Micropalaeontologic and palaeofloristic content of Sarmatian from

Draft copy
Micropalaeontologic and palaeofloristic content of Sarmatian from
southern Moldavian Platform – backbulge depozone
Mihai BRÂNZILĂ1, Gabriel CHIRILĂ1, Mihaela JITARU1
1
“University Al. I. Cuza” from Iaşi, Departament of Geology, Bd. Carol I, nr. 20A, 700505, Iasi, Romania, e-mail: mib@uaic.ro,
gabiflogeoc@yahoo.com
Abstract. Southern part of the Moldavian Platform has been developed in complex conditions, partially
similar, with northern part, in a marine environment corresponding to the last stage of evolution of the
foreland basin of the Eastern Carpathians, with an obvious tectonic control. In Stăniţa-Vlădnicele
borehole were identified microfauna taxas as: Quinqueloculina karreri, Q. consobrina, Elphidium
macellum, E. minutum, E. punctatum, E. crispum, E. aculeatum, E. regina regina, E. regina caucasica,
Articulina problema, A. glabra, A. sarmatica, Porosononion subgranosus confirming the presence of the
Sarmatian, starting with Buglovian, Volhynian and most of the Bessarabian. Identified palynomorphs
from the analyzed samples are represented by taxa as: Pityosporites labdacus, Pityosporites alatus,
Pityosporites insignis, Pinuspollenites miocaenicus, Abiespollenites sp., Myricipites bituitus,
Tricolpopollenites liblarensis, Tricolporopollenites henrici, Carpinipites carpinoides, Engelhardtioides
microcoryphaeus, Leiotriletes sp. a.o. The method used for paleoclimatic estimations is „Coexistence
Approach”. The values calculated by us, using coexistence approach method are: MAT 16.5–17.2 °C,
MAP 1300–1355 mm/yr, WMT 23.6–28.5 °C, CMT 9.6–12.5 °C.
Keywords. Sarmatian, Moldavian Platform, backbulge, micropalaeontology, palynomorphs.
Introduction
Analyzed samples, from this study, are from Stăniţa-Vlădnicele borehole (Neamţ County)
located nearby the tectonic limit, which divide Moldavian Platform from Bârlad Platform by Fălciu –
Plopana fault (Ionesi, 1994) (Fig. 1). Lithological column of the well have intercepted entirely Sarmatian
deposits, from the limit of the Badenian anhydrite until the Cryptomactra clays (lower Bessarabian and
the beginning of the upper Bessarabian).
Draft copy
Fig.1 Location of Stăniţa-Vlădnicele borehole
Geological settings
The Moldavian Platform supported a foreland type basin evolution during the Sarmatian, as the
last phase within the transformation of the Carpathian geosynclinal area. There have been identified
characteristic depozones (wedge top, foredeep, forebulge and backbulge) that due to particular facial
conditions allowed the evolution of some specific faunal assemblages (Grasu et al., 2002). Within all
non-biotic factors, the water salinity evolved towards a freshwater one, representing along with the
sedimentary process, the main cause that had a great influence on the foraminifers assemblages
(Brânzilă, 2005). The Intra-Volhynian tectogenesis, especially taking part in the external zone of the
Carpathians, have strongly affected the evolution of the Paratethys basins. In the terminal part of the
Badenian, the Moldavian Platform has functioned as continental area, the sedimentation process lasting
until the lower Sarmatian (Buglovian)( Brânzilă, 2005, Brânzilă & Ţabără, 2005)
Beginning with the Lower Sarmatian, in the Eastern Carpathian foreland, because of the
advancement of the orogeny above the top of the Moldavian Platform, a series of characteristic
depozones were outlined. Based on sedimentological criteria, from west to east, four depozones have
been identified: wedge-top, foredeep depozone, forebulge and backbulge. The basinal waters have a
much lower salinity as compared with that during the Badenian (Brânzilă, 1999; Grasu et al., 2002).
Southern part of the Moldavian Platform has been developed in complex conditions, partially
similar, with northern part, in a marine environment corresponding to the last stage of evolution of the
foreland basin of the Eastern Carpathians, with an obvious tectonic control. Deposits of this interval
belong to the first stage of evolution of the foreland basin where the subsidence was polarized from
North-East to South-West and was inducted by the influence of the Carpathian thrust (Ionesi, 1994,
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Ionesi et al., 2005). In such conditions we have seen the presence of the microfauna and paleoflora
assemblage corresponding to the backbulge depozone.
Fig. 2 Lithologic column of Staniţa-Vlădnicele borehole.
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Micropalaeontological assemblage
Micropalaeontological assemblage identified in samples from Stăniţa-Vlădnicele borehole has
two aspects, distinctive for Miocene biofacies from Moldavian Platform; one aspect regarding marine
and the second one related to brackish deposits. In the sample 301 from 975 m, located under Badenian
anhydrite, micropalaeontological content is exclusively marine been represented by benthic and
planktonic foraminifera, which developed under normal salinity, with many taxas and many individuals.
From this sample were determined: Uvigerina perornata, Bulimina elongata, Globigerina brevispira,
Orbulina universa, Cibicides lobatulus, C. dutemplei, Entoselenia marginata, Melonis pompilioides,
Pullenia bulloides, Sphaeroidina austriaca, Spiroplectamina sp., Quinqueloculina sp.
In the deposits located above Badenian anhydrite, the lithology is predominantly composed of
shale, sands, sandstones with thin lamination of limestone. Samples P 301-309, from the interval 140950 m are attributed to Sarmatian. Micropalaeontological assemblage has brackish characteristic, and the
number of taxas is lower. Cibicides taxa (Cibicides badenensis, C. lobatulus) are present only in sample
309 (950 m), alongside with reworked taxas: Ammonia beccarii, Quinqueloculina sp., and Globigerina
sp. In the analyzed samples between 140 and 890 m, although micropalaeontological assemblage is poor
and is represented by miliolidae and unionidae; Quinqueloculina karreri, Q. consobrina, Elphidium
macellum, E. minutum, E. punctatum, E.crispum, E. aculeatum, E. regina regina, E. regina caucasica,
Articulina problema, A. glabra, A. sarmatica, Porosononion subgranosus.
Micropalaeontological assemblage identified in the analyzed samples from Stăniţa-Vlădnicele
borehole is assigned to Badenian (sample P 310 from 975 m) and to Sarmatian (samples P 301-309 from
140 to 975 m), been possible even an distribution on stages. The assemblage determined from sample
309 (from 950 m) can be attributed to Buglovian, samples P 305-308 (from 550-895 m) are assigned to
Volhynian and samples P 301-304 (from 140-550m) are attributed to Bessarabian.
Taxa
Table 1. Micropalaeontological assemblage from analyzed samples of Stăniţa-Vlădnicele borehole
P
P
P
P
P
P
P
P
P
301
302
303
304
305
306
307
308
309
Uvigerina perornata Pischw.
P
310
X
Bulimina elongata d'Orb.
X
Globigerina brevispira Subb.
X
Orbulina universa d'Orb.
x
Cibicides dutemplei (d'Orb.)
x
Entoselenia marginata (W et B)
x
Melonis pompilioides F.et H.
x
Pullenia bulloides (d'Orb.)
x
Sphaeroidina austriaca d'Orb.
x
Spiroplectamina sp.
x
Quinqueloculina sp.
x
x
Cibicides lobatulus W.et J.
x
x
Cibicides badenensis d'Orb.
x
Quinqueloculina karreri Reuss.
Quinqueloculina consobrina d'Orb.
Articulina problema Bogd.
+
+
+`
+
+
+
+
+
×
+
+
+
+
+
+
Articulina sarmatica (Karrer)
Articulina glabra (Cushm.)
Elphidium macellum (F.et M.)
Elphidium minutum Reuss.
+
×
×
+
+
+
+
+
+
+
+
+
+
Draft copy
+
Elphidium punctatum
Elphidium crispum (Linne)
+
Elphidium aculeatum d'Orb.
Elphidium regina regina d'Orb.
+
+
+
+
+
+
×
+
+
+
+
+
+
+
+
+
+
+
×
+
+
+
+
+
+
+
+
+
+
Elphidium regina caucasica Bogd.
Porosononion subgranosus (Egger)
+
Porosononion martkobi Bogd.
+
Ammonia beccarii L.
Legend
+
× high frequency;
+
+
x
x
+ low frequency
Palynological study
Analysis of the pollen content from samples is the principal technique available for determining
vegetation response to past terrestrial environmental change. The technique has been in use for nearly a
century, initially as a method for investigating past climatic changes. More recently, the importance for
vegetation change of processes such as human impact, successional change and other biotic and abiotic
factors have been recognized. The palynological study was made using 10 collected from StăniţaVlădnicele borehole (RBN 4 borehole) from interval between 140 - 975 m (Fig. 2). The quantity of
sediments for analysis was approximately 50 g for each sample. Those have been treated with HCl (37%)
to remove the carbonate and afterward with HF (48%) to remove the silicate minerals. The separation of
palynomorphs from the residue resulted from the chemical reaction described above, was made with
centrifugal action using as heavy liquid ZnCl2 with density 2.00 g/cm3. The organic fraction resulted was
inserted in a mixture of glycerine and gelatine, 1-2 drops been mounted on the palynological shim. The
visualisation of the palynomophs was accomplished with a microscope with transmitted light Leica
DM1000, using the amplification of x100, x400.
Palynological assemblage
Palynological assemblage present in the Stănita – Vlădnicele borehole (Table 2) is represented
by a dinoflagelate assemblage (Operculodinium, Spiniferites, Spirogyra, Tytthodiscus) present in low
quantities and a continental assemblage with Gymnospermatophytae (Abiespollenites, Pityosporites,
Cedripites,
Inaperturopollenites,
Podocarpidites,
Zonalapollenites),
Angiospermatophytae
(Graminidites, Caryapollenites, Engelhardtioidites, Intratriporopollenites, Tricolporopollenites),
Pteridophytae (Laevigatosporites, Leiotriletes, Polypodiaceoisporites, Verrucatosporites). From
continental assemblage dominante are Gymnospermatophytae taxas (Pityosporites) and
Angiospermatophytae taxas (Caryapollenites and Tricolporopollenites).
Dinoflagellate assemblage. This assemblage is mainly composed from Operculodinium,
Spiniferites, Spirogyra and few reworked species of Phytoplankton. Higher percentage and diversity is
present in sample 303, from 485 m (Fig. 3). Operculodinium is generally reported as a cosmopolitan
species that might have low relative abundances in the tropics and high relative abundances in regions
with cold/temperate waters such as the North Atlantic (Wall et al. 1977; Marret & Zonneveld, 2003).
This species is distributed within a very broad range: temperature (-2.10 C and 29.60 C) and salinity
(16.1–36.8 0/00).
Continental assemblage. Ivanov et al., 2002, 2007, showed that vegetation of the middle and
upper Badenian of Forecarpathian basin (central Paratethys, NW Bulgaria) was characterized by regular
occurrence and abundance of thermophilous species whereas during Sarmatian, subtropical elements like
Engelhardia, Reevesia, Itea, Castanopsis, Symplocaceae, Arecaceae tend to decrease and temperate
elements such as Alnus, Carpinus, Betula, Corylus, Fagus have an increasing trend. A similar vegetation
change is observed in the Sarmatian deposits Stăniţa-Vlădnicele borehole. During Sarmatian favourable
conditions existed in the Forecarpathian Basin for the development of mixed mesophytic forest
characterized by predominance of warm-temperate and subtropical elements together with many
paleotropical elements. Based on the palynological assemblage we have separated following biocenosis
for continental palynomophs: swamp assemblage, mixed mesophytic forest, terrestrial herbs and ferns
assemblage (Fig. 3).
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Fig. 3 Main biocenosis from analyzed samples of Staniţa-Vlădnicele borehole (Diagram accomplished
with Tilia graph 2.0.2)
Draft copy
Swamp assemblage. Aquatic plants like Typha indicate the presence of freshwater in the
depositional environment. Swamp forest defines the lakeshore vegetation with moderate amounts of
Cupressaceae and a low amount of riparian genus Salix.
Mixed mesophytic forest is well represented by species of fossil pollen, such as Carpinus,
Quercus, Ulmus, Betula, Carya, Acer. Pinaceae is very abundant in the mesophytic forest. The ground
cover vegetation of mixed forest is made up of herbaceous plants and the presence of ferns indicate
humidity (Leiotriletes, Laevigatosporites, Polypodiaceoisporites a. o.).
Ferns assemblage is represented by Laevigatosporites, Leiotriletes, Polypodiaceoisporites,
Stereisporites a. o.
Herbs assemblage. This assemblage consists of seven taxa mainly constituted of ground-cover
vegetation in the mesophytic forest. Caryophyllaceae, and Chenopodiaceae are the dominant groups in
this assemblage.
Table 2. Palynological assemblage identified in Stăniţa-Vlădnicele borehole.
P
P
P
P
P
P
30
30
30
30
30
30
Phytoplancton
1
2
3
4
5
6
Deflandrea phosphoritica Eisenack 1938
(reworked)
Operculodinium sp.
P
30
7
P
30
8
P
30
9
P
31
0
x
x
x
Spiniferites sp.
x
Spirogyra sp.
x
Tytthodiscus sp.
x
x
x
x
Pteridophyta
Cicatricosisporites sp.
Echinatisporis sp.
Echinatisporis wiesaënsis KRUTZSCH
1963
Laevigatosporites gracilis WILSON –
WEBSTER 1946
Laevigatosporites haardti (POTONIE et VE
N. 1934) Th. et PFLUG, 1953 subsp.
haardti KRUTZSCH 1967
x
x
x
x
x
x
Laevigatosporites sp.
x
x
x
x
x
x
x
x
x
x
x
x
x
x
x
x
x
x
x
x
Polypodiaceoisporites sp.
Stereisporites sp.
x
Trilobosporites weylandi Döring 1965
Triplanosporites sinuosus (PFLUG. 1952)
TH. – PFLUG 1953
x
x
x
x
x
x
x
x
x
x
x
x
x
Verrucatosporites cf. favus POTONIE 1931
Gymnospermatophyta
Abiespollenites absolutus THIERGART
1937
Abiespollenites cedroides (THOMSON
1953) KRUTZSCH 1971
x
x
x
Leiotriletes wolffi wolffi KRUTZSCH 1962
Polypodiaceoisporites saxonicus
KRUTZSCH 1967
x
x
x
x
x
x
x
Leiotriletes sp.
Leiotriletes wolffi brevis KRUTZSCH 1962
x
x
x
x
x
x
x
Draft copy
Abiespollenites latisaccatus (TREVISAN
1967) KRUTZSCH 1971
x
x
x
Abiespollenites maximus KRUTZSCH 1971
x
x
x
x
Cycadopites miocaenica NAGY 1969
+
+
x
x
x
Piceapollis sp.
x
x
x
x
x
x
x
Pinuspollenites miocaenicus NAGY 1985
Pityosporites alatus (POTONIÉ 1931)
THOMSON et PFLUG 1953
Pityosporites cedrisacciformis KRUTZSCH
1971
Pityosporites insignis (NAUMOVA ex
BOLCHOVITINA 1953) KRUTZSCH
1971
Pityosporites labdacus (POTONIÉ 1931)
THOMSON et PFLUG 1953
Pityosporites microalatus (POTONIÉ 1931)
THOMSON et PFLUG 1953
Pityosporites minutus (ZAKLINSKAJA
1957) KRUTZSCH 1971
x
Pityosporites sp.
Podocarpidites gigantea (ZAKL. 1957)
NAGY 1985
Podocarpidites nageiaformis (ZAKL. 1957)
KRUTZSCH 1971
+
+
x
+
+
x
x
x
x
x
x
x
x
+
+
+
+
+
+
x
x
x
x
x
x
x
x
x
x
x
x
x
+
x
+
x
x
x
x
x
x
x
x
x
x
+
+
x
x
x
x
+
x
x
x
x
x
x
x
x
+
+
x
+
+
x
x
x
x
x
x
x
x
x
x
Sequoiapollenites minor KRUTZSCH 1971
x
x
x
+
x
x
x
x
x
x
x
+
x
x
x
+
x
x
x
x
x
x
x
x
Podocarpidites sp.
Sciadopityspollenites serratus (POTONIE
et VEN. 1934) THIERGART 1937
x
x
x
Pinuspollenites longus NAGY 1985
Zonalapollenites minimus KRUTZSCH
x
x
x
Inaperturopollenites sp.
Piceapollenites neogenicus NAGY 1969
Sciadopityspollenites sp.
Sciadopityspollenites varius KRUTZSCH
1971
x
x
x
Cedripites sp.
Cupressacites bockwitzensis KRUTZSCH
1971
Piceapollis praemarianus KRUTZSCH
1971
x
x
x
Cedripites miocaenicus KRUTZSCH 1971
Ginkgo sp.
Inaperturopollenites concedipites
(WODEHOUSE 1933) KRUTZSCH 1971
Inaperturopollenites hiatus (POTONIÉ
1931) THOMSON et PFLUG 1953
Inaperturopollenites microforatus
KRUTZSCH 1971
x
x
Abiespollenites sp.
Cedripites lusaticus KRUTZSCH 1971
x
x
+
x
x
x
x
Draft copy
1971
Zonalapollenites rueterbergensis
KRUTZSCH 1971
x
x
x
Zonalapollenites sp.
Zonalapollenites verrucatus KRUTZSCH
1971
x
x
x
x
x
x
x
+
Angiospermatophyta. Monocotyledonatae
x
Arecipites sp.
Graminidites media (COOKSON 1947)
POTONIÉ 1960
Graminidites sp.
Monocolpopollenites sp.
Monocolpopollenites tranquillus
(POTONIÉ 1934) THOMSON et PFLUG
1953
x
x
x
x
x
x
x
x
x
x
Typha angustifolia LESCHIK 1956
x
x
x
x
x
x
x
x
x
x
x
x
Angiospermatophyta. Dicotyledonatae
x
Aceripollenites rotundus NAGY 1969
Aceripollenites sp.
Alnipollenites verus (POTONIÉ 1931)
POTONIÉ 1934
Betulaepollenites betuloides (PFLUG 1953)
NAGY 1969
Carpinipites carpinoides (PFLUG 1953)
NAGY 1985
Caryapollenites simplex (POTONIÉ 1931)
KRUTZSCH 1960
Caryapollenites sp.
Chenopodipollis multiplex (WEYLAND et
PFLUG 1957) KRUTZSCH 1966
Cyrillaceaepollenites exactus (POTONIÉ
1931) POTONIÉ 1960
Cyrillaceaepollenites megaexactus
(POTONIÉ 1931) POTONIÉ 1960
Engelhardtioidites microcoryphaeus
(POTONIÉ 1931) THOMSON et
THIERGART ex POTONIÉ 1960
Ericipites ericius (POTONIÉ 1931)
POTONIÉ 1960
Eucommiapollis eucommi (PLANDEROVA
1990) PETRESCU 1999
x
x
x
x
x
x
x
+
x
x
x
x
x
x
+
+
+
+
+
+
+
+
+
+
+
+
+
+
+
+
+
+
x
x
x
x
x
x
x
+
+
+
x
x
x
x
x
+
+
+
x
x
x
x
x
x
x
x
x
x
x
Faguspollenites minor NAGY 1969
Faguspollenites sp.
Ilexpollenites margaritatus (POTONIÉ
1931) POTONIÉ 1960
Intratriporopollenites instructus (POTONIÉ
1931) THOMSON et PFLUG 1953
Juglanspollenites maculosus (POTONIÉ
1931) NAGY 1985
x
Juglanspollenites sp.
x
x
x
x
x
x
x
x
x
x
x
x
x
x
x
x
x
Draft copy
Liquidambarpollenites sp.
x
x
Magnolipollis sp.
Momipites punctatus (POTONIÉ 1931)
NAGY 1969
Myricipites bituitus (POTONIE 1931)
NAGY 1969
x
x
Platycaryapollenites sp.
Porocolpopollenites vestibulum (POTONIÉ
1931) THOMSON et PFLUG 1953
Pterocaryapollenites stellatus (POTONIÉ
1931) THIERGART 1937
x
+
x
+
x
+
x
x
+
+
x
+
+
Quercopollenites petrea NAGY 1969
x
Quercopollenites robur NAGY 1969
x
Quercopollenites sp.
+
x
x
x
x
Ulmipollenites undulosus WOLFF 1934
x
+
Zelkovaepollenites potoniéi NAGY 1969
+
Zelkovaepollenites sp.
+
x
+
Zelkovaepollenites thiergarti NAGY 1969
Gombaspora (Hyphomycetes)(Fung)
Legend: x low frequency
+
+
+
x
x
+
x
x
+
x
x
x
x
x
x
x
x
x
x
Tricolporopollenites sp.
+
x
x
+
x
x
x
+
x
x
Quercopollenites granulatus NAGY 1969
Salixipollenites helveticus NAGY 1969
Tricolpopollenites liblarensis (THOMSON
1950) THOMSON et PFLUG 1953 subsp.
Liblarensis
Tricolporopollenites cingulum (POTONIE
1931) THOMSON et PFLUG 1953 subsp.
pusillus (POTONIE 1934) THOMSON et
PFLUG 1953
Tricolporopollenites henrici (POTONIÉ
1931) KRUTZSCH 1960
Tricolporopollenites marcodurensis
PFLUG et THOMSON 1953
Tricolporopollenites microhenrici
(POTONIÉ 1930) KRUTZSCH 1960
x
x
x
x
x
x
x
x
x
+
x
+
x
x
+
x
x
+
+
+
+
+
x
+
+
x
x
x
x
x
x
x
x
x
x
x
+
+
x
+
x
x
x
+
x
x
x
x
+
+
x
+ high frequency
Conclusions
Micropaleontological assemblage identified in the analyzed samples from Stăniţa-Vlădnicele
borehole is assigned to Badenian (sample 310 from 975 m) and to Sarmatian (samples 301-309 from 140
to 975 m), been possible even an distribution on stages. The assemblage determined from sample 309
(950 m) can be attributed to Buglovian, samples 305-308 (from 550-895 m) are assigned to Volhynian
and samples 301-304 (from 140-550m) are attributed to Bessarabian.
Regarding palynological assemblage, subtropical elements like Engelhardia, Reevesia, Itea,
Castanopsis, Symplocaceae, Arecaceae tend to decrease and temperate elements such as Alnus,
Carpinus, Betula, Corylus, Fagus have an increasing trend. During Sarmatian favourable conditions
existed in the Forecarpathian Basin for the development of mixed mesophytic forests characterized by
predominance of warm-temperate and subtropical elements together with many paleotropical elements.
Based on the palynological assemblage we have separated following biocenosis for continental
Draft copy
palynomophs: swamp assemblage, mixed mesophytic forest, terrestrial herbs and ferns assemblage.
Dinoflagelate assemblage is represented by Operculodinium, Spiniferites, Spirogyra and few reworked
species of Phytoplankton with higher percentage and diversity is present in sample 303, from 485 m.
Acknowledgements
This work has been supported by Romanian Ministry of Education, Research and Innovation under a
PN-II-IDEI No. 975/2008 research grant, directed by prof. dr. Mihai Brânzilă. Gabriel Chirilă wants to
thank to dr. Daniel Tabara to given help in the preparation and determination of palynomorphs.
References
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Plates caption
Plate I
1-3. Melonis pompilioides (Ficht. et Moll). 1. Side view x315; 2. Detail view of fig. 1 x800; 3. Edge view
x340
4. Pullenia bulloides (d’Orb). Edge view x550
5. Sphaeroidina austriaca d’Orb. x360
6. Cibicides pachiderma (Rzehak). Side view x600
7. Cibicides dutemplei (d’Orb). Side view x420
8. Ammonia beccarii (Linne). Side view x440
Plate II
1, 2. Cibicides badenensis (d’Orb). (1. Side view x600; 2. Edge view x560;)
3. Cibicides lobatulus (Walker & Jacob). Side view x400.
4-6. Quinqueloculina karerri Reuss. (4. Apertural view x760; 5. side view x400; 6. Detail of fig 5
x1300)
7. Articulina problema Bogd. Side view x180.
8. Elphidium minutum (Reuss). Side view x500.
9. Elphidium macellum Fichel et Moll. Side view x340.
10. Elphidium crispus (Linne). Side view x300.
Plate III
1-6. Porosononion subgranosus (Egger). 1, 3, 4, 5 Side view (fig 1 x650, fig. 3 x450, fig. 4. x540, fig. 5.
x500); 6. Detail of fig 4. X1000; 2. Edge view x400)
7. Elphidium aculeatum d'Orbigny. Side view x420.
8. Elphidium regina caucasica Bogd. Side view x220.
9. Elphidium regina regina (Linne). Side view x200.
10. Porosononion martkobi (Bogd). Side view x200.
Plate IV
1.Tytthodiscus sp.
2.Zonalapollenites verrucatus KRUTZSCH 1971
3-6.Zonalapollenites neogenicus KRUTZSCH 1971
7. Abiespollenites latisaccatus (TREVISAN 1967) KRUTZSCH 1971
8. Pityosporites labdacus (POTONIÉ 1931) THOMSON et PFLUG 1953
Plate V
1.Quercopollenites robur NAGY 1969
2.Quercopollenites petrea NAGY 1969
3, 5-8. Quercopollenites sp.
4. Quercopollenites robur NAGY 1969
9. Pityosporites macroinsignis KRUTZSCH 1971
10. Pityosporites pristinipollinius (TRAV. 1955) KRUTZSCH 1971
11. Pityosporites insignis (NAUMOVA ex BOLCHOVITINA 1953) KRUTZSCH 1971
12. Pityosporites labdacus (POTONIÉ 1931) THOMSON et PFLUG 1953
13. Podocarpidites gigantea (ZAKL. 1957) NAGY 1985
14. Podocarpidites piniverrucatus KRUTZSCH 1971
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