99 t
EL EP ER
R VR
R F
ER
ER
ER
99 b
EL EP ER
R VR
ER R R
ER
VR ER
98
EL EP
ER ER
R F-C
ER
ER
97
VL EP ER
R VR
R F
ER
ER
r
VR
ER ?ER
96
VL EP
R VR
ER R F
ER
ER
ER
95 t
EL EP
VR
ER R C
ER
ER
95
L
VP
ER
ER R
ER
f
ER
95 b
VL VP
R VR
ER R F
ER
VR
ER ER
94
L
VP
R R
R F-C
ER
?ER
93
VL VP
R VR
R F
ER
ER
ER
92 t
VL EP ER
R VR
R F
ER
ER
ER ER
ER
Table 1a: Distribution of calcareous nannofossils in the Kurovice section. Semi-quantitative data as follows. Nannofossil abundance:
EL (extremely low = 1–10 specimens per 20 FOM); VL (very low = 1–10 specimens per 10 FOM); L (low = 1–10 specimens per FOM);
M (moderately = 10–40 specimens per FOM). Nannofossil total abundance: A (abundant = >5 specimens per FOM); C (common = 1–5 speci-
mens per FOM); F (few = >1 specimen per FOM); R (rare = 0–1 specimen per FOM); VR (very rare = <5 specimens per sample); ER (extremely
rare = 1–2 specimens per sample). Nannofossil preservation: EP (extremely poor = strong etching and overgrowth); VP (very poor = strong
dissolution); P (poor = moderate etching). Nannofossil zones follow Casellato (2010); r = reworked; ? = uncertain specimen; f = fragment.
Stratigraphically significant taxa marked with grey colour.
161
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Chr
onostratigraphy
Zonation (Casellato 2010)
Sample No.
Nannofossil abundance
Nannofossil preservation
Assipetra infracr
etacea
Biscutum ellipticum
Conusphaera mexicana mexicana
Conusphaera mexicana minor
Conusphaera
sp. 1
Cr
etar
habdus
sp.
Cruciellipcis cuvillieri
Cyclagelosphaera ar
goensis
Cyclagelosphaera deflandr
ei
Cyclagelosphaera mar
ger
eli
Cyclagelosphaera r
einhar
dtii
Diazomatolithus lehmanii
Discor
habdus
cf.
ignotus
Ethmor
habdus gallicus
Ethmor
habdus hauterivianus
Favioconus multicolumnatus
Helenea chiastia
Helenea staur
olithina
Hexalithus noeliae
Hexalithus strictus
Lithraphidites carniolensis
Lotharingius hauffii
Lotharingius sigillatus
Manivitella pemmatoidea
Micrantholithus
sp.
Miravestina favula
Nannoconus colomi
Nannoconus compr
essus
Nannoconus erbae
Nannoconus globulus globulus
Nannoconus globulus minor
Nannoconus infans
Nannoconus kamptneri kamptneri
Nannoconus kamptneri minor
Nannoconus puer
Nannoconus steinmannii minor
Nannoconus st. steinmannii
Berriasian
NJT
17 Zone
NJT
17b Subzone
92 b VL VP
R ER ER
ER ER R R
ER
?ER r
ER ER
91
VL EP
R VR ER
?ER R R-F
ER
90
L
P
R VR
?ER ER R R-F
ER
ER
?r
ER
89
VL VP ?ER
R VR ER
R R
ER
ER
r
88
L
VP ?ER
R ER
?ER
R F
ER
?ER
ER
87
EL EP ?ER
R VR ?ER
R R
?ER
?r
86/87 EL EP ER
R VR ER
VR R R
ER
VR
86
VL EP
R R ER
R R-F
ER
?r
ER
T i t h o n i a n
85/86 VL EP
R VR
ER R R-F
VR
?ER
ER
85
VL EP ER
R VR VR
ER
F
ER
ER ER
84
VL EP
R VR ER
R R-F
ER
ER
82
VL EP ER
VR VR
ER R C
ER
ER
?r
81
VL
P
ER R VR
ER R F
ER
ER ER
?ER
79/80 VL VP ?ER?ER R ER
ER
R F
ER
NJT
17a Subzone
79
VL VP
R ER
R F
ER
ER
78
VL EP
ER
fER ER R
ER
75
EL EP
R VR ER
R R-F
ER
ER
71/72 EL EP
R VR
ER R F
VR
70 t
VL VP
ER
VR R
ER
f
?r
?
ER
ER
69
EL EP
R VR
R F
ER
?ER ER
?r
66/67 EL VP
R VR
?ER
R F
VR
ER
ER
?ER
66 t
L
VP
R ER
R
f?
66
VL EP
ER
R
60
L
VP ?ER
VR VR
R R
ER
?ER
ER
ER
55
VL EP
VR ER
R F
ER
NJT
16 Zone
52/52 M VP ?ER
VR VR ER
R R
ER
ER
?ER
50/51 VL EP
?
VR R
46
L
EP
?
ER fER
ER R R
?ER ER
?
44 t
VL EP
ER ? ER
ER R
ER ER ER
43
L
EP
?ER
VR R R
ER
?
42/43
L
EP
ER R
ER
f
40 b VL EP
ER
VR R
?
36
L
EP
VR ER
VR VR R
30
H
VP ?ER
R ER
fER
R F
ER
29
EL EP
ER
ER VR
24/25 L-M P
ER
VR R-F
ER
?ER
20/21
L
EP
VR
ER VR R-F
20
L
EP
fER fER R
14 t
M
P
R ER
ER R F
VR ER
?ER
13
L
EP
ER
ER R
9
L-M VP
VR ER
ER VR F
?
8/9
L
P ?ER
ER R F
VR ER
ER
5 b
M
P
VR
VR VR F
ER
VR VR
ER
3
L
EP
ER ER
ER R
ER
f?
1 t
VH
P
VR R
fER
VR R F
ER ER fER
f? ?ER ER
fER
?
VR
NJT
15 Zone
NJT
15b Sbz
-1
L-M P
ER ER
ER R R
-2
L-M P
ER
R F
ER
-3
L-M P
ER VR ER
VR F
ER
ER
-6
L
P
ER
VR R
ER
-7
L
VP
VR ER
ER ER R
-8
L-M VP
ER ER
ER VR F
-11 L-M P
VR
ER
ER VR F
-13
L
P
R VR ER
VR F
ER
-16
L
P
R ER ER
ER VR R-F
ER
ER
?
?
-17 L-M P
VR ER
ER VR R-F
-19
L
VP
ER R ER ER
ERE VR R
ER ER
-20
VL VP
VR ER
ER ER R
ER
-21
L
P
R ER ER
ER R
ER
-26
EL EP
VR ER ER
R
ER
-28
VL EP
VR
R ER ER
-29 t VL EP
VR
VR
ER
-29
L
VP
VR
VR
R ER ER
ER
Table 1b (continued):
162
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Chr
onostratigraphy
Zonation (Casellato 2010)
Sample No.
Nannofossil abundance
Nannofossil preservation
Nannoconus winter
eri
Nannoconus
sp.
Nannoconus
sp. (cross-section)
Par
habdolithus marthae
Par
habdolithus
sp.
penthaliths
Pickelhaube furtiva
placoliths (outer rims)
Placozygus
sp.
Polycostella beckmannii
Polycostella senaria
Retacapsa octofenestrata
Retacapca schizobrachiata
Retacapsa surir
ella
Retacapsa
sp. (outer rim)
Rhagodiscus nebulosus
Rhagodiscus
sp.
Rotelapillus cr
enulatus
Speetonia colligata
Staur
olithites
sp.
Thoracosphaera
sp.
Umbria granulosa minor
W
atznaueria barnesiae
W
atznaueria biporta
W
atznaueria britannica
W
atznaueria communis
W
atznaueria cynthae
W
atznaueria fossacincta
W
atznaueria manivitiae
W
atznaueria ovata
Zeugr
habdotus cooperi
Zeugr
habdotus ember
gerii
Zeugr
habdotus er
ectus
Zeugr
habdotus fluxus
Zeugr
habdotus
sp. 1 sensu Bown 1992
Zeugr
habdotus
sp.
B e r
r
i a s i a n
NK-1
148
VL EP
ER ER
ER
C
VR
ER VR
ER ER
147 b
VL EP
r
?
ER
VR
F ER VR R ER ER VR
? ER
145
L
VP
ER
f
ER
F-C ER VR R
ER VR
144 s
VL VP
VR
ER
R-F
ER ER ER VR ER
ER
143 b
VL EP
VR ER
r
ER
? ER
C
VR
ER VR VR
142 s L-M P
f
ER
ER
C ER VR VR
VR VR
VR ER
140
EL VP
ER ER
VR
?f
VR
?ER C
VR
VR VR ER
138
L-M VP
ER
ER
F-C ER VR VR
R VR
ER
136
EL EP
ER
R
ER
ER ER
135
L
VP
F
ER VR
VR ER
133/134 VL VP
ER
?
ER
ER
? ER ER
R
?
R
VR VR ER ER ER ER
132
M
P
cf. ER
F-C
VR
ER ER R
ER ER
131
VL EP
ER ER
?ER
F-C
VR
VR R
ER
130 t
L-M VP
ER
F
ER
ER ER VR
ER ER
129
VL EP ?ER VR VR
C-A ER VR ER
ER R
ER
128
EL EP ?ER VR
ER
C ER VR ER
ER R
VR
127
VL VP
ER ER
ER
?ER
C
VR
VR
ER ER
126
L
P
F
ER
ER ER
ER
124
VL VP
VR ER
C-A
VR
VR
ER
NKT
ZONE
122
VL EP ER ER ER
C
VR
ER R
120
M
P ER VR ER
C
VR
VR
ER ER
118
M
P
ER
ER
ER
F-C
R
ER ER R
ER ER
116
VL VP ?ER VR ER
ER
?ER
C
VR
ER ER VR
114
L-M VP
ER
ER
C
VR
ER R
ER
112
L
VP
VR
ER
C
R ER ER
R
ER
111/112 M
P
ER
C
VR
ER ER VR VR ER
110
VL EP
ER ER
ER
ER
C
VR
ER ER R
109
L
VP ?ER VR
ER
C
ER
R
ER
107
VL VP
f?
fER
R
VR
ER ER
106 t
VL VP ER VR ER
ER
A
VR
ER R
ER
106 b
L
VP ?ER ER
ER
A
R ER
ER R
105 s
EL VP
ER
C-A ER VR
R
ER
105 b
L
VP
ER
?
f
F
ER ER VR VR VR VR fER
103
L
VP
R-F
ER
ER ER ER
102
VL VP
VR
C
R
VR R
ER
101 t
L
VP
VR VR
C
R ER
VR VR
ER
cf.
101 y
VL VP
VR ER
R
VR
ER
R
ER
101 x
L
VP
VR ER
C-A ER VR
VR VR
ER
ER
101 b
L
VP
ER ER
R-F
R
ER R ER
100 lime EL EP
ER
ER VR
ER
ER
100 marl L
P
?
F
VR
VR
99 t
EL EP
VR ER
ER
A
R
ER R
ER ER
99 b
EL EP ?VR ER
?ER
A ER R
ER VR R
ER
98
EL EP
ER
ER
A
R
ER ER R
ER
97
VL EP ?ER ER ER
A
VR
VR R
ER
96
VL EP ER VR ER
ER
C
VR
ER
R
ER
95 t
EL EP ER VR
A
VR
ER R ER
ER
95
L
VP
ER
?
F
VR
ER VR
95 b
VL VP ?ER ER ER
C
VR
ER R ER
94
L
VP
ER
?ER
C
R
R
93
VL VP ?ER VR
C
VR
ER
R
ER
92 t
VL EP
VR ER
?r
C
VR
VR
Table 1c (continued):
163
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Chr
onostratigraphy
Zonation (Casellato 2010)
Sample No.
Nannofossil abundance
Nannofossil preservation
Nannoconus winter
eri
Nannoconus
sp.
Nannoconus
sp. (cross-section)
Par
habdolithus marthae
Par
habdolithus
sp.
penthaliths
Pickelhaube furtiva
placoliths (outer rims)
Placozygus
sp.
Polycostella beckmannii
Polycostella senaria
Retacapsa octofenestrata
Retacapca schizobrachiata
Retacapsa surir
ella
Retacapsa
sp. (outer rim)
Rhagodiscus nebulosus
Rhagodiscus
sp.
Rotelapillus cr
enulatus
Speetonia colligata
Staur
olithites
sp.
Thoracosphaera
sp.
Umbria granulosa minor
W
atznaueria barnesiae
W
atznaueria biporta
W
atznaueria britannica
W
atznaueria communis
W
atznaueria cynthae
W
atznaueria fossacincta
W
atznaueria manivitiae
W
atznaueria ovata
Zeugr
habdotus cooperi
Zeugr
habdotus ember
gerii
Zeugr
habdotus er
ectus
Zeugr
habdotus fluxus
Zeugr
habdotus
sp. 1 sensu Bown 1992
Zeugr
habdotus
sp.
Berriasian
NJT
17 Zone
NJT
17b Subzone
92 b VL VP
ER ER
F ER R
R
ER
91
VL EP
ER ER
ER
C-A
VR
ER VR
ER
90
L
P ER
ER
F-C
R
ER ER R
89
VL VP
ER
ER
ER
?
F ER VR
R ER
88
L
VP ?ER ER ER
ER
F
R
?ER
R
ER
87
EL EP ?ER ER
?r
C
R
?ER ER R
ER
86/87 EL EP ER VR
A
R
ER ER R
ER ER
86
VL EP ?ER VR ER
?ER
F
R
ER R
ER
T i t h o n i a n
85/86 VL EP ER VR ER
ER
ER
C
R
ER ER R ER ER
85
VL EP ER VR
ER
F
R ER
ER R
84
VL EP
ER
r
ER
R
R
R
ER
82
VL EP
VR
F
R
ER R
ER
81
VL
P ?ER VR ER
ER
ER
C
VR
ER R
ER
79/80 VL VP ER ER ER
F-C ?ER R
R
NJT
17a Subzone
79
VL VP
ER ER
F ER R
R
78
VL EP
R
ER
fER
ER
75
EL EP
ER
r
ER
ER
C
R
ER
R
ER
71/72 EL EP
ER
F-C
R
ER R
70 t
VL VP
ER
? ?f R-F
VR R ER ER ER
69
EL EP
?
F-C ER R
ER R
ER
66/67 EL VP
VR
?ER
? ?ER F-C
R
R
66 t
L
VP
ER
?
F
VR
R ER
66
VL EP
R
VR
60
L
VP
VR
r
VR
?
F-C ER VR
R
ER
55
VL EP
ER ER
ER
?ER
F-C
VR
ER VR
NJT
16 Zone
52/52 M VP
ER
ER
ER
C ER VR
VR
50/51 VL EP
ER
R-F
VR R
ER R
46
L
EP
ER
f?
R-F
R R
?
R VR ER ER ER
44 t
VL EP
VR
ER
R-F
ER R
VR ER
43
L
EP
ER
C-A
VR
ER R
ER
42/43
L
EP
F
VR R
VR ER
ER
40 b VL EP
?
ER
ER
R-F
VR
?
R VR ER
ER cf.
ER
36
L
EP
ER
C-A
VR
VR R
ER
30
H
VP
r
R
ER
C-A ?ER R
? VR VR ? VR ER
ER
29
EL EP
R
ER
ER
24/25 L-M P
r
r
ER
ER
?f F
VR
R ER
ER
20/21
L
EP
F
VR
VR
ER
20
L
EP
?ER
ER
R
VR
VR ER
14 t
M
P
ER
R
?ER
C
R
R R ER ER
13
L
EP
F
ER ER
9
L-M VP
VR
ER
F-C
ER
ER ER
ER
ER
8/9
L
P
r ER
VR
F-C
VR R-F
R R ER ER
5 b
M
P
r
r
R ER
ER
F-C
R
R VR
ER
3
L
EP
ER
F
ER ER
fER
1 t
VH
P
ER
r ER ?
VR
ER
C-A
VR
R
VR
NJT
15 Zone
NJT
15b Sbz
-1
L-M P
ER
C-A ER VR
ER R
ER ER
-2
L-M P
VR
ER
F
VR
R
ER ER
-3
L-M P
VR
?
F
R
R
VR ER
-6
L
P
?
VR
F
R ER
VR ER
ER ER
ER
-7
L
VP
ER
?
F
R
ER VR
-8
L-M VP
VR
?
F
R
ER VR
ER
-11 L-M P
?
?
r
VR
ER
VR
F
R
R ER
ER
ER
ER
-13
L
P
R
ER
F ER R
ER VR
ER
-16
L
P
?
r
R
?
F
R VR
R VR
VR ER
-17 L-M P
ER
VR
F-C
R
ER VR
ER
-19
L
VP
R
F
ER ?
ER ER
fER
-20
VL VP
VR
ER
F
R
VR
ER
-21
L
P
VR
ER
F-C
VR
ER VR
ER
-26
EL EP
VR
VR
ER
-28
VL EP
?
R-F
VR VR
ER VR
-29 t VL EP
ER
VR
ER
-29
L
VP
r
VR
ER
F ER R VR
VR VR ER
Table 1d (continued):
164
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
radiolaria–spiculae microfacies (wackstones), pelbiomicro-
sparitic limestone of radiolaria–spiculae microfacies and cri-
noidal–radiolaria–spiculae or crinoidal microfacies (packstone)
and pelbiointraclastic limestones (grainstones) belonging to
SMF 2 and SMF 3 were observed (Fig. 8A–C). Radiolarians
and sponges are locally concentrated in clusters, occasionally
as a result of bioturbation. They are calcified, and in some
beds replaced by chalcedony or microcrystalline quartz. Some
bioclasts are silicified or phosphatized. Rocks contain scat-
tered pyrite, less often framboidal pyrite, and a silty clastic
admixture composed of quartz, muscovite, and rare glauco-
nite. Bioclasts impregnated with pyrite sometimes make up
cluster concentrations. Clasts of volcanic rocks were recorded.
The matrix is occasionally penetrated by fractures filled by
calcite. The deposits contain rare aptychi, ostracods, forami ni-
fers, radiolarians, sponge spicules, crinoids, bivalve fragments,
spores of Globochaeta alpina, calcareous cysts of Para
stomiosphaera malmica (Fig. 9A), Colomisphaera carpathica
(Fig. 9C), C. lapidosa (Fig. 9D), less frequent C. cieszynica,
C. radiata (Fig. 9G), C. pieniniensis, Carpistomiosphaera
titho nica (Fig. 9E), Committosphaera pulla, Cadosina semi
radiata fusca (Fig. 9K), C. semiradiata semiradiata (Fig. 9J),
C. semiradiata cieszynica, Stomiosphaera moluccana (Fig. 9B),
Committosphaera czestochowiensis, C. sublapidosa, and
C. ornata (Fig. 9H).
Beds −6 to 35 (~7.7–35.5 m): Micrite limestones — biomi-
critic, pelbiomicritic, pelbiointraclastic and marly limestones
to silty limestones (mudstones, wackestones and packstones),
SMF 2, 3, 4. Rocks are slightly laminated and locally biotur-
bated or they exhibit a slightly recrystallized or silicified
matrix and microfossils. In some places, the gradation of allo-
chems is distinct. Fragments of ostracods, bivalves, crinoids
(including planktonic Saccocoma sp.) may create “allodapic”
beds. Foraminifers, aptychi, the alga Girvanella, microprob-
lematica of Gemeridella minuta and other unrecognizable
microfossils dominate. In the lower part of interval, dinofla-
gellate cysts are more abundant and indicate Cadosina–spicu-
lite–radiolarian microfacies type. Radiolarians and sponge
spicules, occasionally also saccocomids, are replaced by chal-
cedony or microcrystalline quartz. A few bioclasts are phos-
phatized. Locally abundant fractures filled by calcite penetrate
the matrix and frutexites (Fig. 8D). The matrix is rich in pyrite
and organic matter. Rocks contain a silty clastic admixture
composed of quartz, muscovite and rare glauconite. Among
the calcareous cysts, Cadosina semiradiata fusca and C. semi
radiata semiradiata dominate over specimens of the genera
Colomisphaera, Stomiosphaera, Committosphaera, Para sto
mio sphaera and Carpistomiosphaera.
Beds 36–42 (~35.5–37.65 m): Micrite limestones — biomi-
critic, pelbiomicritic of spiculite and radiolarian–spiculite
microfacies (wackestones to packstones), locally bioturbated
or slightly laminated. In some beds smooth laminae rich in
small, occasionally graded bioclasts (crinoid columnals,
Sacco coma sp., and sponge spicules) are present. Rich fram-
boidal pyrite scattered in matrix is documented in a few beds.
Pyrite clusters partially replace bioclasts. Limestones contain
silty quartz, muscovite and glauconite. Calcified radiolarians
and sponge spicules, locally replaced by chalcedony or micro-
crystalline quartz, dominate over rare ostracod and crinoid
fragments. Calcareous dinoflagellate cysts of the genera
Colomisphaera (including C. fortis), Committosphaera and
Cadosina were documented. The presence of the genera
Stomiosphaera, Carpistomiosphaera and Parastomiosphaera
is shown by reworked material from the older, Early Tithonian,
strata.
Beds 42/43–84 (~37.65–51.9 m) are divided into three
intervals:
A) Beds 42/43–51/52 (~37.65–42.9 m): Micrite limestones
— biomicritic, pelbiomicritic locally slightly recrystallized of
spiculite and radiolarian–spiculite microfacies (wackestones,
packstones to mudstones), silty, slightly laminated limestones
of spiculite microfacies (packstones) locally with silt rich
laminae, and siliceous siltstones rich in tiny plant fragments.
The deposits can be interpreted as SMF 2 and SMF 3. Radio-
larians and sponge spicules are concentrated in clusters. A silt
admixture is abundant in places. Some beds are rich in organic
matter and pyrite, which is scattered in the matrix, impreg-
nates bioclasts or creates clusters. Bioclasts are locally phos-
phatized. The matrix is penetrated by numerous fractures and
veins filled by calcite. Calcified radiolarians and sponge spi-
cules dominate over crinoids, ophiurids, ostracods, bivalves,
aptychi, Saccocoma sp. and spores of Globochaete alpina.
The first rare calpionellids are recorded here — Tintinnopsella
remanei, Praetintinnopsella andrusovi, Calpionella alpina
and specimens of the genus Crassicollaria. The occurrence of
calcareous dinoflagellate cysts points to reworking of material
from older Jurassic strata.
B) Beds 52–70 (~42.9–48.25 m): The character of deposits
and microfacies SMF 2 and SMF 3 are similar to the previous
interval. Sample 66 shows the erosion surface which separates
an interval of slightly laminated wackestone to mudstone from
graded pelbiomicrosparitic interval (grainstone) with clasts of
volcanic rocks (SMF 4). Above the erosion surface, frutextites
(Maslov) and radiolarians predominate. The rocks contain
calcified radiolarians, sponge spicules, ostracods, globo-
chaetes, Spirillina sp. and a few further fragments of benthic
forami nifers. Calpionellids are more common and associa-
tions are represented by the genus Crassicollaria (Fig. 10A),
Calpio nella (Fig. 10B–D, J, K) and Tintinnopsella (Fig. 10L).
Some of the crassicollarian loricae are deformed. Dinoflagellate
cysts are represented by the genera Colomisphaera, Committo
sphaera, Stomiosphaera, Cadosina, Carpistomiosphaera, and
Parastomiosphaera. The majority of these are reworked from
older Jurassic strata (Figs. 11, 12).
C) Beds 70/71–84 (~48.25–51.9 m, Košťák et al. 2018):
Micrite limestones — biomicritic, pelbiomicritic, slightly
laminated and locally bioturbated limestones of spiculite–
radiolarian microfacies — wackestones, occasionally mud-
stones or packstones; SMF 3 prevails. Allochems locally show
grading. Some of the bioclasts and matrix are silicified.
Fractures filled by calcite penetrate the matrix in different
directions (three directions are common), and cut small
165
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 8. Important microfacies determinated in the Kurovice section. SMF = standard microfacies type. A — Pelbiomicritic laminated limestone
of crinoid-radiolaria-spiculae microfacies (packstone). SMF 2, sample −9. B — Bioclastic limestone of Cadosina-crinoid microfacies (pack-
stone). SMF 2, sample −2; C — Pelbiomicritic limestone of radiolaria–spiculae microfacies (packstone) with rare Saccocoma sp. SMF 2,
sample −16; D — Frutextite in biomicritic limestone of radiolaria–spiculae microfacies (wackestone). SMF 3, sample 3/1; E — Calpionella
alpina event across the J–K boundary in biomicritic limestone of spiculae–radiolaria microfacies (wackstone). SMF 3, sample 86;
F — Accumulation of bioclasts in bioturbated limestone of spiculae–radiolaria microfacies (wackestone). SMF 3, sample 109; G — Microbreccia
limestone with variable types of extraclasts and bioclasts derived from the shallow carbonate platform environment. SMF 4, sample 105t;
H — Extraclast of the Late Tithonian biomicritic limestone of the Crassicollaria Zone, Intermedia Subzone with large forms of Calpionella sp.
and Crassicollaria intermedia in the Berriasian deposits of the Alpina Subzone of Calpionella Zone. SMF 4, sample 101x.
166
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
caverns filled by silica. The matrix is locally rich in scattered
pyrite and organic matter, in the form of tiny plant fragments.
The rocks contain calcified radiolarians, sponge spicules, and
fewer fragments of ostracods, bivalves and foraminifers.
Among calpionellids, specimens of the genus Crassicollaria
outnumber Calpionella alpina and Calpionella sp., Calpionella
grandalpina, C. elliptalpina and Tintinnopsella carpathica.
Deformed crassicollarian loricae are still present. The abun-
dance of calcareous dinoflagellate cysts decreases. These
include an autochthonous species, Stomiosphaerina proxima,
and reworked specimens of Colomisphaera, Committosphaera,
Cadosina and Parastomiosphaera (Figs. 11, 12).
Beds 85/86 to 148 (~51.9–76.7 m) are also divided into
three intervals (Košťák et al. 2018):
A) Beds 85/86 to 118 (~51.9–68.5 m) are represented by
micrite slightly laminated and locally bioturbated limestones
of spiculite–radiolarian microfacies (wackestones to mud-
stones, SMF 3). Bioturbated intervals contain rich bioclasts
(mainly radiolarians and sponge spicules) concentrated into
“nests”. Marly
intercalations contain clastic admixture, frag-
ments of plants and small clasts of micritic Calpionella bea-
ring limestones are recognized. Further, the microbreccia
limestones (slightly laminated pelbiomicritic) bear the bio-
clasts derived from a carbonate-ramp environment, extraclasts
of dolomitic limestones, limestones with Tithonian crassicol-
larian, shales and volcanic rocks (SMF 4). Bioclasts and
the matrix are slightly silicified and some of bioclasts are
phosphatized. Limestone matrices contains fine silt, composed
of quartz, muscovite, rare glauconite and volcanic ash. Fru-
textites appear in some beds. Abundant fractures filled by cal-
cite penetrate the matrix in different directions. Discontinuous
veinlets (Mišík 1971) of calcitic veins are documented. Micro-
fossils are represented by calcified radiolarians, sponge spi-
cules, less common fragments of ostracods, bivalves, aptychi,
crinoids, ophiurids, bryozoans, and benthic foraminifers
(Nodo saria sp., Dentalina sp., miliolids), and spores of Globo
chaete alpina and Didemnum carpaticum. Small spherical
forms of Calpionella alpina dominate over Crassicollaria
parvula, Calpionella sp., and infrequent C. elliptalpina,
C. grandalpina, and Tintinnopsella carpathica (Fig. 12).
The majority of crassicollarians have deformed loricae. As in
the underlying strata, dinoflagellates include specimens of
the genera Colomisphaera, Cadosina, Stomiosphaerina, Para
stomiosphaera, Colomisphaera, and Carpistomiosphaera. A few
loricae of the larger Calpionella morphotypes, deformed cras-
sicollarians and some dinoflagellate cysts were redeposited
from Jurassic sediments.
B) Beds 119–131 (~68.5–71.8 m): Micrite, locally slightly
laminated and bioturbated limestones (wackestones, sporadi-
cally mudstones and packstones, SMF 3 predominates) and
rare siltstones. The matrix contains rich, scattered pyrite and
a silty admixture, and is sometimes penetrated by fractures
and veins filled by calcite. Some small bioclasts are phospha-
tized. Calcified radiolarians and sponge spicules dominate in
bioclastic wackestones. Moreover, rare fragments of ostracods,
crinoids, bivalves and aptychi, and very rare calpionellids
occur there. Loricae of the genus Remaniella (including
R. catalanoi, R. duranddelgai, R. ferasini and R. colomi) are
observed here for the first time (Fig. 10F–I). They are accom-
panied by Calpionella alpina, Tintinnopsella doliphormis,
T. carpathica, and Lorenziella hungarica (Figs. 11, 12). A large
number of deformed loricae is a typical phenomenon in these
beds. Calpionellid loricae in the autochthonous matrix are thin
and bear marks of dissolution, whereas loricae of reworked
specimens have significantly thicker calcite walls. A small
number of dinoflagellate cysts of the genera Colomisphaera,
Stomiosphaera, Cadosina and Parastomiosphaera malmica
are present. They are considered allochthonous components of
these deposits. Colomisphaera fibrata has been recorded only
here (Fig. 12) and may document erosion of Early Tithonian
strata.
C) Beds 132–148 (~71.8–76.7 m): In this, the highest inter-
val in the quarry sequence, micrite slightly laminated, biotur-
bated or slightly recrystallized limestones of spiculite–
radiolarian microfacies (wackestones, mudstones and also
packstones) and slightly laminated silty limestones (mud-
stones) corresponding to SMF 2 and SMF 3 were documented.
Bioclasts usually create nest-shaped accumulations in biotur-
bated beds. The matrix is rich in scattered pyrite, admixed silt,
and it is penetrated by fractures and veins filled with calcite.
Some small bioclasts are phosphatized. The sediments contain
calcified radiolarians, sponge spicules, rare fragments of
ostra cods and foraminifers. Calpionellids occur rarely and
many of them, mainly remaniellids, have damaged collars,
which makes their identification difficult. Numerous deformed
crassicollarian loricae are still present. Calpionellids are repre-
sented by Calpionella elliptica, C. alpina, Crassicollaria
parvula, Tintinnopsella carpathica and Lorenziella hungarica
(Fig. 10). Cyst associations are mixed and contain reworked
specimens. They include locally abundant Cadosina semira
diata fusca and, as in the underlying strata, Colomisphaera,
Committosphaera, Parastomiosphaera, and Stomiosphaera.
Palynomorphs
Palynomorphs are rare and usually poorly preserved due to
the high CaCO
3
content and the presence of pyrite. Pyrite crys-
tals are often found inside specimens and usually corrode them.
Most rock types provided abundant phytoclasts of brown or
black colour with rare and often broken non-calcareous dino-
flagellate cysts, acritarchs, pteridophyte spores, gymnosperm
pollen, planispiral agglutinated foraminiferal linings and,
occasionally, some prasinophyte algae. The vertical distribu-
tion of palynomorphs is given in Fig. 13. No palynomorph was
detected in samples 33, 39, 41, 43, 46, 56, 70, 97/98, 100/101,
108/109, 130/131, 134/135 and 135/136.
The following spectra were found:
Sample 25: abundant black phytoclasts with non-calcareous
dinocysts of Amphorula dodekovae, A. metaelliptica, Circulo
dinium distinctum, Cometodinium habibii, Cribroperidinium sp.,
Glossodinium dimorphum, Prolixosphaeridium anasillum,
P. mixtispinosum, Subtilisphaera sp., Systematophora daveyi,
167
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 9. Kurovice section, calcareous dinoflagellate cysts. A — Parastomiosphaera malmica, sample −12; B — Stomiosphaera mollucana,
sample −19; C — Colomisphaera carpathica, sample −2; D — Colomisphaera lapidosa, sample −12; E — Carpistomiosphaera tithonica,
sample −2; F — Committosphaera pulla, sample −12; G — Colomisphaera radiata, sample −10; H — Commitosphaera ornata, sample −27;
I — Colomisphaera pieniniensis, sample −20; J — Cadosina semiradiata semiradiata, sample −3; K — Cadosina semiradiata fusca,
sample −2; L — Colomisphaera fortis, sample 148.
168
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
S. orbifera and S. silybum, the acritarch Micrhystridium sp.,
a prasinophyte alga Pterospermella helios, spores of
the fern Cyathidites minor, and gymnosperm Classopollis toro
sus pollen. The palynospectrum corresponds to the Tithonian
age.
Sample 30a: frequent phytoclasts of brown and black colour
with broken non-calcareous dinoflagellate cysts, namely:
Gonyaulacysta sp., Gochteodinia cf. virgula, Ctenidodinium
ornatum, Pareodinia sp., the acritarch Micrhystridium stellatum,
Veryhachium irregulare, and pollen of Classopollis torosus —
often present in tetrads.
Sample 49: frequent phytoclasts of brown and black colour
with a rich assemblage of non-calcareous dinoflagellate cysts
similar to associations in the underlying strata and, additio-
nally, Cribroperidinium globatum, C. sarjeantii, Pareodinia
robusta, Gonyaulacysta helicoidea, Hystrichodinium pulchrum,
Neuffenia willei, Oligosphaeridium pulcherrimum, Sentu
sidinium sp., Stiphrosphaeridium dictyophorum, Systemato
phora areolata, and Tanyosphaeridium isocalamum. Sporadic
Micrhys tridium sp. and gymnosperm pollen, Classopollis
torosus, also occur.
Sample 50: common phytoclasts of brown and black colour,
tracheids of Pinaceae, non-calcareous dinoflagellate cysts,
namely: Dingodinium tuberosum, Oligosphaeridium aff. patu
lum, Chytroeisphaeridia chytroeides, Jansonia sp., isolated
opercula of Cribroperidinium sp. and Wallodinium sp., linings
of planispiral agglutinated foraminifers, the acritarch
Micrhystridium sp., Leiosphaeridia sp., Pterospermella
australiensis, pteridophyte spores Gleicheniidites senonicus,
Neoraistrickia truncata, Lycopodiumsporites sp., Poly cin
gulatisporites and Classopollis torosus, Spheripollenites
subgra nulatus. The palynospectrum corresponds to the Titho-
nian age.
Sample 85: abundant black phytoclasts with Micrhystridium
sp., and the prasinophyte alga Pterospermella. Dinocyst asso-
ciation is similar to underlying strata.
Sample 105: brown and black phytoclasts and radiolarian
remains. Non-calcareous dinocysts are represented both by
species derived from underlying strata and by in situ taxa
Dissiliodinium giganteum, Prolixosphaeridium deirense,
Prolixosphaeridium sp. A sensu Monteil (1993), and Tehama
dinium evittii.
Sample 111/112: abundant black phytoclasts, amorphous
organic matter, broken radiolarian tests, linings of aggluti-
nated foraminifers, rich dinoflagellate cyst association with
species known from the underlying strata as well as Achomo
sphaera neptuni, Circulodinium vermiculatum, Dapsilidinium
multispinosum, Endoscrinium campanula, E. cf. pharo,
Gonyaulacysta sp., Kiokansium polypes, P. anasillum, and
Classopollis torosus. The palynospectrum corresponds to
the Berriasian age with the redeposition of Jurassic species.
Sample 132: brown and black phytoclasts, radiolarian rem-
nants, non-calcareous dinocysts similar to the assemblages of
the underlying strata with new taxa Cyclonephelium hystrix,
Spiniferites sp. and Sirmidiniopsis sp. An admixture of conti-
nental pteridophyte spores (Echinatisporites sp.) and
gymnosperm pollen (Classopollis torosus and Cerebro
pollenites macroverrucosus) is subsidiary. It corresponds to
the Berria sian age with the redeposition of Jurassic species.
Sample 132/133: abundant black phytoclasts, non-calcareous
dinoflagellate cysts Circulodinium sp., Dichadogonyaulax
bensonii, Endoscrinium campanula, Gonyaulacysta sp.,
Leptodinium sp., Oligosphaeridium asterigerum and Prolixo
sphaeridium granulosum. Pteridophyte spores Densoisporites
velatus, Gleicheniidites sp. and conifers of Classopollis
torosus is subsidiary. It corresponds to the Berriasian age with
the redeposition of Jurassic species.
Selected palynomorphs are shown in Figures 14 and 15.
Biostratigraphy
Despite the poor preservation, microorganisms provide
important data that help us to detect the Jurassic/Cretaceous
boundary at Kurovice. According to the calcareous dinoflagel-
late cyst and calpionellid zonations (sensu Reháková 2000;
Reháková & Michalík 1997) the section spans the interval
from the Early Tithonian cyst Malmica Zone up to the Early
Berriasian Calpionella Zone, Elliptica Subzone (Figs. 11, 12,
16). Nannofossils confirm this stratigraphic interpretation,
with a zonal range from NJT 15b up to NK-1 (zones of
Casellato 2010; Bralower et al. 1989).
The following calcareous dinocyst and calpionellid zones
compared to nannofossil events were identified:
The calcareous dinocyst Malmica Zone (Nowak 1968),
early Early Tithonian was established in the lowermost part of
the sequence (samples −29 to −7; ~0–7.7 m) by the presence
of Parastomiosphaera malmica. Nannofossil assemblages
contain Polycostella beckmanii and are assigned to the NJT 15b
Nannofossil Subzone. The first, questionable, small nanno-
conids were found in sample −16 (Table 1b).
The following calcareous dinoflagellate and calpionellid
zones were previously mentioned by Elbra et al. (2018a):
The Semiradiata Zone (Reháková 2000), Early Tithonian
(samples −6 to 35; ~7.7–35.5 m; Elbra et al. 2018a) was
recognized based on the abundance of the cysts Cadosina
semiradiata semiradiata and C. semiradiata fusca. The first
occurrence (FO) of Helenea chiastia (NJT 16 Nannofossil Zone)
was recorded immediately above the base of the Semiradiata
Zone in sample 3.
The Tenuis-Fortis Zone, early Late Tithonian (samples
36–42, ~35.5–37.65 m). It was not possible to strictly separate
the Tenuis from the Fortis zones (Řehánek 1992) because of
the absence of Colomisphaera tenuis. Only one specimen of
Colomisphaera sp. was found in sample 20. Reháková (2000)
assumed that the Fortis Zone coincided with the disappearance
of chitinoidellids and their substitution by the first transitional
hyaline–microgranular calpionellids of the Praetintinnopsella
Zone. A single lorica of Praetintinnopsella andrusovi was
found in the sample 42/43, but in the overlying Crassicollaria
Zone. This phenomenon confirms the opinion of Reháková
(2000).
169
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 10. Kurovice section, calpionellids. A — Crassicollaria massutinianna, sample 100; B — Calpionella grandalpina, sample 101b;
C — Calpionella elliptalpina, sample 88; D — Calpionella sp., sample 125; E — Lorenziella hungarica, sample 124; F — Remaniella durand
delgai, sample 132; G — Remaniella borzai, sample 120; H — Remaniella colomi, sample 125; I — Remaniella ferasini, sample 127;
J — Calpionella elliptica, sample 133; K — Calpionella elliptica, sample 134; L — Tintinopsella carpathica, sample 139.
170
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 11. Kurovice section, lithology and vertical distribution of calpionellids and calcareous dinoflagellate cysts. TFZ — Tenuis–Fortis Zone;
R Sbz — Remanei Subzone; CrZ — Crassicollaria Zone. Open circles indicate reworked specimens. Lithology after M. Bubík in Košťák et
al. (2018). Calpionellid zones after Reháková & Michalík (1997), cyst zones sensu Reháková (2000).
171
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 12. Kurovice section, lithology and vertical distribution of calpionellids and calcareous dinoflagellate cysts. Open circles indicate reworked
specimens. Lithology after M. Bubík in Košťák et al. (2018). Calpionellid zones after Reháková & Michalík (1997), cyst zones sensu Reháková
(2000).
172
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
The Crassicollaria Zone (Remane et al. 1986), early to late
Late Tithonian (samples 42/43–84, ~37.65–51.9 m) is sub-
divided into three subzones:
The Remanei Subzone (Remane et al. 1986) (samples 42/43
–51/52; ~37.65–42.9 m) is identified by very rare calpionel-
lids Tintinnopsella remanei and Crassicollaria intermedia,
followed by rare C. massutiniana, C. parvula and Calpionella
alpina.
The Intermedia Subzone (Remane et al. 1986) (samples
52–70; ~42.9–48.25 m) is clearly recognizable by a frequent
and more diversified association with Calpionella alpina,
C. grandalpina, C. elliptalpina, Crassicollaria intermedia,
C. massutiniana, C. parvula, C. brevis, and Tintinnopsella
carpathica. In the lower part of this interval (sample 55) is
the FO of Nannoconus globulus minor, so that the base of
the NJT 17a Nannofossil Subzone is recorded (Fig. 16). Just
above this bioevent, the last occurrence of Polycostella beck
mannii was identified.
The Colomi Subzone (Pop 1994) (samples 70/71–84;
~48.25–51.9 m) is characterized by the dominance of Crassi
collaria parvula, associated with scarce C. colomi and other
deformed crassicollarians. Larger forms of Calpionella grand
alpina and C. elliptalpina show rapid quantitative decline.
The FO of Nannoconus wintereri was found in the upper part
of this interval in sample 79/80. This bioevent defines the base
of the NJT 17b Subzone which has a short stratigraphic
interval spanning the uppermost Tithonian (Casellato 2010).
The overlying bed, unit 81, yielded the first Nannoconus
globulus globulus.
The Calpionella Zone, Early Berriasian in age, is here sub-
divided again into three subzones.
The Alpina Subzone (sensu Pop 1974; Remane et al. 1986)
was first detected in the sample 85/86 and its top was recorded
in sample 118; spanning the interval from ~51.9 m to 68.5 m
with disappearance of large Calpionella species and domi-
nation of small spherical specimens of Calpionella alpina
(Calpionella alpina event sensu Kowal-Kasprzyk & Reháková
2019). The species Crassicollaria parvula and Tintinnopsella
carpathica are very rare. The base of the calcareous nannofos-
sil NKT Zone is marked by the FO of Nannoconus steinmannii
minor in sample 92.
The Ferasini Subzone (Remane et al. 1986), Early Berriasian
in age (samples 119–131; ~68.5–71.8 m) is distinguished by
a decrease in the number of calpionellids. The Rema niella fera
sini was not recorded in sample 119, so, the base of the bio zone
is fixed on the FO of R. duranddelgai (sample 119) and
the appearance of other remaniellids. The FO of Nanno conus
kamptneri kamptneri (NK-1 Zone) occurs in sample 124.
The Elliptica Subzone (Pop 1974), late Early Berriasian
(samples 132–148; ~71.8–76.7 m) was established on the pre-
sence of Calpionella elliptica accompanied by rare specimens
of the genera Calpionella, Remaniella, Tintinnopsella and
Lorenziella. The FO of Speetonia colligata was registered in
sample 133/134.
The species Nannoconus infans, N. kamptneri minor and
N. steinmannii steinmannii appear sporadically in the limestone
sediments at Kurovice, and for this reason their first occur-
rences are not used in our stratigraphic interpretations
(Table 1).
The above-mentioned stratigraphic data are reinforced by
that provided by palynomorphs. The non-calcareous dino-
flagellate cysts Amphorula metaelliptica, Dingodinium tube
rosum, Systematophora areolata, and S. silybum support
a Tithonian age for sample 30a, the uppermost part of
the Semiradiata Zone, and for sample 50 — an assignment to
the Remanei Subzone. Dinoflagellate cysts of Berriasian age
— Achomosphaera neptunii, Prolixosphaeridium sp. A and
Tehamamadinium evittii — were recorded in samples 105 and
111/112 in the Alpina Subzone and in the samples 132 and
132/133 in the Elliptica Subzone.
Prolixosphaeridium sp. A (sample 105) is mentioned by
Monteil (in Stover et al. 1996) within the ammonite Jacobi
Subzone (within the calpionellid Alpina Subzone) of the Early
Berriasian. According to Leereveld (1995), the FO of Achomo
sphaera neptunii (sample 111/112) is connected to the late
Early Berriasian (uppermost part of the Jacobi ammonite
Zone; calpionellid Elliptica Subzone; Reboulet et al. 2014,
Wimbledon 2017) along with the FO of Dichadogonyaulax
bensonii (sample 132/133). Monteil (1992, 1993) correlates
the FOs of both species in the Berriasian type section with
the late Early Berriasian, the uppermost part of the Alpina
Subzone, respectively. Monteil (1993) and Hunt (2004) com-
bine the first occurrences of the D. bensonii, Endoscrinium
campanula (sample 111/112) and Tehamadinium evittii (sam-
ple 105) as key range bases for correlation with the ammonite
Grandis Subzone (upper Jacobi Zone) and Subalpina subzone
(that is lowest Occitanica Zone). The similar relative age is
indicated by calpionellids and nannofossils.
Paleoecology
According to Elbra et al. (2018a), the sediments at Kurovice
were deposited on the continental slope during the Late
Tithonian–Early Berriasian. The section is characterized by
distal limestone sediments with sporadic turbidites. Košťák et
al. (2018) supposed tsunami deposition/influence which might
explain the presence of debris in the abyssal environment.
Pelagic sediments are characterized by the large proportion of
calcareous and siliceous marine microplankton which pre-
dominates over the turbidity material. These statements are in
line with microfacies analyses (see above). The interpretation
of the deposits as the standard microfacies types SMF 2,
SMF 3 and SMF 4 indicates deposition on a deep shelf margin
within facies zone FZ 3, changing into a basinal environment
in its later/upper part, facies zone FZ 1 (Wilson 1975).
Sedimentation occurred under the influence of enhanced
water dynamics, which affected nutrient supply and caused
the periodical erosion and redeposition of older rocks. The nut-
rient supply is here demonstrated by the quantitative predo-
minance of radiolarians and sponge spicules. Calpionellids are
generally rare and they are represented almost exclusively by
173
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
hyaline species, which first appear in the Late Tithonian.
The absence of typical microgranular chitinoidellids from
the late Early Tithonian and the early Late Tithonian can be
explained by the dominant presence of radiolarians. These
microorganisms with silica tests preferred conditions rich in
nutrients, something not suitable for calpionellids, and their
development was probably inhibited. The location of the depo-
sitional area on the northern margin of Tethys (Golonka et al.
2006) and the possible influence of incoming northern waters
can also not be ignored.
The nannoconids Conusphaera and Polycostella beckma
nnii are referred to as predominantly Tethyan taxa (Bown &
Cooper 1998; Bown et al. 1998). Other nannofossils that con-
firm the Tethyan province are randomly found — Watznaueria
manivitiae, Zeugrhabdotus embergeri, Cruciellipsis cuvillieri,
and Speetonia colligata (Bown & Cooper 1998; Bown et al.
1998). The small percentage of these taxa found in our study
may be explained by the paleogeographic location on the mar-
gin of Tethys (Golonka et al. 2006; Svobodová et al. 2018).
This region could have been affected by cold waters from
Fig. 13. Kurovice section, lithology and vertical distribution of palynomorfs and non-calcareous cysts. Reworked specimens marked with
dashed line. Lithology after M. Bubík in Košťák et al. (2018).
174
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 14. Kurovice section, palynomorphs. Scale bar 10 µm. A–F, L–N, P sample 50 middle, G–K, O sample 132. A — Dingodinium tuberosum;
B — aff. Oligosphaeridium patulum; C — Ctenidodinium ornatum; D — Chytroeisphaeridia chytroeides; E — Jansonia sp.; F — Pterospermella
australiensis; G — Tanyosphaeridium isocalamum; H — radiolarian remnant; I — Circulodinium distinctum; J — Gonyaulacysta cf.
helicoidea; K — Cribroperidinium sp., fragment; L — Gleicheniidites senonicus; M — Neoraistrickia sp.; N — Classopollis torosus;
O — Densoisporites velatus; P — Corollina sp.
175
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Subboreal regions, such as the Russian Platform. The influence
from higher latitudes might also be shown by the scarce pre-
sence of Nannoconus compressus (Fig. 7Y) mentioned in
the Atlantic Ocean (Bralower et al. 1989; Casellato 2010).
Stoykova et al. (2018) mentioned N. compressus from the SW
Bulgaria, and Halásová in Bakhmutov et al. (2018) from
the Crimea (southern Ukraine). The question remains whether
these areas were also under marine influence from the north.
Significantly higher percentages of nannoconids (up to
20 % in the Berriasian), conusphers (up to 50 % in the Late
Tithonian and 20–40 % in the Early Berriasian) and P. beck
mannii (up to 20–30 % in Late Tithonian) are mentioned in
Fig. 15. Kurovice section, non-calcareous dinoflagellate cysts. Scale bar 10 μm. A–F sample 49 middle, G–J sample 105, K–M sample 111/112,
N–P sample 132/133. A — Systematophora daveyi; B — Cometodinium habibii; C — Stiphrosphaeridium dictyophorum, archeopyle;
D — Systematophora orbifera; E — Pareodinia robusta; F — Gonyaulacysta helicoidea; H — Lithodinia sp.; K — Prolixosphaeridium
anasillum; L — Prolixosphaeridium sp. A sensu Monteil (1993); M — Endoscrinium campanula; N — Systematophora areolata;
O — Prolixosphaeridium granulosum; P — Dichadogonyaulax bensonii.
176
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Michalík et al. (2016) from the Pienniny Klippen Belt. Similar
nannofossil percentages were mentioned by Svobodová &
Košťák (2016) from further west in Tethys, on the southern
passive margin of the Iberian Plate.
The occurrence of non-calcareous cavate cysts of Dingo
dinium, proximate cysts of Cribroperidinium, rare chorate
cysts, and the frequent presence of agglutinated microfora-
miniferal linings indicate a shallow sea and probably rewor-
king of terrestrial, brackish and shallow-water species into
a deeper marine environment. Reworking is documented
by the high diversity of Systematophora species, which
characterize a littoral environment. Prasinophyte algae and
acritarchs are known from the brackish to shallow marine con-
ditions (Batten 1996). They could have been flushed into
the shallow sea and continuously transported into the deeper
water.
Discussion
Compared to most localities in Tethys, small differences in
calpionellid succession are evident. Chitinoidellids, the first
calpionellid representatives have not been recorded
(Svobodová et al. 2018). Their absence may be explained by
the blooming of siliceous microorganisms which probably
suppressed chitinoidellids. This phenomenon could also have
been associated with cold water influence at the margin of
Tethys.
The calcareous dinoflagellate Malmica Zone corresponds in
the Kurovice sequence to magnetozone M 21r, as at Brodno
(Central Western Carpathians; Michalík et al. 2009) and Lokút
(Transdanubian range; Grabowski et al. 2010a, 2017). Even
though aragonite shells did not survive sedimentation and
early diagenesis of Kurovice limestones, magnetozones M 20r
to M 17r in the upper part of the section may also be used to
approximate the ammonite zones from Micracanthoceras
microcanthum to Subthurmannia occitanica in the Vocontian
Basin (Wimbledon et al. 2013; Frau et al. 2016a, b, c; Elbra et
al. 2018b).
Nannofossil events and their stratigraphic correlations in
the J/K boundary interval are more or less comparable with
the other localities in Tethys. The first occurrence (FO) of
Nannoconus globulus minor is situated in magnetozone M 19r
and the Intermedia Subzone, as at Puerto Escaño (Svobodová
& Košťák 2016). The last occurrence (LO) of Polycostella
beckmannii was recorded in the lower part of M 19n.2n, still in
the Intermedia Subzone, as with the Brodno locality (Michalík
et al. 2009). The FO of N. wintereri lies in the upper part of
the Crassicollaria Zone, in M 19n.2n as with Puerto Escaño
(Svobodová & Košťák 2016) and Le Chouet (Wimbledon et
al. 2013). The FO of N. wintereri in M 19n.2n is also men-
tioned at Torre de’ Busi (Casellato 2010; Channell et al. 2010),
before the FO of N. globulus globulus. In the Kurovice succes-
sion, the FO of N. globulus globulus occurs just above the FO
of N. wintereri as with Le Chouet (Wimbledon et al. 2013).
The FO of N. steinmannii minor was recorded in the lower part
of the Alpina Subzone, approximately in the middle part of
M 19n.2n similar to the Strapková locality (Central Western
Carpathians) — Michalík et al. (2016). At Brodno (Michalík
et al. 2009), this bioevent also occurs in the lower part of
the Alpina Subzone, but within the M 18r. At Torre de’ Busi,
Casellato (2010) and Channell et al. (2010) mentioned the FO
of N. steinmannii minor in subzone M 19n.1n, and the FO of
N. kamptneri kamptneri in the middle part of the Ferasini
Subzone and M 18n. Generally, Wimbledon (2017) mentions
the FOs of N. wintereri and N. steinmannii minor in Western
Tethys within M 19n.2n, immediately below the Calpionella
Zone, J/K boundary.
The nannofossil record clearly depends on the lithological
character of the strata and this reality may affect the final
stratigraphic and paleoenvironmental interpretations. As men-
tioned above, calcarenites provide scarce fragmen ted speci-
mens, whereas micrite limestones contain rare and poorly
preserved nannofossils. In contrast, marlstone inter calations
contain abundant and diversified assemblages. This could be
the cause of the scarce and irregular occurrence of genus
Nannoconus in some parts of the section, and the fact that
the first occurrences of N. infans, N. kamptneri minor
and N. steinmannii steinmanni could not be relied upon for
stratigraphic interpretations. Strata provided N. wintereri
(Fig. 7AA, AB) and also specimens that can be consider as
an early forms of this species (Fig. 7AC, AD).
Nannofossils were not recognized in thin sections prepared
for the calpionellid and facies investigation.
The quantitative predominance of the genera Watznaueria
and Cyclagelosphaera furnish proof of probable secondary
post-mortem modification of the original nannoflora. Other
placoliths that are easily destroyed are found scarcely and
mostly as fragments.
Through the Kurovice sequence, the irregular occurrence of
unknown specimens of Conusphaera was observed. They are
forms characterized by a thinner structure than Conusphaera
mexicana, and are here mentioned as Conusphaera sp. 1
(Fig. 7I–L). As the ecological affinities of Conusphaera spp.
are unclear (Bornemann et al. 2003; Tremolada et al. 2006),
Conusphaera sp. 1 is an object suitable for further study.
Moreover, specimens that look like C. mexicana cf. minor
(Fig. 7P), but which reach larger dimensions, of about 5 µm,
were recorded. The height given in the original description of
C. mexicana minor does not exceed 4 µm (Bown & Cooper
1989). The high content of calcium carbonate and oxic con-
ditions were also the cause of poor preservation of
palynomorphs.
Sediments throughout the sequence contain reworked
calcareous dinoflagellates, such as Colomisphaera fibrata,
C. tenuis, C. fortis, Stomiosphaera moluccana, Commito
sphaera pulla, Carpistomiosphaera tithonica, C. borzai, and
Parastomiosphaera malmica, which have been mentioned
from the Late Oxfordian and Early Tithonian exclusively
(Lakova et al. 1999; Reháková 2000; Ivanova & Kietzman
2017). Sometimes during the Berriasian, calpionellids such as
Calpionella grandalpina, C. elliptalpina, and Crassicollaria
177
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Fig. 16. Integrated biostratigraphic correlations, microfacial interpretations, important bioevents and magnetostratipgraphy of the Kurovice
section. Magnetostratigraphy as well as calpionellid, calcareous dinoflagellate and nannofossil zonations of 1–148 beds interval are modified
from Elbra et al. (2018a). Black — normal polarity; white — reversed polarity; gray — unclear polarity due to lack of samples or stable mag-
netic component. Magnetostratigraphy of sample beds −1 to −29 is preliminary. TFZ — Tenius-Fortis Zone; MPBL — microfacies prevailed
in biomicrite limestone; SMF — standard microfacies types; FZ — facies zones. Calpionellid zones after Reháková & Michalík (1997);
dinoflagellate cyst zones sensu Reháková (2000).
178
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
massutiniana, were reworked from the Tithonian strata.
The nannofossil species Parhabdolithus cf. marthae has been
found in the lower part of section, in the NJT 16 zone, and it
indicates a source of material of Early Sinemurian age, in
the NJ 2a zone (Bown & Cooper 1998). Scarce Lotharingius
hauffii (NJ 5a–NJ 12a) and L. sigillatus (NJ 5b–NJ 15a)
(Table 1a, b) document source rocks in the upper Pliensbachian–
lower Callovian up to lower Oxfordian interval (Bown &
Cooper 1998; Mattioli & Erba 1999). Reworked non-calca-
reous dinoflagellate cysts of Jurassic age (Systematophora
areolata, Prolixosphaeridium anasillum) were found in sam-
ples 132 and 132–133 in the nannofossil NK-1 Zone and
the Elliptica Subzone. The same strata also provided reworked
Nannoconus compressus that is mentioned only in the Titho-
nian (Bralower et al. 1989; Casellato 2010). A relatively high
number of Polycostella beckmannii which supposedly occurs
exclusively in the Tithonian was found in sample 142s in
the Berriasian (Fig. 4, Table 1c). The presence of these alloch-
thonous microorganisms is testimony to the dynamics of
the depositional area and to repeated sediment erosion.
The ‘Nannofossil Calcification Event’ (NCE) sensu Borne-
mann et al. (2003) could be applied to the nannofossil record
in the Kurovice section. However, it relates only to Assemblage 1
and Assemblage 2 (sensu fig. 17 in Bornemann et al. 2003).
Morphometric measurements were not an aim of this study.
Conclusions
Detailed studies of microfacies and high-resolution recor-
ding of microfossils and calcareous nannofossils in the exten-
ded Kurovice section provide more precise stratigraphic results
and paleoenvironmental interpretations across the Jurassic/
Cretaceous boundary interval.
The stratigraphic range of the sequence is from the Early
Tithonian calcareous dinoflagellate Malmica Zone up to
the Early Berriasian calpionellid Elliptica Subzone, that is
magnetozone M 21r to M 17r, and nannofossil zone NJT 15b
to NK-1. The absence of calpionellid Chitinoidella Zone is
explained by the blooms of silica preferring microorganisms
which could have suppressed the development of microgranu-
lar chitinoidellids. The J/K Calpionella alpina boundary event
indicated by size change of lorice of this species coincides
with the NJT 17b Subzone and M 19n.2n, and with the pre-
sence of Nannoconus wintereri. The dinoflagellate cysts,
Prolixosphaeridium sp. A sensu Monteil 1993, Tehama ma
dinium evittii, Achomosphaera neptunii, Endoscrinium cam
panula, and Dichadogonyaulax bensonii, that are present in
the upper part of the section support an Early Berriasian age.
The identified standard microfacies types SMF 2, SMF 3 and
SMF 4 suggest an origin for the deposits here on the deep shelf
margin, facies zone FZ 3, passing in time into the more distal
basinal conditions, in facies zone FZ 1, with standard micro-
facies types SMF 2 and SMF 3 being formed.
The sediments bear the marks of the enhanced water dyna-
mics that caused nutrient mobility, periodical erosion and
overflow of sediments from the coeval and older Jurassic
strata including also littoral and brackish palynomorphs
accompanied by additional supply of terrestrial pollen and
spores.
The nannofossil record and nannofossil preservation depend
on the lithological character of deposits. The quantitative pre-
dominance of the genera Watznaueria and Cyclagelosphaera
furnish proof of the probable secondary post-mortem modifi-
cation of the nannoflora. Nannoconids — Conusphaera and
Polycostella — and placoliths of Watznaueria manivitiae,
Zeugrhabdotus embergeri, Cruciellipsis cuvillieri, and also
Speetonia colligata, which are referred to as predominantly
Tethyan taxa, formed a significantly small percentage in
assemblages as compared to ones of the same age in other
regions of Tethys. This may be explained by the location of
depositional area at the margin of Tethys where there might
have been some influence of cold waters coming from boreal
regions.
Acknowledgements: We would like to thank M. Košťák,
L. Vaňková, J. Rantuch, M. Bubík, K. Čížková and Š. Kdýr
for their help during field work and measurements and for
valuable cooperation. Special thanks to Petr Pruner for the lea-
ding of the project and for valuable consultations. The authors
are grateful to Prof. Paul Bown of London´s Global University
for consulting on the correct determination of some strati-
graphically important nannofossil species. The authors are also
grateful to William A.P. Wimbledon, Daniela Boorová and
Kristalina Stoykova for their valuable comments and improve-
ments of the manuscript. The research was supported by
the research plan of the Institute of Geology of the Czech
Academy of Sciences, No. RVO67985831 and by the Czech
Science Foundation, project No. 16-09979S „Integrated multi-
proxy study of the Jurassic-Cretaceous boundary in marine
sequences: contribution to global boundary definition“. Micro-
facial and calpionellid investigations were financialy suppor-
ted by the project of the Slovak Grant Agency APVV-14-0118
and by VEGA 2/0034/16 Projects. This work is a contribution
of the Berriasian Working Group of the International Subcom-
mission on Cretaceous Stratigraphy (ICS).
References
Andreini G., Caracuel J.E. & Parisi G. 2007: Calpionellid biostrati-
graphy of the Upper Tithonian–Upper Valanginian interval in
Western Sicily (Italy). Swiss J. Geosci. 100, 179–198.
Andrusov D. 1933: Minor Reports on Geology of the Moravia–
Silesian Carpathians. Věstník Státního geologického Ústavu
Československé republiky 9, 194–199 (in Czech).
Andrusov D. 1945: Geological research of the West Carpathian Inner
part of Klippen Belt IV, V. Práce Št. geol. Úst. 13, 1–176
(in Slovak).
Bakhmutov V.G., Halásová E., Ivanova D.K., Józsa Š., Reháková D.
& Wimbledon W.A.P. 2018: Biostratigraphy and magneto-
stratigraphy of the uppermost Tithonian-Lower Berriasian in
the Theodosia area of Crimea (southern Ukraine). Geol. Quar
terly 62, 2, 197–236.
179
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Batten D.J. 1996: Palynofacies and palaeoenvironmental interpreta-
tions. In: Jansonius J., McGregor D.C. (Eds.): Palynology:
Principles and Applications 3. AASP Foundation, Dallas,
1011–1064.
Bornemann A., Aschwer U. & Mutterlose J. 2003: The impact of
calcareous nannofossils on the pelagic arbonate accumulation
across the Jurassic–Cretaceous boundary. Palaeogeogr. Palaeo
climatol. Palaeoecol. 199, 187–228.
Bown P.R. & Cooper M.K.E. 1989: Conical nannofossils in the
Mesozoic. In: Crux J.A. & van Heck S.E. (Eds.): Nannofossils
and their applications, Ellis Horwood, Chichester, 98–106.
Bown P.R. & Cooper M.K.E. 1998: Jurassic. In: Bown P.R. (Ed.):
Calcareous Nannofossil Biostratigraphy. British Micropalaeon
tological Society, London, 34–85.
Bown P.R., Rutledge D.C., Crux J.A. & Gallagher L.T. 1998: Lower
Cretaceous. In: Bown P.R. (Ed.): Calcareous Nannofossil Bio-
stratigraphy. British Micropalaeontological Society, London,
86–131.
Bralower T.J., Monechi S. & Thierstein H.S. 1989: Calcareous
Nannofossil Zonation of the Jurasssic–Cretaceous Boundary
Interval and Correlation with the Geomagnetic Polarity Time-
scale. Mar
. Micropaleontol. 14, 153–235.
Casellato C.E. 2010: Calcareous nannofossil biostratigraphy of Upper
Callovian–Lower Berriasian successions from the Southern
Alps, North Italy. Rivista Italiana di Paleontologia e Stratigrafia
16, 3, 357–404.
Channell J.E.T., Casellato C.E., Muttoni G. & Erba E. 2010: Magne-
tostratigraphy, nannofossil stratigraphy and apparent polar
wander for Adria–Africa in the Jurasic–Cretaceous boundary
interval. Palaeogeogr. Palaeoclimatol. Palaeoecol. 293,
51–75.
Dunham R.J. 1962: Classification of carbonate rocks according to
depositional texture. In: Ham W.E. (Ed.): Classification of car-
bonate rocks. Am. Assoc. Petrol. Geol. Memoir 1, 108–121.
Elbra T., Bubík M., Reháková D., Schnabl P., Čížková K., Pruner P.,
Kdýr Š., Svobodová A. & Švábenická, L. 2018a: Magneto- and
biostratigraphy across the Jurassic–Cretaceous boundary in
the Kurovice section, Western Carpathians, Czech Republic.
Cretaceous Res. 89, 211–223.
Elbra T., Schnabl P., Čížková K., Pruner P., Kdýr Š., Grabowski J.,
Reháková D., Svobodová A., Frau C. & Wimbledon W.A.P.
2018b: Palaeo- and rock magnetic investigations across Juras-
sic–Cretaceous boundary at St Bertrand’s Spring, Drôme, France
— Applications to magnetostratigraphy. Studia Geophysica et
Geodaetica 62, 323–338.
Eliáš M., Martinec P., Reháková D. & Vašíček Z. 1996: Geology and
stratigraphy of the Kurovice Limestone and Tlumačov Marl
Formation at the Kurovice quarry (Upper Jurassic–Lower Creta-
ceous, Outer Western Carpathians, Czech Republic). Věstník
Českého geologického ústavu 71, 3, 259–275 (in Czech).
Fensome R.A. & Williams G.L. 2004: The Lentin and Williams
Index of fossil dinoflagellates: 2004 edition. American Asso
ciation of Stratigraphic Palynologists Contribution Series 42,
1–909.
Fensome R.A., Williams G.L. & MacRae R.A. 2009: Late Cretaceous
and Cenozoic fossil dinoflagellates and other palynomorphs
from the Scotian Margin, offshore Eastern Canada. J. Syst.
Palaeontol. 7, 1, 1–79.
Flügel E. 2004: Microfacies of Carbonate Rocks. SpringerVerlag,
Berlin, 1–976.
Folk R.L. 1959: Practical classification of limestone. Amer. Assoc.
Petrol. Geol. Bull. 43, 1–38.
Frau C., Bulot L.G., Reháková D., Wimbledon W.A.P. & Ifrim C.
2016a: Revision of the ammonite index species Berriasella
jacobi Mazenot, 1939 and its consequences for the biostrati-
graphy of the Berriasian Stage. Cretaceous Res. 66, 94–114.
Frau C., Bulot L.G., Wimbledon W.A.P. & Ifrim C. 2016b: Sys te-
matic palaeontology of the Perisphinctoidea across the Jurassic/
Cretaceous boundary at Le Chouet (Drôme, France) and
its biostratigraphic implications. Acta Geologica Polonica 66,
157–177.
Frau C., Bulot L.G., Wimbledon W.A.P. & Ifrim C. 2016c: Upper
Tithonian ammonites (Himalayitidae Spath, 1925 and Neocomi-
tidae Salfeld, 1921) from Charens (Drôme, France). Geol.
Carpath. 67, 6, 543–559.
Glöckner E.F. 1841: Über den Jurakalk von Kurowitz in Mähren und
über den darin vorkommenden Aptychus imbricatus. Verh.
Leopold Carol. Akad. naturf. 19, 2, 73–308.
Golonka J., Gahagan L., Krobicki M., Marko F., Oszczypko N. &
Ślączka A. 2006: Plate-tectonic evolution and paleogeography
of the Circum–Carpathian region. In: Golonka J. & Picha F.
(Eds.): The Carpathians and their foreland: Geology and hydro-
carbon resources. AAPG Memoir 84, 11–46.
Grabowski J. 2011: Magnetostratigraphy of the Jurassic/Cre-
ta
ceous boundary interval in the Western Tethys and its
cor relation with other regions: a review. Volumina Jurassica 9,
105–128.
Grabowski J. & Pszczółkowski A. 2006: Magneto- and biostrati-
graphy of the Tithonian–Berriasian pelagic sediments in the Tatra
Mountains (Central Western Carpathians, Poland): sedimentary
and rock magnetic changes at the Jurassic/Cretaceous boundary.
Cretaceous Res. 27, 398–417.
Grabowski J., Haas J., Márton E. & Pszczółkowski A. 2010a: Mag-
neto- and biostratigraphy of the Jurassic/Cretaceous boundary
in the Lókút section (Transdanubian range, Hungary). Studia
Geophysica et Geodaetica 54, 1–26.
Grabowski J., Michalík J., Pszczółkowski A. & Lintnerová O. 2010b:
Magneto-, and isotope stratigraphy around the Jurassic/Creta-
ceous boundary in the Vysoká Unit (Malé Karpaty Mountains,
Slovakia): correlations and tectonic implications. Geol. Carpath.
61, 4, 309–326.
Grabowski J., Schnyder J., Sobień K., Koptíková L., Krzemiński L.,
Pszczółkowski A., Hejnar E. & Schnabl P. 2013: Magnetic sus-
ceptibility and spectral gamma logs in the Tithonian–Berriasian
pelagic carbonates in the Tatra Mts. (Western Carpathians,
Poland): Palaeoenvironmental changes at the Jurassic/Creta-
ceous boundary. Cretaceous Res. 43, 1–17.
Grabowski J., Haas J., Stoykova K., Wierzbowski H. & Brański P.
2017: Environmental changes around Jurassic/Cretaceous tran-
sition: New nannofossil, chemostratigraphic and stable isotope
data from the Lókút section (Transdanu bian range, Hungary).
Sediment. Geol. 360, 54–72.
Guzhikov A.Y., Arkad’ev VV., Baraboshkin E.Y., Bagaeva M.I.,
Piskunov V.K., Rud’ko 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, 261–294.
Hoedemaeker J.P., Janssen N.M.M., Casellato C.E., Gardin S.,
Reháková D. & Jamrichová M. 2016: Jurassic–Cretaceous
boun dary in the Río Argos succession (Caravaca, SE Spain).
Integra ted biostratigraphy of section Z along the Barranco de
Tollo. Revue de Paleobiologie, 35,1, 111–247.
Houša V., Krs M., Krsová M. & Pruner P. 1996: Magnetostratigraphic
and micro-paleontological investigations along the Jurassic–
Cretaceous boundary strata, Brodno near Žilina (Western Slo-
vakia). Geol. Carpath. 47, 3, 135–151.
Houša V., Krs M., Krsová M., Man O., Pruner P. & Venhodová D.
1999: High-resolution magnetostratigraphy and micro paleon -
tology across the J/K boundary strata at Brodno near Žilina,
Western Slovakia: summary results. Cretaceous Res. 20,
699–717.
180
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Houša V., Pruner P., Zakharov V.A., Košťák M., Chadima M.,
Rogov M.A., Šlechta S. & Mazuch M. 2007: BorealeTethyan
correlation of the Jurassic/Cretaceous boundary interval by mag-
neto- and biostratigraphy. Stratigraphy and Geological Correla
tion 15, 297–309.
Hunt C.O. 2004: Palynostratigraphy of the classic Portland and
Purbeck sequences of Dorset, southern England, and the correla-
tion of Jurassic–Cretaceous boundary beds in the Tethyan and
Boreal realms. In: Beaudouin A.B. & Head M.J. (Eds.): The
Paly nology and Micropaleontology of Boundaries. Geol. Soc.
London, Spec. Publ. 230, 257–273.
Ivanova D.K. & Kietzmann D.A. 2017: Calcareous dinoflagellate
cysts from the Tithonian–Valanginian Vaca Muerta Formations
in the southern Mendoza area of the Neuquén Basin, Argentina.
Journal of South American Earth Sciences 77, 150–169.
Kietzmann D.A. 2017: Chitinoidellids from the Early Tithonian–
Early Valanginian Vaca Muerta Formation in the Northern
Neuquén Basin, Argentina. Journal of South American Earth
Sciences 76, 152–164.
Košťák M., Vaňková L., Mazuch M., Bubík M. & Reháková D. 2018:
Cephalopods, small vertebrate fauna and stable isotope (δ
13
C,
δ
18
O) record from the Jurassic–Cretaceous transition (Calpio
nella Zone) of the Outer Western Carpathians, Kurovice quarry
(Czech Republic). Cretaceous Res. 92, 43–65.
Kowal-Kasprzyk J. & Reháková D. 2019: A morphometric analysis of
loricae of the genus Calpionella and its significance for the
Jurassic/Cretaceous boundary interpretation. Newsletter on
Stratigraphy 52, 1, 33–54.
Lakova I. & Petrova S. 2013: Towards a standard Tithonian to
Valanginian calpionellid zonation of the Tethyan Realm. Acta
Geologica Polonica 63, 201–221.
Lakova I., Stoykova K. & Ivanova D. 1999: Calpionellid, nannofossil
and calcareous dinocyst bioevents and intergrated biochrono-
logy of the Tithonian to Valangian in the Western Balkanides,
Bulgaria. Geol. Carpath. 50, 2, 151–168.
Lakova I., Grabowski J., Stoykova K., Petrova S., Reháková D., So-
bień K. & Schnabl P. 2017: Direct correlation of Tithonian/
Berriasian boundary calpionellid and calcareous nannofossil
events in the frame of magnetostratigraphy: new results from
the West Balkan Mts., Bulgaria, and review of existing data.
Geologica Balcanica 46, 2, 47–56.
Leereveld H. 1995: Dinoflagellate cysts from the Lower Cretaceous
Río Argos succession (SE Spain). LPP Contribution Series 2,
1–175.
López-Martínez R., Barragán R., Reháková D. & Cobiella-Reguera J.L.
2013: Calpionellid distribution and microfacies across the Juras-
sic/Cretaceous boundary in western Cuba (Sierra de los Órga-
nos). Geol. Carpath. 64, 195–208.
López-Martínez R., Barragán R. & Reháková D. 2015: Calpionellid
biostratigraphy across the Jurassic/Cretaceous Boundary in San
José de Iturbide, Nuevo León, Northeastern Mexico. Geol.
Quarterly 59, 581–592.
Lukeneder A., Halásová E., Kroh A., Mayrhofer S., Pruner P.,
Reháková D., Schnabl P., Sprovieri M. & Wagreich M. 2010:
High resolution stratigraphy of the Jurassic-Creta ceous boun-
dary interval in the Gresten Klippenbelt (Aus
tria). Geol.
Carpath. 61, 5, 365–381.
Mattioli E. & Erba E. 1999: Synthesis of calcareous nannofossil
events in Tethyan Lower and Middle Jurassic sections. Rivista
Italiana di Paleontologia e Stratigrafia 105, 3, 14–176.
Michalík J. 2011 : Mesozoic paleoeography and facies distribution in
the Northern Mediterrenean Tethys from Western Carpathians
view. Iranian Journal of Earth Sciences 3, 194–203.
Michalík J. & Reháková D. 2011: Possible markers of the Jurassic/
Cretaceous boundary in the Mediterranean Tethys — A review
and state of art. Geoscience Frontiers 2, 475–490.
Michalík J., Reháková D. & Peterčáková M. 1990: To the stratigraphy
of Jurassic-Cretaceous boundary beds in the Kysuca sequence of
the West Carpathian Klippen belt Brodno section near Žilina.
Zemní Plyn a Nafta 9b, 57–71.
Michalík J., Reháková D., Halásová E. & Lintnerová O. 2009:
The Brodno section –— a potential regional stratotype of the
Jurassic/Cretaceous boundary (Western Carpathians). Geol.
Carpath. 60, 3, 213–232.
Michalík J., Reháková D., Grabowski J., Lintnerová O., Svobodová A.,
Schlögl J., Sobień K. & Schnabl P. 2016: Stratigraphy, plankton
communities, and magnetic proxies at the Jurassic/Cretaceous
boundary in the Pieniny Klippen Belt (Western Carpathians,
Slovakia). Geol. Carpath. 67, 4, 303–328.
Mišík M. 1971: Observations concerning calcite veinlets in carbonate
rocks. J. Sediment. Petrol. 41, 2, 450–460.
Monteil E. 1992 : Kystes de dinoflagellés index (Tithonique-Valangi-
nien) du Sud-Est de la France: Proposition d´une nouvelle zona-
tion palynologique. Revue de Paléobiologie 11, 1, 299–306.
Monteil E. 1993: Dinoflagellate cyst biozonation of the Tithonian and
Berriasian of south-east France. Correlation with the sequence
stratigraphy. Bulletin des Centres de Recherches Exploration.
Production ElfAquitaine 17, 249–273.
Nowak W. 1968: Stomiosphaerids of the Cieszyn Beds (Kimme-
ridgian–Hauterivian) in the Polish Cieszyn Silesia and their
stratigraphical value. Rocznik Polskiego Towarzystwa Geolo
gicznego 38, 2, 275–327.
Petrova S., Rabrenović D., Lakova I., Koleva-Rekalova E., Ivanova D.,
Metodiev L. & Malešević N. 2012: Biostratigraphy and micro-
facies of the pelagic carbonates across the Jurassic/Cretaceous
boundary in eastern Serbia (Stara Planina–Poreč Zone). Geolo
gica Balcanica 41, 53–76.
Pícha F.J., Stráník Z. & Krejčí O. 2006: Geology and hydrocarbon
resources of the Outer Western Carpathians and their foreland,
Czech Republic. In: Golonka J. & Pícha, F.J. (Eds.): The Car-
pathians and Their Foreland: Geology and Hydrocarbon
Resources. AAPG Memoir 84, 49–175.
Pop G. 1974 : Les zones des Calpionelles Tithonique–Valanginiens
du silon de Resita (Carpates meridionales). Revue Roumaine de
Géologie Géophysique et Géographie, sér. Géol 18, 109–125.
Pop G. 1994: Calpionellid evolutive events and their use in biostrati-
graphy. Romanian Journal of Stratigraphy 76, 7–24.
Pruner P., Houša V., Olóriz F., Košťák M., Krs M., Man O., Schnabl P.,
Venhodová D., Tavera J.M. & Mazuch M. 2010: High-resolution
magnetostratigraphy and biostrati graphic zonation of the Juras-
sic/Cretaceous boundary strata in the Puerto Escaño section
(southern Spain). Cretaceous Res. 31, 2, 192–206.
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. 2014: Report on the 5
th
Interna-
tional Meeting of the IUGS Lower Cretaceous Ammonite Wor-
king Group, the Kilian Group (Ankara, Turkey, 31
st
August
2013). Cretaceous Res. 50, 126–137.
Reháková D. 2000: Evolution and distribution of the Late Jurassic
and Early Cretaceous calcareous dinoflagellates recorded in
the Western Carpathians pelagic carbonate facies. Mineralia
Slovaca 32, 79–88.
Reháková D. & Michalík J. 1997: Evolution and distribution of cal-
pionellids –— the most characteristic constituents of Lower Cre-
taceous Tethyan microplankton. Cretaceous Res. 18, 493–504.
Remane J., Borza K., Nagy I., Bakalova-Ivanova D., Knauer J.,
Pop G. & Tardi-Filácz E. 1986: Agreement on the subdivision of
the standard calpionellid zones defined at the 2nd Planktonic
Conference Roma 1970. Acta Geologica Hungarica 29, 5–14.
Řehánek J. 1992: Valuable species of cadosinids and stomiosphaerids
for determination of the Jurassic–Cretaceous boundary (vertical
distribution, biozonation). Scripta 22, 117–122.
181
J/K BOUNDARY AND HIGH RESOLUTION BIOSTRATIGRAPHY OF THE KUROVICE SECTION
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Schnabl P., Pruner P. & Wimbledon W.A.P. 2015: A review of magne-
tostratigraphic results from the Tithonian–Berriasian of Nordvik
(Siberia) and possible biostratigraphic constraints. Geol.
Carpath. 66, 6, 489–498.
Skupien P., Ryba J. & Doupovcová P. 2016: The study of deep marine
sediments of Jurassic and Cretaceous boundary interval on
Bruzovice profile. Geoscience Research Reports 49, 209–213.
Stover L.E., Brinkhuis H., Damassa S.P., de Verteuil L., Helby R.J.,
Monteil E., Partridge A.D., Powell A.J., Riding J.B., Smelror M.
& Williams G.L. 1996: Mesozoic–Tertiary dinoflagellates,
acritarchs and prasinophytes. In: Jansonius J. & McGregor D.C.
(Eds.): Palynology: Principles and Applications, vol. 2. Ameri
can Association of Stratigraphic Palynologists Foundation,
Dallas, 641–750.
Stoykova K., Idakieva V., Ivanov M. & Reháková D. 2018: Calca-
reous nannofossil and ammonite integrated biostratigraphy
across the Jurassic–Cretaceous boundary strata of the Kopanista
composite section (West Stradnogorie Unit, southwest Bul-
garia). Geol. Carpath. 69, 2, 199–217.
Svobodová A. & Košťák M. 2016: Calcareous nannofossils of the
Jurassic/Cretaceous boundary strata in the Puerto Es caño section
(southern Spain) — biostratigraphy and palaeo ecology. Geol.
Carpath. 67, 3, 223–238.
Svobodová A., Reháková D. & Švábenická L. 2017: High resolution
stratigraphy across the Jurassic–Cretaceous boundary in the
Kurovice Quarry, Outer Western Carpathians, Czech Republic.
In: Jurassica XIII, Poland, June 19–23, 2017. Abstracts and field
trip quidebook, 57.
Svobodová A., Reháková D., Švábenická L. & Vašíček Z. 2018:
Evidence for short-time connection of the NW margin of Tethys
and Subboreal realm during the Late Tithonian and Early Berria-
sian in the Outer Western Carpathians. In: 19
th
Czech–Slovak–
Polish Palaeontological Conference & MIKRO 2018 workshop,
Abstract Book. Folia Musei Rerum naturalium Bohemiae Occi
dentalis Geologica et Paleobiologica, Spec. Vol., 86.
Švábenická L. 2012: Nannofossil record across the Cenomanian–
Coniacian interval in the Bohemian Cretaceous Basin and
Tethyan foreland basins (Outer Western Carpathians), Czech
Republic. Geol. Carpath. 63, 3, 201–217.
Švábenická L., Bubík M., Krejčí O. & Stráník Z. 1997: Stratigraphy
of Cretaceous sediments of the Magura Group of Nappes in
Moravia (Czech Republic). Geol. Carpath. 48, 3, 179–191.
Švábenická L., Reháková D. & Svobodová A. 2017: Calpionellid and
nannofossil correlation across the Jurassic–Cretaceous boundary
interval, Kurovice Quarry, Outer Western Carpathians. In:
10
th
Inter national Symposium on the Cretaceous Vienna, August
21–26, 2017. Abstracts, 252.
Tremolada F., Bornemann A., Bralower T.J., Koeberl C. & van de
Schootbrugge B. 2006: Paleoceanographic changes across the
Jurassic/Cretaceous boundary: The calcareous phytoplankton
response. Earth Planet. Sci. Lett. 241, 361–371.
Vašíček Z. & Reháková D. 1994: Biostratigraphical investigation at
the Kurovice quarry in 1993 (Outer Carpathians, Tithonian–
Lower Valanginian). Geol. Výzk. Mor. Slez. v r. 1993, 28 (in
Czech).
Wilson J.L. 1975: Carbonate facies in geologic history. Springer,
Berlin, 1–471.
Wimbledon W.A.P. 2017: Developments with fixing a Tithonian/
Berriasian (J/K) boundary. Volumina Jurassica XV, 181–186.
Wimbledon W.A.P., Casellato C.E., Reháková D., Bulot L.G.,
Erba E., Gardin S., Verreussel R.M.C.H., Munsterman D.K. &
Hunt C.O. 2011: Fixing a basal Berriasian and Jurassic/Creta-
ceous (J/K) boundary — is there perhaps some light at the end of
the tunnel? Rivista Italiana di Paleontologie e Stratigrafia 117,
295–307.
Wimbledon W.A.P., Reháková D., Pszczółkowski A., Casellato C.E.,
Halásová E., Frau C., Bulot L.G., Grabowski J., Sobień K.,
Pruner P., Schnabl P. & Čížková K. 2013: An account of the
bio- and magnetostratigraphy of the Upper Tithonian–Lower
Berriasian interval at Le Chouet, Drôme (SE France). Geol.
Carpath. 64, 6, 437–460.
Young J.R., Bown P.R. & Lees J.A. (Eds.) 2013: Nannotax3 website.
International Nannoplankton Association. http://ina.tmsoc.org/
Nannotax3.
Appendix
Lists of microfossils and calcareous nannofossils mentioned in the text in alphabetical order:
Calcareous nannofossils
Assipetra infracretacea (Thierstein, 1973) Roth, 1973
Biscutum ellipticum (Górka, 1957) Grün in Grün and Allemann,
1975
Conusphaera mexicana subsp. mexicana Trejo, 1969
Conusphaera mexicana subsp. minor (Trejo, 1969) Bown & Cooper,
1989
Cretarhabdus conicus Bramlette and Martini, 1964
Cruciellipsis cuvillieri (Manivit, 1966) Thierstein, 1973
Cyclagelosphaera argoensis Bown, 1992
Cyclagelosphaera deflandrei (Manivit, 1966) Roth, 1973
Cyclagelosphaera margerelii Noël, 1965
Cyclagelosphaera reinhardtii (Perch-Nielsen, 1968) Romein, 1977
Diazomatholithus lehmannii Noël, 1965
Discorhabdus ignotus (Górka, 1957) Perch-Nielsen, 1968
Ethmorhabdus gallicus Noël, 1965
Ethmorhabdus hauterivianus (Black, 1971) Applegate et al. in
Covington and Wise, 1987
Faviconus multicolumnatus Bralower in Bralower et al., 1989
Helenea chiastia Worsley, 1971
Helenea staurolithina Worsley, 1971
Hexalithus noeliae Loeblich and Tappan, 1966
Hexalithus strictus Bergen, 1994
Lithraphidites carniolensis Deflandre, 1963
Lotharingius hauffii Grün and Zweili in Grün et al., 1974
Lotharingius sigillatus (Stradner, 1961) Prins in Grün et al., 1974
Manivitella pemmatoidea (Deflandre in Manivit, 1965) Thierstein,
1971
Miravetesina favula Grün in Grün and Allemann, 1975
Nannoconus colomii (de Lapparent 1931) Kamptner 1938
Nannoconus compressus Bralower and Thierstein in Bralower et al.,
1989
Nannoconus erbae Casellato 2010
Nannoconus globulus subsp. globulus Brönnimann, 1955
Nannoconus globulus subsp. minor (Brönnimann, 1955) Bralower in
Bralower et al., 1989
Nannoconus infans Bralower in Bralower et al., 1989
Nannoconus kamptneri subsp. kamptneri Brönnimann, 1955
Nannoconus kamptneri subsp. minor (Brönnimann, 1955) Bralower
in Bralower et al., 1989
Nannoconus puer Casellato 2010
Nannoconus steinmannii subsp. minor (Kamptner, 1931) Deres and
Achériéguy, 1980
Nannoconus steinmanni subsp. steinmannii Kamptner, 1931
Nannoconus wintereri Bralower and Thierstein, in Bralower et al. 1989
Parhabdolithus marthae Deflandre in Deflandre and Fert, 1954
182
SVOBODOVÁ, ŠVÁBENICKÁ, REHÁKOVÁ, SVOBODOVÁ, SKUPIEN, ELBRA and SCHNABL
GEOLOGICA CARPATHICA
, 2019, 70, 2, 153–182
Pickelhaube furtiva (Roth, 1983) Applegate et al. in Covington and
Wise, 1987
Polycostella beckmannii Thierstein, 1971
Polycostella senaria Thierstein, 1971
Retecapsa octofenestrata (Bralower in Bralower et al., 1989) Bown
in Bown and Cooper, 1998
Retecapsa schizobrachiata (Gartner, 1968) Grün in Grün and
Allemann, 1975
Retecapsa surirella (Deflandre and Fert, 1954) Grün in Grün and
Allemann, 1975
Rotelapillus crenulatus (Stover, 1966) Perch-Nielsen, 1984
Speetonia colligata Black, 1971
Umbria granulosa Bralower and Thierstein in Bralower et al., 1989
Watznaueria barnesiae (Black in Black & Barnes, 1959) Perch-
Nielsen, 1968
Watznaueria biporta Bukry, 1969
Watznaueria britannica (Stradner, 1963) Reinhardt, 1964
Watznaueria communis Reinhardt, 1964
Watznaueria cynthae Worsley, 1971
Watznaueria fossacincta (Black, 1971) Bown in Bown and Cooper,
1989
Watznaueria manivitiae Bukry, 1973
Watznaueria ovata Bukry, 1969
Zeugrhabdotus cooperi Bown, 1992
Zeugrhabdotus embergeri (Noël, 1959) Perch-Nielsen, 1984
Zeugrhabdotus fluxus Casellato, 2010
Calcareous dinoflagellates
Cadosina semiradiata cieszynica (Nowak, 1966)
Cadosina semiradiata fusca (Wanner, 1940)
Cadosina semiradiata semiradiata (Wanner, 1940)
Carpistomiosphaera borzai (Nagy,1966)
Carpistomiosphaera tithonica Nowak,1968
Colomisphaera carpathica (Borza, 1964)
Colomisphaera cieszynica Nowak, 1968
Colomisphaera fibrata (Nagy, 1966)
Colomisphaera fortis Řehánek, 1982
Colomisphaera lapidosa (Vogler, 1941)
Colomisphaera minutissima sensu Nowak 1968
Colomisphaera pieniniensis (Borza, 1969)
Colomisphaera radiata (Vogler, 1941)
Colomisphaera tenuis (Nagy, 1966)
Committosphaera czestochowiensis Řehánek, 1993
Committosphaera ornata (Nowak, 1968)
Committosphaera pulla (Borza, 1964)
Committospahera sublapidosa (Vogler 1941)
Parastomiosphaera malmica (Borza, 1964)
Stomiosphaera moluccana Wanner, 1940
Stomiosphaerina proxima Řehánek,1987
Calpionellids
Calpionella alpina Lorenz,1902
Calpionella elliptalpina Nagy, 1986
Calpionella elliptica Cadisch 1932
Calpionella grandalpina Nagy, 1986
Crassicollaria brevis Remane, 1962
Crassicollaria intermedia (Durand-Delga, 1957)
Crassicollaria massutiniana (Colom, 1948)
Crassicollaria parvula Remane, 1962
Lorenziella hungarica Knauer and Nagy, 1964
Praetintinnopsella andrusovi Borza, 1969
Remaniella borzai Pop, 1996
Remaniella catalanoi Pop, 1996
Remaniella colomi Pop, 1996
Remaniella duranddelgai Pop,1996
Remaniella ferasini (Catalano, 1965)
Tintinnopsella carpathica (Murgeanu and Filipescu,1933)
Tintinnopsella doliphormis (Colom, 1939)
Tintinnopsella remanei Borza, 1969
Palynomorphs including non-calcareous dinoflagellates
Achomosphaera neptuni (Eisenack, 1958) Davey and Williams, 1966
Amphorula dodekovae Zotto et al., 1987
Amphorula metaelliptica Dodekova, 1969
Chytroeisphaeridia chytroeides (Sarjeant 1962) Downie and Sarjeant
1965, emend. Davey 1970
Cerebropollenites macroverrucosus (Thiergart) Schulz 1967
Circulodinium distinctum (Deflandre and Cookson 1955) Jansonius
1986
Circulodinium vermiculatum Stover and Helby, 1987
Classopollis torosus (Reissinger) Balme, 1957
Cometodinium habibii Monteil, 1991
Cribroperidinium globatum (Gitmez and Sarjeant, 1972) Helenes,
1984
Cribroperidinium sarjeantii (Vozzhennikova, 1967) Helenes, 1984
Ctenidodinium ornatum (Eisenack 1935) Deflandre 1938
Cyathidites minor Couper 1953
Cyclonephelium hystrix (Eisenack, 1958) Davey, 1978
Dapsilidinium multispinosum (Davey, 1974) Bujak et al., 1980
Densoisporites velatus Weyland and Krieger 1953
Dichadogonyaulax bensonii Monteil, 1992
Dingodinium tuberosum (Gitmez 1970) Fisher and Riley 1980
Dissiliodinium giganteum Feist-Burkhardt, 1990
Endoscrinium campanula (Gocht, 1959) Vozzhennikova, 1967
Endoscrinium pharo Duxbury 1977
Gleicheniidites senonicus Ross 1949
Glossodinium dimorphum Ioannides et al., 1977
Gochteodinia virgula Davey 1982b
Gonyaulacysta helicoidea (Eisenack and Cookson 1960)
Hystrichodinium pulchrum Deflandre, 1935
Kiokansium polypes (Cookson and Eisenack, 1962) Below, 1982
Micrhystridium stellatum Deflandre 1945
Neoraistrickia truncata (Cookson) Potonié 1956
Neuffenia willei
Brenner and Dürr, 1986
Oligosphaeridium asterigerum (Gocht, 1959) Davey and Williams,
1969
Oligosphaeridium patulum Riding and Thomas 1988
Oligosphaeridium pulcherrimum (Deflandre and Cookson, 1955)
Davey and Williams, 1966
Pareodinia halosa (Filatoff, 1975) Prauss, 1989
Pareodinia robusta Wiggins, 1975
Prolixosphaeridium anasillum Erkmen and Sarjeant 1980
Prolixosphaeridium granulosum (Deflandre, 1937) Davey et al.,
1966
Prolixosphaeridium deirense Davey et al., 1966
Prolixosphaeridium mixtispinosum (Klement, 1960) Davey et al.,
1969
Prolixosphaeridium sp. A Monteil, 1993
Pterospermella australiensis (Deflandre and Cookson 1955)
Eisenack 1972
Pterospermella helios Sarjeant 1959
Spheripollenites subgranulatus Couper 1958
Stiphrosphaeridium dictyophorum (Cookson and Eisenack, 1958)
Lentin and Williams, 1985
Systematophora areolata Klement 1960
Systematophora daveyi Riding and Thomas, 1988
Systematophora orbifera Klement, 1960
Systematophora silybum Davey, 1979
Tanyosphaeridium isocalamum (Deflandre and Cookson 1955)
Davey and Williams 1969
Tehamadinium evittii (Dodekova, 1969) Jan du Chêne et al., 1986
Veryhachium irregulare de Jekhowsky 1961