The Inoceramus Beds from the quarry in Szymbark, near Gorlice.

The Inoceramus Beds from the quarry in Szymbark, near Gorlice.
'Y
Maria Dylqianka
Printed in: Roanik Polskiego Towarzystwa Ceologicznego, vol. 1 (for the years 1921 and 1922), pp. 36-81.
Krak6w, 1923.
The age of the Inoceramus beds (formally
known as Ropianka beds) is one of the most
convoluted problems in Carpathian stratigraphy. Beginning in the seventies, depending on
ongoing exploration, the age definition of
these beds had undergone many revisions
mainly because of the controversial relation of
the Inoceramus beds to the Paleogene. They
were assigned consecutively to the Eocene, to
the Neocomian, and to the Late Cretaceous.
This problem has not been resolved to this
day. The Late Cretaceous age used by Walter
and Dunikowski in eighties is commonly
accepted. Uhlig, following the work of Paul,
Thietze, and Vacek, first assumed an Early
Cretaceous age, but finally accepted a Late
Cretaceous age as determined by Polish Geologists, with the assumption that the relationship of the Inoceramus beds to Eocene is not yet
resolved. Aside from difficulties resulting
from assigning these beds to the Tertiary
(accordingto most Polish Geologists they form
an inseparable complex of beds [with the
Cretaceous]), there is the problem of the presence of smaller and larger Znoceramus fragments in the Inoceramus beds. This gives support to the theory of secondary redeposition.
Prof. Grzybowski, conditionally accepting
this theory, was inclined to date the Inoceramus beds from the Gorlice region as Eocene
based on microfauna that shows similarity
with the Eocene oil-bearing beds in the vicinity of Krosno, so long as future micropaleonto-
logical investigations could better resolve this
problem.
Based on observations of the Cenomanian
Inoceramus beds in Muntigl, where large Znoceramus with thin tests occur in soft marly
shales, Prof Szajnocha (1898) concluded:
"there are indeed among the flysch deposits
real Znoceramus layers and these layers must
belong to the Cretaceous if we want to exclusively restrict the presence of these rather
different Znoceramus in this period". Therefore, Szajnocha as well as Grzybowski believed that the presence of the Znoceramus in
the Carpathian flysch can be either
autochthonous or redeposited. It would only be
necessary to distinguish the horizons with
autochthonous Znoceramus from those with
redeposited ones. The fauna from Leszczyny of
WiSniowski (19071, comprised mainly of
Senonian ammonites such as Pachydiscus neubergicus and Scaphites constrictus, helped
resolve many of the uncertainties connected
with the age of the Inoceramus beds in the
Carpathians. However, WiSniowski also recognized the Lower Paleogene in these beds. He
disproved the theory of redeposited Inoceramus in his study area by pointing out that
complete shells of Inoceramus salisburgensis
occur in the deposits in the vicinity of
Dobromil and PrzemySl. However, the age of
the Inoceramus beds in the middle and western
Carpathian remains an open question.
Maria Dylqianka
During holiday trips initiated by Dr W.
Kutniar, I was able to find numerous larger
and smaller fragments of Inoceramus shells in
the quarry in Szymbark. This inspired me to
also collect a few samples of the shales that
occur interbedded between sandstones where
the lnoceramus where found, and study the
microfauna of these beds. In this study I present the current state of my analysis of this
microfauna. Before I begin, I wish to thank
the Director of the Geological Department,
Prof. Szajnocha, for his help and encouragement. I will keep in deep memory the genuine
interest and much advice given by the late
Prof. Grzybowski throughout the course of this
study. Dr. Premik is acknowledged for making
the drawings of the foraminifera.
Geologic setting and lithology of the quany in
Szymbark.
The quarry in Szymbark is situated a half a
kilometre from the Gryb6w-Gorlice road on
the left side of the Bielanski stream, next to
the place where the road coming from
Bielanki village crosses the stream from the
left to the right bank for the first time, a good
distance below the 340 m elevation marker. In
this 16 m high quarry, the Inoceramus beds are
exposed as sandstones and shales interbedded
in six layers'. Their dip is southeast 2S0 3S0
(20-21 hours). In the stream the layers from
the quarry are exposed, as well as older beds
lying at the base of the section with the same
dip, and together with the quarry section
they comprise a single unit.
The shales are interbedded with hieroglyphic sandstones (hieroglyphs on the lower
side) of the shelly type, fine-grained, with
large quantities of mica, repeating six times.
The alterations of shales and sandstones here
are quite distinct. The shales are marly, especially in the lower layers, the upper layers
become more sandy. These also contain some
-
I cannot find any reference to this quarry in the
literature. Szajnocha, in his explanations to his
geological atlas, mentions the Inoceramus beds in
the Bielanski stream, which is above this quarry.
mica. In the lower layers, the sandstones are
thickly-bedded and in the upper part thinly
bedded. In addition, layers four, five and six
of the shales contain thin sandstone interbeds.
Some of these interbeds contain plant detritus.
The colour of the shales is as follows: the
shales of the first two layers are relatively
thinner than the others and are dark gray;
shales of the third layer are brownish-gray,
transitional, and the shales of layers four,
five and six are yellowish-brown. The dark
gray shales have a white coating.
Sandstones interbedded with the dark
gray shales are also dark gray with a white
coating. Sandstones interbedded with the yellowish-brown shales have the same colour
and no coating. The lower sandstones are more
marly, rather hard, and resistant to weathering. The upper sandstones belonging to the
shaly type are weakly lithified. In some of
these parts, the sandstones break into a thin
sheets parallel to bcdding. Among shales as
well as sandstones, there are parts covered
with fucoids. Finally, shales and sandstone
react in HC1, although not always clearly,
and the sandy-marly shales from the upper
layers remain inactive?
The layers at the base of the section, similar to the ones from the quarry, contain a gray
sandstones interbedded with gray shales with
a uniform petrographical character. The
shales that dominate in these deposits are
more clayey then the ones from the quarry and
at places they grade into clays. Sandstones
are hard, and covered with a few small
hieroglyphs. Neither shales nor sandstones
contain any fossils except for a few
foraminiferas. Despite very careful analysis
of this material I did not find not even minute
fragments of lnoceramus shells, whereas in
the quarry they are common. The Inoceramus
[at this point, Dylazanka devotes two pages to
describing the composition of aulhogenic mineral
graim dispersed within the claystones. Because this
description has no bearing on the paleontological
part to follow, it was ornilled from this tramlation.]
In these sandstones, I found a well-preserved
specimen of Spirophyton, 15 cm in diameter.
Szymbark
beds extend a few hundred meters upstream
from the quarry, but this is not the case in the
downstream direction. Here, a few paces from
the quarry on the left bank of the stream, next
to the small bridge, red shales are visible
lying almost horizontally. Farther downstream on the right bank, the same red shales
are exposed intercalated with green, hard,
compacted sandstones with numerous minute
hieroglyphs on their upper surfaces. The
sandstones and red shales exposed in the
stream lie almost horizontally.
The tectonics in this particular area is not
clear to me. By the stream below the quarry
(downstream) for a distance of 150 m, as well
as on the hillside where the quarry is located,
the Inoceramus beds are exposed. Next to the
side road leading to the main road the beds
(dip unknown) have a different appearance. It
looks as if the Inoceramus beds were thrusted
over the younger red, Eocene shales. The layers from the quarry would belong to the overthrusted part. Only studies of the larger area
will solve this problem.
Inoceramus in the Szymbark layers.
"In the deposits rich in fossils the resence of
rneano n or more new form. has no siJcant
ing, description and labeling of incom lete specimens could even be destructive. lfut in the
rocks so poor in fossils as the Inoceramus beds
of the Ca athians, each of the recopwed specimens c a x a v e double meaning pa eontolo 'cal
and stratigraphical."(Friedberg 1907, p. 6#
In the sandstones lying interbedded with the
shales, numerous larger and smaller fragments
of Znoceramus can be found. Larger and more
numerous Znoceramus occur in the upper sandstone layers. A large, incomplete shell, covered with characteristic hieroglyphs, was
preserved on the upper surface of a relatively
hard plate of sandstone. The specimen is not
preserved well enough to be identifiable, but
the thickness of the shell and its size is significant considering that we are dealing with
an incomplete specimen. The length of the
shell is 13 cm,the width 12 cm, the thickness
near the top, where it is the largest, is up to 2
mm and closer to the edges of the shell 0.7 to
199
0.9 mm. In respect to the thickness of the
shell, this specimen resembles Znoceramus
cripsi Mant. reported by Friedberg from the
Inoceramus beds in the vicinity of Rzesz6w.
The size of a specimen from Kwiaton which
Prof. Szajnocha calls "huge" agrees more or
less with the specimen from Szymbark. Additionally, in the same yellowish brown sandstones I found a fragment of the shell of this
Inoceramus of a significant thickness with
preserved ornamentation in the form of parallel thicker and thinner costae similar to Znoceramus salisburgensis from the Inoceramus beds
in Muntigl, which are presently dated as
Upper Senonian (Pachydiscus neuergicus).
The thickness of the fragment from Szymbark is 4 mm, therefore one of the largest
known. The size of the fragment is not important because the thickness as well as its width
is 4 an.Judging from the size of the shell the
specimens must belong to the large ones.
Numerous, smaller fragments have shells 0.5 3.0 mm thick. The Znoceramus from Muntigl
near Salzburg reach a significant size up to 20
an diameter and have thin shell up to 3 mm.
They occur in the marly shales which
excludes the hypothesis of their redeposition
which Prof. Szajnocha (1898) strongly
emphasizes.
How can the hypothesis of redeposited
Znoceramus in the Inoceramus beds from
Gorlice (Grzybowski, 1901) be applied to the
deposits from the quarry in Szymbark? In the
Szymbark quarry, in the sandstones interbedded with shales smaller and larger fragments
of Znoceramus occur. They are better preserved
in the upper part in thickly bedded sandstones
as well as in the uppermost, thinly bedded
sandstones that often are intercalated with
shales. In the shales I did not find any larger
fragments of Znoceramus, but in the processed
material from all the shale layers I found
numerous crystals of aragonite that could well
be nothing more than fragments of Znoceramus
preserved in the form of loose rhombic prisms,
to clusters comprised of few to many crystals. I
do not have complete, well-preserved shells
such as in the material from Muntigl, but it is
difficult to assume that in the 16 m thick beds,
200
Znoceramus were found entirely as a result of
redeposition, especially since in the upper
portion of the quarry shell fragments are more
abundant and better preserved than in the
lower sandstones layers.
Layers of gray sandstone intercalated
with gray clayey shales (which dominate
over sandstones) located at the base of the
quarry and also outcropping in the nearby
Bielanka stream, appear to be without any
fossils. In the complex of the basal layers, I
did not find even a trace of Znoceramus. How
then could redeposited Znoceramus be found in
the younger beds in the quarry, if they were
not present in the lower, older layers that
have no fossils except for a sparse microfauna?
These findings do not question the presence of
the redeposited Znoceramus fragments in the
Carpathian flysch in general, but at least in
the quarry in Szymbark this theory is ruled
out.
Now I would like to present the compilation of the results of the paleontological studies of the foraminifera from this quarry. First,
I present the list of all the species found in the
individual layers [Table 11 and then a table
containing the comparisons of the
foraminifera from the quarry in Szymbark
with the foraminifera from other localities
[Table 21.
General paleontological character of
foraminifera.
The foraminifera1 material is comprised of six
samples (one sample per layer). The samples
from the first two layers were significantly
smaller than the one from the upper layers,
which is due to the smaller number of specimens in the first two layers. The samples from
the layer I and 2 were rather difficult to process, they had to be soaked for a long time and
boiled several times; other samples were
much easier to prepare. The preservation of
foraminifera from Szymbark is in general
quite good, but in several cases tests are secondarily compressed and deformed. It especially
pertains to the genus Reophax and Trochammina. Test of the genus Globigerina are very
Maria Dylqianka
well preserved; they are the best preserved
specimens in this material.
In the foraminifera1 material from Szymbark the following families were present:
Miliolidae, Astrorhizidae, Lituolidae, Textularidae, Lagenidae, Globigerinidae, Rotalidae and Nummulitidae. Out of these only
Astrohizidae, Lituolidae and Globigerinidae
are abundant. The remaining five families are
rather poor in the number of genera and
species as well as the total number of specimens. Miliolidae are represented only by two
genera: Nubecularia and Spiroloculina, of
which Nubecularia has only one species and
only a few specimens. Species of these two
genera are mainly present in the two upper
layers and are known only from the Inoceramus beds, namely: Spiroloculina inclusa was
first described by Grzybowski from the Inoceramus beds from Gorlice, and Spiroloculina
waageni by Schubert from the Inoceramus beds
from Gbellan.
Textularidae are also poor in the number
of genera and species, occurring only in two
genera and two species, and are present in even
fewer numbers than Spiroloculina. Both of
these species (Bulimina preslii and
Caudryina trochus) are known from the Inoceramus beds as well as from the Upper Cretaceous of the Bavarian Alps. They are therefore important in t m s of their occurrences.
Lagenidae are represented by few forms,
which are mostly cosmopolitan. Rotalidae
are present as only one genus and one specimen.
This specimen is strongly pyritized, and
unidentifiable. Nummilitidae are represented
by only one species, Operculina cretacea,
which is known from the Cretaceous.
The remaining three families, Astrorhizidae, Lituolidae and Globigerinidae,
are represented by the largest number of
species and specimens. Astrorhizidae are present in four genera and 14 species, of which
D e n d r o p h r y a has three species, R h a b dammina has four, Bathysiphon has one, and
H y p e r a m m i n n has the most species.
Hyperammina is also the most abundant form,
especially H . subnodosa and H . grzybowskii
n.sp.. Grzybowski regarded Hyperammina to
Szymbark
Table 1. List of species found in each layer.
202
Maria Dylqianka
Table 1. [continued].
-
ROTAI-IDAE:
Operculina cretacea Reuss
i
I
Szymbark
Table 2 Foraminifera from the quarry in Szymbark compared with other localities.
203
204
Table 2 [continued].
Maria Dylqianka
Szymbark
be a rare form in the Inoceramus beds near
Gorlice, but in Szymbark it is one of the most
common forms. Among the common cosmopolitan forms in Szymbark are Rhabdammina
linearis and Bathysiphon filiformis, the latter of which is known mostly from the
Cretaceous.
Lituolidae, as in the Inoceramus beds near
Gorlice where they comprise of 61% of all
species, also belong to the most abundant in
terms of species and sometimes specimens in
the deposits from Szymbark. Here belong 47
speaes in six genera, which constitutes more
than half of all the species, with Reophax,
Ammodiscus, and Trochammina being the most
abundant. Reophax placenta is the most abundant species in the Reophax group, except in
the lowest gypsum-bearing layers, where the
number of species and specimensis poorer. This
pattern can be traced to all the groups of
foraminifera with the exception of Globigerinidae. Ammodiscus incertus is the most
abundant in its group, much the same way as
in the Inoceramus beds in the vicinity of
Rzesz6w and Debica. In general, most of the
Ammodiscus speaes resemble their counterparts from the Inoceramus beds of Gorlice,
with the possible exception of Ammodiscus
glomeratus, which in this material displays
more variety in its construction, sometimes
taking on strange shapes.
Genus Trochammina counts for 18 (or 33%)
of all the species of Lituolidae, but the actual
number of specimens is rather poor. The excep
tion is Trochammina coronata and Trochammina contorta that are more abundant, especially the former. Trochammina contorta,
according to Grzybowski, is the most common
form found in the Inoceramus beds near
Gorlice. Friedberg also calls it a "not uncommon" form. In the deposits from Szymbark it
belongs to the average as far as the frequency
of occurrences is concerned. Haplophragmium
and Cyclammina are among the least common
forms.
Reussina, one of the most interesting
groups as far as the overall construction is concerned, resembling the shape of Globigerinae,
is present in here in all its four currently-
205
known species, but it is not abundant in terms
of number of specimens. In the Inocerarnus beds
near Gorlice studied by Grzybowski, this
group is missing. Friedberg in his study of the
Inoceramus beds from the vicinity of Rzesz6w
and Debica cited only one species. The agglutinated forms described above mostly belong to
the benthonic forms. There is one more group
that needs to be discussed, of planktonic character - the Globigerinidae - typical for this
formation since its major stage of development
occurs in the Cretaceous. This family occurs
only in the top two layers, in the shales intercalated with gypsum, and is represented by
eight species, of which three of them,
Globigerina cretacea, Globigerina linneana,
Globigerina aequilateralis, are known mainly
from Getaceous. According to the newer literature (Schubert, 19021, several of them, such
as Globigerina cretacea, are present in Upper
Cretaceous. Egger cites eight species of
Globigerina from the Upper Cretaceous of
Bavaria, of which five of them are also
present in the deposits from Szymbark. Considering the number of specimens, this family
occurs rather commonly, in particularly when
one accounts for the fact that they belong to
the smaller forms, and as such could easily be
lost during washing or overlooked during picking stages. Some of the specimens can be pyritized as well, which was observed in a few
specimens of Globigerina bulloides and
Discorbina. In case of the first species, the
pyritization process was just beginning, but the
calcareous test of Discorbina was already
fully pyritized.
The dependence of foraminiferal test material
on the chemical composition of the sediment.
Friedberg, using HCL on his foraminiferal
material, proved that material that did not
react in HCL did not contain forms with calcareous tests and inversely. The best proof of
this can be provided by an analysis showing
the percentage composition of CaC03 in sediments where the foraminifera are present
(this was already suggested by Friedberg in
Maria Dylqianka
206
his study of the foraminifera from the Inoceramus beds in the vicinity of Rzesz6w and
Debica), since the HCL method will not tell us
anything about the quantitative composition
of the rocks. I intend to perform these analysis
in the future. In the material from Szymbark,
even without any chemical analysis, a striking relation is visible between the petrographical character of the rock and its faunal
contents.
In layers 1 and 2, which are of a darkgray colour, clayey-marly, and contain gypsum, which proves that this rock contains
CaC03 (in :his case in shales), calcareous
forms occur alongside a poorer number of
siliceous and agglutinated forms, equally
with respect to the number of species and specimens. In layer 1,26 species occur out of which
33% are calcareous forms. In layer 2, out of 30
species 25% consists of calcareous forms. In the
next layer, number 3, which is intermediate
between layers 2 and 4 (it shows traces of gypsum) out of 37 species only two are calcareous
forms or 5%. In the following layers, which
are clayey-sandy, with yellow-brown colour,
where not even a trace of gypsum can be found,
the calcareous forms are do not occur, and
exclusively siliceous and agglutinated forms
are present. In layer 4, I counted 44 species,
and in layer 5, 38 species, all with siliceous
and agglutinated tests. Only in the last layer,
layer 6, I found one calcareous species, Operculina cretacea, out of the 31 species present
there.
Distinction of two facies.
Based on the petrographical and faunal composition of the deposits from Szymbark, two
facies can be distinguished: a deep-water
facies, with its dark gray, clayey-marly
shales with a Globigerina fauna (open seas),
and a shallower-water facies with clayeysandy near-shore sediments with an agglutinated fauna. Layer 3 would represent the transitional stage between the deep-water and
shallow-water stages, which is consistent
with miaofaunal trends. Inoceramus, which
live in the shallower seas, and are present in
numerous fragments, larger and better preserved in the upper layers in the quarry, represent facies that give evidence of a shallowing and strongly oscillating (thin intercalation of sandstones) sea level.
Therefore the deposits from Szymbark can
be used to show a whole number of oscillation
in sea level, which are connected with the
tectonic movements in this geosyncline area.
During this process the Inoceramus sea was at
times spreading over a wider and deeper area,
and at other times becoming shallower, taking
on the trait of a more near-shore area.
Continuing oscillation in the positive and
negative directions can also be demonstrated
in the sandstones intercalated with the
shales. The lower sandstones are more marly,
the upper ones more sandy and thicklygrained, similar like the shales.
Furthermore, the Inoceramus sea must
have belonged to the colder type of seas,
which is supported in the character of the
miaofauna, consisting largely of agglutinated
forms. Most likely, at that time there must
have been a connection in the form of some
kind of bay between the Inoceramus sea,
which was a part of the geosyncline, and
therefore of the type of southern seas, and the
cold, northern seas. Today the agglutinated
forms of Trochammina, Reophax, Rhabdammina, commonly present in the deposits in
Szymbark, are mainly known from the depths
below 1000 m or from the shallower depths up
to 200 m in the arctic seas. Depending on the
temperature of the seas, this forms live either
at deeper or shallower depths.
General conclusions
Of 82 species of foraminifera, 13 (or 17%)
have calcareous tests, the rest have agglutinated tests. This relationship changes only in
the lower gypsum-bearing layers, where
mostly calcareous forms occur.
The foraminiferal fauna from Szymbark
most closely resembles the flysch faunas in
general, therefore it can be best compared
with other fauna from the Inoceramus beds,
especially those regarded as belonging to the
Szymbark
Upper Getaceous. Today, we have three studies on the foraminifera from the Inoceramus
beds. These are the works of Grzybowski
(19011, Friedberg (19011, and Liebus and
Schubert (1902).
Studies have also been carried out on the
Tertiary: two by Grzybowski (1896 and 18981,
one by Schubert from Bolognano (1902) and
Noth (1912) from Komamok. Considering the
Globigerinidae family that occurs in the
Lower gypsum-bearing layers I also take into
comparison the study by Egger (1899) on the
Upper Cretaceous from the Bavarian Alps and
for the same reason I also take into account the
Getaceous of Lvov.
I am especially concerned with number of
occurrences in common. In the Inoceramus beds
near Gorlice out of 100 species (99 siliceous, one
calcareous) there are 39 forms in common with
Szymbark. In the Inoceramus beds in the vicinity of Rzeszbw and Rbica out of 92 species (46
calcareous, 48 siliceous) there are 31 common
forms with Szymbark. In the Inoceramus beds
from Gbellan out of 100 species (20 siliceous, 80
calcareous) there are nine forms in common.
From the Upper Cretaceous from Bavaria out
of 448 species (only 64 siliceous) we have 15 in
common. From this compilation of common
occurrences it is clear that the 40% of common
species occurs with the Inoceramus beds near
Gorlice, 33% with the beds in the vicinity of
Rzeszdw and Dgbica, but this relation is
affected by the fact that almost half of the
forms from there are calcareous. I£ we compare
only the relationship of the siliceous forms
from Szymbark and the forms from Rzeszbw
and Dgbica then we have 55% in common. In
the layers from Gbellan the smallest number
of forms in common forms were found, but
among them are important ones that identify
the Cretaceous formation, such as Globigerina
cretacea and Globigerina linneana. The same
is true about the relationship of Upper Cretaceous from Bavaria to the deposits in Szymbark. Among the common forms, the more important are found, such as Globigerina
cretacea, G. linneana, G. aequilateralis, and
others. In summary, the whole group of
Globigerinidae, except for Globigerina
207
inflata, occurs in the Upper Cretaceous from
the Bavarian Alps.
How does the fauna in Szymbark correlate
with the known faunas from the Tertiary
flysch? In the oil-bearing deposits near
Krosno out of 105 species (23 calcareous, 82
siliceous) there are 34 in common. In the red
clays in Wadowice out of 112 species (50calcareous, 62 siliceous) there are 21 common
forms. From the lower Tertiary of Bolognano
out of 28 species (six calcareous, 22 siliceous),
nine are in common. In the red clays in
Komarnok out of 30 species (three calcareous,
27 siliceous), there are 10 common forms. These
Tertiary faunas (with the exception of
Wadowice 28%) have 35% of the forms in
common. This compilation proves that the
fauna in Szymbark most closely resembles the
fauna of the Inoceramus beds from Gorlice,
Rzeszow and Debica. The fauna from Szymbark can also be compared with the one from
the oil-bearing deposits in the vicinity of
Krosno. Now, if we separate the individual
species according to the formation in which
they occur, assuming that the Inoceramus beds
belong to the Cretaceous, out of 70 species
(including 12 new species) the following relationship is present: 48 species are known from
the Cretaceous, other formations and the
Recent (which is more than half), 13 species
are known only from the Cretaceous, five
species are from Tertiary, and four species
come from Tertiary and modem faunas. Therefore, the forms from the Cretaceous and other
formations greatly outnumber the others, similar as in Friedberg's fauna, where out of 92
species, 44 were known from the Cretaceous
and other formations. Friedberg had 22
species that occur in Tertiary and the modem
seas, therefore significantly more then found
in Szymbark. Only an insignificant number of
species in Szymbark occur only in Tertiary.
Now, I will summarize how other authors
interpreted the age of the Inoceramus beds in
general. Szajnocha, in the VI notebook for the
Geological Atlas of Galicia (p. 1371, remarked
that the Inoceramus beds in general "based on
the newer fossils found, mostly outside
Galicia, are tentatively assigned to the mid-
208
d!e Cretaceous and younger". Grzybowski, in
his work on Inoceramus beds near Gorlice, at
first stated:
"the Lower Cretaceous Carpathian deposits contain Inocemus, at least in some stages, then it is
probable that the deposits paleontologically
determined as belonging to the Lower Cretaceous
lie underneath the younger Carpathian deposits
over a large area, beginning insilesia, up to their
last-documented point at Dobmmil; that the
Inocemmus beds underwent a tmnsgression, as
determined at one locality, where their base is
visible overlying the Lower Cretaceous deposits,
and that the later could constitute the base of
these deposits. Finally, that we have many sites
where Inocemmus fragments occur as a result of
the secondary deposition. Taking into considemtion all of the above, we cannot either ignore or
categorically contradict the fact that the
Inoceramus from the Ropianka Beds in Gorlice
indicate secondary redeposition, hence we can
place them entirely in the Eoaene."
In conclusion, he stated the following:
"1.The Inocemmus beds cannot be differentiated
at the top from the d clays and the nummulite
layers, the age of which was paleontologically
determined as late Eocene. And together with
these beds they display petrographical and
faunal continuity, fonning in its entire thickness
a unified, inseparable complex. 2. The
Inocemmus beds must belong to the lower Eocene
and Upper Senonian."
Friedberg, based on his foraminiferal fauna
from the Inoceramus beds in the vicinity of
Rzeszow and Debica, which shows transitional traits between the Cretaceous fauna
from the Bavarian Alps and the fauna of the
Inoceramus beds near Gorlice, stated the following:
"I must note, that I am not able to solve the question of the age of the Ropianka beds, because the
result of my comparisons is that foraminifera, as
long-lived forms, are not useful for determining
the age of sediments.
The results of my work suggest, that even if we
attempt to use foraminifera for correlation of
Maria Dylqianka
sediment horizons, they do not contradict the
supposed Cretaceous age for the Ropianka
beds. However in this case, it would be best
assign them a Late Cretaceous age." Schubert
dated the deposits from Gbellan as Late Cretaceous, based mainly on the planktonic forms
such as Globigerina cretacea, Globigerina linneana and Pseudotextularia striata.
Wisniowski (1905) goes furthest in his
conclusions narrowing the age limits of the
Inoceramus beds
'Therefore, not only in the vicinity of Dobmmil,
and also in the Pnemysl and Jamslaw district,
we will look for the Cenomanian in the lowest
layen of the cement-like, fukoidal marls, but not
in the Inoceramus-bearing sandstones which
constitute, in addition to the upper Senonian,
also the Danian, and perhaps even the oldest
layers of Paleogene".
In conclusion, for the Inoceramus beds in
Dobromil as well as in the adjacent parts of
the Carpathians, in contrary to Szajnocha's
opinion, we must accept a scheme wherein the
lower, marly part of this deposits is dated as
probably Cenomanian, and certainly Turonian
and Senonian, up to and including the Pachydiscus neubergicus Zone; the upper part of the
sandstones, with Paleogene variegated clays
at the top matches the uppermost layer of the
Pachydiscus neubergicus Zone and the Danian
stage, and most likely also the oldest Paleogene. Regarding Grzybowski's interpretations,
despite the fad that I did not find the contad
of the Inoceramus beds with the nummulite
sandstones outside the quarry in Szymbark, I
dismiss the theory of redeposited Inoceramus
in these deposits. This would require the
deposits from the quarry to be dated as late
Senonian and early Eocene.
The deposits in Szymbark resemble the
sandy-shaly type of deposits from Dobromil
studied by WiSniowski, who dated this horizon as late Senonian with Pachydiscus neubergicus including in it the Danian together with
the ("most likely") oldest level of the Paleogene. WiSniowski suggests that "detailed
studies of the foraminiferal fauna of the uppennost layers of the Inmramus beds, exclud-
Szymbark
ing the red clays of Paleogene age, should
provide an answer", if the Inoceramus beds extend beyond the Upper Cretaceous up to the
lower Paleogene. If we accept Wi§niowskils
hypothesis for the deposits in Szymbark then
we must make an assumption. I do not want to
extend the age of the upper layers of the Inoceramus beds (of the sandy-shaly type) up to
the Paleogene. These and especially the uppermost ones constitute uniform deposits without any trace of Nummulites. If we accept an
earliest Eocene age for the uppermost layers in
the quarry, we would also have to accept insitu deposition of Inoceramus in the early
Eocene. This would even further convolute the
already difficult Carpathian stratigraphy.
The next question, what should be done
with the lower layers from the quarry, which
show facies differences with the upper layers,
including a different type of fauna with the
characteristic Globigerinidae such as Globigerina cretacea, G. linneana, G. aequilateralis,
all regarded in the literature as Cretaceous
forms cited from the Cenomanian of the
Bavarian Alps (Egger, 1899). They should be
placed among the fucoid marls, which are
dated by Wisniowski as Cenomanian to Senonian up to the Pachydiscus neubergicus Zone,
and probably in the uppermost part of this
group, most likely in the uppermost part of
the Lower Senonian.
In conclusion, two horizons can be distinguished in the deposits in Szymbark: a lower
one with gypsum-bearing, marly shales dominated by the family Globigerinidae (probably
the upper part of the lower Senonian) and an
upper level with sandy shales with the
siliceous fauna and well preserved Znoceramus
fragments (probably upper Senonian and
Danian according to WiSniowski). No doubt,
more micropaleontological studies of the beds
overlying and underlying the beds from the
quarry are needed to better understand the
stratigraphy of the Inoceramus beds4
[Nanr&ossil assemblagesfrom Dylazanka's
original samples (kindly analysed by Dr. Jackie
Burnett, UCL) are comprised of solution-resistant
SYSTEMATICPALEONTOLOGY
Family MILIOLIDAE
1. Nubecularia t i i i a Jones and Parker
Construction agrees with Brady's descriptions.
Several specimens found in layers 3 and 6.
2. Spiroloculina inclusa Grzybowski
Agrees with Grzybowski's description. Few
specimens found in layers 1,2 and 6. Known
only from the Inoceramus beds near Gorlice.
3. Spiroloculina w a a g e n i Liebus arid
Schubert
Test construction the same as in Liebus and
Schubert's descriptions. The texture of the test
resembles a calcareous form. Two specimens
found in layer 1.
4. Spiroloculina sp. aff. S. arenaria Brady
pl. 1, fig. 1
This form closely resembles Spiroloculina
arenaria Brady. Test elongated, flattened,
extending into a long neck. On the periphery,
below the neck, is a distinctive depression.
Similar depression can be found in Spiroloculina arenaria but not as pronounced. Individual segments are not visible from the outside due to the agglutinated texture, similar
as in S. arenaria. The main difference is the
acute periphery, which in S. arenaria is subacute. Size: 0,4 mm. Specimen found in layer 4.
Family ASTRORHIZIDAE
5. Dendrophrya excelsa Grzybowski
Construction the same as in Grzybowsfi:is
species. Length up to 2 mm; width 0.5-1.0 XI r
Schubert includes in this species Dendrophryn
latissima and Dendrophrya robusta, pointing
out that the thickness and width of the test
wall cannot be used as distinctive traits.
Rather common, test fragments occur in all the
layers in Szyrnbark.
Upper Cretaceousspecies with Micula staurophora
and Lucimrhabduv cayeuu'i, indicating that the
Imeramus be& in the quarry section are no older
than Santonian.]
210
6. Dendrophrya latissima Grzybowski
Several specimens found in fragments up to 2
1/2 mm long in all layers. They agree with
the one described by Grzybowski but are narrower. Width: 0.4-1 mm, thickness: 0.2-0.3
mm.
7. Dendrophrya robusta Grzybowski
Rather common, test fragments found in all
layers in Szymbark except layer 2. Agrees
with the one described by Grzybowski.
Width: 0.6-1.8 mm; length: 1-3 mm. Friedberg
separated as var. maxima the very wide
forms (up to 2 mm). I do not agree with this,
since in Dendrophrya robusta the thickness of
the wall, not the width of the test (which
varies among different specimens), is the
distinctive trait.
8. Rhabdammina linearis Brady
Test construction as in the forms described by
Brady. Length 0.6-2 1/2 mm, width 0.24.4
mm. Found in all layers, rather mmmon.
9. Rhabdammina abyssorum M. Sars
Specimens in Szymbark resemble Grzybowski's drawings and descriptions, less so
Brady's because the ramifications are not very
pronounced, perhaps because this species was
found only in fragments. Width 0.34.5 mm,
length 0.6-1.3 mm. Found in all layers except 1
and 2.
10. Rhabdammina subdiscreta Rzehak
Test construction resembles that of Rzehak's
species. Width 0.4 length 0.9-1.2 mm. Several
specimens found in layer 3 and 4.
11. Rhabdammina sp.
pl. 1, fig. 2
Test tubular, large, built of very large
siliceous grains, which makes the surface very
coarse and rough, much more so than in other
species of Rhabdammina. Test even, in crosssection the inner channel shows deep constrictions. Rather broad channel. Test wall is very
thick. I found only one fragment in layer 5,4.5
mm long and 0.8 nun wide. This form resembles
Rhabdammina linearis Brady in its outer test
Maria Dylqianka
construction, and Hyperammina su bnodosa in
the construction of its inner channel. This last
trait brings this form closer to Astrorhiza
crassatina Brady.
12. Hyperammina noda ta Grzybowski
Test construction resembles forms described by
Grzybowski. Length 0.8-1.2 mm, width 0.10.25 mm. Found in a few fragments in layer 4.
13. Hyperammina subnodosa Brady
Test construction resembles that of Brady's.
Width 0.34.7 mm, length 1.3-3.0 mm. Rather
common, found in all layers except layer 1.
14. Hyperammina grzybowskii n.sp.5
Many fragments of this species were found in
all the layers in Szymbark, which makes it
possible to separate this form as a new
species. Because Grzybowski found only one
fragment in the Inoceramus beds near Gorlice,
he did not designate the new species but only
described and illustrated this form.
Fragments found in Szymbark have tubular, flattened, siliceous tests with a glossy
smooth surface. The test widens and narrows
into a flask-shape form. This process is
repeated several times at regular intervals. In
the middle of the test is a longitudinal
depression. The chamber interior, as seen on
glycerine slides, coincides with it. I took the
liberty of calling this species Hyperammina
grzybowskii. Length 0.5-3 1/2 mm, width 0.20 5 mm.
15. Hyperammina dilata ta Rzehak
Test construction agrees with Rzehak and
Grzybowski's descriptions. Several specimens
found in layer 4.
16. Hyperammina vagans Brady
In test construction resembles Brady's form.
Rare fragments found in layer 5 and 6.
Schubert proposes, without explanation, to
remove Hyperammina vagans from Hyper-
[This species was designated the type species of
fhe genus Silicotuba Vialov,1966.1
Szymbark
ammina and place it in Girvanella. Because in
this material H. vagans is found only in fragments, I cannot make this kind of judgement.
17. Hyperammina excelsa nsp.
pl. 1, fig. 3
In the deposits in Szymbark small forms are
commonly found that differ in construction
from Hyperammina. Test smooth, with glossy
texture, comprised of a row of equal size, uniserial, pear-shaped, broadening, chambers
narrowing strongly in their initial part. The
walls of test, as seen on glycerine slides, are
very thin. The inner channel is extremely narrow, and barely visible only in glycerine.
Common, 1
4chambered fragments 0.3-1.4mm
long and 0.3-0.4 mm wide are found in all
layers except layer 1 and 2.
18. Bathysiphon filiformis Sars
In test construction resembles Egger and
Schubert's descriptions. In loose fragments 0.81mm wide and 1-6mm long found in all layers
except for 1 and 2.
Family LITUOLIDAE
19. Reophax placenta Grzybowski
Test construction the same as in Grzybowski's
form. Commonly found in all layers in Szymbark. Known from many other localities in the
Inweramus beds, such as vicinity of Rzeszbw,
Debica, Gbellan and Gorlice.
20. Reophax difflugiformis Brady
Test built in two varieties resembling Grzybowski and Friedberg's forms. Rare, found in
all layers except layer 3.
21. Reophax grandis Grzybowski
In test construction resembles Grzybowski's
descriptions. Several well preserved specimens found in layers 4,s and 6.
22. Reophax duplex Grzybowski
Found in a few varieties (the same as those of
Grzybowski and Noth), rather common in all
layers in Szymbark.
211
23. Reophax guttifera var scalaria Grzybowski
The form from Szymbark does not resemble
closely the one described by Grzybowski. It
differs above all in its conical shape. Schubert
also questions Grzybowski's designation but
due to scarce and poorly preserved material
did not make a new one. For this reason the
material from Szymbark cannot be used for a
new designation. Found in all layers except
layer 1.
24. Reophax pilulifera Brady
In test construction agrees with Brady's
descriptions. Common in layer 3 to 6.
25. Reophax scorpiurus Montfort
Test construction the same as Brady's. Only
one specimen found in layer 3.
26. Reophax bacillaris Brady
On the outside the individual chambers are
only slightly noticeable. This distinguishes
this form from the one described by Grzybowski from the Inweramus beds of Gorlice. In
glycerine, inner chambers connected by channels are clearly visible. A rare form, found in
layer 2 and 3.
27. Reophax nodulosa Brady
Test built like in Brady's form with the exception of Brady's chamber being more elongated
that the one from Szymbark. A rare form,
found only in layer 3.
28. Reophax triloba nsp.
pl. 1, fig. 5
Test siliceous, surface rather smooth, comprised of three flat, discoidal chambers
arranged in a spiral. On the last, the largest
chamber on its periphery there is a aperture
in a form of a neck.In respect to its construction
scheme, this form varies from other forms of
Reophax. The individual chambers resemble
Reophax placenta Grzybowski in their degree
of compression. Width 1.2 mm, length 0.9 mm.
One well preserved specimen was found in
layer 5.
Maria Dylqianka
212
29. Reophax placenta Grzybowski var. globulosa n.var.
pl. 1, fig. 6
Test siliceous, almost spherical, on both sides
slightly concave in the middle. Built of a
coarse sand grains, loosely cemented, with a
rough surface. This form best resembles
Reophax placenta Grzybowski, but it differs
in its almost spherical shape and rough surface. Size 0.6-0.9 mm, thickness 0.4-0.7 mm.
Rather common, found with Reophax placenta
in all layers except 1 and 2.
30. Reophax duplex Grzybowski var. acuta
n.var.
pl. 1, fig. 4
Test siliceous, surface smooth, comprised of
two chambers, a larger, spherical one and
smaller acute one at the distal end. Both
chambers are flat, attached at the edge. In
numbers of chambers, this form resembles
Reophax duplex Grzybowski. Length 1.5 mm.
A single well preserved specimen was found in
layer 5.
31. Haplophragmium latidorsatum Hantken
Specimens from Szymbark are slightly flattened, but fully resemble Egger's description.
Found in layers 2,3 and 6.
32. Haplophragmium terquemi Berthelin?
This form agrees with Egger's description.
Found in layer 4.
33. Haplophragmium canariense d'Orbigny
Test construction the same as in Brady's forms.
Several specimens found in layer 2.
34. Reussina bulloidifomis Grzybowski var.
a
This and similar forms were separated from
Haplophragmium by Grzybowski and placed
in a separate subgenus Reussina. In their construction they resemble Globigerina, especially Globigerina bulloides. This raises the
question is Reussina just a siliceous form of
Globigerina.Two specimens were found in layers 3 and 6.
35. Reussina bulloidifomis Grzybowski var /3
Test constructed the same way as Grzybowski's form. Several specimens found in
layers 2 and 4.
36. Reussina quadriloba Grzybowski
Test constructed as in Grzybowski's form. One
specimen found in layer 4.
37. Reussina sp.
pl. 1, fig. 7
On one side three spherical chambers
arranged in a clover leaf, on the other two
small, flat chambers are visible in the middle. This form resembles best Reussina trifolium, but due to the lack of literature ated
by Schubert I cannot be certain. On one side
this form also somewhat resembles Reussina
quadrilobum and Reussina bulloidiforme var /3
but on the other it differs in the number of
chambers and smooth surface. Size 0.8 mm. A
single specimen found in layer 3.
38. Ammodiscus tenuissimus Grzybowski
Test construction as in Grzybowski's description. Common, found in all layers in deposits
in Szymbark.
39. Ammodiscus glomeratus Grzybowski
Test construction as in Grzybowski's description. Rather common, found in all layers.
40. Ammodiscus incertus d'Orbigny
All forms have great number of whorls, up to
10. Otherwise test built as in Haeusler's
forms. Found in layers 34.
41. Ammodiscus incertus Parker and Jones
Test construction resembles that of Brady's
forms. One well preserved specimen found in
layer 4.
42. Ammodiscus gordialis (Jones and Parker)
Construction of the test somewhat different
than Brady's type, but displays coiling like a
ball of yarn, that goes in two opposing directions. Great differences are observed in the
construction of the test among various specimens. Rare, found in layers 2,3 and 4.
Szymbark
construction of the test among various specimens. Rare, found in layers 2,3 and 4.
43. Ammodiscus irregularis Grzybowski
Test construction agrees with Grzybowski's
description. A single well preserved specimen
found in layer 4.
44. Ammodiscus angustus Friedberg
Test constructed as in Friedberg's forms. Several specimens were found in layers 3,4 and 6.
45. Ammodiscus latus Grzybowski
Constructed the same way as Grzybowski's
forms. Several specimens found in all layers.
46. Ammodiscus septatus Grzybowski
Test built like Grzybowski's forms. The new
species Ammodiscus karpathicus described by
Noth from the red clays in Barwinek and
Komarnok appears to be Ammodiscus septatus.
On both sides the last whorl has this
constriction typical for the species. Rather
common in Szymbark, found in layers 1 and 5.
47. Ammodiscus pusillus Geinitz
Construction the same as in Haeusler's type.
Ammodiscus serpens, described by Grzybowski
appears to me to be identical with
Ammodiscus pusillus. Rather common, found in
all layers except layers 1 and 3.
48. Trochammina pauciloculata Brady
In most cases tests are highly deformed, and
they agree with Brady's forms only in the
number of chambers. Rare, found in layer 4 and
5.
49. Trochammina intermedia Rzehak
Specimens from Szymbark mostly resemble
forms described by Grzybowski; they differ
only in the number of inner chambers. Found in
layers 3 and 4.
50. Trochammina oariolaria Grzybowski
Test construction resembles Grzybowski's
forms. Rare, found in layers 2,3 and 5.
51. Trochammina coronata Brady
213
Specimens from Szymbark show extreme regularity in construction. Up to 7 whorls, which is
more than in Brady and Grzybowski's forms.
Rather common, found in all layers.
52. Trochammina subcoronata Rzehak
Construction type the same as in Grzybowski's
forms. A rather common form, several specimens found in layers 3,4 and 5.
53. Trochammina contorta Grzybowski
In the last whorl there ar 5-9 chambers,
somewhat fewer than the specimens described
by Grzybowski from the Inoceramus bed near
Gorlice. Common, found in all layers except
layer 1 and 2.
54. Trochammina deformis Grzybowski
Same type of construction as in Grzybowski's
forms. Several specimens found in layers 2 and
5.
55. Trochamminafolium Grzybowski
Test construction the same as the forms
described by Grzybowski. Rather common,
found in all the layers.
56. Trochammina squamata Jones and Parker.
Test construction the same as in forms
described by Brady. Several specimens found
in layers 4 and 6.
57. Trochammina uoifonnis Grzybowski
Test built like Grzybowski's forms. Several
specimensfound in layers 1,2 and 4.
58. Trochammina mitrata Grzybowski
Test built like Grzybowski's forms. Several
specimensfound in layers 4 and 5.
59. Trochammina ammonoides Grzybowski
Test construction the same as Grzybowski's
forms. Several specimens found in layers 4 and
5.
60. Trochammina mirabilis Friedberg
Test agglutinated, surface rough, oval in
shape shows differences in construction on
umbilical and spiral sides similar as in forms
Maria Dylqianka
214
described by Friedberg. Several specimens
found in layers 4 and 5.
30 small, flat chambers. Size 1 mm. Single
61. Trochammina simplex Friedberg
Test construction same as Friedberg's forms.
One specimen found in layer 5.
66. Trochammina sp.
pl. 1, fig. 9
Test siliceous, rough, circular shape. On one
side six flattened chambers, elongated toward
the centre, create a sort of rosette. On the
other side there is a row of irregular chambers. Periphery acute, lobate. Size 1 mm.
Single specimen was found in layer 3.
62. Trochammina a c m u l a ta Grzybowski
The specimen from Szymbark differs from the
one desaibed by Grzybowski, but resembles
Friedberg's type in preservation as well as in
shape. A single specimen found in layer 3.
63. Trochammina heteromotpha Grzybowski
In general, the test construction is the same as
Grzybowski's description. A single specimen
found in layer 3.
64. Trochammina intermedia Rzehak var.
szymbarkensis nvar.
pl. 1, fig. 8
Test siliceous, round in shape, surface rough,
comprised of nine chambers. On one side all
nine chambers are visible, arranged in similar
manner as in Trochammina intermedia; at
first four peripheral chambers, on top of them
four smaller ones and a single, smallest one in
the middle. This gives four peripheral and
five central chambers. On the other side four
large, peripheral chambers, are visible, narrowing toward the centre and creating a small
depression in the middle. Periphery acute and
lobate as in Trochammina intermedia. Size 0.8
mm. A single well preserved specimen was
found in layer 3.
65. Trochammina uoifonnis Grzybowski var.
multiloba n.var.
pl. 1, fig. 10
Test siliceous, elongated, pear shaped, comprised of numerous minute chambers, slightly
irregular. Only in the cent~alpart can it be
recognized that the chambers arranged in a
row coil into a knot. One side test is highly
convex and on the other flat. This form resembles Trochammina uviformis, but differs from
it in the number of chambers and their size.
Trochammina uviformis is comprised of 10-15
large, spherical chambers. This form has up to
specimen was found in layer 4.
67. Cyclammina setosa Grzybowski
Specimens from Szymbark differ from the one
desaibed by Grzybowski. They are flattened,
which could be a secondary process, especially
since the surface of the test is deformed. Size
0.8 mm.Several specimens found in layer 5.
Family TEXTULARIDAE
68. Bulimina preslii Reuss
The form from Szymbark agrees with
Olszewski's description. Found in layer 4.
69. Gaudryina trochus d'Orbigny
Identical to the ones described and illustrated
by Egger and Schubert. It is one of the most
interesting forms. For a long time it was designated as Textularia (a biserial form) until the
phylogeny proved that it is derived from
Verneuilina, a triserial form. Found in layer 5.
Family LAGENIDAE
70. Lagena globosa Walker
Fully agrees with Brady's drawings. Several
specimens were found in layer 3.
71. Lagena elipsodalis Schwager
Test built like Egger's forms. Several specimens were found in layer 1.
72. Lagena sp.
pl. 1, fig. 11
Test at first spherical, slightly flattened,
turns into a narrow neck with the aperture. On
the opposite side there is a small button separated from the main chamber by a groove (this
could be a secondary process). It looks like a
second, very small chamber. Surface smooth,
Szymbark
Family GLOBIGERWIDAE
73. Globigerina bilobata d'Orbigny
Test calcareous, highly porous with Globigerina-like texture, comprised of two spherical
chambers, a smaller one and a larger one.
Through the middle of the smaller chamber
runs a sort of constriction, but only slightly
visible. This feature is not found in the form
described by Bagg. Brady described a similar
form as Orbulina universa with the lack of
aperture being the characteristic trait. Specimens from Szymbark do not have an aperture
but only seemingly a scar after an aperture.
Two well preserved specimens were found in
layers 1 and 2.
74. Globigerina triloba Reuss
Fully agrees with Egger's description. Found
in layer 2.
75. Globigerina bulloides d'Orbigny
Specimens from Szymbark are very well preserved and resemble the specimens described
by Brady and Egger. Several specimens were
found in layers 1,2 and 3.
76. Globigerina cretacea d'Orbigny
Fully agrees with Brady's description. Several specimens were found in layers 1 and 2.
215
77. Globigerina bulloides var. triloba Brady
The form from Szymbark fully resembles
Brady's specimens. Several specimens were
found in layers 1 and 2.
78. Globigdna linneana d'Orbigny
Agrees with Brady's drawings. Several specimens were found in layers 1 and 2.
79. Globigerina aequilateralis Brady
Test construction the same as in the form
described by Brady. Found in layers 1 and 2.
80. Globigerina inflata d'orbigny
The form from Szymbark resembles Brady's
drawing but it is slightly smaller. A single
specimen found in layer 2.
Family ROTALIDAE
81. Discorbina sp.
Test pyritized, which does not allow its precise identification. In its structure it resembles
Discorbina tabernacularis. A single specimen
found in layer 1.
Family NUMMULITIDAE
82. Operculina cretacea Reuss
The form from Szymbark resembles the one
described and illustrated by Egger. A single
specimen found in layer 6.
Maria Dylqianka
Explanation to Plate
Fig. 1.
Spiroloculina sp. aff. S. arenaria Brady
Fig. 2.
Rhabdammina sp.
Fig. 3.
Hyperammina excelsa n.sp.
Fig. 4.
Reophax duplex Grzybowski var. acuta n.var.
Fig. 5.
Reophax triloba n.sp.
Fig. 6.
Reophax placenta Grzybowski var. globulosa n.var.
Fig. 7.
Reussina sp.
Fig. 8.
Trochammina intermedia Rzehak var. szymbarkensis n.var.
Fig. 9.
Trochammina sp.
Fig. 10.
Trochammina uviformis Grzybowski var. multiloba n.var.
Fig. 11.
Lagena sp.
Q''4
.c,.
dl-
~.
,
References
References to 1923
Alth, A. (1850). Geognostisch palaeontologische Beschreibung d. nachsten Umgebung von Lemberg. Haidingers naturwissensch. Abhandlungen, 3,171-284.
Archiac, A. d., & Haime, J. (1853-1854). Desuiption des animaux fossiles du groupe nummulitique
de l'Inde, prCcCdCe d'un rhumb ghlogique et d'une monographic des Nummulites. Gide et J.
Baudry, Paris. 223 pp + 15 pl.
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