GEOLOGIJA 25/2, 213—227 (1982), Ljubljana
UDK 561:551761(497.12) = 836
Quantitative palynologîcal analysis of Julian clastic rocks
from the lead-zinc deposit of Mežica
Kvantitativna palinološka analiza
julijskih klastičnih kamenin v mežiškem rudišču
Bogomir Jelen
Geološki zavod, 61000 Ljubljana, Parmova 37
Janko Kušej
Rudnik in topilnica svinca Mežica, 62392 Mežica
Abstract
The calcareous-dolomitic sequence of the Karnian at Mežica is inter-
bedded with three horizons of clastic rocks. Through the palynological
assemblages of the 1st horizon a deltaic environment is reflected; spores
of pteridophytes being abundant. An ammonoid biocoenose, reported from
this horizon previously, may possibly not be autochthonous. The 2nd hori-
zon is characterized by the spores of mangrove trees. In the 3rd horizon
xerophytic elements prevail. By the frequency distribution of spores, pol-
len, and acritarchs a decreasing deltaic influence and an ever increasing
marine influence is indicated from the 1st through the 2nd to the third
horizon. By the combination Camerosporites secatus and Ovalipollis pseu-
doalatus the northern belt of the equatorial Karnian palynofloristic do-
main is recognized.
Kratka vsebina
V zaporedju apneno-dolomitnih plasti karnijske stopnje v Mežici so
trije horizonti klastičnih kamenin. Palinološki facies 1. horizonta kaže na
okolje rečne delte. Vsebuje veliko spor pteridofitov. Amonoidna bio-
cenoza, o kateri poročajo v literaturi, pa verjetno ni avtohtona. Za drugi
horizont so značilne spore vegetacije mangrova. V 3. horizontu prevladu-
jejo kserofitni elementi. Iz pogostnosti spor, peloda in akritarhov izhaja,
da je vpliv rečne delte na sedimentaci j o postopno ponehaval od prvega
prek drugega do tretjega horizonta in da je v tej smeri naraščal vpliv
morskega okolja. Camerosporites secatus in Ovalipollis pseudoalatus po-
menita, da je bila v karnijski dobi Mežica del severnega pasu širokega
ekvatorialnega palinoflorističnega območja.
214 Bogomir Jelen & Janko Kušej
Introduction
Mežica lead-zinc mine is situateci north of the Periadriatic lineament in the
eastern part of the Northern Karawanken Alps (fig. 1). In the Karnian deposits
of this region carbonate rocks - limestone and dolomite - prevail. Between the
carbonates maries, shales and sandstones are interbedded. These clastic rocks
have played an important role in the genesis of ore as well as in tectonic move-
ments. The miners called them "Cardita" and/or "Raibler" beds (A. Z o r c , 1955).
There are three horizons of clastic rocks, recently designated as the 1st, 2nd
and the 3rd shale. Since the lithology of the 1st, 2nd and the 3rd shale is not
uniform it is however incorrect to apply the term "shale". I. Struci (1971)
mentioned in the "shales" the following types of rocks: shales, maries, marly
limestone and sandstone. For this reason in this paper the terms 1st, 2nd, and
the 3rd shale are changed into the 1st, 2nd and the 3rd clastic horizon.
Not only in the mining area but also in the Northern Karawanken Alps
as a whole, these horizons are playing an important role in the stratigraphi-
cal subdivision of Karnian rocks (fig. 2). Because the tectonic setting is rather
complicated the stratigraphical and structural position of individual clastic
horizons is usually not clear, even when rare micro- or macrofossils occur.
The problem of the stratigraphical and structural position is well marked
in exploration boreholes where a small part of rock is examined.
In the Mežica mining area there are still many unsolved geological problems.
For example the clastic horizon bordering the lead-zinc deposit Graben to the
south has an unknown stratigraphical and tectonic position. The question is
whether the ore bearing reef limestone occurs in normal or in inverse position,
and whether it is Cordevolian or Julian in age. A reliable answer to this question
is important for the mining development in this area.
There are more problems in the southern part of the Northern Karawanken
Alps where a lagoonal facies of Longobardian and Karnian age passes laterally
into a deeper facies — the Partnach facies. In the absence of realistic criteria
it has always been very difficult to correlate chronostratigraphically both facies.
Because of the possibilities of palynology in Triassic stratigraphy, we intro-
duced palynological research as an aid to the solution of geological problems,
important for the mining development.
Quantitative palynological analysis
Palynological research of the three clastic horizons in the Mežica mining area
includes both qualitative and quantitative analysis. A paper on the qualitative
analysis is in preparation.
The quantitative analysis is based on relative frequencies of morphological
groups of palynomorphs. This method was introduced by H. Visscher and
C. J. van der Zwan (1981). Histograms, corresponding to each of the clastic
horizons are presented in fig. 2. The observed range of relative frequencies for
each morphological group is shown in fig. 3. Additional statistical analysis is in
progress. However, the information so far available about the quantitative distri-
bution of palynomorphs in the three clastic horizons in the Mežica mining area
is already a sufficient base for their stratigraphical subdivision on a local scale.
Quantitative palynological analysis of Julian clastic rocks from Mežica
215
The histograms of fig. 2 represent the most characteristic examples of rela-
tive frequencies of morphological groups of palynomorphs found in assemblages
from each of the three clastic horizons.
The histograms (N = 5) from the 1st clastic horizon are characterized by the
bimodal distribution of morphological groups of palynomorphs. The highest peak
is on the side of the typical hygrophytic elements. The small peak is found on
the side of xerophytic elements.
Fig. 1. Geology (after I. Struci, 1970) and location of the palynological
samples examined in the Mežica mine
SI. 1. Geologija (po I. Štruclu, 1970) in lokacija palinoloških vzorcev
v mežiškem rudniku
1 Upper Miocene beds
Zgornjemiocenske plasti
2 Mezozoic beds
Mezozojske plasti
3 Palynologically examined area
Palinološko raziskano področje
4 Paleozoic mica schist, phyllite and greenschist
Paleozojski sljudni skrilavec, filit in zeleni skrilavec
5 Porphyritic dacite
Porfiritni dacit
6 Tonalité
Tonalit
7 Diabase
Diabaz
8 Granodiorite
Granodiorit
9 Erosional unconformity
Erozijska diskordanca
10 Fault with down thrown side
Prelom z ugreznjenim krilom
11 Overthrust
Nariv
216 Bogomir Jelen & Janko Kušej
A Monolete acavate spores
Monoletne akavatne spore
B Trilete acavate laevigate or apiculate spores
Triletne akavatne levigatne in apikulatne spore
C Trilete acavate murornate spores
Triletne akavatne murornatne spore
D Trilete cingulate and zonotrilete spores
Triletne cingulatne in conotriletne spore
E Aratrisporites group
Skupina Aratrisporites
F Porcellispora complex
Porcellispora kompleks
G Monosulcate pollen grains
Monosulkatni pelod
H Ovalipollis complex
Ovalipollis kompleks
I   Alete (proto) bisaccate pollen grains
Aletni (proto) bisakatni pelod
J  Samaropollenites
K Taeniate (proto) bisaccate pollen grains
Teniatni (proto) bisakatni pelod
L Triadispora complex
Triadispora kompleks
M Vesicate pollen grains
Vezikatni pelod
M фт-otoì monosaccate pollen grains
'■"'^roto) monosakatni pelod
O rircumpollis group
Circumpollis skupina
U Leiosphaeridia
V Micrhystridium
Z  Dictyotidium
Y Veryhachium
U V Z Y Microphytoplankton — Acritarchs
Mikrof itoplankton — akritarhi
Hygrophile elements
Higrofilni elementi
A B C D E F GIH I JIK L M N O
Xerophile elements
Kserofilni elementi
Fig. 2. Relative frequency distribution of the morphological groups of palynomorphs
from three clastic horizons in the Mežica ore deposit (Code of the samples examined:
M—7/+549, II/l and III/l).
Method introduced by H. Visscher and C. I. van der Zvann (1981) Columnar section
after J. Kušej
SI. 2. Porazdelitev relativnih frekvenc morfoloških skupin palinomorf iz treh klastič-
nih horizontov mežiškega rudišča (Oznake vzorcev: M—7/ + 549, II 1 in III/l).
Metoda po H. Visscherju in C. I. van der Zwannu (1981). Stratigrafsko zaporedje po
J. Kušeju
Quantitative palynological analysis of Julian clastic rocks from Mežica
217
218
Bogomir Jelen & Janko Kušej
The histograms (N = 3) from the 2nd clastic horizon are characterized by
a third peak represented by the morphological group E (Aratrisporites). The
prominence of the first and the second peaks varies considerably within indi-
vidual assemblages. The peak of morphological group E is always very high.
The histograms (N = 3) from the 3rd clastic horizon are characterized by
the absence of a peak on the side of the typical hygrophytic elements. The
increase of the relative and the absolute frequency of the microphytoplankton
is a new characteristic of this horizon.
Fig. 3. Range of variation of the relative frequency for morphological groups of palynomorphs
from the clastic horizons at Mežica
SI. 3. Variacij ske širine relativne frekvence morfoloških skupin palinomorf iz klastičnih hori-
zontov v Mežici
From the quantitative analysis we may conclude that the morphological
groups of palynomorphs A, B, E, G, M, N, O, V, Z have a constant distributional
trend from the 1st through the 2nd to the 3rd clastic horizon (fig. 3). The clear-
ness of this trend is obscured by the range of variation of the relative frequency
for morphological groups from the 2nd clastic horizon (for example morpholo-
gical group A) as well as by the range of variation of relative frequency of
morphological group in samples taken just under the top of the 1st clastic hori-
zon (for example maximum values of the relative frequency of groups M, N, and
O). We believe that this irregularity could well be caused by the unstable-transi-
tional-conditions in the time between deposition of the 1st and the 3rd clastic
horizon.
The relative frequency of morphological groups A, B, and G is decreasing
from the 1st to the 3rd clastic horizon. On the other hand the relative frequency
of groups M, N, O, V, Z is increasing in the same direction. Stratigraphical
discrimination between the 1st and the 3rd clastic horizon is possible on the base
of the relative frequencies of morphologicah groups A, B, N, O, and Z. Additio-
Quantitative palynological analysis of Julian clastic rocks from Mežica
219
naly we can use the maximum values of the relative frequency of groups G, M,
V. The 2nd clastic horizon is discriminated from the 1st and the 3rd horizon by
the value of the relative frequency of the morphological group E.
Distributional trends of spores, pollen grains and acritarchs from the 1st
through the 2nd to the 3rd clastic horizon is shown on a diagram of mean
values of relative frequencies (fig. 4). The prevailing hygrophytic elements in the
1st clastic horizon reflect the existence of a fluviatile-deltaic environment and
we can speculate about a strong influence of this environment on the sedimen-
tation of the 1st clastic horizon. Among the hygrophytic elements spores of
pteridophytes, typical for the coal facies of the Alpine Lunz beds and the Ger-
manic "Schilfsandstein" are dominant. The Lunz beds and the "Schilfsand-
stein" represent a fluviatile-deltaic coal-bearing facies within an arid climatic
Fig. 4. Distribution trend of spores, pollen and acritarchs in the direction from
the 1st towards the 3rd clastic horizon interbedded in the limestone and
dolomite succession at Mežica
SI. 4. Tendenca v porazdelitvi spor, peloda in akritarhov od 1. proti 3. klastič-
nemu horizontu v Mežici
220 ^ Bogomir Jelen & Janko Kušej
belt (H. Visscher & C. J. van der Zw ar, 1981, 632). A regional arid
background is evident by the small peak on the side of xerophytic elements. The
relative frequency of hygrophytic and xerophytic elements in the 2nd clastic
horizon varies considerably. From the information on fig. 3 one may deduce
interruptions in the regime of fluviatile-deltaic environment. The peak of the
xerophytic elements is sometimes rather prominent. The absolute frequency of
xerophytic elements is also increasing. The peak of the Aratrisporites group
suggests optimal conditions for the flourishing of lycopodiophytic mangrove
vegetations, a new environment during the time of sedimentation of the 2nd
clastic horizon.
The hygrophytic elements strongly decrease in the 3rd clastic horizon. Here
we can always find a large peak on the side of the xerophytic elements. The
elements of an upland flora and the flora of salt swamps of undoubted or
presumed coniferalean affinity prevail. Our conclusion is that the fluviatile-
-deltaic regime had disappeared.
Relative and absolute frequencies of acritarchs are increasing from the 1st
through the 2nd to the 3rd clastic horizon (figs. 3, 4). The formgenera Leiosphae-
ridia and Micrhystridium are supposed to have lived in more agitated water
near the coastline (I. K. L e n t i n & G. L. W i 11 i a m s , 1980, 13; F. L. S t a p -
lin, 1961, 397). The first-mentioned authors also suggest that Leiosphaeridia
and Micrhystridium characterize the beginning and the end of transgressions,
the formgenus Veryhachium is not present in the 1st clastic horizon. According
to A. Horowitz (1975, 75) this formgenus inhabited a more open, shallow
and quiet marine environment. Some palynologists (W. A. B r u g m a n) state
that the formgenus Dictyotidium had the same ecological preference as Very-
hachium. According to the distribution of spores, pollen grains and acritarchs
in the 1st, 2nd and the 3rd clastic horizon it is supposed that the marine influ-
ence during the time of sedimentation of the 1st clastic horizon was subordinate.
The marine influence was increasing in the 2nd clastic horizon, and completely
prevails in the 3rd clastic horizon.
We expect that the research of oxygen and carbon isotope composition of
the rock and the macrofauna from the three clastic horizons will confirm the
picture as based on the distribution of spores, pollen grains and acritarchs.
From the 1st clastic horizon ammonoids are known (A. Ramovš, 1974,
128; B. Jurkovšek, 1978). Not only the present palynological but also
sedimentological investigations (M. Pungartnik et all., in preparation)
question the autochthonous nature of this ammonoid biocoenose.
Palynological assemblages of the three clastic horizons belong to the northern
palynofloras of the wide equatorial palynofloristic domain. These assemblages
are characterized by the Camerosporites secatus-Ovalipollis pseudoalatus asso-
ciation (H. Visscher & C.J. van  der Zwan, 1980,629).
Conclusions
(1) We can use the distribution of relative frequencies of morphological
groups of palynomorphs for the palynostratigraphical discrimination of the
three clastic horizons on a local scale. (2) The possibility of a palynostratigraphi-
cal discrimination may be practically applied with regard to the solution of stra-
Kvantitativna palinološka analiza julijskih klastičnih kamenin v Mežici 221
tigraphical and tectonic problems related to mining geology. (3) Hygrophytic
elements from the 1st clastic horizon, among which the spores of pteridophytes
typical for the coal bearing facies of the Lunz beds and the "Schilfsandstein"
prevail, reflect a fluviatile-deltaic environment. (4) By the frequency distri-
bution of spores, pollen grains, and acritarchs an decreasing deltaic influence
and an ever increasing marine influence is indicated from the 1st trough the
2nd to the 3rd horizon. (5) A new environment is reflected in the 2nd clastic
horizon by the flourishing of a mangrove vegetation. (6) The influence of the
fluviatile-deltaic regime disappears at the end of the 3rd clastic horizon. (7) At
the time of deposition of the 3rd horizon prevail the xerophytic elements of an
upland flora and the flora of salt swamps with an undoubted or presumed
coniferalean affinity. (8) There is a question, whether the ammonoids from
the 1st clastic horizon represent an autochthonous biocoenose. (9) Palynological
assemblages belong to the northern palynofloras of the equatorial domain of
Ladinian-Karnian times.
Acknowledgments
One of the authors (B. Jelen) obtained a scholarship from the Govern-
ment of the Netherlands for study at the Laboratory of Paleobotany and Paly-
nology, State University of Utrecht. He received much aid from the staff and
students. He has benefited greatly from the courtesy and kind advice of mentors
Prof. Dr. H. Visscher, Dr. W. A. Brugman and Dr. R. E. B e s e m s.
They transmited their original ideas to him without any hesitation.
Kvantitativna palinološka analiza
julijskih klastičnih kamenin v mežiškem rudišču
Povzetek
V mežiškem rudišču se večkrat srečujemo s problemom določitve prave
geološke lege določenih plasti. Kot primer naj navedemo problematiko v zvezi
z nezanesljivo stratigrafsko uvrstitvijo klastičnega pasu, ki omejuje rudišče
Graben proti jugu. бе vedno je sporno, ali gre v tem rudišču za normalno lego
rudonosnega grebenskega apnenca pod klastičnim horizontom, ali za inverzno.
Možnih je več interpretacij, ni pa potrebno posebej poudarjati, kako pomembna
je za nadaljnje raziskave stratigrafska uvrstitev rudonosnega grebenskega
apnenca.
Se več problemov se pojavlja v južnih delih severnih Karavank, kjer lagunske
karbonatne sedimentne kamenine langobardske in cordevolske podstopnje za-
menjujejo globokomorski sedimenti partnaškega faciesa. Kjer so te sedimentne
kamenine v stiku z julijskimi plastmi, je njihova stratigrafska razmejitev pro-
blematična.
Da bi prispevali k reševanju geološke problematike, smo se lotili kvantita-
tivne palinološke analize klastičnih horizontov v krovnini rudonosnega apnenca
mežiškega rudišča. Pripravlja pa se tudi kvalitativna analiza inventarja (B. Je-
len & J. Kušej neobjavljeno poročilo).
Uporabljena kvantitativna metoda temelji na določevanju relativnih frek-
venc morfoloških skupin palinomorf. Metodo sta uvedla H.  Visscher in
222 Bogomir Jelen & Janko Kušej
C. J. van der Zwan. Ustrezni histogram je za vsak klastični horizont pri-
kazan na si. 2. Variacijska širina vrednosti relativne frekvence posameznih
morfoloških skupin palinomorf pa je dana na si. 3. Statistična analiza je še v
delu. Toda že sedanja stopnja poznavanja kvantitativne porazdelitve palinomorf
v treh horizontih klastičnih kamenin mežiškega rudišča je omogočila njihovo
razlikovanje na lokalnem nivoju tudi v primerih, ko njihov stratigrafski položaj
ni bil določen.
Na si. 2 vidimo histograme, ki kažejo značilno porazdelitev morfoloških
skupin palinomorf v klastičnih horizontih julijske podstopnje na območju
mežiškega rudišča.
Za histograme 1. klastičnega horizonta (N = 5) sta značilna dva viška; prvi,
večji, na strani tipičnih higrofitnih elementov in drugi, manjši, na strani tipič-
nih kserofitnih elementov.
V histogramih 2. klastičnega horizonta (N = 3) se pojavi še tretji višek.
Velikosti prvega in drugega viška sta lahko zelo razli.čni. Tretji, ki ga da
morfološka skupina E, je vedno visok.
Za histograme 3. klastičnega horizonta (N = 3) je značilno, da nimajo več
viška tipičnih higrofitnih elementov. Dvig relativne frekvence mikrofitoplank-
tona je naslednja značilnost 3. klastičnega horizonta.
Kvantitativna analiza je pokazala, da imajo morfološke skupine palinomorf
A, B, E, G, M, N, O, V, Z stalno porazdelitveno tendenco, ki je vidna iz zbirnega
diagrama variacijskih širin na si. 3. Razločnost porazdelitvene tendence v smeri
od 1. proti 3. klastičnemu horizontu motijo variacijske širine relativne frek-
vence morfoloških skupin v 2. klastičnem horizontu (npr. morfološka skupina
A 2. klastičnega horizonta) in relativne frekvence morfoloških skupin tik pod
krovnino 1. klastičnega horizonta (npr. maksimalne vrednosti morfoloških sku-
pin M, N, O). Motnje so verjetno posledica nestabilnih — prehodnih — razmer
v dobi med 1. in 3. klastičnim horizontom. Za morfološke skupine A, B, G je
značilno upadanje relativne frekvence od 1. proti 3. klastičnemu horizontu,
medtem ko relativna frekvenca morfoloških skupin M, N, O, V, Z v isti smeri
narašča.
1. in 3. klastični horizont se ločita med seboj po relativnih frekvencah mor-
foloških skupin A, B, N, O in Z. Dodatno so uporabne tudi visoke vrednosti
relativnih frekvenc G, M in V. Drugi klastični horizont se loči od prvega in
tretjega po vrednosti relativne frekvence morfološke skupine E.
Porazdelitveno težnjo spor, peloda in akritarhov od 1. proti 3. klastičnemu
horizontu kaže diagram srednjih vrednosti njihove relativne frekvence na
si. 4.
V prevladovanju higrofitnih elementov v 1. klastičnem horizontu se odraža
močan vpliv fluviatilno-deltnega okolja na sedimentacijo. Med elementi pre-
vladujejo spore pteridofitov, tipične za premogov facies, npr. za lunškega ali
schilfsandsteinskega, ki sta fluviatilna faciesa aridnega klimatskega pasu
(H. Visscher & C. J. van der Zwan, 1981, 632). V manjšem višku na
strani kserofitnih elementov in v njihovi majhni absolutni frekvenci se odra-
ža vpliv aridnega zaledja.
Vrednosti relativne frekvence higrofitnih in kserofitnih elementov v drugem
horizontu so zelo različne. Slika 3 kaže, da je v času njegove sedimentacije
ponehaval vpliv fluviatilno-deltnega okolja. Zato se višek na strani kserofitnih
Kvantitativna palinološka analiza julijskih klastičnih kamenin v Mežici 223
elementov poveča, na levi pa zmanjša. Poveča se tudi absolutna frekvenca ksero-
fitnih elementov. Veliki višek skupine Aratrisporites, tj. spor likopodofitov,
tvorcev vegetacije mangrova, kaže na optimalno okolje za njihov razcvet, torej
na novo okolje.
Higrofitni elementi so popolnoma nazadovali v času sedimentacije 3. klastič-
nega horizonta. Veliki višek se preseli na stran kserofitnih elementov. Prevladu-
jejo elementi kopenske flore in flore slanih močvirij, ki bi mogli pripadati
iglavcem. Vpliv fluviatilno-deltnega okolja na sedimentacije je prenehal.
Relativna in absolutna frekvenca akritarhov naraščata od prvega proti tret-
jemu horizontu (si. 3 in 4). Oblikovna rodova Leiosphaeridia in Micrhystridium
sta značilna za energijsko razgibani priobalni pas in naj bi označevala začetek
in konec transgresije (J. K. Lentin & G. L. Williams, 1980,13; F. L.
S t a p 1 i n, 1961, 397). Oblikovni rod Veryhachium v 1. horizontu ne nastopa.
Veryhachium je značilen za bolj odprto plitvo mirno morsko okolje (A. H o r o -
witz, 1975, 75). Nekateri raziskovalci so mišljenja, da je imel oblikovni rod
Dictyotidium podobno ekološko preferenco (W. A. Brugman, v razgovoru).
Na podlagi porazdelitve spor, peloda in akritarhov predpostavljamo, da je bil
morski vpliv v času sedimentacije prvega klastičnega horizonta neznaten.
Porastel je v drugem in je bil najmočnejši v tretjem horizontu.
V 1. klastičnem horizontu so našli amonite (A. Ramovš, 1974, 128;
B. Jurkovšek, 1978). Vendar palinološko-facialne in sedimentološke
(Pungartnik et all., v pripravi za tisk) raziskave nasprotujejo možnosti
obstoja avtohtone amonitne biocenoze v 1. klastičnem horizontu.
Združba peloda v julijskih klastičnih horizontih mežiškega rudišča pripada
severnemu pasu širokega ekvatorialnega palinoflorističnega področja karnijske
dobe, ki ga karakterizira palinoflora Camerosporites secatus-Ovalipollis pseudo-
alatus. Na jugu meji na osrednji pas mešane palinoflore z elementi severnega
in južnega ekvatorialnega pasu Camerosporites secatus-Ovalipollis pseudoalatus-
- Samar opollenites speciosus, ki se razteza čez južno in zahodno obrobje Paleo-
tetide (H. Visscher & C. J. van  der Zwan, 1981, 629).
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224 Bogomir Jelen & Janko Kušej
Plate 1 — Tabla 1
1. Leschikisporis aduncus (morph. gr. A) X 600
2. Aulisporites astigmosus (morph. gr. B) X 600
3. Rogalskaisporites cicatricosus (morph. gr. C) X 900
4. Camerozonosporites rudis (morph. gr. D) X 600
5. Aratrisporites sp. (morph. gr. E) X 600
6. Porcellispora sp. (morph. gr. F) X 600
7. Cycadopites sp. (morph. gr. G) X 900
8. Ovalipollis pseudoalatus (morph. gr. H) X 600
morph. gr. = morphological group — morfološka skupina
Plate 1 — Tabla 1
2 — Geologija 25/2
226 Bogomir Jelen & Janko Kušej
Plate 2 — Tabla 2
1 Alete (proto) bisaccate pollen grain (morph. gr. I) X 600
Aletni (proto) bisakatni pelod
2 Lunatisporites acutus/noviaulensis (morph. gr. K) X 600
3 Enzonalasporites vigens (morph. gr. M) X 600
4 Patinasporites densus (morph. gr. N) X 600
5 Paracirculina maljawkinae (morph. gr. O) X 600
6 Leiosphaeridia sp. (morph. gr. U) X 600
7 Micrhystridium sp. (morph. gr. V) X 600
8 Veryhachium sp. (morph. gr. Y) X 900
9 Dictyotidium tenuiornatum (morph. gr. Z) X 600
morph. gr. = morphological group — morfološka skupina
Plate 2 — Tabla 2