The Inoceramus Beds from the quarry in Szymbark, near Gorlice.
Transcription
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. Bornemann, J. G. (1855). Die mikroskopische Fauna des Septarienthones von Hermsdorf bei Berlin. Zeitschrift der Deutschen Geologischen Gesellschaft, 7,307-371. Bosquet, (1852). Description des Entomostraces fossiles des terrains tertiares de la France et de la Belgique. MCmoires CouronnCs et MCmoires Savants ~ t r a n ~ e rAs .c a d h i e Royale de Sciences et Belles-Lettres de Bruxelles 24,142 pp. Brady, H. B. (1881). ijber einige arktische Tiefsee Foraminiferen gesarnmelt warend der osterreichisch-ungarischen Nordpol-Expedition in den Jahren 1872-74. Denkschriften der Kaiserlichen Akademie der Wissenschaften, Wien, Mathematisch-Naturwissenschaftlichen Classe, 43,9-110. Brady, H. B. (1884). Report on the Foraminifera dredged by H.M.S Challenger, during the years 1873 - 1876. In: Murray, J. (ed.) Reports of the scientific results of the voyage of the H.M.S. Challenger. Zoology, 9 , l - 814. Carpenter, W. B., Parker, W.K. and Jones T. R. (1862). Introduction to the study of the foraminifera. London: Robert Hardwicke, London for the Ray Society. 319 p p + 22 pl. d'Orbigny, A. (1846). Foraminiferes fossiles du Bassin Tertiaire de Vienne (Autriche). Paris: Gide et Compe. dlOrbigny. (1840). MCmoire sur les Foraminiferes de la a a i e blanche du bassin de Paris. MCmoires de la SociCt6 Geologique de France 4,l-51. de la Harpe, (1881-1883). Etude des Nummulites de la Suisse, et revision des esp&ces b d n e s genres Nummulites et Assilina. MCmoires. de la SociCtC Palhntologique. Suisse 7,10, part 1, pp. 1-104, pl. 12 ;part 2, pp. 105-140, part 3, vol. 10, pp. 141-180,5 pls. Dunikowski, E.L. (1879). Nowe foraminifery kredowego marglu lwowskiego. Kosmos 4,102-110; 121-135 [in two parts]. Egger, J.G. (1858). Die Ostrakoden der Miociin-Schichten bei Ortenburg in Nieder-Bayern. Neues Jahrbuch fiir Minerologie, Geognosie, Geologic, und Petrefaktenkunde 1858,403443 + 6 pl. Egger, J.G. (1899). Foraminiferen und Ostrakoden aus den Kreidemergeln der Oberbayerischen Alpen. Abhandlungen der Mathematisch-Physikalischen Classe der koniglich Bayerischen Akademie der Wissenschaften, 21,l-230. Friedberg, W., (1898). Przyczynek do znajomdci otwomic kredowego marglu lwowskiego. Kosmos 22, (1897), 263-289. Friedberg, W., (1906). Drobny przyczynek do fauny warstw inoceramowych. Sprawozdania Komisji fizj. Akademii Umiejetndci w Krakowie, 42,58. Friedberg, W. (1901). Otwornice warstw inoceramowych okolicy Rzeszowa i Rbicy. Rozprawy Akademii UmiejetnoSci w Krakowie, Wydzial Matematyczno-Przyrodniczy,Krakbw, ser. 2, 41,601-668 + 2 pl. References 2 19 Grzybowski, J. (1894). Mikrofauna piaskowca karpackiego z pod Dukli. Rozprawy Akademii Umiejetnobd w Krakowie, Wydziat Matematyczno-Rzyrodniczy,Krak6w, ser. 2,29,181-214 + 5 pl. Grzybowski, J. (1896). Otwornice czerwonych il6w z Wadowic. Rozprawy Akademii UmiejetnoSci w Krakowie, Wydziat Matematyczno-Przyrodniczy,Krakbw, ser. 2, 30, 261308. Grzybowski, J. (1896). Studja mikroskopowe nad zielonymi zlepiencami wschodnich Karpat. Kosmos, 21,4442. Grzybowski, J. (1898). Otwornice poklad6w naftonosn ych okolicy Krosna. Rozprawy Akadernii UmiejetnoSa w Krakowie, Wydziat Matematyczno-Przyrodniczy,Krakbw, ser. 2, 33, 257305, + 3 pl. Grzybowski, J. (1901). Otwornice warstw inoceramowych okolicy Gorlic. Rozprawy Akademii UmiejetnoSa w Krakowie, Wydziat Matematyczno-Przyrodniczy,Krakbw, ser. 2, 41, 219288, + 2 pl. Giimbel, C. W. (1868). Beitrage zur Foraminiferenfauna der nordalpinien Eociingebilde. Abhandlungen der Mathematische-Physikalischen Classe der koniglich Bayerischen Akademie der Wissenschaften, 10(2), 581-730. Giimbel, C. W. (1871). Die sogenannten Nulliporen (Lithothamniurn und Dactylopora). Abhandlungen der Mathematisch-Physikalischen Classe der koniglich Bayerischen Akademie der Wissenschaften, 11(11, 14-52 +2 pl. Hantken, M. v. (1875). A Clavulina szab6i rkterek Faunija. I. Foraminiferak. [Die Fauna der Clavulina szaboi - Schichten.] Magyar Kir5lyi Foldtani Intkzet Evkonyve, 4, 1-82, + 16 pl.. Haeussler, R. (1883).Die Astrorhiziden und Lituoliden der Bimammatuszone. Neues Jahrbuch fiir Minerologie, Geognosie, Geologie, und Palaeontologie, 1,5541 +2 pl.. Haeussler, R., (1890). Monographie der Foraminiferenfauna der schweizerischen TransversariusZone. Abhandlungen der schweizerischen palaeontologischen Gesellschaft, 17, Karrer, F. (1861).h r das Auftreten der Foraminiferen in den marinen Tegel des wiener Beckens. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften Wien, MathematischNaturwissenschaftliche Classe, 44,427-458, + 2 pls. Karrer, F. (1865 [for 18641). h r das Auftreten der Foraminiferen in den Mergeln der marinen Uferbildungen (Leythakalk) des Wiener Beckens. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften Wien, Mathematisch-Naturwissenschaftliche Classe, 50, 692-721 + 2 pl. Karrer, F. (1866). h r das Auftreten von Foraminiferen in den iilteren Schichten des Wiener Sandsteins. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften Wien, Mathematisch-Naturwissenschaftliche Klasse, 52, 121-193. Karrer, F. (1867). Zur Foraminiferenfauna in ~sterreich.Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften Wien, Mathematisch-Naturwissenschaftliche Klasse, 55, 331-368. Karrer, F. 1868. Die miocene Foraminiferenfauna von Kostej im Banat. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften Wien, Mathematisch-Naturwissenschaftliche Klasse, 58,121-193, + 5 pls. Liebus, A. (1901). h r die Foraminiferenfauna des Bryozoenhorizonthes von Riabonia. Neues Jahrbuch fiir Minerologie, 1,111-134. 220 References Liebus, A. (1902).Ergebnisse einer mikroskopischen Untersuchung des organischen Einschlusse des oberbayrischen Molasse. Jahrbuch der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien, 52, 71-104. Liebus, A. (1906). ijber die Foraminiferenfauna der Tertiiirschichten von Biaritz. Jahrbuch der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien, 56,351-366. Liebus, A., and Schubert, R.J. (1902). Die Foraminiferen der karpathischen Inoceramenschichten von Gbellan in Ungarn (Puchover Mergel). Jahrbuch der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien, 52, 285-310. NiedZwiedzki, J. (1896). Mikrofauna kopalna ostatnich pr6bek wiercenia we Lwowie r. 1894. Kosmos, 21,240-247. Noth, R., (1912) Die Foraminiferenfauna der roten Tone von Barwinek und Komarnok. Beitrage zur Palaontologie dsterreich und des Orients, 25,l-22. Neugeboren, J.L., 1856. Die Foraminiferen aus der Ordnung der Stichostegier von Ober-Lapugy in Siebenburgen. Denkschriften der Kaiserlichen Akademie der Wissenschaften, Mathematisch-Naturwissenschatliche Classe, 12, 65-108. Olszewski, (1875). Zapiski paleontologiczne. Sprawozdania komisji fyzyogr. Akademii Umiejetndci w Krakowie, 9, Paul, C.M. (1883). Die neueren Fortschritte der Karpathensandstein-Geologie. Jahrbuch der Kaiserlich-Koniglichen geologischen Reichanstalt in Wien, 33, 659-690. Paul, C.M. (1888). Bemerkungen zur neueren Literatur uber die westgalizischen Karpathen. Jahrbuch der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien, 38, 703728. Paul, C.M. (1898). Der Wienerwald. Ein Beitrag zur Kenntniss der nord-alpinen Flyschbildungen. Jahrbuch der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien, 48,53178. Reuss, A. E. (1845). Die Versteinerungen der Bomischen Kreideformation. E. Schweizerbart'sche Verlagsbuchhandlung, Stuttgart. 148 pp + 51 pl. Reuss, A. E. (1850). Neue Foraminiferen aus den Schichten des osterreichischen Tertiarbeckens. Denkschriften der Kaiserlichen Akademie der Wissenschaften, Mathematisch-Naturwissenschatliche Classe, 1, 365-390. Reuss, A. E. (1850). Die fossile Entomostraceen des osterreichischen Tertikbeckens. Haidingers Naturwissenschaftliche Abhandlungen, 3,l-92. Reuss, A. E. (1851). Die Foraminiferen und Entomostraceen des Kreidemergels von Lemberg. Haidingers Naturwissenschaftliche Abhandlungen, Wien, 4, 17-52. Reuss, A. E. (1851). Ueber die fossilen Foraminiferen und Entomostraceen der Septarienthone der Umgegend von Berlin. Zeitschrift der Deutschen Geologichen Gesellschaft, Berlin, 3,49-91. Reuss, A. E. (1855). Ein Beitrag zur genaueren Kenntnis der Kreidegebilde Mecklenhurgs. Zeitschiit der Deutschen Geologischen Gesellschaft, Berlin, 7, 261-292. Reuss, A. E. (1856). Beitrtage zur Charakteristik der Tertiiirschichten der nordlichen und mittleren Deutschlands. Sitzungsberichte der K. Akademie der Wissenschaften in Wien, Mathematisch-Naturwissenchaftliche Classe, 18, 197-274. Reuss, A. E. (1860). Die Foraminiferen der Westphalischen Kreideformation. Sitzungsberichte der K. Akademie der Wissenschaften in Wien, Mathematisch-Naturwissenchaftliche Classe, 40, 147-238. References 221 Reuss, A. E. (1861). Beitrage zur Kenntniss der t e r t i h n Foraminiferen-Fauna. Sitzungsberichte der K. Akademie der Wissenschaften in Wien, Mathematisch-Naturwissenchaftliche Classe, 42,355-370 + 2 pl. Reuss, A. E. (1861).Entwurf einer systematischen Zummenstellung der Foraminiferen. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften, Wien, 44(1), 355-396. Reuss, A. E. (1863). Die Foraminiferen des Schreibkreide v. Riigen. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften in Wien, Mathematisch-Naturwissenschaftliche Classe 44, Reuss, A. E. (1863). Die Foraminiferen des norddeutschen Hils und Gault. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften in Wien, Mathematisch-Naturwissenschaftliche Classe (18621, &(I), 5-100 + 13 pl. Reuss, A. E. (1863). Die Foraminiferen Familie der Lagenideen. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften in Wien, Mathematisch-Naturwissenschaftliche Classe, &(I), 308-342 + 8 pl. Reuss, A. E. (1863). Beitrage zur Kenntniss der tertiaren Foraminiferen-Fauna. III Die Foraminiferen des Septarienthones von Offenbach. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften in Wien, Mathematisch-Naturwissenschaftliche Classe, 48(1), 36-71 + 8 pl. Reuss, A. E. (1864). Zur Fauna der deutschen Oberoligociins. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften in Wien, Mathematisch-Naturwissenschaftliche Classe, 50(1), 435482, + 5 pl. Reuss, A. E. (1866). Die Foraminiferen und Ostrakoden der Kreide am Kanara-See bei Kiistendsche. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften in Wien, Mathematisch-NaturwissenschaftlicheClasse, 52(1), 445470 + 1 pl. Reuss, A. E. (1866). Die Foraminiferen, Antozoen und Bryozeon des deutschen Septarienthones. Denkschriften der Kaiserlichen Akademie der Wissenschaften, Mathematisch-Naturwissenschatliche Classe, 25,117-214 + 11 pl. Reuss, A. E. (1867). Die fossile Fauna der Steinsalzablagerung von Wieliczka in Galizien. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften in Wien, MathematischNaturwissenchaftliche Classe, 55(1), 17-182 + 8 pl. Rothpletz, A. (1891). Fossile Kalkalgen aus den Familien der Codiaceen und der Corallineen. Zeitschrift der deutschen geologischen Gesellschaft, 43, 295-322. Rzehak, A. (1887). Die Foraminiferenfauna des griinen Oligocenth~nesvon Nikoltschitz. Verhandlungen der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien (1887),87-88. Rzehak, A. (1887). Die Foraminiferen des blauen Oligocenthones von Nikoltschitz. Verhandlw-gen der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien, (1887), 133-134. Rzehak, A. (1888). Ueber eine bartonisch ligurische Foraminiferenfauna vom Nordrande des Marsgebirges in Mahren. Verhandlungen der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien, (1888), 190-192. Rzehak, A. (1888). Die Foraminiferen der Nummuliten-schichten des Waschbergers und Michelsbergers bei Stockerau in Nieder-Osterreich. Verhandlungen der KaiserlichKoniglichen geologischen Reichsanstalt, (18881, 226-229. Rzehak, A. (1888). Die Foraminiferenfauna des kieseligen Kalkes von Nieder-Hollebriinn und des Melettemergels der Umgebung von Bruderndorf in Niederosterreich. Annalen des Kaiserlich-Koniglichen Naturhistorischen Hofrnuseums, Wien, 3,257-270 + 1 pl. References 222 Rzehak, A. (1891). Die Foraminiferenfauna der alttertiiiren Ablagerungen von Brudemdorf in Niederosterreich, mit Beriichsichtigung des angeblichen Kreidevorkommens von Leitzersdorf. Annalen des Kaiserlich-Koniglichen Naturhistorischen Hofrnuseums, 6, 1-12. Rzehak, A. (1895). Ueber einige mekwurdige Foraminiferen aus osterreichischen Tertiar. Annalen der Kaiserlich-Koniglichen Naturhistorischen Hofmuseums, Wien, 10,213-230. Schlicht, E. v. (1870). Die Foraminiferen des Septarienthones von Pietzpuhl. Wiegandt & Hempel, Berlin. 98 pp. + 38 pl. Schwager, C. (1883). Die Foraminiferen aus den Eocaenablagerungen der libyschen Wuste und Aegyptens. Paleontographica, 30, 79-153. Sherborn, C. D. (1893).An index to the genera and species of the foraminifera. Smithsonian Miscellaneous Collections, 856,l-240. Schubert, R.J. (1900). Bemerkungen uber einige Foraminiferen der ostgalizischen Oberkreide. Jahrbuch der geolog. Reichsanstalt in Wien, 50,659462. Schubert, R.J. (1902). h e r die Foraminiferen Gattung Textularia Defrance und ihre Verwandschaftsverhaltnisse. Jahrbuch der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien, 53,80-85. Schubert, R.J. (1902). Neue und interessante Foraminiferen aus dem sudtiroler Alttertiar. Beitrage zur Palaontologie ~sterreich-ungarnsund des Orients, 14,9-26 + 1 pl. Szajnocha, W. (1896).Atlas geologiczny Galicji, tekst do zeszytu VI. Krakow. Szajnocha, W. (1898). Z wycieczek geologicznych. 1. Muntigl. Kosmos, 23,487-498. Terquem, 0. (1882). Les foraminferes de 1180c&ne des environs de Paris. MCmoires del la SociCtC Gklogique de France, d r . 3,2(3), 1-193. Terquem, O., and Berthelin, G. (1875).8tude microscopique des marnes du Lias moyen d'Essey-16sNancy, zone inferieure de l'assise Amonites margaritatus. MCmoires de la SociCt6 Geologique de France, ser. 2,10,1-126. Tietze, E. (1896).Beitrage zur Geologie von Galizien h e r einen neuen Versuch, Foraminiferen zur Alterbestimmungen der karpathischen Schichtglieder zu verwenden. Jahrbuch der Kaiserlich-Koniglichen geologischen Reichsanstalt in Wien, 46,385-410 Uhlig, V. (1882). h e r einige oberjurassische Foraminiferen mit aglutinierender Schale. Neues Jahrbuch fiir Minerologie, 1882,152-155. Uhlig, V. (1883). Foraminiferen aus den rjasanischen Omathenthone. Jahrbuch der geolog. Reichanstalt in Wien, 33, 735-774. Uhlig, V. (1883). Beitrage zur Geologie der westgalizischen Karpathen. Jahrbuch der geolog. Reichanstalt in Wien, 33,443-560 + 1 pl. Uhlig, V. (1886). Ueber eine Mikrofauna aus dem Alttertiar des westgalizischen Karpathen. Jahrbuch der geolog. Reichsanstalt in Wien, 36,141-214, + 4 pls. Uhlig, V. (1894). Bemerkungen zur Gliederung karpathischer Bildungen. Jahrbuch der geolog. Reichsanstalt in Wien, 44, 183-232. Walter, H., and Dunikowski, E.L. (1883).Geologiczna budowa naftonoSnego obszaru zachodniogalic. Karpat. Kosmos 7-8, 263-309. Walther, J. (1894). Einleitung in die Geologie als historische Wissenschaft. Jena. Wibniowski, T. (1905). 0 wieku karpackich warstw inoceramowych. Rozprawy Akademii Umiejetnobci w Krakowie, Wydzial Matematyczno-Przyrodniczy, Krakbw, ser. 3, 5,132-152. - References 223 WiSniowski, T. (1907). ijber die obersenone Flyschfauna von Leszuyny, Beitrage zur Palaontologie Osterreich-ungarns und des Orients, 20, Wojcik, K. (1903). Dolno-Oligacenska fauna Kruhela malego pod Przemyslem (Warstwy z Clavulina szaboi). Cze& 1. Otwornice i mieczaki. Rozprawy Akademii Umiejetnosci w Krakowie, Wydzial Matematyczno-Przyrodniczy, Krak6w, ser. 3,3,489-569. Zittel, C. (1902). Handbuch der Paleontologie. References cited in Footnotes Bieda, F. (1946). La stratigraphie du Flysch des Karpates centrales polonaises b a d e sur les grands Foraminiferes. Rocznik Polskiego Towarzystwa Geologicznego, 16,l-52. Bieda, F. (1950).Sur quelque foraniniferesnouveaux ou peu cunnus du flysch des Karpates polonaises. Rocznik Polskiego Towarzystwa Geologicznego, 18,153-168. Blaicher, J. (1967). Assemblages of small foraminifera from the sub-menilite Globigerina marls in the Carpathians. Instytut Geologiczny Biuletyn 211,355-364. Geroch, S. & Gradzinski, R. (1955). Stratigrafia serii podslaskiej zywieckiego okna tektonicznego. Racznik Polskiego Towarzystwa Geologicznego, 24,342. Glaessner, M.F. (1937). Studien h e r Foraminiferen aus der Kreide und dem Tertiar des Kaukasus; 1. Die Foraminiferen der altesten Tertiarschichten des Nordwest-Kaukas. Problems of Paleontology, 2-3,349-408. Moscow. Hanzlikova, E. (1972). Carpathian upper Cretaceous foraminifera from Moravia (TuronianMaestrichtian). Rozpravy Ustredniho Ustavu Geologickeho, 39,5-160. Huss, F. (1966).Otwornice aglutynujace serii podslgskiej jednostki ropondnej Weglowki (Polskie Karpaty Fliszowe) [Agglutinated foraminifera of the oil-bearing subsilesian series in Weglowka (Polish Flysch Carpathiansl. Prace Geologiczne, Polska Akademia Nauk, 34, 776. Kaminski, M.A., and Gerach, S. (1992). Trochamminoides grzybowskii, nom. nov. a new name for Trochammina elegans Grzybowski, 1898. Journal of Micropalaeontology 11,64. Ksiaikiewicz, M. (1950). 0 wieku pstrych margli we fliszu Karpat zachodnich. On the age of the Veriegated Marls of the western Carpathians. Racznik Polskiego Towarzystwa Geologianego 19,315-358. Liszkowa, J. (1967). Microfauna of the Upper Cretaceous in the Sub-Silesian of the Wadowice Region (Western Carpathians). Instytut Geologiczny Biuletyn 211,341-350. Liszka, S. and Liszkowa, J. (1981). Revision of J. Grzybowski's paper (18%) "Foraminiferaof the red clays from Wadowice". Rocznik Polskiego Towarzystwa Geologicznego, 51,153-208. Loeblich, A.F. and Tappan, H. (1964). Sarcodina chiefly 'Thecamoebians" and Foraminiferida. In: Moore, R.C. (ed.) Treatise on invertebrate paleontology, part C, Protista. University of Kansas Press. 900 pp. Loeblich, A.F. and Tappan, H. (1988). Foraminiferal genera and their classification. Van Nostrand Reinhold Co., 970 pp. Majzon, L. (1943). Adatok egyes Karpataljai Flis-retegekhez, tekintettel a Globotruncanakra. [Beitrage zur Kenntniss einiger Flysch-Schichten des Karpaten-Vorlandes mit Rucksicht auf die Globotruncanenl. A magyar Kirdlyi Foldtani Intezet, fivkonyve, 37,l-170. [Hungarian]. 224 References Malecki, J. (1963). Bryozoa from the Eocene of the Central Carpathians between GryMw and Dukla. Prace geologiczne 16,158 pp. [Polish with English Summaryl. Maslakova, N.I. (1955). Stratigrafiya i fauna melkikh foraminifer paleogenovykh otlozhenii Vostochnykh Karpat. [Stratigraphy and smaller foraminifera1 fauna of the Paleogene deposits of the eastern Carpathians]. Materialy po Biostratigrafi zapadnykh oblastii Ukrainskoi SSR, 5-132. Moskva. [in Russianl. Mjatliuk, E.V. (1966). K voprosu o foraminiferakh c kremnevnyrn skeletom. [On the question of foraminifera with a siliceous skeleton]. Voprosy Mikropaleontologii, 10, 255-269. [in Russianl. Mjatliuk, E.V. (1970). Foraminifery flishevykh otlozhenii vostochnykh Karpat (MelPaleogen). [Foraminifera of the flysch deposits of the eastern Carpathians (CretaceousPaleogene)]. Trudy Vsesoyuznogo Nauchno-Issledovatel'skogo Geologorazvedochnogo Instituta VNIGRI, 282,l-225. Leningrad. [in Russian]. Moussavian, E., and Kuss, L. (1990). Typification and status of Lithothamnium aschersoni Schwager, 1883 (Corallinaceae, Rhodophyta) from Paleocene limestones of Egypt: a contribution to the synonymy and priority of the genera Archeolithothamnium Rothpktz and Sporolithon Heydrich. Berliner geowissenschaftliche Abhandlungen 120, 929-942. Neugeboren, J.L. (1852). Foraminiferen von Ober-Lapugy; vierter Artikel (Schluss).Siebenb. Ver. Naturwissen. Hermamstadt, Verh. Mitt. Jahrg 3 (4). Neumeyer, M. (1887). Die natiirlichen Verwandschaftsverhaltnisse der schalentragenden Foraminiferen. Sitzungsberichte der Kaiserlichen Akademie der Wissenschaften in Wien, Mathematisch-NaturwissenschaftlicheClasse, 95 (lo), 156-186. Olszewska, B. (1984). Otwornice bentoniczne podmenilitowych margli globigerinowych polskich karpat zewnetrznych [Benthonic foraminifera of the sub-menilite Globigerina marls of the Polish Outer Carpathiansl. Instytut Geologiczny Prace 110, 37 pp. [Polish with English Summaryl. Olszewska, B. (1985). Otwornice warstw menilitowych polskich Karpat zewnetrznych [Foraminifera of the Menilite Beds (Polish External Carpathiansll. Annales Societatis Geologorum Poloniae 55,201-250. [Polish with English Summaryl. Pokorny, V. (1950). Mikrofauna eocknneho zelenkho jilu z NikolGic. [On the microfauna of the Eocene green clay of NikolGice (Moravia, Czechos1ovakia)l. Rozpr. Ces. Akad. mat- prir. 59 (15),1-38. [Czech with English Summaryl. Smigielska, T. (1960). Rzadkie otwornice z fliszu Karpat polskich w Swietle dawniejszych i najnowszych badafi mikropaleontologicznych. Sprawozdania z posiedziefi Komisji PAN, oddzial w Krakowie, 1960,133-135. [in Polishl. Smigielska, T. (1960). Otwornice z warstw menilitowych okolic Dukli. Sprawozdania z posiedziefi Komisji PAN, oddzial w Krakowie, 1961,244-246. [in Polishl. Szczechura, J. (1992). Bicorniferidae: Cheilostomatous Bryozoa with articulated colony branches. Acta Paleontologica Polonica 36, Van Couvering, J.A., Aubry, M.-P., Berggren, W.A., Bujak, J.P., Naeser, C.W., and Wieser, T. (1981). The terminal Eocene event and the Polish connection. Paleogeography, Paleoclimatology, Paleoecology 36,321-362. Woelkerling, W.J. (1985). Proposal to conserve Lithothamnion against Lithothamnium (Rhodophyta: Corallinaceae). Taxon 34, 302-303.