GeolCarp_Vol63_No3_201

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, JUNE 2012, 63, 3, 201—217 doi: 10.2478/v10096-012-0018-2

Introduction

In the territory of the Czech Republic, both Upper Cretaceous
marine  epicontinental  sediments  of  the  West  European
Platform  (Bohemian  Cretaceous  Basin)  and  deformed  sedi-
ments  of  the  Tethyan  foreland  basins  (Outer  Western
Carpathians) occur (Fig. 1A). In this setting Tethyan and Boreal
influences can be observed in closely spaced sections. A sea-
way  between  these  two  areas  existed  during  the  latest
Cenomanian—Coniacian  at  the  present  Blansko  trough
(Uličný et al. 2009). In some cases, nannofossil stratigraphy
has allowed higher resolution than macrofauna or foramini-
fers  especially  in  the  Western  Carpathians  (Stráník  et  al.
1996). The results of biostratigraphic and paleoenvironmental
nannofossil  research  were  published  in  partial  works  in
English and Czech with English abstracts or they are mentioned
in unpublished manuscripts.

The aim of this work is to give an overview of the biostrati-

graphic evaluation and mutual correlations of the Cenoma-
nian-Coniacian sediments in the Bohemian Cretaceous Basin
and in the individual units of the Outer Western Carpathians
according to calcareous nannofossil biostratigraphy.

Nannofossil record across the Cenomanian—Coniacian

interval in the Bohemian Cretaceous Basin and Tethyan

foreland basins (Outer Western Carpathians), Czech Republic

LILIAN ŠVÁBENICKÁ

Czech Geological Survey, Klárov 131/3, 118 21 Praha, Czech Republic; lilian.svabenicka@geology.cz

(Manuscript received September 13, 2011; accepted in revised form March 13, 2012)

Abstract: Nannofossil biostratigraphy and mutual correlation was worked out for the Cenomanian-Coniacian deposits of
the Bohemian Cretaceous Basin (BCB) and Outer Western Carpathians (OWC) in the territory of the Czech Republic.
Similar assemblages of the BCB and from sediments deposited on the SE slopes of West European Platform, Waschberg-
Ždánice-Subsilesian Unit, OWC support the hypothesis that the two areas were connected by a sea way (nowadays the
Blansko trough). The nannoflora of the Silesian Unit, OWC show more afinity to high latitudes as is documented by the
presence of Marthasterites furcatus in the Lower Turonian, UC6b and UC7 Zones. Turonian and Coniacian deep-water
flysch sediments of the Silesian Unit and Magura Group of Nappes provide nannofossils on rare occassions. Strongly
atched nannofossils dominated by W. barnesiae from Cenomanian black shales of the BCB are comparable to those of the
Silesian Unit and reflect a similar shallow nearshore sea. In the BCB, uppermost Cenomanian is marked by the last
occurrence (LO) of Axopodorhabdus albianus and first occurrence (FO) of Quadrum intermedium (6 and 7 elements) and
lowermost Turonian by a sudden quantitative rise in nannoflora and by the FO Eprolithus octopetalus. First Eiffellithus
eximius and thus the base of the UC8 Zone was recorded in the upper part of ammonite Zone Collignoniceras woollgari in
the lower Middle Turonian. Lithastrinus grillii is the stratigraphically youngest nannofossil species in this region and
indicates the uppermost Coniacian. In the OWC, the Albian-Cenomanian boundary was recorded in the Silesian Unit and
is marked by the LO Crucicribrum anglicum and FO Prediscosphaera cretacea and Corollithion kennedyi in the upper-
most Albian. The Turonian-Coniacian boundary found both in the BCB and Waschberg-Ždánice-Subsilesian Unit, OWC
is indicated by the FO Broinsonia parca expansa and by the base of the interval with common Marthasterites furcatus. In both
areas, events were found closely below the FO inoceramid species Cremnoceramus waltersdorfensis. The Coniacian-Santonian
boundary interval (Waschberg-Ždánice-Subsilesian and Foremagura Units, OWC) is indicated by Lithastrinus grillii occa-
sionally accompanied by Lucianorhabdus ex gr. cayeuxii, Hexalithus sp. and Arkhangelskiella specillata.

Key words: Cenomanian-Coniacian, Outer Western Carpathians, Bohemian Cretaceous Basin, correlations,
biostratigraphy, calcareous nannofossils.

Previous studies

Bohemian Cretaceous Basin

The Upper Cenomanian marine ingression and Cenoma-

nian-Turonian  boundary  interval  and  their  correlations  with
nannofossils,  foraminifers  and  macrofauna  (inoceramids)
were studied by Hradecká & Švábenická (1995) and Čech et
al.  (2005).  Correlation  of  macrofauna  and  nannofossils  was
worked  out  for  the  Turonian  and  Coniacian  deposits  by
Čech  et  al.  (1987),  Čech  &  Švábenická  (1992)  and  Lees
(1998). Attention was paid to the interval with common oc-
currence of Braarudosphaera bigelowii and to a short range
of  Liliasterites  angularis  and  their  correlation  with  global
events  (Švábenická  1999).  Stratigraphic  subdivision  of  the
Upper  Turonian  sediments  was  suggested  by  Valečka  &
Švábenická (2009) and Švábenická (2009a) and for the Tu-
ronian-Coniacian  boundary  interval  by  Švábenická  (2010)
and  Švábenická  &  Valečka  (2011).  Micro-  and  nannofossil
content  was  analysed  in  the  “rocky  coast  facies  (zone)”  of
the  south  margin  of  the  basin  (Bubík  &  Švábenická  2001;
Hradecká & Švábenická 2007).

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Outer Western Carpathians

In the Outer Group of Nappes, the biostratigraphic evalua-

tion of the Turonian—Coniacian interval was worked out for
the  Waschberg-Ždánice-Subsilesian  Unit  according  to  a
study  of  macrofauna,  foraminifers  and  nannofossils
(Švábenická 1992; Stráník et al. 1996; Stráník & Švábenická
2000).  The  Upper  Cretaceous  sediments  of  the  Zdounky
Unit were biostratigraphically evaluated by foraminiferal mi-
crofauna  and  nannofossils  (Bubík  et  al.  1995).  Microfossils
and palynomorphs were studied in anoxic dark pelites of Al-
bian and Cenomanian age (Svobodová et al. 2004) and with-
in  the  transition  interval  from  dark  anoxic  to  red  oxic  beds
(Švábenická  2006;  Skupien  et  al.  2009).  In  the  Magura
Group  of  Nappes,  Rača  Unit,  nannofossils  were  mentioned
from  “black  shales”  of  the  Cenomanian  age  (Bubík  et  al.
1993)  and  from  matrix  of  breccias  deposited  by  repeated

gravity flows in a continental rise within the Coniacian—San-
tonian interval (Švábenická et al. 1997). Comparison of the
nannofossil record of the Bohemian Cretaceous Basin and
Outer Western Carpathians with adjacent areas of Central
Europe was published by Švábenická et al. (2002).

For stratigraphic evaluation of Upper Cretaceous sedi-

ments  the  following  standard  nannofossil  zones  were  used:
CC zones were used by Sissingh (1977) emended by Perch-
Nielsen (1985), and UC zones by Burnett (1998). For the last
two decades, the focus of attention has been the nannofossil
record  on  stage  boundaries.  The  Albian—Cenomanian  inter-
val was studied by Gale et al. (1996, 2011) and Kennedy &
Gale (2006), the Cenomanian-Turonian boundary by Lamolda
et al. (1994, 1997), Paul et al. (1999) and Luciani & Cobianchi
(1999),  the  Turonian—Coniacian  by  Lees  (2008)  and
Kedzierski  (2008)  and  the  Coniacian—Santonian  by  Melinte
& Lamolda (2007) and Howe et al. (2007).

Fig. 1. A – Simplified geological map of the Bohemian Cretaceous Basin and Outer Western Carpathians in the territory of the Czech Repub-
lic. B – Simplified geological map of the Bohemian Cretaceous Basin and localities mentioned in the text. After Čech (1989), modified. Bore-
holes: BJ-21 Kouty, DB-1 Dolní Bousov, HP-20 Nymburk, KN-5 Sobčice, L7J Rokytnice, Muž-1 Mužský, Ro-16 Bystřice, SK-15 Benátky
near Hořice, Vf-1 Volfartice, V-800 Střeleč.

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Material

Sediments from the Bohemian Cretaceous Basin were ob-

tained both from outcrops and boreholes. The biostratigraphic
evaluation of the majority of boreholes is mentioned in the
unpublished manuscripts stored in the Archive of the Czech
Geological Survey.

The autochthonous Upper Cretaceous deposited on SE

margin of the West European Platform was studied from
boreholes drilled by Oil and Gas Company Hodonín in the
1960s and 1970s.

Sediments from the Outer Western Carpathian region were

sampled mainly from isolated localities during geological re-
search and mapping. Because of the soft flysch usually cov-
ered by Quaternary deposits and landslides, the best outcrops
were  available  mainly  in  riverbeds  after  heavy  rains  and
floods or in the grooves of newly built roads. Unfortunately,
the majority of these outcrops were quickly covered again by
mud  and  vegetation.  No  boreholes  were  drilled  in  recent
years. The last one (Pavlov-5 borehole, Ždánice-Subsilesian
Unit)  was  drilled  in  1989.  Considering  the  fact  that  nanno-
fossils  were  investigated  from  isolated  chip  sampling,  they
provided important data about the relative age of strata and
development of depositional areas in the Carpathian region.

Smear-slides are stored in the Department of Collections

of the Czech Geological Survey, Prague.

Methods

Nannofossils were investigated in the fraction of 2—30 µm

separated by decantation method using 7% solution of H

The heavy-fraction was allowed to settle for 3 minutes in a
45 mm  water  column  and  removed,  the  fine-fraction  was
saved for slide preparation after 45 minutes. Simple smear-
slides  were  mounted  by  Canada  Balsam  and  inspected  at
1000   magnification,  using  oil-immersion  objective  on  a
Nikon  Microphot-FXA  transmitting  light  microscope.  Bio-
stratigraphic data were interpreted applying Sissingh (1977)
CC zones and Burnett (1998) UC zones. Nannofossil mark-
ers within the NC10 Zone were used from Bown (in Gale et
al.  2011).  Semiquantitative  analyses  were  done  according
the method of Burnett & Whitham (1999). Lithostratigraphic
units of the Bohemian Cretaceous Basin are mentioned after
Čech et al. (1980), of Outer Western Carpathians after Picha
et al. (2006).

The nannofossil record and its biostratigraphic

evaluation

Bohemian Cretaceous Basin

Upper Cenomanian sediments are represented mostly by

dark grey siltstones and claystones with admixture of organ-
ic  matter  and  belong  to  the  Peruc-Korycany  Formation,
Pecínov  Member  (Fig. 2).  Marine  ingression  is  marked  by
poor  nannofossils.  Their  preservation  is  not  particularly
good  and  high  percentage  of  Watznaueria  barnesiae  gives

evidence for a higher degree of dissolution of nannoflora
(Švábenická 2004; Čech et al. 2005).

The oldest deposits with nannofossil content were found in

the Nymburk HP-20 borehole (117.0 m) and included Corol-
lithion  kennedyi,  Lithraphidites  acutus  and  Axopodorhabdus
albianus  (Čech  et  al.  2005),  Fig. 1B.  A  similar  association
with  C. kennedyi and L. acutus was recorded in the Bystřice
Ro-16 borehole (527.0 m) and in the Benátky SK-15 borehole
(279.0 m) near Hořice (Fig. 3—1,3,5,6). In the overlying strata,
the gradual last occurrences (LO in the text) of C. kennedyi, L.
acutus  observed in Sobčice KN-5 borehole (168.0 m, Švábe-
nická 2004),  Cretarhabdus  striatus and  A.  albianus  (Čech  et
al.  2005)  are  stratigraphically  important.  The  species  W.
barnesiae  quantitatively prevails and species  Broinsonia  sig-
nata and Prediscosphaera columnata are relatively common.
The broadly elliptical specimens of Manivitella pemmatoidea
(8—13 µm in long axis) are typical features of the assemblages.
In  the  uppermost  part  of  the  Cenomanian,  scarce  Quadrum
intermedium  (6—7  elements)  appears.  The  uppermost  part  of
the  Cenomanian  and/or  the  Cenomanian-Turonian  boundary
sediments of the Bystřice Ro-16 borehole (519.3 m) and Dolní
Bousov  DB-1  borehole  (418.7—418.5 m)  provided  an  assem-

Fig. 2. Bohemian Cretaceous Basin, lithostratigraphic units after
Čech et al. (1980, 2005). Age (Ma) after Ogg et al. (2004).

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blage with the first Cribrosphaerella ehrenbergii and last
Helenea chiastia (Švábenická 2004).

Special attention was paid to the “rocky coast facies” of

the  rocky-shore  zone  exposed  in  south  margin  of  basin,
where  the  Upper  Cretaceous  transgression  spread  over  the
crystalline rocks of the Bohemian Massif. At the locality of
Kaňk  near  Kutná  Hora,  matrix  of  basal  conglomerates  pro-
vided  poor  nannofossils  with  Prediscosphaera  cretacea,
Lithraphidites  cf.  acutus  and  relatively  high  numbers  of
specimens  of  the  genus  Broinsonia.  According  to  the  pres-
ence of the foraminifer species Pseudotextulariella cretacea
in  matrix,  conglomerates  are  correlated  with  the  Cenoma-
nian-Turonian interval (Hradecká & Švábenická 2007). The
overlying claystones contained Lower Turonian nannofossils
with  Eprolithus  moratus.  The  next  studies  of  this  facies  in
the  surroundings  of  Kolín  (Švábenická  2004)  and  Kladno
(locality  Vrapice – Bubík  &  Švábenická  2001)  showed  a
similarly  poor  nannofossil  content.  Absence  of  A.  albianus
and  rare  occurrences  of  C.  ehrenbergii,  H.  chiastia  and
Ahmuellerella  octoradiata  indicated  the  Cenomanian-Turo-
nian  boundary  interval.  The  lowermost  Turonian  is  marked
by  the  first  occurrence  (FO)  of  Eprolithus  octopetalus
(Fig. 3.9) and by the input of high numbers of medium-well
preserved nannofossils.

The Early Turonian transgression is reflected not only by a

change  in  lithology  (to  grey  claystones  of  the  Bílá  Hora
Formation – see Fig. 2), but also by a sudden quantitative rise
in nannoflora and its high species diversity. This phenomenon
was  mentioned  by  Čech  et  al.  (2005)  and  also  observed  in
Kouty  BJ-21  borehole  (174.5—178.5)  within  the  interval  of
macrofossil  Zone  Watinoceras  devonense.  The  great  number
of  medium-well  preserved  nannofossils  (> > 50  specimens / 1
field of view of the microscope) included rare specimens of E.
octopetalus, C. ehrenbergii and Q. intermedium (6 elements).

Fig. 3. Calcareous nannofossils of the Cenomanian—Coniacian interval, Czech Republic. BCB – Bohemian Cretaceous Basin, OWC – Outer
Western Carpathians. Photographs in cross-polarized light, PPL – plane-polarized light. For magnification see fig. 1. 1 – Corrolithion
kennedyi, Upper Cenomanian, BCB, Nymburk HP-20 borehole, 117.0 m, Upper Cenomanian. 2 – Corollithion exiguum, BCB, Kněžmost-
Podolí CV120, Upper Turonian. 3 – Lithraphidites acutus, Upper Cenomanian, BCB, Běchary Bch-1 borehole, 402.8 m, Upper Turonian.
4 – Lithraphidites carniolensis, BCB, Rokytnice L7-J borehole, 406—407 m, Middle Turonian. 5, 6 – Axopodorhabdus albianus, 5 – BCB,
Běchary Bch-1 borehole, 402.8 m, 6 – OWC, Štramberk Quarry Š0/VIII, Lower Cenomanian, etched specimen. 7 – Helenea chiastia,
OWC, Štramberk Quarry Š49C/VIII, Lower—Middle Cenomanian. 8 – Eprolithus floralis, BCB, Kněžmost-Všeň CV24b, Upper Turonian.
9 – Eprolithus octopetalus, BCB, Běchary Bch-1 borehole, 401.2 m, Lower Turonian. 10 – Eprolithus moratus, BCB, Rokytnice L7-J
borehole, 406—407 m, Middle Turonian. 11 – Lithastrinus septenarius, BCB, Kněžmost-Podolí CV120, Upper Turonian. 12 – Lithastri-
nus grillii, BCB, Lužice 189/2000, Upper Coniacian. 13 – Gartnerago theta, BCB, Běchary Bch-1 borehole, 401.8 m, Upper Cenomanian.
14 – Gartnerago obliquum, BCB, Kněžmost-Podolí CV120, Upper Turonian. 15 – Tegumentum stradneri, BCB, Rokytnice L7-J bore-
hole, 76—77 m, Upper Turonian. 16 – Chiastozygus litterarius, BCB, Zbožíčko MP-7 borehole, 78 m, Lower Turonian. 17 – Ahmuellerel-
la octoradiata  Reinhardt,  BCB,  Střeleč  V-800  borehole  19.9 m,  Lower  Coniacian. 18  –  Cribrosphaerella ehrenbergii,  BCB,  Zbožíčko
MP-7 borehole, 61 m, Lower Turonian. 19 – Bukrylithus ambiguus, BCB, Kněžmost CV24b, Upper Turonian. 20 – Prediscosphaera co-
lumnata,  BCB,  Nymburk  HP-20  borehole,  117.0 m,  Upper  Cenomanian.  21  –  Prediscosphaera  ponticula,  OWC,  Foremagura  Unit,
Chomýž 252, Coniacian-Santonian boundary interval. 22 – Prediscosphaera spinosa, BCB, Střeleč V-800 borehole, 141.5 m, Upper Turo-
nian. 23 – Prediscosphaera cretacea, Střeleč V-800 borehole, 141.5 m, Upper Turonian. 24 – Prediscosphaera cf. grandis and Eproli-
thus floralis, BCB, Kněžmost-Podolí, CV120, Upper Turonian. 25 – Broinsonia signata, BCB, Nymburk HP-20 borehole, 117.0 m, Upper
Cenomanian.  26  –  Broinsonia  enormis,  BCB,  Kněžmost  CV30,  Upper  Turonian.  27,  28  –  Broinsonia  parca  expansa,  BCB,  Kněžmost
CV01, Upper Turonian. 29, 30 – ?Rhagodiscus plebeius, BCB, Rokytnice L7-J 406—407 m, Lower Turonian; 29 – PPL. 31 – Rhagodiscus
angustus, BCB, Kněžmost-Podolí CV120, Upper Turonian. 32 – Rhagodiscus asper, BCB, Kněžmost CV24b, Upper Turonian. 33 – Manivi-
tella pemmatoidea, Zbožíčko MP-7 borehole, 138.8—138.9 m, Lower Turonian. 34 – Grantarhabdus coronadventis, BCB, Kněžmost-Podolí
CV120, Upper Turonian. 35, 36 – Kamptnerius magnificus, BCB; 35 – Střeleč V-800 borehole, 55.3 m, Turonian-Coniacian boundary inter-
val; 36 – Mužský Muž-1 borehole, 9.2 m, Lower Coniacian.

The succession of the first occurrence of marker species

during  the  Turonian  stage  is  following  (Fig. 4):  Eprolithus
octopetalus,  E.  moratus,  Lucianorhabdus  sp.,  Octolithus
multiplus,  Lucianorhabdus  maleformis,  Quadrum  gartneri
(scarce), Eiffellithus eximius, Kamptnerius magnificus, Heli-
colithus turonicus, Ottavianus giannus (recorded only in the
Upper Turonian), Lithastrinus septenarius,  Liliasterites an-
gularis  (Fig. 5.13),  Marthasterites  furcatus  (rare  and  not
continual,  Fig. 5.14),  Zeugrhabdothus  biperforatus,  Quad-
rum-Micula  (Fig. 6.22,23),  Broinsonia  parca  expansa,  M.
furcatus (common and continual, acme) (Čech & Švábenická
1992;  Švábenická  1999,  2010  and  Švábenická  in  print  a;
Čech et al. 2010; Valečka & Švábenická in print). Placoliths
of  Helenea  chiastia  were  found  occasionally  only  in  basal
Turonian sediments (Bubík  & Švábenická 2001; Čech et al.
2005).

The Coniacian stage is marked with the top of the interval

with common M. furcatus (Švábenická & Valečka 2011) fol-
lowed  by  the  FO  of  Micula  adumbrata  (see  Fig. 6.25,26,
Švábenická  in  print  b),  Micula  staurophora  (Čech  et  al.
1987;  Čech  &  Švábenická  1992;  Lees  2008)  and  Lithastri-
nus grillii (Bubík et al. 2001). The species H. turonicus and
O.  giannus  are  already  absent.  The  stratigraphically  young-
est  nannofossils  were  found  in  the  western  part  of  basin  at
the locality of Lužice near Ústí nad Labem, the classical pa-
leontological  locality  of  Luschitz  described  by  Reuss  in
1844.  The  medium-well  preserved  and  diversified  assem-
blages comprise L. grillii in association with M. staurophora
and M. furcatus and indicate the Upper Coniacian or possi-
bly the Coniacian-Santonian boundary (Bubík et al. 2001).

On very rare occasions, reworked specimens from older

Albian-Cenomanian (Owenia sp., Crucibiscutum hayi) and
Jurassic (genus Stephanollithion) strata are to be found in the
Turonian and Coniacian sediments.

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Autochthonous Upper Cretaceous sediments

deposited on the SE slopes of the West European

Platform

Sediments of the Glauconitic Sand Formation (Picha et al.

2006) contain rare and badly preserved long-ranging nanno-
fossils (Fig. 7). In poor assemblages, only the Turonian age

Fig. 4. Comparison of Cenomanian-Coniacian UC zones with data
from the Bohemian Cretaceous Basin. Nannoplankton UC zones by
Burnett (1998), selected macrofauna zones from Burnett (1998),
macrofauna events by Čech (2009 and personal communication),
* – Březno locality (Lees 2008), ** – foraminifers after Hradecká
(in Čech et al. 2005).

is documented by Quadrum gartneri (Stráník et al. 1996).
Sediments are not available in outcrops and data were ob-
tained only from wells.

Outer Western Carpathians

Waschberg-Ždánice-Subsilesian Unit

In the Waschberg sector (sensu Picha et al. 2006 – see

Fig. 7)  of  the  Pavlovské  vrchy  Hills  (Fig. 8),  Upper  Creta-
ceous  sediments  spread  over  the  Ernstbrunn  Limestone
(Tithonian  to  ?Hauterivian).  In  the  remnant  of  glauconitic
sandstones  and  marlstones  that  are  sandwiched  within  this
limestone, Bubík et al. (2011) documented Lower Cenoma-
nian  by  planktonic  foraminifers  assigned  to  the  Rotalipora
globotruncanoides  Zone.  However,  the  poor  nannofossils
with  dominant  speciments  Watznaueria  barnesiae,  rare
Manivitella pemmatoidea (fragments of the large broadly el-
liptical  specimens),  Seribiscutum  primitivum,  Eprolithus
floralis, Watznaueria biporta and Broinsonia signata did not

Fig. 5.  Calcareous  nannofossils  of  the  Cenomanian—Coniacian  in-
terval,  Czech  Republic.  BCB  –  Bohemian  Cretaceous  Basin,
OWC  –  Outer  Western  Carpathians.  Photographs  in  cross-polar-
ized light, PPL – plane-polarized light. For magnification see fig. 1.
1  –  Eiffellithus  turriseiffelii,  BCB,  Střeleč  V-800  borehole,  55.3  m,
Turonian-Coniacian boundary interval. 2 – Eiffellithus gorkae, BCB,
Rokytnice  L7-J  borehole,  406—407 m,  Middle  Turonian.  3  –  Eiffel-
lithus eximius, BCB, Střeleč V-800 borehole, 55.3 m, Turonian-Coni-
acian  boundary  interval.  4  –  Stoverius  achylosus,  BCB,  Hořátev
HO-19 borehole, 112.3 m, Upper Cenomanian. 5 – Cylindralithus
biarcus, BCB, Mužský Muž-1 borehole, 8.32 m, Lower Coniacian.
6  –  Tetrapodorhabdus  decorus,  BCB,  Rokytnice  L7-J  borehole,
56—57 m, Upper Turonian. 7, 8 – Helicolithus compactus, specimen
in  0°  and  15°,  BCB,  Rokytnice  L7-J  borehole,  413—414 m,  Middle
Turonian. 9 – Helicolithus trabeculatus, BCB, Rokytnice L7-J bore-
hole,  409—410 m,  Middle  Turonian.  10  –  Helicolithus  turonicus,
BCB, Střeleč V-800 borehole, 141.5 m, Upper Turonian. 11 – Rote-
lapillus crenulatus, BCB, Rokytnice L7-J borehole, 406—407 m, Mid-
dle Turonian, PPL. 12 – Amphizygus brooksii, BCB, Rokytnice L7-J
borehole, 56—57 m, Upper Turonian. 13 – Liliasterites angularis,
BCB,  Střeleč  V-800  borehole,  123.5 m,  Upper  Turonian,  PPL.
14 – Marthasterites furcatus, BCB, Kněžmost-Všeň CV024b, Upper
Turonian,  PPL.  15  –  Marthasterites  inconspicuus,  BCB,  Mužský
Muž-1  borehole,  6.9 m,  Lower  Coniacian,  PPL.  16  –  Tranolithus
minimus,  BCB,  Branžež  borehole,  82—84 m,  Upper  Turonian.
17 – Tranolithus gabalus, BCB, Branžež borehole, 82—84 m, Upper
Turonian. 18  – Tranolithus orionatus, BCB, Rokytnice L7-J bore-
hole, 413—414 m, Middle Turonian. 19 – Seribiscutum primitivum,
BCB, Střeleč V-800 borehole, 127.8 m, Upper Turonian. 20 – Cru-
cibiscutum  hayi,  BCB,  Střeleč  V-800  borehole,  129.5 m;  reworked
specimen from older Cenomanian strata. 21 – Biscutum ellipticum,
OWC,  Štramberk  Quarry  Š29/IV,  ?Middle—Upper  Cenomanian.
22  –  Biscutum  melaniae,  BCB,  Střeleč  V-800  borehole,  135.5 m,
Upper  Turonian.  23  –  Retacapsa  angustiforata,  BCB,  Branžež
borehole,  70—72 m. 24  –  Retacapsa ficula,  BCB,  Rokytnice  L7-J
borehole, 409—410 m, Middle Turonian. 25 – Retacapsa crenulata,
BCB, Kněžmost-Podolí CV120, Upper Turonian.  26, 27  – Solla-
sites horticus, BCB, Zbožíčko MP-7 borehole, 41 m, Lower Turonian.
26 – PPL. 28 – Placozygus fibuliformis, BCB, Kněžmost CV24b,

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include any Cenomanian sensu stricto marker species. How-
ever,  breccia  filling  the  clastic  dykes  in  limestones  in  the
same  area  provided  poor  nannofossils  of  the  Turonian  age.
Grey clayey-micritic matrix contained Gartnerago obliquum
and  problematic  specimens  of  Eprolithus  cf.  octopetalus,
and clayey glauconitic silt to sandstone provided Eiffellithus
eximius  and  Kamptnerius  magnificus  (Stráník  et  al.  2006;
Poul et al. 2010).

Fig. 6. ... Lower Coniacian. 8 – Cyclagelosphaera reinhardtii, BCB, Kněžmost CV24, Upper Turonian. 9 – Ottavianus giannus, BCB,
Střeleč V-800 borehole, 138.5 m, Upper Turonian. 10—12 – Octolithus multiplus, specimen in 0°, 15

and 45°, BCB, Rokytnice L7-J bore-

hole, 52.7 m, Upper Turonian. 13, 14 – Octolithus sp., specimen in 0° and 15°, BCB, Rokytnice L7-J borehole, 52.7 m, Upper Turonian.
15 – Owenia sp. (basal plate of genus Isocrystallithus), BCB, Rokytnice L7-J borehole, 406—407 m, reworked specimen from older Cenoma-
nian strata. 16 – Calculites ovalis (Stradner), BCB, Střeleč V-800 borehole, 141.5 m, Upper Turonian. 17 – Lucianorhabdus cf. maleformis,
BCB, Rokytnice L7-J borehole, 406—407 m, Middle Turonian. 18 – Lucianorhabdus sp., BCB, Střeleč V-800 borehole, 141.5 m, Upper Turo-
nian. 19 – Lucianorhabdus maleformis, BCB, Rokytnice L7-J borehole, 409—410 m, Middle Turonian. 20 – Lucianorhabdus quadrificus,
BCB, Mužský Muž-1 borehole, 8.3 m, Lower Coniacian. 21 – Quadrum gartneri, BCB, Mužský Muž-1 borehole, 8.3 m, Lower Coniacian.
22, 23 – Quadrum-Micula, specimen in 0° and 30°, BCB, Mužský Muž-1 borehole, 4.9 m, Lower Coniacian. 24 – Lapideacassis sp. cf. L.
cornuta, BCB, Zbožíčko MP-7 borehole, 78 m, Lower Turonian. 25, 26 – Micula adumbrata, specimen in 0° and 30°, BCB, Kněžmost-
Mužský CE-051, Lower Coniacian. 27 – Micula staurophora, OWC, Foremagura Unit, Chomýž 252, Coniacian-Santonian boundary interval.
28, 29 – Quadrum-Uniplanarius, BCB, Mužský Muž-1 borehole, 4.9 m, Lower Coniacian; 28 – PPL. 30 – Nannoconus elongatus, BCB,
Rokytnice L7-J borehole, 409—410 m, Middle Turonian, PPL. 31 – Braarudosphaera bigelowii parvula, BCB, Kněžmost-Podolí CV120, Up-
per Turonian. 32 – Braarudosphaera bigelowii bigelowii, BCB, Střeleč V-800 borehole, 55.3 m, Turonian-Coniacian boundary interval.
33 – Thoracosphaera operculata, BCB, Rokytnice L7-J borehole, 56—57 m, Upper Turonian. 34 – Stephanolithion sp., BCB, Střeleč V-800
borehole, 129.5 m, reworked specimen from older Jurassic strata. 35 – “Cube” of questionable origin. BCB, Rokytnice L7-J borehole, 29.1 m,
Upper Turonian; occasionally, such cubes form a component of Turonian sediments in BCB.

Fig. 7. Outer Western Carpathians, Cenomanian—Coniacian interval. Lithostratigraphic units after Picha et al. (2006), modified. Waschberg-
Ždánice-Subsilesian Unit and Silesian units after Skupien et al. (2009). Age (Ma) after Ogg et al. (2004). 1 – tectonic detachment, 2 – trans-
gression, * – sediments barren of calcareous nannofossils.

In the overlying Turonian and Coniacian deposits,

Klement Formation, the nannofossil record shows similarity
to that from the Bohemian Cretaceous Basin (Švábenická in
Hamršmíd 1991; Švábenická 1992). The first M. furcatus
was recorded together with the foraminifer species Archaeo-
globigerina cretacea in the Upper Turonian and the first K.
magnificus below the interval with common M. furcatus
(Stráník et al. 1996), Fig. 9.

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Fig. 8. Simplified geological map of the Outer Western Carpathians and localities mentioned in the text. Autochthonous Cretaceous depos-
its on the SE slopes of the Bohemian Massif are covered by the Neogene of the Carpathian Foredeep. 1 – Bohemian Massif, 2 – Neogene
of the Carpathian Foredeep, 3 – Neogene of Vienna Basin, 4 – Waschberg-Ždánice-Subsilesian Unit and Pouzdřany Unit (unit without
Cretaceous rocks), 5 – Silesian Unit, 6 – Foremagura and Zdounky Units, 7 – Magura Group of Nappes, 8 – Jurassic-Lower Creta-
ceous Limestone, 9 – Pienniny Klippen Belt. After Picha et al. (2006), simplified. PV-5 Pavlov borehole.

The Upper Coniacian and Coniacian-Santonian boundary

interval, Pálava Formation is marked by the first Lithastrinus
grillii followed by Arkhangelskiella specillata and Luciano-
rhabdus ex gr. cayeuxii (Švábenická 1992).

In the Subsilesian sector, nannofossils have not been

found.  Nevertheless,  Hanzlíková  (1969)  mentioned  plank-
tonic  foraminifers  of  the  latest  Turonian  and  Coniacian  age
from the Frýdek Formation. These foraminifers were exami-
nated  from  wells  drilled  in  the  1960s.  Unfortunately,  this
rocky  material  was  not  available  for  nannofossil  study  and
outcrops did not provide any calcareous strata.

Zdounky Unit

In the studied interval, nannofossils with Micula stauro-

phora,  Lithastrinus  septenarius  and  relatively  common  M.
furcatus  proved  the  Coniacian  age,  UC10  Zone  (locality
Újezdsko 333), see Fig. 8. Cenomanian and Turonian nanno-
fossil  assemblages  have  not  been  found  yet.  Lithostrati-
graphically, the sediments go with the lower sequence of the
unit (sensu Picha et al. 2006 – see Fig. 7).

Silesian Unit

Black organic carbon-enriched sediments of the Cenoma-

nian age, the Baška Subunit (see Fig. 7), contain diminished

assemblages.  Nannofossil  tests  show  signs  of  strong  etching
and  dissolution  (Figs. 3—6).  The  oldest  assemblages  contain
Prediscosphaera  cretacea  and  Corollithion  kennedyi.  Next
come  the  first  occurrences  of  Gartnerago  theta  and
Lithraphidites  acutus.  The  assemblages  are  complemented
with  rare  specimens  of  Helenea  chiastia,  Axopodorhabdus
albianus  and  Manivitella  pemmatoidea  (Svobodová  et  al.
2004). Similar nannofossils with C. kennedyi and Cretarhabdus
striatus  were  found  at  the  locality  Dub  (sample  A35)  near
Hustopeče  nad  Bečvou,  Kelč  Subunit.  The  uppermost
Cenomanian  strata  with  Gartnerago  obliquum  and  Quadrum
intermedium (5 elements) were recorded in the same subunit
at  the  locality  of  Němetice  MB16F  near  Valašské  Meziříčí
(Skupien et al. 2009).

The Turonian and Coniacian deposits of the Kelč Subunit

provided  scarce  nannofossils  (see  Fig. 9).  The  species  M.
furcatus was found in association with Eprolithus moratus in
the  Lower  Turonian  at  the  locality  Choryně  (Skupien  et  al.
2009; Švábenická 2009b). In the overlying strata, the follow-
ing  nannofossil  markers  were  recognized:  Q.  gartneri
(Němetice  MB16A  and  Choryně  MB25F),  L.  septenarius
(Němetice MB16X2 and Starý Jičín 3A/96). Matrix from the
conglomerates  of  Starý  Jičín  provided  poor  nannofossils
with  M.  furcatus  and  M.  staurophora  of  the  Coniacian  age
(Stráník  et  al.  1997).  Relatively  common  specimens  of  M.
staurophora and  M.  furcatus accompanied  by  rare L.  grillii

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were found at the locality of Choryně (MB25B). Assemblages
with L. grillii and Arkhangelskiella cf. specillata may docu-
ment the Coniacian-Santonian boundary interval (Hranické
Loučky A43).

Foremagura Unit

The green and grey clayey deposits of the Submenilitic

Formation (Fig. 7) provided rich and medium-well preserved
nannofossils of the Late Coniacian age. This is documented
at the locality Chomýž 252 (north of Zlín) by the presence of
L. grillii and Hexalithus sp. The sediments of the locality
Mojena 32 provided assemblages with higher numbers of M.
staurophora and M. furcatus and few L. grillii and Predisco-
sphaera cf. grandis, that may be correlated with the Conia-
cian-Santonian boundary interval.

Magura Group of Nappes

Nannofossils were recorded only in the flysch lithofacies

zone of the Rača Unit, Rajnochovice Formation (“black
shales”, Gault flysch) (see Fig. 7). The Cenomanian is docu-
mented by C. kennedyi and H. chiastia at the locality of
Mikulůvka No. 1/6 (Švábenická et al. 1997) and by E. turriseif-
felii and L. acutus at the locality of Tesák (Bubík et al. 1993).

Red-brown non-calcareous clays of the Kaumberg Forma-

tion  deposited  below  CCD  in  the  abyssal  zone  span  the
Turonian—Coniacian interval. Naturally, these sediments are
barren  of  calcareous  nannofossils.  The  matrix  of  the  sedi-
mentary  breccias  of  the  Kurovice  Klippe  are  an  exception.
Variegated  clays  provided  poor  nannofossil  content  with
Micula staurophora and a few Marthasterites furcatus docu-
menting the Coniacian age (Švábenická et al. 1997).

In the Bílé Karpaty Unit, deposits of Kaumberg Formation

did not provide any calcareous nannofossils. The strata were
deposited in the abyssal zone below CCD and offer only ag-
glutinated foraminifers.

Nannofossil record across the stage boundary

intervals

The uppermost Albian and/or Albian-Cenomanian boundary

was  recognized  in  black  shales  of  the  Outer  Western  Car-
pathians, Silesian Unit, at the locality of the Štramberk-Kotouč
Quarry  (Švábenická  &  Hradecká  2005).  The  Upper  Albian  is
marked by the presence of Eiffellithus turriseiffelii and succes-
sive  events,  namely  the  LO  Crucicribrum  anglicum  and  FO
Corollithion kennedyi (UC1a). The first Prediscosphaera creta-
cea (oval specimens with cross-bars aligned between the major
axes) occasionally occurs with C. kennedyi. Signs of this inter-
val were also found in the surroundings of Hranice na Moravě,
localities Polouvsí A81, Dub MB3 and Petřkovice ZS27.

The Cenomanian-Turonian boundary interval was record-

ed  in  the  central  and  southern  part  of  the  Bohemian  Creta-
ceous Basin (Švábenická 2004; Čech et al. 2005). The Upper
Cenomanian  marine  strata  are  subdivided  into  two  distinct
parts according to the LO Axopodorhabdus albianus. Above
this  event,  the  chain  of  FO  Gartnerago  obliquum,  Ahmuel-

lerella  octoradiata  and  Quadrum  intermedium  (6  a  7  ele-
ments) is evident (Čech et al. 2005). The rocky coast facies
spanning  the  Cenomanian—Turonian  interval  provided  A.
octoradiata,  Helenea  chiastia  and  Cribrosphaerella  ehren-
bergii.  The  lowermost  Turonian  is  well  marked  by  the  FO
Eprolithus octopetalus.

The Turonian-Coniacian boundary interval was document-

ed both from the Bohemian Cretaceous Basin and Outer West-
ern Carpathians, Waschberg-Ždánice-Subsilesian Unit. In the
Bohemian Cretaceous Basin, the boundary was recognized in
the Ohře River region (western part of the basin) at the type
locality of the “Priesener Schichten” (Krejčí 1869) in Březno
(Čech & Švábenická 1992; Lees 2008) and in the central part
of the basin including the Střeleč V800 borehole (Švábenická
2010). The uppermost Turonian is marked by the FO Broinso-
nia parca expansa (BC9c Zone) and LO Helicolithus turonicus
(Fig. 10).  The  base  of  acme  Marthasterites  furcatus  (more
than 6 % in assemblage) was recorded closely below the FO
of inoceramid species Cremnoceramus waltersdorfensis. The
acme of M. furcatus probably spans the interval with Cremno-
ceramus deformis erectus, that is supposed to be a marker spe-
cies for the base of the Coniacian (Čech 2009), and continues
up to the Lower Coniacian without regard to change in litho-
logy  (Švábenická  2010).  The  top  of  acme  M.  furcatus  was
found  below  the  first  occurrence  of  Micula  staurophora
(Švábenická  &  Valečka  2011).  In  the  Waschberg-Ždánice-
Subsilesian Unit, this boundary is accessible at the locality of
Turold (Švábenická in Hamršmíd 1991; Stráník & Švábenická
2000).  The  base  of  acme  M.  furcatus  in  association  with  B.
parca expansa/Thiersteinia ecclesiastica was recorded closely
below the sandstone bed of lumachelle of C. waltersdorfensis.

Indications of the Coniacian-Santonian boundary interval

were found in the Outer Western Carpathians in the Wasch-
berg-Ždánice-Subsilesian and Foremagura Units, but only in
individual samples. Nannofossil assemblages contain Lithas-
trinus  grillii  scarcely  accompanied  by  Arkhangelskiella
specillata,  Hexalithus  sp.  and  Lucianorhabdus  ex  gr.  cay-
euxii.  In  the  Bohemian  Cretaceous  Basin,  the  species  L.
grillii of the Lužice locality may indicate the uppermost Co-
niacian. In both areas, no continuous cross-section spanning
this boundary interval has been available for detailed study.

Discussion

Poor nannofossil preservation in black organic matter en-

riched  shales  of  the  Cenomanian  age  both  in  the  Bohemian
Cretaceous Basin and Outer Western Carpathians is caused by
carbonate  dissolution  and  etching  that  is  documented  by  the
dominance  of  Watznaueria  barnesiae  ( ± 40 %,  Čech  et  al.
2005) in assemblages (Roth & Krumbach 1986). This chemical
process  probably  occurred  during  sediment  burial  as  a  result
of liberation of organic acids during decomposition of organic
matter  enclosed  in  shallow  water  and  nearshore  sediments.
Poor  preservation  or  absence  of  nannofossils  in  some  flysch
deposits and red clays is probably caused by post mortem dis-
solution  of  nannofossil  tests  within  or  below  the  carbonate
compensation  depth  (CCD)  and  indicates  bathyal  or  abyssal
paleoenvironment (Švábenická & Bubík 1992).

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Fig. 10.  Correlation  between  nannofossils  and  other  important  events
across  the  Turonian-Coniacian  boundary  in  Střeleč  V-800  and  Mužský
Muž-1 boreholes, central part of the Bohemian Cretaceous Basin. Nanno-
fossil  UC  zones  by  Burnett  (1998),  first  occurrence  of  lamellibranch
Cremnoceramus  waltersdorfensis  and  interval  with  presupposed  occur-
rence of C. deformis erectus and thus also presupposed base of Coniacian
(*) by Čech (2009). Lithostratigraphic units by Čech et al. (1980). From
Švábenická (2011), modified.

According to Čech et al. (2005), the Cenomanian-Turonian

sequence of the Bohemian Cretaceous Basin is interrupted by
major  or  prominent  bounding  surfaces  associated  with  ero-
sional surface and stratigraphic condensation of the uppermost
Cenomanian strata. This hypothesis is also supported by nan-
nofossils. The interval between LO Axopodorhabdus albianus
and first Eprolithus octopetalus provides poor and poorly pre-
served  nannofossils  with  abundant  W.  barnesiae  (35—40 %)
and without any other markers. Rare specimens of  Quadrum
intermedium (6 and 7 elements) and Ahmuellerella octoradia-
ta  that  were  recorded  in  boreholes  Dolní  Bousov  DB-1  in
418.7—419.0 m and Bystřice Ro-16 in 519.3 m are exceptions
(Švábenická 2004).

The first Octolithus multiplus (Fig. 6—10 to 12) occurs dur-

ing the Early Turonian of the Bohemian Cretaceous Basin,
close to the FO Lucianorhabdus sp.

In the Bohemian Cretaceous Basin, the first occur-

rence of Eiffellithus eximius was repeatedly recorded in
the  upper  part  of  Collignoniceras  woollgari  Zone  or
pertinently in its overlying strata. The ammonite Colli-
gnoniceras  woollgari,  the  FO  of  which  is  regarded  as
the marker for the base of Middle Turonian, was found
in the Rokytnice L7J borehole in the interval of UC6b—
UC7 nannoplankton Zones, and so without E. eximius
(Švábenická  in  print  a).  Burnett  (1998)  mentioned  the
FO E. eximius and thus the base of the UC8 Zone in the
uppermost part of the Lower Turonian, and so close be-
low Collignoniceras woollgari Zone (sensu Hancock et
al. 1993). For this reason, the FO E. eximius cannot be
used as the marker for the uppermost Lower Turonian
or the base of the Middle Turonian in the basin.

The Zone Liliasterites angularis was defined by

Stradner  &  Steinmetz  (1985)  as  the  interval  from  the
first  occurrence  of  the  nominate  species  to  the  first
Marthasterites furcatus below the Turonian-Coniacian
boundary  in  the  Angola  Basin,  Atlantic  Ocean.  In  the
Bohemian  Cretaceous  Basin,  common  L.  angularis
was recorded before the first M. furcatus in the Middle
to Upper Turonian at the locality Kystra, SW Bohemia
(Ohře river region) in the uppermost part of the Jizera
Formation  immediately  below  the  “coprolite  bed”
(Švábenická in Hamršmíd 1991; Stradner et al. 2010).
The next discoveries of this species were sporadic,  in
low  numbers  and  already  associated  with  M.  furcatus
in  the  Upper  Turonian:  in  the  lowermost  part  of  the
Teplice Formation of the Úpohlavy Quarry, NW Bohe-
mia  (Švábenická  1999)  and  in  the  Střeleč  V-800  and
Rokytnice L7J boreholes (Švábenická 2010 and Švábe-
nická  in  print  a).  In  the  Outer  Western  Carpathians,
rare badly preserved specimens of L. angularis accom-
panied by higher numbers of M. furcatus were found in
the  Waschberg-Ždánice-Subsilesian  Unit,  Waschberg
sector,  Pavlov  Pv-5  borehole  (135.0—140.6 m).  This
species  has  no  significance  for  biostratigraphic  correla-
tions  because  of  its  only  occasional  occurrence.  If
present  in  association  with  M.  furcatus,  it  can  indicate
overlying  strata  of  a  regionally  important  horizon  of
“contact  glauconitic  bed”  in  the  Bohemian  Cretaceous
Basin (see Fig. 10).

The interval with common occurrence of M. furcatus

across the Turonian-Coniacian boundary interval may reflect
sea-level  changes  in  this  region.  It  may  correspond  to  the
acme  event  of  Braarudosphaera  and  Nannoconus  of  the
same age described by Wyton et al. (2007) from SE England
that  may  represent  a  response  to  shallowing  during  this
boundary interval.

In the Bohemian Cretaceous Basin, the Early Santonian age

was mentioned apart from other things in the Volfartice Vf-1
borehole by study of benthic foraminifers (Hercogová in Čech
et al. 1987). Nevertheless, sediments provided only poor nanno-
fossils with Micula staurophora, M. furcatus, Lithastrinus sep-
tenarius and Broinsonia parca expansa without any Upper
Coniacian or Santonian nannofossil markers. Nannofossil scar-
city may be explained here by flyschoid facies with sandy inter-
calations that is not favourable for their preservation.

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Watznaueria quadriradiata was rarely recorded in the Up-

per Turonian of the Střeleč V-800 borehole and in the Upper
Coniacian in association with Lithastrinus grillii at the local-
ity of Lužice (Bubík et al. 2001). Burnett (1998) mentioned
first W. quadriradiata from the Santonian.

Conclusions

– Nannofossil assemblages of the Bohemian Cretaceous

Basin  and  from  sediments  deposited  on  the  SE  side  of  the
North  European  Platform,  Waschberg-Ždánice-Subsilesian
Unit, show similar character and support the hypothesis that
the  two  areas  were  connected  by  a  sea  way  (the  present
Blansko trough);

– Some differences of regional character were recorded in

the nannoplankton assemblages. An example is the diachronic
occurrence of Marthasterites furcatus in the Lower Turonian,
UC6b Zone of the Outer Western Carpathians, Silesian Unit,
and in the Upper Turonian, UC9 Zone of the Bohemian
Cretaceous Basin and Outer Western Carpathians, Waschberg-
Ždánice-Subsilesian Unit;

– Nannofossils are absent in some stratigraphic intervals

of the Silesian and Foremagura Units and Magura Group of
Nappes because sediments (flysch and red beds) were depos-
ited within fluctuating CCD or below CCD in bathyal or
abyssal environments and calcareous nannofossils were dis-
solved after death;

– The Albian-Cenomanian boundary interval was found

in the Outer Western Carpathians, Silesian Unit. The upper-
most Albian is marked by the LO Crucicribrum anglicum
and FO Corollithion kennedyi;

– The Cenomanian nannofossils from the black shales of

the Bohemian Cretaceous Basin are comparable to those of the
Outer Western Carpathians, Silesian Unit. They are represent-
ed by diminished assemblages dominated by Watznaueria
barnesiae, higher number of Broinsonia specimens and frag-
ments of large broadly elliptical Manivitella pemmatoidea.
Nannofossils show signs of strong etching and dissolution and
document shallow nearshore waters;

– The Cenomanian-Turonian boundary, Bohemian Creta-

ceous Basin: the Upper Cenomanian is marked by a chain of
events – LO Corollithion kennedyi, LO Lithraphidites acutus,
LO Axopodorhabdus albianus (important event in the area)
and rare irregular occurrence of Quadrum intermedium (6 and
7 elements). The Lower Turonian is well identified by first
Eprolithus octopetalus. The poor nannofossil record after the
LO A. albianus is explained by interrupted sequence associated
with erosional surface and stratigraphic condensation;

– Turonian and Coniacian nannofossils are usually medi-

um-well preserved and highly diversified both in the Bohe-
mian Cretaceous Basin and Outer Western Carpathians,
Waschberg-Ždánice-Subsilesian Unit. In the Silesian and
Foremagura Units and Magura Group of Nappes, nannofos-
sils occur on rare occasions exclusively in calcareous inter-
calations within the flysch deposits.

– The first occurrence of Eiffellithus eximius (and base of

UC8 Zone) was recorded in the upper part of ammonite Zone

Collignoniceras woollgari, and so in the lower Middle Turo-
nian of the Bohemian Cretaceous Basin;

– The Turonian-Coniacian boundary was recorded both in

the Bohemian Cretaceous Basin and Outer Western Car-
pathians, Ždánice-Subsilesian Unit. The uppermost Turonian is
marked by the first Broinsonia parca expansa and by the base
of the interval with common Marthasterites furcatus. In both
areas, events were found closely below the first occurrence of
the inoceramid species Cremnoceramus waltersdorfensis;

– The Upper Coniacian was identified in the western part

of  the  Bohemian  Cretaceous  Basin  by  Lithastrinus  grillii.
This species is the youngest nannofossil marker found in this
area. In the Outer Western Carpathians, the Upper Coniacian
or  Coniacian-Santonian  boundary  interval  was  observed  in
the  Waschberg-Ždánice-Subsilesian  and  Foremagura  Units.
In  addition  to  L.  grillii,  the  species  Lucianorhabdus  ex  gr.
cayeuxii, Hexalithus sp. and  Arkhangelskiella specillata are
occasional constituents of assemblages.

Acknowledgment: The financial support of the Grant Agen-
cy  of  the  Czech  Republic  (Project  No. P210/10/0841  “Bio-
stratigraphic and paleoenvironmental nannofossil correlation
across  the  Late  Cretaceous  in  the  Bohemian  Massif  and
Western  Carpathians”)  is  gratefully  acknowledged.  The  au-
thor  thanks  Miroslav  Bubík,  Stanislav  Čech,  and  Zdeněk
Stráník,  Czech  Geological  Survey  for  fruitfull  discussions
regarding lithostratigraphic and biostratigraphic correlations,
Anna Trubačová, Czech Geological Survey for figure prepa-
ration.  Suggestions  and  comments  of  reviewers  Mihaela  C.
Melinte-Dobrinescu,  Institut  National  de  Geologie  si  Geo-
ecologie  Marina,  Bucuresti  and  Christian  Linnert,  Ruhr
University Bochum helped improve the manuscript.

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Ahmuellerella octoradiata Reinhardt
Amphizygus brooksii Bukry
Arkhangelskiella specillata Vekshina
Axopodorhabdus albianus (Black) Wind & Wise
Biscutum ellipticum (Górka) Grün
Biscutum melaniae (Górka) Burnett
Braarudosphaera bigelowii parvula Stradner
Braarudosphaera bigelowii bigelowii (Gran & Braarud)

Deflandre

Broinsonia enormis (Shumenko) Manivit
Broinsonia signata (Noël) Noël
Broinsonia parca expansa Wise & Watkins
Bukrylithus ambiguus Black
Calculites ovalis (Stradner) Prins & Sissingh
Chiastozygus litterarius (Górka) Manivit
Corollithion exiguum Stradner
Corollithion kennedyi Crux
Cretarhabdus striatus (Stradner) Black
Cribrosphaerella ehrenbergii (Arkhangelsky) Deflandre
Crucibiscutum hayi (Black) Jakubowski
Crucicribrum anglicum Black
Cyclagelosphaera margerelii Noël
Cyclagelosphaera reinhardtii (Perch-Nielsen) Romein
Cylindralithus biarcus Bukry
Eiffellithus eximius (Stover) Perch-Nielsen
Eiffellithus gorkae Reinhardt
Eiffellithus turriseiffelii (Deflandre) Reinhardt
Eprolithus floralis (Stradner) Stover
Eprolithus moratus (Stover) Burnett
Eprolithus octopetalus Varol
Gartnerago obliquum (Stradner) Noël
Gartnerago theta (Black) Jakubowski
Grantarhabdus coronadventis (Reinhardt) Grün
Haqius circumradiatus (Stover) Roth
Helenea chiastia Worsley
Helicolithus compactus (Bukry) Varol & Girgis
Helicolithus trabeculatus (Górka) Verbeek
Helicolithus turonicus Varol & Girgis
Hexalithus gardetae Bukry
Kamptnerius magnificus Deflandre
Lapideacassis cornuta (Forchheimer & Stradner) Wind & Wise
Liliasterites angularis Švábenická & Stradner
Lithastrinus septenarius Forchheimer
Lithastrinus grillii Stradner
Lithraphidites acutus Verbeek & Manivit
Lithraphidites carniolensis Deflandre
Lucianorhabdus cayeuxii Deflandre
Lucianorhabdus maleformis Reinhardt

Lucianorhabdus quadrificus Forchheimer
Manivitella pemmatoidea (Deflandre) Thierstein
Marthasterites furcatus (Deflandre) Deflandre
Marthasterites inconspicuus Deflandre
Micula adumbrata Burnett
Micula staurophora (Gardet) Stradner
Nannoconus elongatus Brönnimann
Octolithus multiplus (Perch-Nielsen) Romein
Ottavianus giannus Risatti
Placozygus fibuliformis (Reinhardt) Hoffmann
Prediscosphaera columnata (Stover) Perch-Nielsen
Prediscosphaera cretacea (Arkhangelsky) Gartner
Prediscosphaera cf. grandis Perch-Nielsen
Prediscosphaera ponticula (Bukry) Perch-Nielsen
Prediscosphaera spinosa (Bramlette & Martini) Gartner
Quadrum gartneri Prins & Perch-Nielsen
Quadrum intermedium Varol
Reinhardtites anthophorus (Deflandre) Perch-Nielsen
Retacapsa angustiforata Black
Retacapsa ficula (Stover) Burnett
Retacapsa crenulata (Bramlette & Martini) Grün
Rhagodiscus angustus (Stradner) Reinhardt
Rhagodiscus asper (Stradner) Reinhardt
Rhagodiscus plebeius Perch-Nielsen
Rotelapillus crenulatus (Stover) Perch-Nielsen
Seribiscutum primitivum (Thierstein) Filewicz et al.
Sollasites horticus (Stradner) Čepek & Hay
Stoverius achylosus (Stover) Perch-Nielsen
Tegumentum stradneri Thierstein
Tetrapodorhabdus decorus (Deflandre) Wind & Wise
Thiersteinia ecclesiastica Wise & Watkins
Thorascosphaera operculata Bramlette & Martini
Tranolithus gabalus Stover
Tranolithus minimus (Bukry) Perch-Nielsen, BCB,
Tranolithus orionatus (Reinhardt) Reinhardt
Watznaueria barnesiae (Black) Perch-Nielsen
Watznaueria biporta Bukry
Watznaueria britannica (Stradner) Reinhardt
Watznaueria ovata Bukry
Watznaueria quadriradiata Bukry
Zeugrhabdothus bicrescenticus (Stover) Burnett
Zeugrhabdothus biperforatus (Gartner) Burnett
Zeugrhabdothus diplogrammus (Deflandre) Burnett
Zeugrhabdothus embergeri (Noël) Perch-Nielsen
Zeugrhabdothus noeliae Rood et al.
Zeugrhabdothus sigmoides (Bramlette & Sullivan) Bown &

Young

Zeugrhabdothus trivectis Bergen

Appendix 1

List of calcareous nannofossils mentioned in the text, in alphabetical order of genera epithets.