GeolCarp_Vol63_No3_181

www.geologicacarpathica.sk

GEOLOGICA CARPATHICA

, JUNE 2012, 63, 3, 181—190 doi: 10.2478/v10096-012-0015-5

Introduction

The Tournaisian-Visean (T-V) boundary was intensively in-
vestigated  during  the  last  two  decades  because  of  growing
evidence that the former T-V stratotype at Bastion in Dinant
Synclinorium  in  Belgium  does  not  fulfill  the  conditions  re-
quired  for  GSSP  and  has  to  be  replaced  (Kalvoda  1983,
1990;  Devuyst  2006).  The  Working  Group  on  the  T-V
boundary  was  set  up  in  1995  by  the  Subcommission  on
Carboniferous  Stratigraphy  in  order  to  find  a  section  to
replace  the  inadequate  GSSP  of  the  base  of  the  Visean
(Bastion  section,  Namur-Dinant  Basin,  southern  Belgium)
and to establish the criterion (appearance of the foraminifer
Eoparastaffella simplex; Devuyst et al., 2003 and references
therein). The studies showed that the historical criterion for
the base of the Visean can be retained, as E. simplex is part
of  an  evolutionary  lineage  starting  in  the  latest  Tournaisian
(Hance  &  Muchez  1995;  Hance  1997;  Devuyst  2006).  The
Pengchong  section  of  Guangxi  (southern  China)  was  pro-
posed as the best candidate for a new stratotype for the base
of the Visean (Hance 1997; Devuyst et al. 2003). The highest
occurrence  of  the  conodont  Scaliognathus  anchoralis
europensis, at about 30 m below the boundary in the GSSP
at Pengchong.

The Mokrá Quarry exposes one of the best successions for

the  biostratigraphy  of  the  T-V  boundary  interval  and  even
though complicated by tectonics, and active quarrying, it can
serve  as  a  reference  section  for  Europe.  Abundant  and
diverse foraminifers and conodonts are accompanied here by
rich  trilobite  fauna  (Kalvoda  et  al.  2010).  The  goal  of  the
present  work  is,  therefore,  to  describe  the  distribution  of

New Mississippian trilobite association from the Brno vicinity

and its significance (Moravian Karst, Czech Republic)

ŠTĚPÁN RAK

, JIŘÍ KALVODA

and FRANCOIS-XAVIER DEVUYST

Charles University in Prague, Faculty of Science, Institute of Geology and Palaeontology, Albertov 6, CZ-128 43 Praha 2,

Czech Republic; deiphon@geologist.com

Masaryk University, Faculty of Science, Kotlářská 267/2, 611 37 Brno, Czech Republic; dino@sci.muni.cz

Carmeuse Lime & Stone, Technology Center, 3600 Neville Road, Pittsburgh PA15225, USA; devuyst@hotmail.com

(Manuscript received May 2, 2011; accepted in revised form March 13, 2012)

Abstract: Eleven trilobite species (Archegonus (Archegonus) aequalis philliboloides R. Hahn, 1967, Bollandia persephone
(Hahn & Hahn, 1970), Bollandia cf. megaira (Hahn & Hahn, 1970), Liobole (Panibole) cf. jugovensis (Osmólska, 1968),
Liobole (Sulcubole) glabroides (Richter & Richter, 1949), Semiproetus (Macrobole) drewerensis latipalpebratus (Osmólska,
1973), Proliobole vigilax (Chlupáč, 1961), Cyrtoproetus (Cyrtoproetus) cracoensis cracoensis (Reed, 1899), Carbonocoryphe
(Carbonocoryphe) bindemanni Richter & Richter, 1950, Tawstockia (Beleckella) milleri (Hahn & Hahn, 1971), Cummingella
(Cummingella) cf. auge Hahn & Hahn, 1968) are described for the first time from the shales of the Březina Formation in
Mokrá Quarry near Brno (Bohemian Massif, Moravian Karst). This typical trilobite association – comparable to that
previously described from the Erdbacher Kalken of Steeden in Hessen (Germany) – was found during excavation in the
Mokrá Quarry but they do not come from the exact Tournaisian-Visean boundary. Stratigraphical correlation and compari-
son of material is mentioned below, as is the history of the trilobite research from the Moravian Karst.

Key words: Carboniferous, Moravian Karst, paleontology, biostratigraphy, trilobites.

trilobites and to calibrate them precisely in terms of the fora-
miniferal and conodont zonation.

Research on Mississippian trilobites from the

Moravian Karst

There was no systematic study of Lower Carboniferous

trilobites from Moravia until the 1960. Just a few papers re-
porting  sporadic  fragments  of  trilobites  exist.  Chlupáč
(1956) found Carboniferous trilobites in greenish shales of the
Březina  Formation  (Mississippian)  during  his  statigraphical
investigations  near  Hranice  na  Moravě.  At  that  time  these
shales were supposed to be Devonian in age. Because of the
stratigraphical importance of this discovery trial pits, which
helped  to  understand  the  relation  of  stratigraphy  correctly
were excavated. Trilobite fauna described from pelitic facies
from Moravia are derived just from three localities until to-
day. All these sites were challenged during Chlupáč’s inves-
tigation  of  Moravia  in  1956—65.  Six  trilobite  taxa  were
described by Chlupáč (1966) from greenish and brown-red-
dish  silt  shales  from  fields  along  the  eastern  border  of  the
village of Březina, ca. 400 m from the crossroads near west-
ern  border  of  this  village.  The  trilobite  association  derived
from this site is stratigraphically older than the trilobite taxa
from  the  new  found  facies  in  the  Mokrá  Quarry.  In  1956
Chlupáč described six trilobite taxa from the northern border
of the Marian Valley  (Mariánské údolí) from greenish shales
of the Březina Formation (Mississippian) from a field south
of  the  village  of  Zbrašov  near  Hranice  na  Moravě.  He  no-
ticed  another  occurrence  of  Lower  Carboniferous  trilobites

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from the Říčka Valley (Údolí Říčky), (about 100 m, N of the
new bathing place), and established two other trilobite taxa.

All the trilobite associations studied by Chlupáč during the

years  1956—65  belong  to  the  Upper  part  of  the  Pericyclus
Stage cu II   ( = Lower Visean). Chlupáč (1965) noted the tri-
lobite  occurrence  from  test  pits  from  the  neighbourhood  of
the Mokrá Quarry, but they derived from carbonate facies of
the Hády-Říčka Limestones and not from shales. There is no
published paper discussing a  presence of Lower Carboniferous
(Mississippian) trilobites of the Březina Formation.

Geological settings of the Mokrá Quarry near Brno

The village of Mokrá is situated northwest of Brno (Czech

Republic),  in  the  southernmost  part  of  the  Moravian  Karst
(Fig. 1). Devonian and Carboniferous rocks cropping out in
the  Mokrá  Quarry  represent  the  sedimentary  cover  of  the
Brunovistulian Unit which were situated on the southern tip
of Laurussia during the Variscan time (Kalvoda et al. 2003).
It  is  often  regarded  as  the  eastern-most  continuation  of  the
Rhenohercynian Zone (Franke 1989; Kalvoda 1998; Kalvoda
et al. 2002, 2003, 2008) and was involved in the collision with
the  Lugodanubian  terranes  (Armorican  Terrane  Assemblage
of Tait et al. 1997; Kalvoda et al. 2008).

In the large quarries of the cement works, a sequence of

Frasnian reefoid limestones (Macocha Formation), Famennian
to Visean calciturbidites and rarely also hemipelagites (Líšeň
Formation),  transitional  flysch  sediments  (Březina  Forma-
tion) and typical flysch (Rozstání, Myslejovice Formations)
is  cropping  out  (Fig. 2).  Different  facies  developments  are
tectonically  convergent  here,  they  underwent  a  polyphase
deformation  and  complex  overthrusting  (Rez  2004a,b).  In
the  late  Tournaisian—early  Visean,  a  lithologically  different
facies  development  of  turbidites  represents  a  facies  change
from different granulometric types of limestones (Hády-Říčka

Limestones)  to  limestones  with  reddish  to
greenish  shale  intercalations  and  shales  with
limestone  intercalations  (Březina  Formation)
(Fig. 2).  Both  facies  interfinger  and  the
boundary  between  them  is  often  hard  to
determine.  The  limestones  contain  abundant
foraminiferal  fauna,  locally  rugose  corals,
variable amounts of conodont fauna and in its
deeper facies developments also trilobite fau-
na  and  brachiopods  associated  with  bivalves
and ammonoids (Kalvoda et al. 2010). The T-V
boundary  was  studied  both  in  the  uppermost
Hády-Říčka  Limestones  and  in  the  Březina
Formation  which  crop  out  in  the  eastern
benches of the quarry.

Biostratigraphy

The high resolution biostratigraphy of the

T-V boundary interval is primarily based on

Fig. 1. Location of the Moravian Karst region within the Bohemian Massif and the
Czech Republic; B – Location of Mokrá Quarry (showed by a star).

Fig. 2. General lithostratigraphical table of the Upper Devonian and
Lower Carboniferous in the Mokrá quarries.

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SIGNIFICANCE OF NEW MISSISSIPPIAN TRILOBITE ASSOCIATION (MORAVIAN KARST, CZECH REPUBLIC)

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GEOLOGICA CARPATHICA, 2012, 63, 3, 181—190

the  foraminiferal  fauna.  The  search  for  a  new  stratotype  of
the T-V boundary in the last decade contributed to the sub-
stantial  refinement  of  the  biostratigraphical  resolution  by
Devuyst (2006) and Devuyst & Kalvoda (2007). In the zona-
tion of Devuyst & Hance (2006) the T-V boundary is placed
at  the  base  of  MFZ9  which  is  characterized  by  the  appear-
ance  of  Eoparastaffella  simplex.  The  base  of  MFZ8  coin-
cides  then  with  the  appearence  of  the  first  fusulinid
Eoparastaffella (Fig. 3). Higher in the sequence, the first oc-
currence  of  Eoparastaffella  vdovenkoae  and  closely  related
species E. interiecta and E. macdermoti (Eoparastaffella ex
gr. interiecta), Lysella gadukensis and Eoparastaffella ex gr.
florigena  represent  an  important  biostratigraphic  marker
(Fig. 3). As the first E. simplex are not always very common,
the  appearance  of  Eoparastaffella  ovalis  Morphotype 2  and
Eoparastaffella  asymmetrica  represent  additional  guides  of
the MFZ9 (Devuyst 2006; Devuyst & Kalvoda 2007). In the
Pengchong  stratotype,  transitional  forms  between  E.  ovalis
M2  and  E.  simplex  occur  shortly  before  the  first  Eopara-
staffella  simplex  (Devuyst  2006).  The  disappearance  of
Elevenella parvula in late MFZ8 or close to the T-V bound-
ary represents another important bio-event.

In terms of conodont zonation, the disappearance of

Scaliognathus anchoralis below the base of the Visean rep-
resents  the  most  reliable  event  at  this  stratigraphical  level
that  can  be  traced  worldwide.  The  stratigraphic  interval  be-
tween  the  last  appearence  datum  of  S.  anchoralis  and  the
first appearence datum of Gnathodus homopunctatus, an in-
dex  species  of  the  first  Visean  conodont  zone,  commonly
contains  abundant  Gnathodus  (in  particular  G.  pseudosemi-
glaber)  and  was  recently  named  the  Gnathodus  Interzone

(Devuyst  &  Kalvoda  2007).  The  additional  important  bio-
events  are  represented  by  the  appearance  of  Mestognathus
beckmanni  from  its  ancestor  M.  praebeckmanni  slightly
below the T-V boundary.

Material and methods

During the first author’s thesis research, focused on sys-

tematical  investigation  of  the  Mokrá  Quarry,  highly  fossili-
ferous levels of the Březina Formation were discovered. All
fragments  of  fossils  were  documented  and  photographed,
then restored using CorellDRAW computer programme with
axis cross to establish the original shape of trilobite remains.
At the same time, the tectonic processes in layers of sections
can  be  studied  according  to  the  type  of  their  deformation.
Limestones in the upper and lower layers of reddish shales of
the  Březina  Formation  were  dissolved  by  using  acetic  acid.
The  main  goal  of  this  research  was  to  establish  the  occur-
rence and stratigraphy of found conodont taxa. The study of
the  newly  found  trilobite  assemblage  will  enable  a  corella-
tion  with  other  fauna  from  the  W  European  occurrences,
such as the Erdbacher Kalken (Harz; Hahn G. 1967), which
show  a  close  affinities  to  taxa  from  the  Mokrá  Quarry.  A
thorough functional morphological analysis of trilobite frag-
ments  (see  Thomas  &  Lane  1984;  Fortey  &  Owens  1999)
can show us their feeding habits. The taphonomic conditions
in pelitic sediments – dorsoventral and lateral deformation
– made difficult the final determination of trilobite taxa.

Among the associated faunal components, isolated col-

umns of crinoids were also collected. It consists of the fol-

Fig. 3. Important conodont and foraminifer bioevents close to the Tournaisian—Visean boundary. MFZ 8 and MFZ 9 are foraminiferal bio-
zones of Devuyst & Hance (in Poty et al. 2006).

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lowing taxa: Laudonomphalus sp., Cyclocaudex plenus
Moore & Jeffords, 1968, Cyclocaudiculus cf. longus
Gluckowski, 1986, Cyclocaudiculus edwardi Prokop & Pek,
1998, Stenocrinus sp., Heterostelechus sp.

The brachiopod fauna of the Mokrá Formation is remark-

ably diverse. Two discrete but very probably mixed brachio-
pod associations can be tentatively differentiated. The first is
probably  subautochthonous,  of  deep-water  origin  and  com-
prises large smooth rhynchonellids similar to Ilopsyrhynchus,
small  chonetids  Rugosochonetes  sp.  and  arhipidomellid
Aulacella sp. These taxa are mostly deformed but commonly
complete  with  valves  articulated;  a  minute  discinacean
Orbiculoidea sp. is very rare but probably belongs to the same
association.

The second fossil association is represented by brachiopod

fragments, commonly associated with coarse biodetritic and
clastic  material.  It  includes  the  spiriferid  genera  Prospira
and  Tylothyris,  medium-sized  reticulariid  Reticularia,  large
chonetoids  referable  to  Rugosochonetes,  a  rhipidomellid
Rhipidomella sp. and two or three poorly preserved produc-
tids,  of  which  Plicatifera  is  characteristic.  These  taxa  are
probably allochthonous, and represent fauna of the shallower
shelf. There were also poor remains of deformed goniatites,
corals and other groups of fossils.

Description of sections and occurrences of trilobites

and other fauna

All studies about the autecology of trilobites from the Czech

Republic until today were focused on the Barrandian area. The
major  studies  about  the  Cambrian  and  Ordovician  trilobite
autecology  was  published  by  Šnajdr  (1978),  Havlíček  &
Vaněk  (1990),  Fusco  G.  et  al.  (2004),  Budil  et  al.  (2007),
Mergl et al. (2007) concentrated on the autecology of Silurian
trilobites but also studied a Devonian trilobite assemblage and
their autecology from the Chýnice Limestones.

Chlupáč (1983) and Chlupáč et al. (1985) concentrated on

a trilobite assemblage from the Lochkovian—Pragian interval
in the Prague Basin. Havlíček & Vaněk (1998) studied bra-
chiopod and trilobite assemblages and the main Pragian bio-
facies  of  the  Prague  Basin.  Surprisingly,  there  has  been  no
work about the autecology of Lower Carboniferous trilobites
from  the  Moravian  Karst.  In  the  last  few  years  Lower
Carboniferous  shales  of  the  Březina  Formation  with  very
common  fragments  of  trilobites  were  uncovered  in  the
Mokrá  Quarry.  After  comparison  with  foreign  material  and
modern literature (Hahn G. & Hahn R. 1988; Hahn G. 1990;
Hahn  G.  et  al.  1996),  twelve  taxa  of  trilobites  were  distin-
guished  and  knowledge  of  Lower  Carboniferous  trilobites
was  extended.  The  occurrence  of  the  typical  conodont  and
foraminiferal  taxa  makes  these  trilobite  finds  the  youngest
found  in  the  Březina  Formation  from  the  entire  Moravian
Karst. Eleven species of trilobites have been identified from
the Mokrá Quarry, of which the majority originate from the
Moravian Karst for the first time (Rak 2004). All specimens
from pelitic shales show clear evidence of dorsoventral and
lateral  deformations.  However,  preservation  is  sufficient  to
enable  comparison  with  the  type  material  of  these  species

from coeval carbonate sequences (Erdbach Limestone) in the
Harz Mountains. Later investigations at the Mokrá Quarry
concentrated mainly on the T-V boundary and study of fora-
miniferal and conodont fauna (Kalvoda & Ondráčková 1999,
2003; Ondráčková 2000, 2001).

At present 978 fragments of trilobites (241 kranidia, 47

librigena, 9 cephala, 197 pygidia, 11 articulated exoskeletons
and 6 exuviae, etc.) of eleven taxa have been found. Activities
have to be done in an active quarry, therefore it has a strong
aspect of preservation work.

Systematics of Trilobita

Family: Proetidae Hawle & Corda, 1847

Subfamily: Archegoninae Hahn G. & Brauckmann, 1984

Genus: Archegonus Burmeister, 1843

Subgenus: Archegonus (Archegonus) Burmeister, 1843 [non

(Phillibole) Richter & Richter, 1937]

Type species: Archegonus (Angustibole) winterbergensis

Hahn G., 1965.

Archegonus (Archegonus) aequalis (H. v. Meyer, 1831)

Archegonus (Archegonus) aequalis philliboloides R. Hahn,

1967

Fig. 4.1

1967 Archegonus (Archegonus) aequalis philliboloides – R. Hahn,

101, 102

1968 Archegonus (Archegonus) aequalis philliboloides – R. Hahn,

208—210

1975 Archegonus (Archegonus) aequalis philliboloides – Hahn &

Hahn, 43

H o l o t y p e : Cranidium SMF (Senckenberg Museum Frank-

furt) 22002.

N e w m a t e r i a l a n d h o r i z o n : Three articulated exosk-

eletons preserved in shale, (SR 10). Latest Tournaisian S. an-
choralis conodont Zone, foraminiferal Zone MFZ8.

D e s c r i p t i o n : Three large articulated exoskeletons pre-

served in a row, on one slab of shale (see Fig. 4.1).

Despite dorsoventral deformation, all characteristic features

are preserved and comparable to the type material (see R.
Hahn, 1968).

Subfamily: Bollandiinae Hahn & Brauckmann, 1988

Bollandia Reed, 1943

Type species: Asaphus globiceps Phillips, 1836.

Bollandia persephone (Hahn & Hahn, 1970)

1966 Griffithides sp. – Hahn, p. 349—350
1967 Griffithides sp. – Hahn, p. 183—184
1970 Griffithides (Bollandia) persephone sp. n. – Hahn & Hahn,

p. 211—212

1971 Griffithides (Bollandia) persephone – Hahn & Hahn, p. 136—141
1975 Griffithides (Bollandia) persephone – Hahn & Hahn, p. 60
1977 Griffithides (Bollandia) persephone – Gandl, p. 190
2003 Bollandia persephone – Hahn et al. p. 60

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N e w m a t e r i a l a n d h o r i z o n : Two incomplete

cranidia, five incomplete pygidia (Figs. 2A—K, 244 Fig. 3),
SR 3—9. S. anchoralis Zone.

R e m a r k s : All the specimens are assigned to Bollandia

persephone (Hahn & Hahn, 1970) because they correspond to
the type specimens especially in the sculpture of the glabella,
the straight, broad, shallow S1, the proportions, convexity and
general outline of the pygidium (see Rak & Aubril 2009).

Bollandia cf. megaira (Hahn & Hahn, 1970)

N e w m a t e r i a l a n d h o r i z o n : A single poorly pre-

served weathered pygidium. S. anchoralis Zone.

D e s c r i p t i o n : Sculpture as far as can be determined,

pygidium entirely smooth with very convex axis and rings
(see Rak & Aubril 2009).

R e m a r k s : Because only one incomplete specimens is

available, it is left in open nomenclature; additional material
is required for confident specific determination.

Genus: Liobole Richter & Richter, 1949

Subgenus: Liobole (Panibole) Gröning, 1985

Type species: Phillipsia glabra Holzapfel, 1889.

Liobole (Panibole) cf. jugovensis (Osmólska, 1968)

Fig. 4.3

1843 Schwanzschild von Altwasser – Burmeister, 121
1900 Phillipsia aff. aequalis – Scupin, 2—5, pl. 1, fig. 10 (cranidium)
1968 Archegonus (Phillibole) culmicus cf. jugovensis – Osmólska,

133—136

1986 Liobole (Panibole) cf. jugovensis – Gröning, 60—62

H o l o t y p e : Cranidium IG 442, II. (Osmólska, 1968: 4a,

Abb. 23a,b).

N e w m a t e r i a l a n d h o r i z o n : Articulated exoskele-

ton and incomplete cephalon (SR 12). Latest Tournaisian S.
anchoralis conodont Zone, foraminiferal Zone MFZ8.

Subgenus: Liobole (Sulcubole) Gröning, 1985

Type species: Phillibole (Liobole) glabroides Richter &

Richter, 1949.

Liobole (Sulcubole) glabroides (Richter & Richter, 1949)

1921 Phillipsia cf. glabra – R. & E. Richter in H. Schmidt, Ober-de-

von-Culm von Warstein und Belecke, 297

1949 Phillibole (Liobole) glabroides – Richter & Richter, 71, 79, 82—84
1961 Liobole glabroides – Erben, Blinding Proetidae, 90
1962 Liobole glabroides glabroides – Osmólska, 169
1966 Liobole glabroides – Chlupáč, 62
1971 Liobole cf. glabroides glabroides – H. Zakowa, Zone Goniatites

granosus in the Galezice syncline (Góry Swietokrzyskie), 70

1975 Liobole glabroides – Hahn & Hahn, 9, 44
1985 Liobole (Sulcubole) glabroides – Gröning, 142
2000 Liobole (Sulcubole) glabroides – Hahn, Hahn & Müller, 166—167

H o l o t y p e : Cranidium SMF X 1336a (Richter & Richter,

1949: pl. 3, fig. 30).

N e w m a t e r i a l a n d h o r i z o n : Four cranidia. Latest

Tournaisian S. anchoralis conodont Zone, foraminiferal
Zone MFZ8.

Genus: Semiproetus Reed, 1943

Subgenus: Semiproetus (Macrobole) Richter & Richter, 1951

Semiproetus (Macrobole) drewerensis Richter & Richter, 1951

Type species: Proetus (Semiproetus) twistonensis Reed

1943.

Semiproetus (Macrobole) drewerensis latipalpebratus

(Osmólska, 1973)

Fig. 4.6

1973 Phillibole drewerensis latipalpebratus – Osmólska, 61, 65—66,

67, tab. 1, pl. 1, figs. 7—9, text-fig. 1C

1975 Archegonus (Phillibole) drewerensis longipalpebratus – Hahn &

Hahn, 42

1977 Archegonus (Phillibole) latipalpebrata – Gandl, Tril. Alba-

Schichten, 155, 159

1981 Archegonus (Phillibole) drewerensis latipalpebrata – Brauck-

mann, Kulm-Tril. cuI, 99

1985 Archegonus (Macrobole) drewerensis latipalpebrata – Oliveira

et al., 116

1988 Archegonus (Phillibole) drewerensis latipalpebratus – Flajs &

Feist, 75, 77—78, pl. 11, figs. 1—3, 5, 6 (non pl. 11, fig. 4)

1989 Archegonus (Phillibole) drewerensis latipalpebrata – Xiang in

Ji Qiang et al., 121, pl. 35, fig. 7a—b

1991 Archegonus (Phillibole) drewerensis latipalpebratus – Archinal,

194

1992 Archegonus (Phillibole) drewerensis latipalpebratus – Archinal,

46—47, fig. 34a—b (cr) (with further synonymy)

H o l o t y p e : Cranidium Z. Pal. No. Tr. III/9a (Osmólska

1973: pl. 1, fig. 8).

N e w m a t e r i a l a n d h o r i z o n : One cranidium (SR 15).

Latest Tournaisian S. anchoralis conodont Zone, foramini-
feral Zone MFZ8.

D e s c r i p t i o n : Lateral furrows on glabella are not clear,

convexity of glabella and occipital ring as preglabellar field
and border are typical for this taxon.

Genus: Proliobole Archinal, 1991

Type species: Phillipsia nitida Holzapfel, 1889.

Proliobole vigilax (Chlupáč, 1961)

Fig. 4.4

1961 Cyrtosymbole (Macrobole) vigilax – Chlupáč, 230, pl. 2, fig. 1
1965 Archegonus (Phillibole) vigilax – G. Hahn, 251
1966 Cyrtosymbole (Macrobole) vigilax – Chlupáč, 45
1969 Archegonus (Phillibole) vigilax – Hahn & Hahn, 106
1987 Archegonus (Phillibole) vigilax – Hahn et al., Tril. Belg.

Kohlenkalk, 9, 144

1991 Proliobole vigilax – Archinal, 195
1992 Proliobole vigilax – Archinal, 67—69, figs. 47—48 (with further

synonymy)

H o l o t y p e : Cranidium ICh 1092 (Chlupáč 1961: pl. 2,

fig. 1; 1966: pl. 8, fig. 5, text-fig. 13).

187

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GEOLOGICA CARPATHICA, 2012, 63, 3, 181—190

N e w m a t e r i a l a n d h o r i z o n : Two incomplete exo-

skeletons in one slab of shale (SR 13). Latest Tournaisian S.
anchoralis conodont Zone, foraminiferal Zone MFZ8.

D e s c r i p t i o n : Preserved are just incomplete cranidia with

remarkable branches in occipital convex ring, L3 convex. Oc-
cipital tubercle is not preserved. Axis flat and wide, composed
of eight tight flat pleuras. Interpleural furrows deep and nar-
row. Pygidium of semicircular outline, with remarkably wide
axis and border. Interpleural furrows not visible.

Genus: Cyrtoproetus Reed, 1943

Subgenus: Cyrtoproetus (Cyrtoproetus) Reed, 1943

Type species: Phillipsia cracoensis Reed, 1899.

Cyrtoproetus (Cyrtoproetus) cracoensis (Reed, 1899)

Cyrtoproetus (Cyrtoproetus) cf. cracoensis cracoensis

(Reed, 1899)

Fig. 4.5

1899 Phillipsia cracoensis – Reed, 241—245, pl. 10, figs. 1—7
1943 Cyrtosymbole (Crytoproetus) cf. cracoensis – Reed, 64
1959 Cyrtoproetus cf. cracoensis – J.M. Weller, 413
1968 Archegonus (Cyrtoproetus) cf. cracoensis – Osmólska, 142—144
1969 Crytoproetus cf. cracoensis – Hahn & Hahn, 54—55
1987 Cyrtoproetus (Cyrtoproetus) cf. cracoensis cracoensis – Brauck-

mann & Tilsley, 148—149, pl. 1, figs. 1—3, text-figs. 1—2 (with
further synonymy)

1998 Cyrtoproetus (Cyrtoproetus) cf. cracoensis cracoensis – Hahn et

al., 175

L e c t o t y p e : Cranidium Sedgwick Museum, Cambridge,

E3532 (Reed 1899: pl. 10, fig. 1; Osmólska 1968: pl. 5, fig. 3).

N e w m a t e r i a l a n d h o r i z o n : One cranidium (SR 14).

Latest Tournaisian S. anchoralis conodont Zone, foramini-
feral Zone MFZ8.

D e s c r i p t i o n : A complete cranidium with badly pre-

served glabellar furrows and branches in occipital convex,
wide, ring. Occipital tubercle is well preserved. Preglabellar
border is flat and narrow.

Genus: Carbonocoryphe Richter & Richter, 1950

Subgenus: Carbonocoryphe (Carbonocoryphe) Richter &

Richter, 1950

Type species: Carbonocoryphe bindemanni Richter &

Richter, 1950.

Carbonocoryphe (Carbonocoryphe) bindemanni Richter &

Richter, 1950

1950 Carbonocoryphe bindemanni – Richter & Richter, 278—280,

pl. 1, fig. 1—7

1975 Carbonocoryphe bindemanni–Hahn & Brauckmann, 329, fig. 20a—b

H o l o t y p e : Cranidium SMF X 1333a (Richter & Richter

1950: pl. 1, fig. 1a—b).

N e w m a t e r i a l a n d h o r i z o n : One incomplete pygidi-

um. Latest Tournaisian S. anchoralis conodont Zone, fora-
miniferal Zone MFZ8.

D e s c r i p t i o n : Only the incomplete right half of the py-

gidium is preserved. It has deep and characteristic pleural
furrows. Axis with wide and flat axis.

Subfamily: Cystispininae Hahn & Hahn, 1982

Genus: Tawstockia Brauckmann, 1974

Subgenus: Tawstockia (Beleckella) Hahn, Hahn &

Brauckmann, 1992

Type species: Phillibole? (Cytispina) nasifrons Richter &

Richter, 1949.

Tawstockia (Beleckella) milleri (Hahn & Hahn, 1971)

Fig. 4.7

1971 Spatulina spatulata milleri – Hahn & Hahn, 485—487, pl. 2,

fig. 16—20, text-fig. 10

1972 Spatulina spatulata milleri – Hahn & Hahn, 432—433
1973 Tawstockia milleri – C. Brauckmann, Kulm-Trilobiten von

Aprath, 165

1992 Tawstockia (Beleckella) milleri – Hahn et al., 104, 114, 116,

tab. 1

1993 Tawstockia (Beleckella) milleri – Hahn & Hahn, 87—89, fig. 68

(with further synonymy)

H o l o t y p e : Librigena SMF 22766 (Hah & Hahn 1971:

pl. 2, fig. 16, text-fig. 10).

N e w m a t e r i a l a n d h o r i z o n : One cephalon with hy-

postoma (SR 16). Latest Tournaisian S. anchoralis conodont
Zone, foraminiferal Zone MFZ8.

R e m a r k s : Cephalon with both complete genal spines

and with hypostoma displaced to the left side from its posi-
tion in situ is preserved. Preglabellar field is wider than in
the type species. Well preserved duplicature on ventral side
and the 3-dimensional terminal part of left genal spine. Gla-
bellar field is broken off and displaced anteriorly.

Subfamily: Cummingellinae Hahn & Hahn, 1967

Genus: Cummingella Reed, 1942

Subgenus: Cummingella (Cummingella) Reed, 1942

Type species: Phillipsia jonesii Portlock, 1843.

Cummingella (Cummingella) cf. C. auge Hahn & Hahn, 1968

Fig. 4.2

1968 Cummingella cf. C. auge – Hahn & Hahn, 450—453, text-figs. 2—3,

pl. 1, figs. 6—7

1998 Cummingella (Cummingella) cf. C. auge – Hahn, Hahn &

Müller, 191—192, pl. 4, figs. 11—12

N e w m a t e r i a l a n d h o r i z o n : Two pygidia preserved

on one slab of a shale (SR 11). Latest Tournaisian S. ancho-
ralis conodont Zone, foraminiferal Zone MFZ8.

D e s c r i p t i o n : Two incomplete semicircular convex py-

gidia are preserved. Pleural and intepleural furrows are not
favourably preserved.

R e m a r k s : Based on typical outline of pygidium, pygidi-

al axis and reduction of pleurae it seems to be a representa-
tive of this species. Pygidium of semicircular outline, with
convex lateral lobes and axis. Rhachis convex, wide, com-

188

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GEOLOGICA CARPATHICA, 2012, 63, 3, 181—190

posed of eleven convex rings. Interpleural furrows are not
visible, pygidial border narrow. Despite dorsoventral defor-
mation, all characteristic features are preserved and compa-
rable to the type material (see Hahn R. 1968).

Conclusion

The discovery of a new trilobite assemblage in the Březina

Shales  (Březina  Formation)  in  the  Mokrá  Quarry  comple-
ments Chlupáč’s research from 1966 on Lower Carboniferous
trilobite  taxa  derived  from  pelitic  facies  of  the  Březina
Formation. It signifantly enriches our knowledge concerning
Moravian Carboniferous trilobite fauna, its diversity and the
occurrence of different taxa. In this work, the biostratigraphy
position  of  discovered  trilobite  fauna  in  Moravan  Karst  is
documented for the first time. The obvious paleogeographi-
cal  affinities  of  Moravian  trilobite  assemblages  with  other
European  Carboniferous  faunas,  especially  that  of  the  Harz
Mountains (Hahn et al. 1998, 2003) are proved.

The large diversity of trilobite, brachiopod and other asso-

ciated fauna shows the importance of the Mokrá Quarry in
the cosmopolitan context of Mississippian sites.

Acknowledgments: We are grateful to Carsten Brauckmann,
Rudolf Prokop, Michal Mergl for determination of non-trilo-
bite  fauna  Petr  Budil  and  Oldřich  Fatka  for  valuable  com-
ments.  Štěpán  Rak  also  thanks  the  Grant  Agency  of  the
Czech  Academy  of  Science  for  its  support  by  means  of  the
Project No. 205/08/J015. The contribution was supported by
the Project MSM 0021620855.

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