GEOLOGICA CARPATHICA, 51, 2, BRATISLAVA, APRIL 2000
109119
UPPER JURASSIC RADIOLARITES OF THE CZERTEZIC
SUCCESSION AND COMPARISON WITH THE KYSUCA SUCCESSION
IN THE EAST-SLOVAK PART OF THE PIENINY KLIPPEN BELT
(WESTERN CARPATHIANS, SLOVAKIA)
LADISLAVA OVOLDOVÁ, JOZEF JABLONSKÝ and LENKA FRANTOVÁ
Department of Geology and Paleontology, Faculty of Science, Comenius University, Mlynská dolina G, 842 15 Bratislava, Slovak Republic
(Manuscript received June 22, 1999; accepted in revised form December 8, 1999)
Abstract: In the more shallow-water Czertezic Succession, the stratigraphical interval of maximum deepening of the
Pieniny sedimentary basin in the Upper Jurassic is not represented by typical radiolarite sequences with radiolarians,
representing middle Callovianearly Oxfordian to late Oxfordianearly Kimmeridgian (U.A.Zone 8U.A.Zone 10), as
we can observe in the deep-water Kysuca Succession, but by radiolarian limestones with radiolarian cherts and irregular
layers of radiolarites. Their sedimentation began here only in the Oxfordian. The radiolarian microfauna is of middle-
late Oxfordian to late Oxfordianearly Kimmeridgian age (U.A.Z.9U.A.Z.10). In four sections in the locality Litmanová
fifty-eight taxons and one new species Archaeospongoprunum mizutanii Ovoldová, n.sp. were identified in the assem-
blages. The high content of spumellarians (7080 %) could reflect the paleogeographical and paleoceanographical con-
ditions of sedimentation.
Key words: Jurassic, Western Carpathians, Pieniny Klippen Belt, radiolarian limestones, radiolarites, radiolarians.
Introduction
The first data on radiolarian microfauna from radiolarites of
the studied area were provided during the geological research
of Nemèok et al. (1986) by Ondrejíèková (1985). The radi-
olarian assemblages were regarded as late Middle Jurassic
early Late Jurassic in age.
Further investigation was performed by Ovoldová &
Frantová (1997) in the Podsadek locality near Stará ¼ubovòa
in the Pieniny part and the ariské Jastrabie, Kyjov, Lúèka
and Milpo localities in the ari part of the Pieniny Klippen
Belt (Fig. 1b,c).
The study of the Litmanová locality sections (Fig. 1c,d)
described in this paper is further continuation of the radiolar-
ian research in this area.
Geological setting
The Pieniny Klippen Belt is an unusually long zone of
complicated structure, separating the Flysh Belt of the Outer
Carpathians from the Inner Carpathians. This zone is
marked by rigid blocks of Jurassic-Lower Cretaceous rocks,
flowing in a soft Late Cretaceous-Paleogene matrix. The Ju-
rassic/Lower Cretaceous Kysuca-Pieniny Succession is de-
veloped in pelagic facies, while the Czorsztyn Succession is
represented by a swell facies suite. The Czertezic and Pruské
(Niedzica) Successions with slope deposits are the transition-
al successions between these two units.
The radiolarites in the studied area occur in the Kysuca
and Czertezic Successions. According to the determination
of Birkenmajer (1977) they can be assigned to the Sokolica
Radiolarite Formation (grey-green, dark-grey or black radi-
olarites with typical coatings of Mn-minerals) and to the
Czajakowa Radiolarite Formation (the middle part green
radiolarites of Podmajerz Radiolarite Member and the upper
part upper red radiolarites of Buwald Radiolarite Mem-
ber). They underlie the Czorzstyn Limestone Formation.
Lithostratigraphy
Ovoldová & Frantová (1997) studied radiolarites in the
Lúèka, ariské Jastrabie and Kyjov localities, belonging to
the Kysuca Succession and in the Podsadek near Stará
¼ubovòa and Milpo localities, representing the Czertezic
Succession (Fig. 1b,c).
The radiolarites of the Kysuca Succession are non-calcare-
ous or slightly calcareous (max. 0.36 % of CaO) and separat-
ed by thin shale intercalations. In the lower part they are of a
brown-grey and green-grey colour, sometimes with a rusty-
red part, with black-blue coatings of Mn minerals (max. val-
ue 3.16 % of Mn), typical for the Sokolica Radiolarite For-
mation. The Mn coatings disappear in the upper part and
green-grey radiolarites (Podmajerz Radiolarite Member) and
rusty red radiolarites (Buwald Radiolarite Member) of the
Czajakowa Radiolarite Formation overlie them. They are
overlain by Kimmeridgian red nodular limestones of the
Czorsztyn Limestone Formation. Underlying rocks are not
exposed in this area.
Radiolarites of the Czertezic Succession, representing the
Czajakowa Radiolarite Formation include a large quantity of
radiolarian limestone layers and the irregular layers of radi-
olarites mostly have a fair calcareous admixture. They over-
lie crinoidal limestones and underlie Kimmeridgian-Titho-
nian limestones.
110 OVOLDOVÁ, JABLONSKÝ and FRANTOVÁ
Fig. 1. a Location of the investigated area, b geological outline of this area, c situation of the studied localities, d location of
Litmanová sections ( Ls
1
, Ls
2
).
Fig. 2. Location of the sections and sampling in Litmanová Ls
1
.
The next locality with the occurrence of radiolarites of the
Czertezic Succession is Litmanová, situated in the Pieniny
part of the Pieniny Klippen Belt (Fig. 1b), ca. 10 km North
of Stará ¼ubovòa. The lithostratigraphical character of the
sequences of the Czertezic Succession in this locality was
described by Scheibner (1966).
In the klippe Ls
1
(Fig. 1d), which occurs ca. 1 km NW from
the Litmanová village radiolarian limestones and radiolarites
UPPER JURASSIC RADIOLARITES OF PIENINY KLIPPEN BELT 111
(the Czajakowa Radiolarite Formation) underlie Kimmerid-
gian red nodular limestones of the Czorsztyn Limestone For-
mation. The underlying strata are not exposed in this klippe,
but the same radiolarites overlie crinoidal limestones (Krupi-
anka Limestone Formation according to Birkenmajer 1977) at
the northern end of Litmanová village (Fig. 1dLs
2
). Red nod-
ular limestones are overlain by Tithonian pelagic limestones of
the Pieniny Limestone Formation (according to Birkenmajer
1977), occurring in the left part of the outcrop only (Fig. 2,
section 1).
Samples for the radiolarian research (38) were taken from
four sections (nos. 1, 2, 3, 4 Fig. 2). The Czajakowa Radi-
olarite Formation is formed by silicified marly limestones with
radiolarians (radiolarian wackestone-packstone) and with radi-
olarian cherts and irregular layers (35 cm, max.15 cm) of most-
ly calcareous radiolarites. The lower part of this strata is mainly
of a grey-green or pink-grey colour (Podmajerz Radiolarite
Fig. 3. Lithostratigraphical column of section 4 in Litmanová Ls
1
.
Member) and the upper part has a rusty-red colour (Buwald Ra-
diolarite Member). The border between these two members is
not sharp. The max. thickeness of the exposed part of these lay-
ers is approx. 4 m (section 4, Fig. 2). The lithostratigraphical
column of the section 4 is shown in Fig. 3.
Overlying Kimmeridgian red nodular limestones with nod-
ules and irregular layers of a rusty-red radiolarite (Fig. 2, sec.
1, samp. C) contain filaments (juvenile shells of Bositra),
Saccocoma, mainly calcified radiolarians, aptychi and juve-
nile amonites (filament-Saccocoma-radiolarian packstone).
The whole complex, as well as the contacts between indi-
vidual lithological parts are affected by tectonic movements.
The largest tectonic reduction of the thickness of radiolari-
an limestones with radiolarites is in the section 3, where only
the lower part of the strata of grey-green colour occurs.
The lithostratigraphical correlation of the Litmanová sec-
tions (L4, L1) of the Czertezic Succession and ariské Jas-
trabie sections (JP, JDD) of the Kysuca Succession is
shown in Fig. 4.
Fig. 4. Lithostratigraphical correlation of the sections from the
Kysuca (loc. ariské Jastrabie) and Czertezic Successions (loc.
Litmanová).
112 OVOLDOVÁ, JABLONSKÝ and FRANTOVÁ
Fig. 5. Quantitative composition of radiolarians in the assemblage
of sample 4A (Litmanová Ls
1
, sec. 4).
Emiluvia
27%
Hagiastridae
17%
Other nassellarians
13%
Multicyrtid nassellarians
10%
Archaeospongoprunum
9%
Haliodictya ( ?) antiqua
5%
Archaeocenosphaera
4%
Triactoma blakei
4%
Pantanellium
2%
Other spumellarians
6%
Praeconosphaera
3%
Biostratigraphy
Radiolarians from the siliceous and siliceous-calcareous
samples were extracted with 5 % HF (12 days). Calcareous
samples were treated with 5 % HCl or 12 % acetic acid. Af-
ter sieving through 40
µ
m screen and drying residue was pre-
pared for picking up of specimens under the binocular micro-
scope. Species determination was made by SEM.
The biostratigraphical evaluation of radiolarian assemblag-
es was based on the biozonation of Baumgartner et al.
(1995).
Well preserved radiolarians from radiolarites of the Kysu-
ca Succession in the locality ariské Jastrabie represent
U.A.Z.8 middle Callovianearly Oxfordian in the lower
part and U.A.Z.9U.A.Z.10 middle-late Oxfordian to late
Oxfordianearly Kimmeridgian in the upper part of the sec-
tions. A poor radiolarian assemblage from the locality Lúèka
shows the stratigraphical range U.A.Z.9U.A.Z.10
middle-late Oxfordian to late Oxfordianearly Kimmerid-
gian. The important result is the fact, that the radiolarites
with the Mn coatings (Sokolica Radiolarite Formation) ex-
tend in the section JDD (loc. of ariské Jastrabie) (Fig. 4)
to middle Oxfordian (on the basis of the presence of the spe-
cies Podocapsa amphitreptera Foreman). If we compare the
composition of assemblages, we can observe the gradual in-
crease of spumellarian abundance from the stratigraphic in-
terval U.A.Z.8 to U.A.Z.10 middle Callovianearly Ox-
fordian to late Oxfordianearly Kimmeridgian. In the
locality Kyjov, sample from a scree contain radiolarians, rep-
resenting U.A.Z.8U.A.Z.10.
Radiolarian limestones with radiolarite layers of the Cz-
ertezic Succession in the Podsadek locality near Stará
¼ubovòa contain radiolarians, which indicate the middle-late
Oxfordian to late Oxfordianearly Kimmeridgian age
(U.A.Z.9U.A.Z.10). A very poor radiolarian assemblage
from the Milpo locality shows, that it is not older than
U.A.Z.9 ranging from middle to late Oxfordian.
In the Litmanová locality radiolarians occur in all the sam-
ples taken (38), but the possibility of their preparation was
complicated by frequent calcification of the tests or occur-
rence of molds only.
In the klippe Ls
1
,
sections no. 4 and no. 1 (Fig. 1d, Fig. 2)
were the most suitable for the study of radiolarian microfau-
na. Spumellarians strongly prevail in the assemblages (7080
%) (Pls. IIII). The quantitative composition of sample 4A
from section no. 4 shows, that Emiluvia, a representative of
the Hagiastridae family and Archaeospongoprunum are
dominant (Fig. 5). In the last mentioned genus, Archaeospon-
goprunum mizutanii Ovoldová, n.sp. is relatively abundant.
In section 1, radiolarian microfauna is much more poorly
preserved.
The assemblages in sections 4 and 1 (Fig. 6) represent the
following U.A.Zones and the stratigraphic ranges in order
from the lower to the upper part of the sections:
Section 4
Sample 4J U.A.Z.9U.A.Z.10 middle-late Oxford-
ian to late Oxfordianearly Kimmeridgian, (the species Emi-
luvia ordinaria Ovoldová with Paronaella mulleri Pessag-
no and Tritrabs casmaliaensis (Pessagno));
Sample 4G U.A.Z.9U.A.Z.10 middle-late Oxford-
ian to late Oxfordianearly Kimmeridgian, (the species Ful-
tacapsa sphaerica (Ovoldová) with Tritrabs casmaliaensis
(Pessagno));
Sample 4F U.A.Z.8U.A.Z.10 middle Callovianear-
ly Oxfordian to late Oxfordianearly Kimmeridgian (the spe-
cies Paronaella broennimanni Pessagno with Emiluvia orea
Baumgartner);
Sample 4D U.A.Z.10U.A.Z.11 late Oxfordianearly
Kimmeridgian to late Kimmeridgianearly Tithonian (the
species Paronaella pristidentata Baumgartner with Crucella
theokaftensis Baumgartner and Haliodictya (?) antiqua
(Rüst));
Sample 4A U.A.Z.10 late Oxfordianearly Kim-
meridgian (the species Paronaella pristidentata Baumgartner
with Pseudocrucella adriani Baumgartner, Paronaella mul-
leri Pessagno, Paronaella broennimanni Pessagno and Tri-
trabs casmaliaensis (Pessagno)). The new species Archaeo-
spongoprunum mizutanii Ovoldová, n.sp. was described in
the sample.
Section 1
Sample 1J U.A.Z.9U.A.Z.10 middle-late Oxfordian
to late Oxfordianearly Kimmeridgian (the species Fultacapsa
sphaerica (Ovoldová) with Paronaella broennimanni Pessa-
gno);
Sample 1G U.A.Z.8U.A.Z.10 middle Callovianearly
Oxfordian to late Oxfordianearly Kimmeridgian (the species
Emiluvia orea Baumgartner with Paronaella mulleri Pessagno);
Sample 1D U.A.Z.9U.A.Z.10 middle-late Oxfordian
to late Oxfordianearly Kimmeridgian (the species Emiluvia
ordinaria Ovoldová with Paronaella mulleri Pessagno);
Sample 1A U.A.Z.9U.A.Z.10 middle-late Oxfordian
to late Oxfordianearly Kimmeridgian (the species Angulo-
bracchia biordinalis Ovoldová with Paronaella broenniman-
ni Pessagno);
UPPER JURASSIC RADIOLARITES OF PIENINY KLIPPEN BELT 113
Fig. 6. Distribution of radiolarians in the samples from the sections in the Litmanová locality (Ls
1
, sections 4 and 1) with their relative abun-
dance in richer assemblages (abundant more than 7 specimens., common 37 spec., rare 2 spec.).
Section n.4
Section n.1
Samples
4A
4D
4F
4G 4H 4J
1C
1D
1F
1G
1H
1J
Radiolarian fauna
Acastea diaphorogona (Foreman)
*
Acanthocircus trizonalis (Rüst)
*
*
Actinomma siciliensis Kito et De Wever
*
Alievium (?) echinus Dumitrica
Angulobracchia biordinalis Ovoldová
Archaeocenosphaera sp.
*
*
*
Archaeodictyomitra patricki Kocher
Archaeospongoprunum imlayi Pessagno
*
*
*
*
Archaeospongoprunum mizutanii n.sp.
*
Archaeospongoprunum sp.
*
Complexapora tirolica Kiessling
Crucella angulata Yang
Crucella theokaftensis Baumgartner
Crucella sp.
Emiluvia grandipora (Ovoldová)
*
Emiluvia chica Foreman
Emiluvia ordinaria Ovoldová
*
Emiluvia orea Baumgartner
*
*
*
*
Emiluvia cf. orea Baumgartner
Emiluvia salensis Pessagno
*
*
*
*
Emiluvia sedecimporata (Rüst)
*
*
Emiluvia cf. omanensis Kiessling
Fultacapsa sphaerica (Ovoldová)
*
*
Haliodictya (?) antiqua (Rüst)
*
*
Loopus primitivus (Matsuoka et Yao)
Mirifusus dianae s.l. (Karrer)
Napora lospensis Pessagno
Obesacapsula sp. A sensu Widz 1991
Pantanellium aff. riedeli Pessagno
*
Paronaella broennimanni Pessagno
*
Paronaella mulleri Pessagno
*
*
Paronaella pristidentata Baumgartner
Paronaella sp.
*
Parvicingula cf. elegans Pessagno et Whalen
Perispyridium ordinarium s.l. (Pessagno)
*
Podobursa spinosa (Ovoldová)
*
Podobursa triacantha (Fischli)
*
Praecanetta (?) sp.
Praeconosphaera sphaeroconus (Rüst)
Praeconosphaera spinosa Yang
Protunuma cf. multicostata (Heitzer)
Pseudocrucella adriani Baumgartner
Pseudodictyomitrella sp.
Saitoum dercourti Widz et De Wever
*
*
Sethocapsa leiostraca Foreman
*
Spongocapsula perampla (Rüst)
*
Syringocapsa spinellifera Baumgartner
Syringocapsa sp.
Teichertus (?) catenarius (Ovoldová)
Tethysetta dhimenaensis (Baumgartner)
Tetraditryma cf. pseudoplena Baumgartner
Tetratrabs bulbosa Baumgartner
*
Triactoma jonesi (Pessagno)
*
Tripocyclia trigonum (Rüst)
*
*
Tritrabs casmaliaensis (Pessagno)
Tritrabs ewingi (Pessagno)
*
Tritrabs ewingi worzeli (Pessagno)
*
Tritrabs exotica (Pessagno)
*
*
abundant
common
rare
absent
present
114 PLATE I
PLATE II 115
116 PLATE III
UPPER JURASSIC RADIOLARITES 117
Plate II: Litmanová (Ls
1
) Fig. 1. Crucella angulata Yang 4A, 5688, 110
×
. Fig. 2. Paronaella mulleri Pessagno 4A, 4875, 140
×
. Fig.
3. Paronaella broennimanni Pessagno 4A, 5755, 130
×
. Fig. 4. Paronaella pristidentata Baumgartner 4D, 5677, 150
×
. Fig. 5.
Pseudocrucella adriani Baumgartner 4A, 5738, 195
×
. Fig. 6. Tetraditryma cf. pseudoplena Baumgartner 4A, 5691, 125
×
. Fig. 7. Pa-
ronaella sp. A 4A, 5681, 125
×
. Fig. 8. Crucella theokaftensis Baumgartner 4A, 5722, 185
×
. Fig. 9. Tetratrabs bulbosa Baumgartner
4A, 4896, 80
×
. Fig. 10. Angulobracchia biordinalis Ovoldová 4A, 5767, 150
×
. Fig. 11. Tritrabs ewingi worzeli (Pessagno) 1C,
4888, 110
×
. Fig. 12. Tritrabs casmaliaensis (Pessagno) 4A, 5726,140
×
. Fig. 13. Tritrabs exotica (Pessagno) 1C, 4891, 100
×
. Fig. 14.
Napora lospensis Pessagno 4A, 5756, 125
×
. Fig. 15. Loopus primitivus (Matsuoka & Yao) 4A, 5747, 250
×
. Fig. 16. Syringocapsa
spinellifera Baumgartner 4A, 5737, 150
×
. Fig. 17. Archaeodictyomitra patricki Kocher 4A, 5758, 350
×
. Fig. 18. Saitoum dercourti
Widz & De Wever 4A, 5773, 300
×
. Fig. 19. Perispyridium ordinarium s.l. (Pessagno) 4A, 5703, 180
×
. Fig. 20. Fultacapsa sphaerica
(Ovoldová) 4A, 5702, 125
×
. Fig. 21. Syringocapsa sp. 4A, 5777, 165
×
. Fig. 22. Complexapora tirolica Kiessling 4A, 5706, 250
×
.
Plate III: Litmanová (Ls
1
) Fig. 1. Obesacapsula sp. A sensu Widz 1991 4A, 5748, 135
×
. Fig. 2. Praecanetta (?) sp. 4A, 5704, 250
×
.
Fig. 3. Pseudodictyomitrella sp. 4A, 5775, 350
×
. Fig. 4. Spongocapsula perampla (Rüst) 1H, 4862, 140
×
. Fig. 5. Sethocapsa leiostra-
ca Foreman 4A, 5732, 150
×
. Fig. 6. Parvicingula cf. elegans Pessagno & Whalen 4A, 5785, 200
×
. Fig. 7. Protunuma cf. multicostata
(Heitzer) 4A, 5769, 200
×
. Fig. 8. Protunuma cf. multicostata (Heitzer) lateral view of Fig. 7, 5771, 250
×
. Fig. 9. Spongocapsula sp.
4A, 5723, 135
×
. Fig. 10. Fultacapsa sphaerica (Ovoldová) 4G, 5778, 150
×
. Fig. 11. Acanthocircus trizonalis (Rüst) 4J, 4853, 130
×
.
Fig. 12. Paronaella mulleri Pessagno 4J, 4847, 195
×
. Fig. 13. Haliodictya (?) cf. antiqua (Rüst) 4J, 4868, 150
×
. Fig. 14. Emiluvia cf.
omanensis Kiessling 4A, 5684, 150
×
. Fig. 15. Emiluvia chica Foreman 4D, 5668, 205
×
. Fig. 16. Podobursa spinosa (Ovoldová)
4J, 4854, 110
×
.
Plate I: Litmanová (Ls
1
) Fig. 1. Archaeospongoprunum mizutanii Ovoldová, n.sp. 4A, 5739, 170
×
. Fig. 2. Archaeospongoprunum mi-
zutanii Ovoldová, n.sp. holotype, 4A, 5683, 140
×
. Fig. 3. Archaeospongoprunum mizutanii Ovoldová, n.sp. 4A, 5740, 170
×
. Fig. 4.
Archaeospongoprunum mizutanii Ovoldová, n.sp. 4A, 5669, 170
×
. Fig. 5. Praeconosphaera spinosa Yang 4A, 5736, 200
×
. Fig. 6.
Emiluvia grandipora (Ovoldová) 4A, 5764, 190
×
. Fig. 7. Actinomma siciliensis Kito & De Wever 4A, 5700, 200
×
. Fig. 8. Haliod-
ictya (?) antiqua (Rüst) 4A, 5751, 100
×
. Fig. 9. Teichertus (?) catenarius (Ovoldová) 4A, 5689, 150
×
. Fig. 10. Archaeospongo-
prunum sp. A 4A, 5712, 165
×
. Fig. 11. Acastea diaphorogona (Foreman) 4A, 5696, 140
×
. Fig. 12. Emiluvia salensis Pessagno 4A,
5731, 200
×
. Fig. 13. Emiluvia sedecimporata (Rüst) 4A, 5690, 220
×
. Fig. 14. Pantanellium aff. riedeli Pessagno 4A, 5697, 170
×
. Fig.
15. Crucella sp. A 4A, 5762, 140
×
. Fig. 16. Emiluvia cf. orea Baumgartner 4A, 5685, 110
×
. Fig. 17. Emiluvia cf. orea Baumgartner
lateral view of Fig. 16, 4A, 5686, 100
×
. Fig. 18. Alievium (?) echinus Dumitricã 4A, 5711, 250
×
. Fig. 19. Emiluvia orea Baumgartner
4A, 5743, 135
×
. Fig. 20. Emiluvia ordinaria Ovoldová 4A, 5749, 150
×
. Fig. 21. Emiluvia orea Baumgartner lateral view of Fig.19,
4A, 5744, 150
×
. Fig. 22. Triactoma jonesi (Pessagno) 4H, 4863, 150
×
. Fig. 23. Mirifusus dianae s.l. (Karrer) 4A, 5672,120
×
. Fig. 24.
Triactoma jonesi (Pessagno) 4A, 5753, 110
×
.
▲
▲ ▲
▲ ▲ ▲
On the basis of these data the studied strata represent the
stratigraphic range middle-late Oxfordian to late Oxford-
ianearly Kimmeridgian (U.A.Z.9U.A.Z.10).
The samples from the klippe Ls
2
at the northern end of the
village (Fig. 1d) provided only very poor radiolarian fauna,
but in the sample, taken 1.5 m above the contact of the radi-
olarian limestones with the underlying crinoidal limestones
the determinable species Fultacapsa sphaerica (Ovoldová)
occurs. This indicates, that the assemblage is not older than
U.A.Z.9 (middle-late Oxfordian).
Conclusions
In the studied area the results from radiolarite research in the
Kysuca and Czertezic Successions show the following data:
In the Kysuca Succession, the maximum deepening of the
sedimentary basin in the MiddleUpper Jurassic is manifest-
ed by non-calcareous or slightly calcareous brown-grey,
green-grey radiolarites with black-blue Mn coatings (Sokoli-
ca Radiolarite Formation) in the lower part and grey-green
and rusty-red ones (Czajakowa Radiolarite Formation) in the
upper part of the sequence. The radiolarian assemblages rep-
resent the stratigraphic interval middle Callovianearly
Oxfordian to late Oxfordianearly Kimmeridgian (U.A.Z.8
U.A.Z.10).
In the more shalow-water Czertezic Succession sedimenta-
tion of radiolarian limestones with radiolarian cherts and ir-
regular layers of radiolarites, representing the Czajakowa
Radiolarite Formation began only in the Oxfordian. The radi-
olarian assemblages correspond to the stratigraphic interval
middle-late Oxfordian to late Oxfordianearly Kimmerid-
gian (U.A.Z.9U.A.Z.10). In the assemblages of this interval
in the locality Litmanová (sample 4A, section 4, Ls
1
) the
new species Archaeospongoprunum mizutanii Ovoldová,
n.sp. was described.
Radiolarians of both successions were evaluated using the
biozonation of Baumgartner et al. (1995).
If we compare the composition of assemblages in the
Kysuca Succession, gradual increasing of spumellarian
abundance from the stratigraphic interval U.A.Z.8U.A.Z.10
middle Callovianearly Oxfordian to late Oxfordianear-
ly Kimmeridgian can be observed. In the more shallow-water
Czertezic Succession the abundance of spumellarians in the
range of U.A.Z.9U.A.Z.10 is as much as 7080 %. The
stratigraphic interval U.A.Z.8 (middle Callovianearly Ox-
fordian) does not contain favourable lithology for the finding
of radiolarians in this succession.
118 OVOLDOVÁ, JABLONSKÝ and FRANTOVÁ
Kiessling (1996), who first evaluated the importance of
nassellarian-spumellarian ratio (N/S) in pre-Cretaceous sedi-
ments in Tethyan localities, proved that the N/S ratio is posi-
tively correlated with the bathymetry (or with the distance
from the shelf).
On the basis of these data, increasing trend observed in
spumellarian abundance from U.A.Zone 8 to U.A.Zone 10
can be explained by continual shallowing of the sedimentary
area, which is in a good accordance with the paleogeographi-
cal and paleoceanographical conditions.
Systematic Paleontology
Subclass Radiolaria Müller 1858
Order Polycystina Ehrenberg 1838, emend. Riedel 1967
Suborder Spumellaria Ehrenberg 1875
Family Sponguridae Haeckel 1862
Genus Archaeospongoprunum Pessagno 1973
Type species: A. venadoensis Pessagno 1973
Archaeospongoprunum mizutanii Ovoldová, n.sp.
(Pl. I: Figs.14)
1981 Archaeospongoprunum sp. A S. Mizutani, p. 171, pl. 57,
figs. 2, 3
1997 Archaeospongoprunum sp. L. Ovoldová & L. Frantová,
pl. 3, fig. 4
Holotype: No. 5683, Pl. 1, Fig. 2, deposited in the Slovak
National Museum in Bratislava (SNM-21803).
Type locality: Litmanová village ¼ubovnianská vrchovi-
na Highland.
Stratotype: middle Oxfordianearly Kimmeridgian of the
Czajakowa Radiolarite Formation.
Denomination: This species is named in honour of S. Mi-
zutani for his contribution to radiolarian research.
Description: A spongy, broad ellipsoidal to subspherical
test with tetragonal to polygonal pore frames. Stout, bipolar
spines, nearly equal in length with six grooves and six ridg-
es. One spine is straight with three primary grooves and
three secondary grooves between six ridges. The other spine
is stouter with six grooves and six ridges, twisted in the
clockwise direction in the distal part.
Comparison: This species differs from A. patricki Jud (Jud
1994, p. 63, pl. 4, figs. 24) by being stouter and having
shorter spines and by the spines twisted in the clockwise di-
rection. It differs from A. cortinaensis Pessagno (Pessagno
1973, p. 60, pl. 9, figs. 46, 1977, p. 29, pl. 1, fig. 8) by hav-
ing a more spherical test and stouter spines and from A. car-
rierensis Pessagno (Pessagno 1977, p. 29, pl. 1, figs. 6, 7, 9)
by stouter and shorter spines.
Dimensions (mm): (based on 9 specimens)
holotype av. min. max.
Total length
0.427 0.384 0.364 0.427
Length test
0.178 0.145 0.129 0.178
Width test
0.150 0.124 0.105 0.150
Length straight spine
0.128 0.117 0.111 0.128
Length twisted spine
0.121 0.122 0.117 0.121
Genus Emiluvia Foreman 1973, emend. Foreman 1975,
emend. Pessagno 1977
Type species: E. chica Foreman 1973
Emiluvia grandipora (Ovoldová 1975) nov.comb.
(Pl. I: Fig. 6)
1975 Staurolonche grandipora n.sp. Ovoldová, p. 76, pl. 100,
fig. 1
Remark: The species was described in the locality Keblie in
the Kysuca Succession of the Pieniny Klippen Belt
(Ovoldová 1975). On the basis of the genus signs of this
species we can assign it to the genus Emiluvia Foreman.
Stratigraphical range: Up to now known U.A.Z.9
UA.Z.10 middle-late Oxfordian to late Oxfordianearly
Kimmeridgian (according to Baumgartner et al. 1995).
Acknowledgement: The authors are very grateful to Prof.
M. Miík (Department of Geology and Paleontology, Facul-
ty of Natural Sciences, Comenius University, Bratislava,
Slovakia), Dr. W. Kiessling (Museum of Natural Sciences,
Berlin, Germany) and Dr. M. B¹k (Institute of Geological
Sciences, Jagiellonian University, Cracow, Poland) for their
critical reading of the text and valuable advice. The radiolari-
an research was supported by grant of VEGA No. 4281.
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