◄ Carnets Geol. 18 (4) ►
Outline:
[Introduction]
[Geologic framework]
[The Lower Cretaceous succession in the study section]
[The Boueina level]
[Conclusion]
[Bibliographic references] and ...
[Plates]
* Corresponding author
Babeş-Bolyai University, Department of Geologie and Center for Integrate
Geological Studies, M. Kogălniceanu str. 1, 400084 Cluj-Napoca (Romania)
Serbian Academy of Sciences and Arts, Knez-Mihailova 35, 11000 Beograd (Serbia)
Babeş-Bolyai University, Department of Geologie and Center for Integrate
Geological Studies, M. Kogălniceanu str. 1, 400084 Cluj-Napoca (Romania)
Geological Survey of Serbia, Rovinjska 12, 11000 Beograd (Serbia)
Babeş-Bolyai University, Department of Geologie and Center for Integrate
Geological Studies, M. Kogălniceanu str. 1, 400084 Cluj-Napoca (Romania)
Rudarski institut, Batajnički drum 2, 11080 Beograd-Zemun (Serbia)
Published online in final form (pdf) on April 12, 2018
DOI 10.4267/2042/66509
[Editor: Bruno Granier]
Boueina hochstetteri Toula (type-species of the genus) was published by Toula (1884) in the 10th report of his travel through the Balkan region. He considered this species to be a problematic organism with uncertain systematic affiliation. Later, Steinmann (1901) assigned this fossil to the calcareous algae. Our own field work performed in the autumns of 2015 and 2016 in the Pirot area (SE Serbia) led to re-identification of the rich Boueina hochstetteri type level, close to the confluence of the Temska and Nišava Rivers, the type locality of Toula. The rich Boueina level is part of a succession of bioclastic limestones. The fragments of Boueina thalli are occasionally branched, a feature supporting the interpretation of Boueina as an inarticulate udoteacean alga with rare branching.
• Calcareous
green algae;
• Udoteaceae;
• Boueina;
• Lower Cretaceous;
• Carpatho-Balkanides;
• Eastern Serbia
Bucur I.I., Sudar M.N., Săsăran E., Jovanović D., Pleş G. & Polavder S. (2018).- Rediscovery of the type locality of the Udoteacean alga Boueina hochstetteri Toula, 1884, in the Lower Cretaceous of Serbia.- Carnets Geol., Madrid, vol. 18, no. 4, p. 123-137.
Redécouverte de la localité-type de l'algue udoteacée Boueina hochstetteri Toula, 1884, dans le Crétacé inférieur de Serbie.- Boueina hochstetteri Toula (espèce-type du genre) a été publiée par Toula (1884) dans le dixième rapport de son voyage à travers les Balkans. Il a considéré cette espèce comme un organisme problématique à affinité systématique incertaine. Plus tard, Steinmann (1901) a attribué ce fossile aux algues calcaires. Nos propres recherches sur le terrain à l'automne 2015 et à l'automne 2016 dans la région de Pirit (SE de la Serbie) ont permis de retrouver le niveau-type de Boueina hochstetteri, à proximité de la confluence des rivières Temska et Nišava, la localité type de Toula. Le niveau riche en Boueina appartient à une succession de calcaires bioclastiques. Les fragments de thalles de Boueina sont parfois ramifiés, une caractéristique qui permet de justifier l'appartenance de Boueina aux algues udotéacées inarticulées mais occasionellement ramifiées.
• Algues vertes calcaires ;
• Udoteacées ;
• Boueina ;
• Crétacé inférieur ;
• Carpatho-Balkanides ;
• Serbie orientale
In 1884, Franz Toula published the 10th report of his travel through the Balkan region, more specifically the region between Pirot (SE Serbia) and Sofia (Bulgaria). In the proximity of the Temska and Nišava Rivers confluence, close to Pirot (Serbia), Toula observed some carbonate deposits which he assigned to the Upper Neocomian. From these deposits, he illustrated and described several fossil organisms. Among others, he found a rock consisting of an agglomeration of calcareous tubes, up to 10 mm in length and 2.5-3.5 mm in diameter, for which he could not provide a clear systematic affiliation. In 1876, Toula sent samples from this material to Wilhelm von Gümbel, who was an expert in "dactyloporides", i.e. dasycladaleans, in that time considered to be foraminifers. Following the sample investigation, Gümbel decided that this material could not be assigned to the "dactyloporides", but could represent some sponges. Subsequently, Toula sent further material to Professor Karl von Zittel, who first interpreted the fossils as sponges, but then decided that this material is hardly comparable with other known animal or plant rests.
Toula followed the advice of Zittel and assigned a scientific name to this fossil (Boueina hochstetteri), despite its problematic systematic affiliation. In 1901, Gustav Steinmann - who also received part of the original material collected by Toula, published a paper focusing on the similarities between the inner structure of these tubes and that of Halimeda segments. Accordingly, the author stated that Boueina hochstetteri Toula belongs to the Codiacean green algae related to Halimeda. Nevertheless, Steinmann noticed that Boueina does not seem to be segmented and probably also not branched - features that distinguished the newly-identified fossil from Halimeda. Unfortunately, the type material collected by Toula seems to have disappeared (destroyed?) in the interval between World War I and II, in the 20th century. Later on, Boueina hochstetteri was assigned besides other fossil species either to Codiaceans (Pia, 1927), to Udoteaceans (e.g., Bassoulet et al., 1983), or even to Halimedaceans (Bucur, 1994). Basically, like in the case of the other udoteaceans-halimedaceans, this species was considered to be a segmented green alga.
A recent publication (De Castro et al., 2008) has recalled the discussion about the thallus organization in the Boueina species. This review has revived interest in the study of the type material, in order to clarify these aspects.
Studies
published in the last decades of the 20th century did not mention
anymore the type locality for the species, while the profiles studied by Toula
were assumed to be currently covered by soil and vegetation. Everything
suggested that the type locality for Boueina
hochstetteri would be difficult to recover. Luckily, the recent construction
works at Niš-Sofia highway have uncovered most of the carbonate deposits in the
proximity of the Temska and Nišava Rivers (Fig. 1 
). In the framework of a collaboration
project between the Romanian Academy and the Serbian Academy of Sciences and
Arts, during the autumns of 2015 and 2016 we have performed field work in the
above-mentioned region. Within a carbonate succession dominated by bioclastic
limestones, we have found the level rich in Boueina hochtetteri. Undoubtedly, this must represent the same level
from where some 130 years ago Toula had described the mysterious
calcareous tubes that he has scientifically named. Our own-collected topo-typic
material -- partly illustrated in this work-- will be subsequently used for a
review of the species Boueina hochstetteri
Toula.
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Figure 1:
Geological map of the area near the confluence of the Temska and Nišava Rivers
(Staničenje village). Legend: 1. Quaternary; 2. Pliocene; 3. Paleogene; 4.
Upper Cretaceous; 5. Lower Cretaceous (Barremian-Aptian; a, bioclastic
limestones); 6. Lower Cretaceous (Berriasian-Hauterivian); 7. Upper Jurassic
(Tithonian); 8. Upper Jurassic (Oxfordian-Kimmeridgian; 9. Devonian; 10.
Magmatic rocks; 11. Location of the studied section (Redrawn after Andjelković
et al., 1975, and Vujisić et al.,
1997). |
The section containing the type locality of Boueina hochstetteri Toula is situated in the central part of the Carpatho-Balkanides which in the Serbian geological literature has different names, e.g., Kučaj Zone (Krstić & Maslarević, 1989, 1990), Kučaj Terrane (Karamata et al., 1997) or Getic Nappe (Kučaj-Ljubaš-Sredna Gora Unit) in Getic Units (Kräutner & Krstić, 2003), etc.. It is a continuation of the Reşiţa-Moldova Nouă Zone of the Romanian South Carpathians and extends to the East Kraishte Unit in SE Serbia and southwestern Bulgaria. This is the largest Alpine unit in the Serbian part of the Carpatho-Balkanides. This unit is made of different Precambrian, Paleozoic, Mesozoic and Neogene igneous, sedimentary, metamorphic and volcano-sedimentary rocks with very complex geological evolution, structural fabrics, particularly in its western part.
The Lower Cretaceous part of the sequence has a large extent in the Kučaj Zone, especially in the areas of the following mountains: Beljanica, Kučaj, Ozren, Devica, Svrljiške Planine, Suva Planina, Belava, southwestern and western slopes of Stara Planina, Tresibaba, Grnčar, and Tupižnica. The Lower Cretaceous is represented by shallow-water carbonate platform sediments several hundreds of meters thick, and can be separated into: (a) Valanginian-Hauterivian stratified micritic limestones locally with cherts, marly limestones, marls, (b) Barremian-Lower Aptian (Urgonian facies) massive limestones, marls and oolitic limestones, and (c) Albian glauconite sandstones, sandstones and conglomerates.
Important investigations of the Urgonian sediments in the Eastern Serbia have been made by Jankičević (1978, 1996). On the basis of his study Jankičević concluded that these Urgonian deposits of upper Barremian and lower-middle Aptian age form a single carbonate-terrigenous unit, named Tupižnica Formation. It consists dominantly of limestones with rudists ("true Urgonian"), bioclastic limestones with orbitolinids, and terrigenous rocks with orbitolinids and different macrofauna (bivalves, gastropods, brachiopods, etc.).
In the Niš-Pirot area, except for older investigations related to the geological mapping (Basic Geological Map, 1:100,000), very few publications exist, documenting Valanginian microfossils from the limestones earlier mapped as Barremian in the Jerma River canyon, south of Pirot (Bucur et al., 1995). Hauterivian orbitolinids from Kamenica section near Niš (Svrljiške Planine area) were described by Polavder (2014).
The study section is located about 10 km north-west from Pirot, close to
Staničenje village in the proximity of the confluence of the Temska and Nišava
Rivers (coordinates: x 7624319, y 4786680; Fig. 1 ). The outcrop, a few hundred
meters in length and several meters in height (Fig. 2 ), was created as a result
of the Niš-Sofia new highway construction works. In this section, bioclastic
and bioclastic-oolitic limestones are interlayered with marls and sandstones (Fig. 3 ). In the lower part of the carbonate succession, medium-grain limestones
represented by bioclastic grainstone with frequent peloids and micritized
intraclasts with fragments of bivalves, gastropods, echinoderms and bryozoans,
frequent foraminifers and rare fragments of Boueina crop out (Pl.
2.F ). They are separated by a marly
interlayer from the main body of the bioclastic-oolitic limestones - where the
extremely rich-Boueina level is
located.
The
limestones located at the base of the Boueina-rich
level contain several microfacies types. These are mainly bioclastic grainstone
and packstone/wackestone, sometimes containing frequent ooids (bioclastic-ooidic
grainstone) with fragments of bivalves, gastropods and echinoderms, and locally
with frequent fragments of bryozoans, brachiopods, corals and sponges, annelid
worm tubes, foraminifers and calcareous algae (Pls. 1
- 2 ). The
micropaleontological association of the whole succession includes benthic
foraminifers and calcareous algae. Among the foraminifers occur: Charentia cuvillieri Neumann
(Pl. 3.A ), Paracoskinolina? jourdanensis
(Foury & Moullade) (Pl.
3.B ), ?Orbitolinopsis sp., Pfenderina
globosa (Foury) (Pl. 3.C ),
Akcaya minuta (Hofker), Everticyclammina
sp., Coscinophragma sp., Ammobaculites sp., Mayncina sp.,
Meandrospira sp., Coscinoconus
sp., Neotrocholina cf. theodori (Rigaud,
Schlagintweit & Bucur) (Pl.
3.D ), Lenticulina sp.,
miliolids and small textulariaceans. The calcareous algae are represented by: Actinoporella
podolica (Alth), "Cylindroporella" elliptica (Bakalova),
Falsolikanella cf. nerae (Dragastan,
Bucur & Demeter), Montiella
elitzae (Bakalova) (Pl. 4.A ), Zittelina
hispanica Masse, Arias & Vilas
(Pl. 4.C ), Suppiluliumaella
elliotti Bakalova (Pl. 4.D-E ), Neomeris
sp., Salpingoporella muehlbergii (Lorenz) (Pl.
4.F ), Salpingoporella pygmaea (Gümbel),
Similiclypeina conradi Bucur,
Terquemella sp., Boueina hochstetteri Toula, Arabicodium sp., Nipponophycus
sp., Permocalculus minutus Bucur,
Sporolithon rude (Lemoine), and
rare rivulariacean-type cyanobacteria. The problematicum Carpathoporella
occidentalis Dragastan is also present.
Overall, the micropaleontological association points to a Barremian-Lower Aptian age. The presence of species Parakoskinolina? jourdanensis is more an index for Lower Barremian (Foury & Moullade, 1966; Clavel et al., 2010), at least for the succession located at the base of the rich-Boueina level.
Both the microfacies types and the micropaleontological association suggest an open carbonate (external) platform environment, with moderate water depth, from a few meters to several tens of meters.
The calcareous Boueina-rich
level (Figs. 2
- 3 , arrow) is about 1.5-2 m thick. The rock is a
packstone, mainly containing fragments of Boueina
hochstetteri Toula (Fig. 2.C-D ;
Pl. 5.E-F ). Additionally, fragments of
bivalves, gastropods, echinoderms, bryozoans, annelid worm tubes, fragments of
sponges and small coral fragments, rare ooids and intraclasts, rare foraminifers
and dasycladalean algae are also present. Among the microfossils identified in
association with Boueina hochstetteri,
we can mention: Coscinophragma sp. and
Ichnusella sp. (among the
foraminifers), and Griphoporella cretacea (Dragastan)
(Pl. 4.B ), Montiella elitzae (Bakalova),
Suppiluliumaella elliotti (Bakalova),
and Salpigoporella pygmaea (Gümbel)
(among the dasycladaleans).
Boueina
hochstetteri clearly
dominates the fossil assemblage; it is present as thalli fragments agglomerated
as wackestone/packstone (at the base), gradually passing to compact packstone
towards the top of the level (Pl. 5 ). The fragments of Boueina thalli can be easily noticed on weathering surfaces
(Fig. 2.C-D ; Pl.
5.A-B ) and on polished surfaces
(Pl. 5.C-D ). Thin sections of these
samples (Pl. 5.E-F ;
Pl. 6 ) reveal the inner structure of the alga. The inner
area consists of medullary filaments (siphons) parallel to the longitudinal axis
of the thallus fragments: they gently bend and bifurcate toward the exterior,
thus leading to the formation of thin cortical external filaments (siphons) that
slightly widen distally. Thallus branching occurs rarely (Pl.
5.A-B ), a feature
that additionally supports the interpretation of De Castro et
al. (2008) for the genus Boueina:
inarticulate thallus with rare branching. Based on the rich material we
collected from the type locality, we will provide additional information on Boueina
hostetteri's inner structure and variability in a future publication.
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Figure
2:
Outcrop aspects. A) General view of the outcrop containing the limestone bank very
rich in Boueina hochstetteri
(arrow). B) Detail with the Boueina
bank (arrows). C-D) Weathering
surfaces of the limestone showing the agglomeration of Boueina
thallus fragments. |
|
Figure
3:
Succession of the Lower Cretaceous deposits from the studied
outcrop with sample location. Arrow points to the level rich in Boueina
hochstetteri Toula. Legend: 1. bioclastic packstone with Boueina;
2. bioclastic-ooidic limestone; 3. bioclastic limestone; 4. fine bioclastic-peloidal limestone; 5. marl; 6. sandstone; 7. fault. |
Outcrops referring to Boueina hochstetteri Toula's type locality have been recently rediscovered, due to construction works for the Niš-Sofia highway (East Serbia, in the Carpatho-Balkanides area). The 1.5-2 m-thick very rich Boueina level is located within a dominant bioclastic limestone succession. It corresponds to wackestone-packstone and packstone mainly consisting of fragmented Boueina thalli. The thalli are sometimes branched, a feature that supports the interpretation of De Castro et al. (2008) who defined B. hochstetteri Toula as an inarticulate udoteacean alga with rare branching.
The present study represents a contribution to the bilateral research project of the Romanian Academy and the Serbian Academy of Sciences and Arts: "Comparison between the Lower Cretaceous deposits in the Resita-Moldova Noua Zone (South Carpathians, Romania) and the Kučaj Zone (Carpatho-Balkanides, Eastern Serbia)". We gratefully acknowledge the constructive comments of the reviewers, Felix Schlagintweit and Bruno Granier, that helped to improve the manuscript. We also thank Stephen Kershaw for corrections of the English.
Andjelković J., Krstić B., Ćirić A., Martinović D. & Bogdanović P. (1975).- Basic Geological Map of SFRY, 1:100,000, Sheet Pirot (K 34-34).- Savezni geološki zavod, Beograd (Zavod za geološka i geofizička istraživanja, Beograd, 1964-1968).
Bassoulet J.-P., Bernier P., Deloffre R., Génot P., Poncet J. & Roux A. (1983).- Les algues Udotéacées du Paléozoïque au Cénozoïque.- Bulletin des Centres de Recherche Exploration-Production elf-Aquitaine, Pau, vol. 7, no. 2, p. 449-621.
Bucur I.I. (1994).- Lower Cretaceous Halimedaceae and Gymnocodiaceae from Southern Carpathians and Apuseni Mountains (Romania) and the systematic position of the Gymnocodiaceae.- Beiträge zur Paläontologie, Wien, vol. 19, p. 13-37.
Bucur I.I., Conrad M.A. & Radoičić R. (1995).- Foraminifers and calcareous algae from Valanginian limestones in the Jerma River Canyon, Eastern Serbia.- Revue de Paléobiologie, Genève, vol. 14, no. 2, p. 349-377.
Clavel B., Busnardo R., Charollais J., Conrad M. & Granier B. (2010).- Répartition biostratigraphiques des orbitolinidés dans la biozonation à ammonites (plate-forme urgonienne du Sud-est de la France. Partie 1 : Hauterivien supérieur-Barrémien basal.- Carnets Geol., Madrid, vol. 10, no. A06, p. 1-53.
De Castro P., Cimmino M.G. & Barattolo F. (2008).- On some infrageneric rank-changes within the Mesozoic Boueina (Chlorophyta, Caulerpales).- Atti dell'Academia Pontaniana ( N.S.), Napoli, vol. LVII, p. 175-182.
Foury G. & Moullade M. (1966).- Orbitolinidae nouveaux du Barrémien (Faciès Urgonien) des Alpilles (Bouches-du-Rhône).- Revue de Micropaléontologie, Paris, vol. 8, no. 4, p. 249-257.
Jankičević J. (1978).- Barrémien et Aptien des parties moyennes des Carptho-Balkanides dans la Serbie orientale au point de vue du développement d'Urgonien.- Geološki Anali Balkanskoga Poluostrva, Beograd, vol. 42, p. 103-194 [in Serbo-Croatian, French summary].
Jankičević J. (1996).- Urgonian of the Carpatho-Balkanides of Serbia in the light of the formation analysis.- Geološki Anali Balkanskoga Poluostrva, Beograd, vol. 60, no. 2, p. 29-40 [in Serbian and English].
Karamata S., Krstić B., Dimitrijević M.D., Dimitrijević M.N., Knežević V., Stojanov R. & Filipović I. (1997).- Terranes between the Moesian Plate and the Adriatic Sea.- Annales Géologiques des Pays Helléniques (1e série), Athènes, vol. 37 (1996-1997), p. 429-477.
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Plate 1:
Microfacies. A) Wackestone-packstone
with large fragments of corals and fragments of bivalves, gastropods,
echinoderms, bryozoans and annelid tubes. Sample 14692; B) Wackestone-packstone with large fragments of sponges (Chaetetids
and Cladocoropsis) and corals,
bivalves, bryozoans, and relative frequent fragments of Boueina. Arrow points to a lithophagid bivalve boring. Sample 14693;
C) Bioclastic-ooidic packstone-grainstone with frequent bryozoans, fragments of bivalves,
gastropods, echinoderms, foraminifers, and dasycladalean algae. Sample 14689; D)
Packstone with large fragments of sponges and corals, bivalves, echinoderms,
bryozoans, foraminifers, dasycladalean algae, and rare fragments of Boueina. Sample 14687; E)
Packstone-grainstone
with fragments of sponges, bivalves, gastropods, echinoderms, annelid tubes and
bryozoans, rare ooids and intraclasts, foraminifers, and dasycladalean algae.
Sample 14688; F) Coarse bioclastic
grainstone with fragments of sponges, bivalves, gastropods, echinoderms,
bryozoans and annelid tubes, peloids, intraclasts, foraminifers, dasycladalean
algae, and rare fragments of udoteacean algae. |
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Plate 2:
Microfacies. A) Coarse bioclastic-intraclastic grainstone with fragments of
sponges, bivalves, gastropods, echinoderms, annelid tubes, bryozoans,
foraminifers, and dasycladalean algae. Sample 15563; B) Coarse bioclastic grainstone with ooids and fragments of corals, bivalves,
gastropods, echinoderms, bryozoans, udoteacean and dasycladalean algae. Sample
14704; C) Bioclastic-peloidal-intraclastic packstone with fragments of bivalves,
echinoderms, bryozoans, foraminifers, and dasycladalean algae. Sample 14701; D) Medium-grained bioclastic-peloidal grainstone with micritized intraclasts
and fragments of bivalves, gastropods, echinoderms, bryozoans, foraminifers, and
udoteacean and dasycladalean algae. Sample 14690; E) Bioclastic grainstone with fragments of sponges, bivalves, gastropods,
echinoderms, bryozoans, foraminifers and dasycladalean algae. Sample 14700; F) Peloidal-bioclastic grainstone with frequent miliolid and small
textulariacean foraminifers, and rare dasycladalean algae. Sample 15562. |
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Plate 3:
Foraminifers. A) Charentia cuvillieri Neumann.
Equatorial section, sample 14690; B) Paracoskinolina?
jourdanensis (Foury & Moullade). Subaxial section, sample 14700;
C) Pfenderina
globosa Foury. Oblique section, sample 14690; D) Neotrocholina sp. Axial section,
sample 14690. |
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Plate 4:
Dasycladalean algae. A) Montiella elitzae (Bakalova).
Oblique section, sample 15566; B) Griphoporella
cretacea (Dragastan). Longitudinal section, sample 14695; C) Zittelina hispanica Masse,
Arias & Villas. Fragment in transverse-oblique section, sample 15563;
D-E) Suppiluliumaella
elliotti Bakalova; D) transverse-oblique section, sample 14687; E)
transverse section, sample 15563; F) Salpingoporella
muehlbergii (Lorenz). Oblique section, sample 14688. |
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Plate 5:
Boueina hochstetteri Toula. A-B) Thallus fragments on a
weathered surface of the rock; A, sample
14695; B, sample FN; C-D) Polished
surfaces showing fragments of the thallus in longitudinal, oblique and
transverse sections; C, sample 14695;
D, sample 14686; E-F) Microfacies
with Boueina in thin section (Boueina
packstone); E, sample 14695; F,
sample 14676. |
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Plate 6:
Boueina hochstetteri Toula. A) Polished surface showing a branched specimen (arrow). sample 14686; B)
A branched specimen of Boueina
hochstetteri in thin section. Sample 15566; C) Longitudinal section. Sample 15566;
D-E) Oblique sections; D, sample 15566; E, sample 14685; F-G) transverse
sections; F, sample 14678; G, sample 15566. The medullary filaments (siphons) in
longitudinal section in C and in
transverse section in F and G, as well as the cortical filaments (siphons) arranged
perpendicularly to the external surface are clearly visible in all specimens
from B to G. |
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