Babeş-Bolyai University, Department of Geology€¦ · Middle Jurassic (Bajocian) echinoids of Bucegi Mountains (Eastern Carpathians, Romania ... Oxfordian, southern Poland ... Microfacies

Babeş-Bolyai University, Department of Geology

Seventh Romanian Symposium on Palaeontology

Cluj-Napoca, 22-24 october 2009

Abstract book

Edited by Ioan I. Bucur, Emanoil Săsăran & Dana Pop

Cluj University Press, 2009

CONTENT

1. B. U. BAYSHASHOV & E. M.E. BILLIA Records of Tapiroidea Gill, 1872 (Mammalia, Perissodactyla) from Kazakhstan – An overview………………………………………...…………………………………

p.1-4

2. C. BELDEAN, S. FILIPESCU & C..AROLDI Early Miocene paleoenvironments in NW Transylvanian Basin: interpretation based on foraminiferal assemblages…………………………………………………………

p. 5-6

3. E. M.E. BILLIA

Occurrences of Stephanorhinus kirchbergensis (Jäger, 1839) (Mammalia, Rhinocerotidae) in Eurasia…………………………………………………………….

p. 7-8

4. A.-V. BOJAR, H.-P. BOJAR, F. OTTNER & D. GRIGORESCU Distribution of heavy mineral assemblages in the Maastrichtian continental deposits of the Hateg basin, Romania: tectonic and palaeogeographic implications…………..

p. 9-10

5. M. BRÂNZILĂ, G. CHIRILĂ & . JITARU

Micropaleontological and paleofloristic content of Sarmatian from southern Moldavian Platform – backbulge depozone…………………………………………..

p. 11

6. A. BRICEAG, G. OAIE, M. STOICA & M. C. MELINTE-DOBRINESCU Holocene paleobiotas in the NWrn Black Sea…………………………………………

p. 12

7. M.BRUNET In Sahelo-Saharian Africa (Chad, Egypt, Libya) on the track of a new cradle of mankind. ………………………………………………………………………………

p. 13-14

8. I. I. BUCUR, J.-P. SAINT MARTIN, E. SĂSĂRAN & S. FILIPESCU

Green algae (Dasycladales, Bryopsidales) in the Middle Miocene deposits from Podeni (western border of the Transylvanian Basin)………………………………….

p. 15

9. C. CATINCUŢ & I. I. BUCUR Microfacies and microfossils in a limestone sequence (Piatra Corbului) from the Meteş Formation (Metaliferi Mountains)……………………………………………..

p. 16-17

10. C. M. CHIRA, D.-T. JURAVLE & M. V. POPA Paleogene-Neogene boundary in Bucovina, Romania: Raşca -Vatra Moldoviţei area…….........................................................................................................................

p. 18-19

11 C. M. CHIRA, D.-T. JURAVLE, P. Z.FODOR & M. . POPA

Cretaceous-Paleogene nannoflora and the K/P boundary in Putna - Suceviţa area (Bucovina, Romania)………………………………………………………………….

p. 20-21

12 D. CIOBANETE, I. LAZAR & A. PANAIOTU

Biometrical quantitative analyses and taphonomy of the Upper Jurassic Lacunosella brachiopod assemblage from Hǎghimaş Mountains (Eastern Carpathians, Romania)..

p. 22-23

13 V. A. CODREA, Z. CSIKI, D. GRIGORESCU, M. VREMIR3, E. SĂSĂRAN & C. JIPA New Upper Cretaceous (Maastrichtian) exposures in Haţeg Basin ………………….

p. 24-25

14 V. A. CODREA & Ş. V. FEIGI The Upper Pliocene Bovidae Pliotragus ardeus (Croizet & Jobert, 1828) (Mammalia, Artiodactyla) at Colteşti (Dacic Basin) …………………………………

p. 26

15 G. C. CORNEANU & M. CORNEANU Cytological and morphological indices used in the study of vegetal fossil species and their actual correspondent species…………………………………………………….

p. 27-28

16 R. CROITOR Phylogeny and speciation in Quaternary cervid genera Eucladoceros and Praemegaceros (Cervidae, Mammalia)……………………………………………….

p. 29-30

17 Z. CSIKI, R. REDELSTORFF & D. GRIGORESCU

Bone histology in the Ornithopods from the Maastrichtian of Haţeg Basin – were these dinosaurs really dwarfs?.......................................................................................

p. 31-32

18 A. DELINSCHI & I. NICOARA

Studies of some Late Turolian Lagomorpha from the Moldavian platform (Republic of Moldova) …………………………………………………………………………..

p. 33

19 F. DIACONU

Contribution concerning the Pontian flora in soutwest Oltenia………………………. p. 34

20 L. DOBRE, C. PANAIOTU & E. GRADINARU Preliminary observations on Middle Triassic mud-mound limestones from Mahmudia (Tulcea unit, North Dobrogean Orogen)………………………………….

p. 35

i

21 O. N. DRAGASTAN & D. K. RICHTER

Stromatolites and calcareous algae of Münder Formation (Tithonian-Berriasian) from NW Germany……………………………………………………………………

p. 36-37

22 J. GALLEMÍ & I. LAZĂR Middle Jurassic (Bajocian) echinoids of Bucegi Mountains (Eastern Carpathians, Romania)………………………………………………………………………………

p. 38-39

23 H. GIELISCH The Ruhr Basin in Central Germany - Review and Outlook…………………………

p. 40

24 E. GIUREA, I. TANŢĂU & M. V. POPA

Palynological study of the Pliocene deposits from Panga quarry (Vâlcea, Romania).. p. 41

25 E. GRĂDINARU & A. SEILACHER

Middle Jurassic Zoophycos in North Dobrogea: An early onshore/offshore migration p. 42

26 E. GRĂDINARU & E. SOBOLEV

First discovery of Rhabdoceras suessi Hauer (Ammonoidea, Upper Triassic) in the exotic Triassic from the East Carpathians…………………………………………….

p. 43

27 M. GRǍDINARU, C. PANAIOTU, L. PETRESCU & I. LAZǍR Sedimentary patterns, carbonate diagenesis and geochemistry of the Jurassic hardgrounds from Bucegi Mountains (Eastern Carpathians)………………………….

p. 44-45

28 D. GRIGORE Kimmeridgian – Lower Tithonian ammonite assemblages from Ghilcoş - Hăghimaş Massif (Eastern Carpathians – Romania)……………………………………………..

p. 46-48

29 S. IAMANDEI, E. IAMANDEI & V. BOZUKOV Is “Pobitite kamani” a Petrified Forest of Varna?.........................................................

p. 49

30 S. IAMANDEI, E. IAMANDEI & V. CODREA A carbonized fossil wood in Ocna-Mureş salt deposit………………………………..

p. 50

31 E. IAMANDEI, S. IAMANDEI & F. DIACONU Fossil woods in the collection of Drobeta-Tr. Severin Museum...................................

p. 51

32 E. IAMANDEI, S. IAMANDEI & E. GRĂDINARU Liassic Petrified Wood in the Carpathian Mountains…………………………………

p. 52

33 S. IAMANDEI, E. IAMANDEI & M. SABĂU DUMITRESCU Petrified wood from Căprioara Valley, Feleac, Cluj………………………………….

p. 53

34 V. IONESI & G. CHIRILĂ New data regarding Congeria fauna from Bârnova-Muntele Formation……………...

p. 54

35 V. IONESI & F. PASCARIU The Formation with Cryptomactra in Palas area (Iaşi, Romania)…………………….

p. 55

36 D. IVANOV Palaeoclimatic reconstructions for the Late Miocene in Southwest Bulgaria based on palynological data……………………………………………………………………..

p. 56-58

37 D. IVANOVA, E. KOLEVA-REKALOVA & N. MALESEVIC Correlation of Upper Jurassic-Lower Cretaceous carbonate platforms in Western Bulgaria and Eastern Serbia based on foraminiferal record and microfacies…………

p. 59-60

38 Š. JÓZSA

Late Aptian planktonic foraminiferal biostratigraphy of the West Carpathian Pieniny Klippen Belt and Fatric units (Choč Mts., Malá Fatra Mts.)…………………………

p. 61

39 D.-T. JURAVLE, C. M. CHIRA, C. MICLĂUŞ, C. GRASU & A. JURAVLE Lithostratigraphical units of the external flysch of the Eastern Carpathians. Terminology issues …………………………………………………………………...

p. 62-64

40 M. A. KAMINSKI & G. SOTO The systematic position of the foraminiferal genus Cubanina Palmer, 1936 and its relationship to Columinella Popescu, 1998…………………………………………...

p. 65

41 B. KOŁODZIEJ, A. JURKOWSKA, M. BANAŚ & D. IVANOVA Cathodoluminescence as a tool in foraminiferal studies: a case study from Oxfordian, southern Poland…………………………………………………………...

p. 66-67

42 F. de LAPPARENT DE BROIN, V. A. CODREA, T. SMITH & P. GODEFROIT

New turtle remains (Kallokibotionidae, Dortokidae) from the Upper Cretaceous of Transylvania (Romania)………………………………………………………………

p. 68-69

43 A. LUNGU & T. OBADĂ

Data on Deinotherium Kaup in the Republic of Moldova …………………………... p. 70

44 D. MERLE, B. CAZE, J.-P. SAINT MARTIN & J.-M. PACAUD

The residual colour patterns of the European Cenozoic molluscs: a new taxonomic

ii

tool…………………………………………………………………………………… p. 71 45 M. MICHETIUC & I. I. BUCUR

Microfacies and microfossils of the Upper Jurassic–Lower Cretaceous limestones from Vâlcan Mountains: an overview………………………………………………..

p. 72-73

46 A. MICLEA & S. FILIPESCU

Preliminary data on the microfauna from Vârciorog (Vad-Borod basin, Romania)… p. 74

47 C.de MUIZON

De la Terre à la Mer, l’histoire évolutive des Cétacés From Earth to Sea, the evolutionary history of Cetaceans…………………………………………………….

p. 75

48 Th. NEAGU & M. DUMBRAVA

Turonian marker Foraminifera associations from the southern part of the Eastern Carpathians: Valea Dambovitei - Intorsura Buzaului area……………………………

p. 76-77

49 I. NICOARA, A. LUNGU & A. DELINSCHI

Fossil squirrels (Rodentia, Mammalia) from the late Miocene of Republic of Moldova………………………………………………………………………………

p. 78

50 L. OLARU, C. GRASU & M. CHIHAIA

Dămuc series of Hăghimaş syncline from East Carpathians, Romania. New petrographical and palynostratigraphical data……………………………………….

p. 79-80

51 V. PARASCHIV Paleofloristic diversity of the Sarmatian deposits (Middle Miocene) from Oltenia province, southern Romania…………………………………………………………

p. 81

52 M. PICKFORD

Geology and palaeontology of Middle Eocene localities in Namibia………………. p. 82-83

53 S. POLAVDER & S. FIŠTER

Valserina primitiva, orbitolinid (Framinifera) from the Upper Hauterivian of Eastern Serbia…………………………………………………………………………………

p. 84-85

54 M. V. POPA

Badenian small gastropods from Borod Basin (NW Romania). Pyramidellidae family…………………………………………………………………………………

p. 86

55 M. E. POPA & A. ZAHARIA Plant-insect interactions in the Lower Jurassic continental formations of the South Carpathians, Romania…………………………………………………………………

p. 87

56 G. POPESCU & I.-M. CRIHAN

Miocene globigerinas from Romania…………………………………………………. p. 88

57 D. A. POPESCU & L. G. POPESCU

Microbial structures in Triassic carbonate deposits from the Eastern Carpathians (northern compartment of the Crystalline Mesozoic Area)…………………………...

p. 89

58 E. POSMOŞANU Middle Triassic cyamodontoid reptiles from Romania……………………………….

p. 90-91

59 M. ROBU, E. ŞTIUCĂ, V. DRĂGUŞIN & C. DIEDRICH Upper Pleistocene Panthera leo spelaea (Goldfuss, 1810) skeleton from Urşilor Cave, Romania……………………………………………………………………….

p. 92-97

60 J.-. SAINT MARTIN, I. I. BUCUR, P. MOISSETTE, J.-J. CORNÉE, M. KAZMER & A. DULAI

Bioconstructions and crusts in Sarmatian carbonate platforms of Hungary…………

p. 98-99

61 S. SAINT-MARTIN, J. RENAUDIE & T. DANELIAN The Middle Eocene Climatic Event (MECO) revealed by siliceous phytoplankton…

p. 100

62 L. SASARAN, E. SASARAN & I. I. BUCUR Sedimentological and paleoecological study of rudist deposits in Gosau facies from Valea Neagra de Criş (Borod Depression)…………………………………………..

p. 101

63 B. SENUT

La paléontologie: de la science à l’éducation............................................................. p. 102-103

64 L. SILYE, B. SZABÓ, S. FILIPESCU & F. WANEK Middle Miocene (Late Sarmatian) foraminifera and ostracoda from the western part of the Transylvanian Basin………………………………………………………….

p. 104

65 J. S. STEYER

Darwin, the amphibians, and the natural selection………………………………… p. 105

66 M. STOICA & I. LAZĂR Middle Jurassic microfaunal assemblages from Bucegi mountains (Strunga – Strunguliţa area)……………………………………………………………………….

p. 106

iii

iv

67 I. TANŢĂU, S. FĂRCAŞ, M. MÎNDRESCU & B. HURDU Pollen analysis in Maramureşului Mountains…………………………………………

p. 107

68 R. TIŢĂ Early Badenian mollusk fauna from Bahna Basin (Southern Carpathians)…………..

p. 108

69 V. TURI, E. SĂSĂRAN & I. I. BUCUR

Upper Jurassic – Lower Cretaceous limestone from Hodobana-Gârda Seacă area (Bihor Mountains)…………………………………………………………………….

p. 109-110

70 D. ŢABĂRĂ & G.l CHIRILĂ

Palaeoclimatic and palaeoenvironmental interpretation of the Sarmatian deposits of Şupanu Formation from Comăneşti Basin (Bacău County)………………………….

p. 111-112

71 P. ŢIBULEAC

First records of nautilids in the Lower Jurassic klippe of Praşca Peak (Rarău Syncline, Eastern Carpathians, Romania) ……………………………………………

p. 113-114

72 D. UNGUREANU & E. BARBU

Upper Jurassic spongolithic atolls in Central Dobrogea……………………………... p. 115

73 S. VASILE, Z. CSIKI & D. GRIGORESCU Reassessment of the spatial extent of the fossil-bearing Maastrichtian middle member, Densus-Ciula formation (Hateg Basin, Romania)………………………….

p. 116-117

74 M. VENCZEL

Middle–Late Miocene snakes from the Pannonian Basin…………………………… p. 118

75 M. M. VREMIR Insect-related traces associated to the Maastrichtian vertebrate assemblages of Alba-Iulia and Haţeg areas (Romania)…………………………………………………….

p. 119-121

76 M. M. VREMIR & V. A. CODREA

Late Cretaceous turtle diversity in Transylvanian and Haţeg basins (Romania)…… P. 122-124

77 M. M. VREMIR, D. M. UNWIN & V. A. CODREA

A giant Azhdarchid (Reptilia, Pterosauria) and other Upper Cretaceous reptiles from Râpa Roşie - Sebeş (Transylvanian basin, Romania) with a reassessment of the age of the “Sebeş Formation”……………………………………………………………

p. 125-128

Records of Tapiroidea Gill, 1872 (Mammalia, Perissodactyla) from Kazakhstan – An overview

Bolat U. BAYSHASHOV1 & Emmanuel M.E. BILLIA2

1 Institute of Zoology, Akademgorodok, Almaty, Kazakhstan, 050060, [email protected] 2 via Bacchiglione 3, 00199 Roma, Italy, [email protected]

Keywords: Tapiroidea, Tapiridae, Lophialetidae, Deperetellidae, Helaletidae, Isectolophidae, Kazakhstan.

Kazakhstan is rich in deposits that have brought to light an extremely vast

collection of fossil remains ranging in age from Paleocene to Pleistocene; the fossil record became more abundant especially starting with the Oligocene. The peak of the Tapiroidea development occurred during the Eocene, therefore almost in all the Eocene and in some Oligocene Kazakh deposits representatives of Tapiroidea were found. Borisyak (1918) was the first author to perform systematic studies on Tapiroidea in Kazakhstan. Based also on the results of further studies, currently the five Tapiroidea families – Tapiridae, Lophialetidae, Deperetellidae, Helaletidae, and Isectolophidae – seem to be rather well represented in Kazakhstan.

Familia Tapiridae Burnett, 1830 (= Taperidae Gray, 1821). According to

Biryukov (1972:169-170), Protapirus gromovae Birjukov, 1972 nov. sp. was attested by a second upper molar (IZ AN KazSSR 1055-21/48-T) found in 1948 in a ravine of Early Oligocene–Late Miocene age along the Ashut River (Turgay Depression, central Kazakhstan), previously attributed by Gromova (1960) to Protapirus Filhol, 1877 (collections: Laboratory of Palaeobiology, Zoological Institute of the Kazakh Academy of Sciences, Almaty).

Other Early Oligocene-Late Miocene remains of the same species were also found in the Turgay region.

Familia Lophialetidae Radinsky, 1965 (= Lophiodontidae Gill, 1872) Subfamilia Lophialetinae Matthew & Granger, 1925. Eoletes gracilis Birjukov,

1974 nov. gen. nov sp. was testified by a Middle Eocene skull (IZ AN KazSSR 5088/69-Chzh) and several other remains from the right bank of the Shynzhyly River (about 8 km north of Kabanbai Village, Alakol District, Taldy-Kurgan region, Northern Jungarya, south-eastern Kazakhstan) (Biryukov, 1974a:57-73).

Familia Deperetellidae Radinsky, 1965. Teleolophus beliajevi Birjukov, 1974

nov. sp. was proved by a P1-M3 dental range (IZ AN KazSSR 4847/68-Chzh) of Middle Eocene age from the right bank of the Shynzhyly River (south-eastern Kazakhstan) (Biryukov, 1974b:78). Further studies performed on this material pointed out the great similarity of this species with Teleolophus medius Matthew & Granger, 1925, therefore it was declared as a synonym (Lucas, Emry & Bayshashov, 1997).

A third lower molar (IP AN GruzSSR L-33) from the Middle Eocene of Obayla (Zaysan Basin, eastern Kazakhstan) was attributed to Teleolophus zaisanicus Gabunia, 1984 nov. sp. (Gabunya, 1984) (collections: Institute of Palaeobiology, Georgian Academy of Sciences, Tbilisi).

Bucur I.I. et al. (eds.) – 7th Romanian Symposium on Palaeontology-Abstracts. Cluj-Napoca, 2009, 1-4

B.U. Bayshashov & E.M.E. Billia - Records of Tapiroidea Gill, 1872 (Mammalia, Perissodactyla) from Kazakhstan

Familia Helaletidae Osborn, 1892 Subfamilia Helaletinae Osborn, 1892 (= Helaletinae Wortman & Earle, 1893).

Remains of Helaletes mongoliensis (Osborn, 1923) came from the Eocene of the Zaysan Basin (eastern Kazakhstan) (Reshetov, 1979:15-16).

H. mongoliensis remains were also recovered from the Eocene of Mongolia, Northern China, and Northern America.

Osteological remains of Ergilia kazachstanica Gromova, 1960 (Ergilia = Ardynia Matthew & Granger, 1923) were identified in:

– Middle Oligocene deposits in a ravine at Shyntuzsay (about 40 km southeast of Turgay, Turgay Depression, Kustanay Region, central Kazakhstan) (IZ AN KazSSR 1182-25/48-T) (Gromova, 1960);

– Late Eocene-Early Oligocene deposits in the Kiin-Kerish Mountain (Northern Prizaysan’, Zaysan Basin) (IZ AN KazSSR 3K-57 257/469 and 0 233/57-3) and from the Middle Oligocene of Myneskisuyek (central Kazakhstan) (Biryukov, 1972:160-166);

– Early-Middle Oligocene of Aktau (Aktau Mountains, Southwestern Jungarya, south-eastern Kazakhstan) (Bajanov & Kostenko, 1961).

However, Ardynia (Ergilia) kazachstanica - considered as a species belonging to the Helaletidae family by Gromova (1952) was later assigned to the Hyracodontidae rhinoceros family by Radinsky (1965, 1967) on the basis of its skeletal remains from Mongolia.

An Eocene new genus-new species – Veragromovia desmatotheroides Gabunia, 1961 – from the Obayla Formation along the Obayla River (Zaysan Basin, eastern Kazakhstan) was described starting from a third upper molar (IP AN GruzSSR 3-V) by Gabunya (1961) (vide autem in Reshetov, 1979:16).

According to some authors (Radinsky, 1965; Prothero & Schoch, 1989), this species is identical with Helaletes nanus Marsh, 1871 known from the North American Middle Eocene.

Finally, along the Obayla River near Maykapchagay (Zaysan Basin) a tapiroid premolar which may confidently be ascribed to the Helaeletidae family was identified (Reshetov, 1979:17-18).

Subfamilia Colodontinae Wortman & Earle, 1893. Colodon orientalis Borissjak, 1918 is represented by an upper jaw fragment provided with P1-M3 dental range from the Middle Oligocene deposits of Shalkarteniz (Chelkar-Teniz Lake, central Kazakhstan) (Borissyak, 1918) (collections: Palaeontological Institute, Russian Academy of Sciences, Moscow, PIN AN 1442-49). Later, Gromova (1960:79-107) and Biryukov (1972:166-169) described some other postcranial remains belonging to C. orientalis from the same locality.

C. orientalis remains were also found in the Middle Oligocene beds of Northern Prizaysan’ (Kiin-Kerish Mountains, Zaysan basin) (Belyaeva & al., 1962:311-312; Reshetov, 1979:18-19) as well as in both Asian and North American Early-Middle Oligocene.

Subfamilia Breviodontinae Reshetov, 1975. From Eocene beds in Obayla (Zaysan Basin) originated a second lower molar assigned to Breviodon sp. (Reshetov, 1979:27).

Subfamilia Rhodopaginae Reshetov, 1975. Middle Eocene remains of Rhodopagus aff. R. minutissimus Reshetov, 1979 were discovered at Chakpaktas (Zaysan Basin). A Rhodopagus sp. third upper premolar was recovered from Eocene beds along the Obayla River near Maykapchagay (Zaysan Basin) (Reshetov, 1979:30-31).

2


Familia Isectolophidae Peterson, 1919. According to Gabunya (1961), two

Isectolophidae (gen. indet.) fragmentary upper molars (M1 and M2) originated from Obayla (Zaysan Basin).

Other representatives of Lophialetidae, Deperetellidae, Helaletidae, and

Isectolophidae families from the Eocene deposits of Chaibulak, Aksyjr, Ulken Ulasty, Obayla, and Kalmakpay (Zaysan Basin) are also known (Gabunya, 1984), as well as finds of representatives of both Lophialetidae and Deperetellidae families from the Eocene of Shynzhyly (south-eastern Kazakhstan) (Kojamkulova & Orlovskaya, 1971).

Investigations carried out during 1993-1995 in the Zaysan Basin by the Kazakh-American scientific team led to an increase of the previous knowledge on Tapiroidea in this region. Skeletal remains of Eoletes sp. Were recovered from the Shakpaktas Formation deposits (Eocene) of Mozhevelnik (Zaysan Basin) (Emry, Lucas & Holbrook, 2001). Furthermore, the above-mentioned authors assumed that remains from the same site ascribed to Subhyracodon tshakpaktasensis (Gabunya, 1999) should be actually assigned to Eoletes sp. Moreover, tapiroids such as Rhodopagus sp. and two other genera falling into the Lophialetidae family – Lophialetes Matthew & Granger, 1925 and Schlosseria Matthew & Granger, 1926 – were also found in the same deposits (unpublished material).

Obviously, this paper does not pretend to sum up all the tapiroid occurrences in Kazakhstan.

As far as the former Soviet Union is concerned, Rhodopagus aff. R. minutissimus remains were found at Andarak (Kyrgyzstan) (Gabunya, 1983:456-457). Tapiridae remains are recorded from three localities only: a Tapirus cf. T. arvernensis Croizet & Jobert, 1828 tooth comes from the Middle Pliocene of Kuchurgan River valley (Odessa, Ukraine) (Korotkevich, 1967:1074-76) and T. arvernensis remains come from the Miocene beds of Khutor Khmel’na (Circassia, Ukraine) (Dubrovo & Kapelist, 1979), while a T. cf. T. arvernensis mandibular fragment provided with some teeth was found in the Pliocene levels of “Kosyakinsky kar’er” [“Kosyakin quarry”] (Stavropol’ District, northern Caucasus) (Belyaeva, 1948:83; Vereshchagin, 1959:52).

More details about USSR tapiroids (Kazakhstan included) and Mongolia are available in Reshetov (1979:12-42) and in Dmitrieva & Nesmeyanov (1982).

REFERENCES

Bajanov V.S. & Kostenko N.N., 1961. Geologicheski razrez Jungarskogo Aktau i ego paleozoologicheskoe obosnovanie [Geological section of the Jungaryan Aktau and its palaeozoological significance] [in Russian]. AN KazSSR (Institut Zoologii), Materialy po istorii fauny i flory Kazakhstana, III: 47-52, Alma-Ata.

Belyaeva E.I., 1948. Katalog Mestonakhozhdenii Tretichnykh Nazemnykh Mlekopitayushchikh na Territorii SSSR [Catalogue of the Localities of Finds of Tertiary Terrestrial Mammals on USSR Territory] [in Russian]. Trudy Paleontologicheskogo Instituta AN SSSR, XV (3): 36-114, Moskva.

Belyaeva E.I., Gromova V.I. & Yanovskaya N.M, 1962. Otryad Perissodactyla (Neparnopalye) [Ordo Perissodactyla] (in: Osnovy Paleontologii – Mlekopitayushchie) [in Russian]. PP. 311-312, Moskva.

Biryukov M.D., 1972. Novye dannye o faune tapiroobraznykh (Tapiridae) Kazakhstana [New data on the fauna of the tapiroids (Tapiridae) of Kazakhstan] [in Russian]. Teriologya, 1: 160-171, Novosibirsk.

Biryukov M.D., 1974a. Novy rod semeystva Lophialetidae iz Eocena Kazakhstana [New genus of the Lophialetidae Family from the Eocene of Kazakhstan] (in: Fauna i Flora iz Mezokaynozoya

3


4

Yuzhnogo Kazakhstana) [in Russian]. AN KazSSR (Institut Zoologii), Materialy po istorii fauny i flory Kazakhstana, VI: 57-73, Alma-Ata.

Biryukov M.D., 1974b. Novy vid roda Teleolophus iz severnoy Jungarii [A new species of the genus Teleolophus from Northern Jungarya] [in Russian]. Teriologya, 2: 78-82, Moskva.

Borisyak A.A., 1918. Ob ostatkakh lofiodontoidnoy formy iz indrikoterievykh sloev Turgayskoy oblasti [On the remains of a lophiodontoid form from the Indricotherium beds of the Turgay region] [in Russian]. Izvestya Rossiyskoy AN, s. VI, 12 (13): 1319-1322, Petrograd.

Dmitrieva E.L. & Nesmeyanov S.A., 1982. Mlekopitayushchie i Stratigrafya Kontinental’nykh Tretichnykh Otlozheniy Yugo-Vostoka Sredney Asii [Mammals and Stratigraphy of Tertiary Continental Sediments of South-East Middle Asia] [in Russian]. Trudy Paleontologicheskogo Instituta AN SSSR, 193: 1-138, Izd-vo “Nauka”, Moskva.

Dubrovo I.A. & Kapelist N.V., 1979. Katalog Mestonakhozhdeniy Tretichnykh Pozvonochnykh USSR [Catalogue of the Localities of the Finds of the Ukrainian SSR Tertiary Mammals] [in Russian]. Izd-vo “Nauka”, 159 pp., Moskva.

Emry R.J., Lucas S.G. & Holbrook L.T., 2001. The lophialetid ceratomorph Eoletes from the Eocene of the Zaysan basin, Kazakstan. Journal of Vertebrate Paleontology (Abstracts of papers), P. 47, Northbrook, Ill.

Gabunya L.K., 1961. Obaylinskaya fauna – Drevneyshy kompleks iskopaemykh mlekopitayushchikh SSSR [Obaylian fauna – The oldest fossil mammalian complex in USSR] [in Russian]. Soobshchenya AN GruzSSR, 27 (6): 711-713, Tbilisi.

Gabunya L.K., 1983. Chakpaktasskaya fauna eozenovykh mlekopitayushchikh [Eocene Chakpaktas mammalian fauna] [in Russian]. Doklady AN SSSR, 283 (2): 456-458, Moskva.

Gabunya L.K., 1984. Kratki obzor faun paleogenovykh mlekopitayushchikh Zaysanskoy vpadiny [Brief review of the Paleogene mammalian fauna from the Zaysan basin] (in: Gabunya L.K., Flora i Fauna Zaysanskoy Vpadiny) [in Russian]. PP. 115-123 (130-132), Tbilisi.

Gabunya L.K., 1999. O novom predstavitele Hyrachyidae iz Eozena Zaysanskoy vpadiny (Vostochny Kazakhstan) [On a new representative of Hyrachyidae from the Eocene of the Zaysan basin (Eastern Kazakhstan)] [in Russian]. Paleontologicheski zhurnal, 5: 88-93, Moskva.

Gromova V.I., 1952. Primitivnye tapiroobraznye iz Paleogena Mongolii [Primitive Tapiroids from the Mongolian Paleogene] [in Russian]. Trudy Paleontologicheskogo Instituta AN SSSR, 41 (1): 99-119, Moskva.

Gromova V.I., 1960. Novye materialy po paleogenovym tapiroobraznym Azii [New Paleogene Tapiroids material from Asia] [in Russian]. Trudy Paleontologicheskogo Instituta AN SSSR, 77 (4): 79-107, Moskva.

Korotkevich O.L., 1967. Persha znakhidka vikopnogo tapira na Ukraini [First find of a fossil tapir in Ukraine] [in Ukrainian]. Dopovidi AN UkrRSR (Paleontologiya), 12: 1074-1076, Kïv [Kiev].

Kojamkulova B.S. & Orlovskaya E.R., 1971. Fauna pozvonochnykh i flora yuzhnoy poloviny Kazakhstana v Mezozoe i Kainozoe [Mesozoic and Caenozoic vertebrate fauna and flora from the southern half of Kazakhstan] [in Russian]. Vestnik AN KazSSR, 5: 25-29, Alma-Ata.

Lucas S.G., Emry R.J. & Bayshashov B.U., 1997. Eocene Perissodactyla from the Shinzhaly river, Eastern Kazakhstan. Journal of Vertebrate Paleontology, 17 (1): 235-246, Northbrook, Ill.

Prothero D.R. & Schoch R.M., 1989. Classification of the Perissodactyla (in Prothero D.R. & Schoch R.M., eds: The Evolution of Perissodactyls). Oxford University Press, pp. 530-537, New York.

Radinsky L.B., 1965. Early Tertiary Tapiroidea of Asia. Bulletin of American Museum of Natural History, 129: 182-263, New York.

Radinsky L.B., 1967. A review of the rhinocerotoid family Hyracodontidae (Perissodactyla). Bulletin of American Museum of Natural History, 136: 1-45, New York.

Reshetov V.YU., 1979. Rannetretichnye tapiroobraznye Mongolii i SSSR [Early Tertiary Tapiroids of Mongolia and USSR]. Trudy SSMPE (Sovmestnaya Sovetsko-Mongol’skaya Paleontologicheskaya Ekspedizya), 11: 1-144, Izd-vo “Nauka”, Moskva.

Vereshchagin N.K., 1959. Mlekopitayushchie Kavkaza – Istorya Formirovanya Fauny [Mammals of Caucasus – History of the Faunal Formation] [in Russian]. AN AzerbSSR, Izd-vo AN SSSR, p. 52 + fig. 25/3, Moskva/Leningrad.

Early Miocene paleoenvironments in NW Transylvanian Basin: interpretation based on foraminiferal assemblages

Claudia BELDEAN1, Sorin FILIPESCU1 & Carlo AROLDI1

1 Babes-Bolyai University, Department of Geology, 1, M. Kogalniceanu Str., 400084, Cluj-Napoca. E-mails: [email protected]; [email protected]; [email protected] Keywords: Foraminifera, Lower Miocene, Hida Formation, Transylvanian Basin

Lower Miocene deep-marine turbidites and coarse-grained fan deltas in north-western Transylvanian Basin belong to the Hida Formation. These were deposited in the flexural basin in front of the Pienides (Krézsek & Bally, 2006).

Our aim was to separate the type foraminifera assemblages and to give new data on the depositional environment based on the identified assemblages.

All the subdivisions of turbiditic depositional environments have been identified in the Hida Formation, from proximal to distal fans with complete Bouma sequences.

The studied sections consist of diverse types of agglutinated foraminifera assemblages, “flysch-type” and slope marl biofacies being dominant. Most characteristic for the “flysch-type” biofacies is the occurrence of coarsely agglutinated forms, such as some species of Psammosphaera, Saccammina, Hyperammina, and thick-walled tubular forms such as Nothia and Psammosiphonella. Foraminifera with carbonatic cement are characteristic for slope marl biofacies: Ammodiscus incertus, Ammodiscus miocenicus, Budashevaella laevigata, Cribrostomoides subglobosus Haplophragmoides sp., Subreophax sp.

Calcareous benthic foraminifera show a high diversity; oxic, suboxic and dysoxic taxa have been separated. Based on benthic foraminifera dissolved oxygen index (BFOI - Kaiho, 1994), changes in oxygen concentration at the sediment-water interface have been emphasized.

Relationships between foraminifera assemblages and sedimentological features indicate a bathyal distribution of facies with frequent intercalations of organic input and bioturbations. All these can be framed into a deep-water marine environment ranging from the outer shelf to the lower slope where the sedimentary supply largely fluctuated.

Planktonic foraminifera identified in the Hida Formation could be included into the Globigerinoides trilobus (Reuss) zone (Popescu, 1975). This zone corresponds to N5-N7 zone (Blow, 1969) or M2-M4 zone (Berggren et al., 1995).

At basinal scale, Lower Miocene deep-water and shelf deposits were separated as distinct lithostratigraphic units (Hida Formation and Chechiş Formation) which coexisted in the same basin as contemporary environments. REFERENCES Berggren W.A., Kent D.V., Swisher C.C., Aubry M.P., 1995. A revised Cenozoic geochronology and

chronostratigraphy. Geochronology Time Scale and Global Stratigraphic Correlation, Special Publication, 54: 129-212.

Blow W. H., 1969. Late Middle Eocene to Recent planktonic foraminiferal biostratigraphy. Ist International Conference of Planktonic Micropaleontology, Geneva, 1: 199-422.

Kaiho K., 1994: Benthic foraminiferal dissolved-oxygen index and dissolved-oxygen levels in the modern ocean. Geology, 22: 719-722.


mailto:[email protected]



C. Beldean et al. - Early Miocene paleoenvironments in NW Transylvanian Basin: interpretation based on foraminiferal assemblages

6

Krézsek C., Bally A.W., 2006. The Transylvanian Basin (Romania) and its relation to the Carpathian fold and thrust belt: Insights in gravitational salt tectonics. Marine and Petroleum Geology 23: 405-42.

Popescu G., 1975. Études des foraminifères du Miocène inférieur et moyen du nord-ouest de la Transylvanie. Mémoires - Institut de Géologie et de Géophysique XXIII: 1-121.

Occurrences of Stephanorhinus kirchbergensis (Jäger, 1839) (Mammalia, Rhinocerotidae) in Eurasia

Emmanuel M.E. BILLIA1

1 via Bacchiglione 3, 00199 Roma, Italy, [email protected]

Keywords: Stephanorhinus kirchbergensis, “nosorog Merka”, Middle Pleistocene, Eurasia

Stephanorhinus kirchbergensis (Jäger, 1839) (= Rhinoceros mercki Jäger, 1839 =

Dicerorhinus kirchbergensis [Jäger, 1839]) – better known in Russia and in all the former Soviet Union as “nosorog Merka” (literally, Merck’s rhinoceros) – was one of the most characteristic members of the Western European late Middle Pleistocene interglacial fauna (Czyzewska, 1962).

The S. kirchbergensis spreading areal would include a large part of the Eurasian landmass – from France up to China – in this context excluding the areas situated at both high and low latitudes. An exception is represented by only one case close to 64° N in Siberia (Dubrovo, 1957) which corresponds to the northernmost S. kirchbergensis record among all the finds regarding this species in Eurasia.

On the basis of fossil evidence – though widely spread throughout Eurasia – the tandem-horned S. kirchbergensis seems to be elsewhere barely represented within this enormous geographical extension. On the whole, its records appear to be more numerous in Western Europe than in the Eastern one, or in Asia.

Mostly frequenting forests, S. kirchbergensis supposedly inhabited Eurasia in the time span from MIS 15-13 up to the Eemian Interglacial (Substage 5e). Remains ascribed to this taxon come from England, France, Germany, Austria, Italy, Slovenia, Croatia, Hungary, Czech Republic, Slovakia, Poland, Romania, Moldova, Ukraine, Armenia, Azerbaijan, Tajikistan, Kazakhstan, Korea, and China.

Both Russian and Italian S. kirchbergensis material has been revised using morphological and non-metric characters by the author (Billia, 2008a, 2008b; Billia & Petronio, 2009).

Unfortunately – at least at present – a large part of the fossil material described in literature and assigned to this taxon is only partly available in the Eurasian museum collections.

Very often diagnostically misidentified with other rhinoceros species – Stephanorhinus megarhinus (de Christol, 1834), S. elatus (Croizet & Jobert, 1828), S. etruscus (Falconer, 1868), S. hundsheimensis (Toula, 1902), S. hemitoechus (Falconer, 1868), Coelodonta antiquitatis (Blumenbach, 1799) – during the last two centuries S. kirchbergensis has been identified with more than thirty other synonyms. Besides, for a long time it was believed that S. kirchbergensis and S. hemitoechus represented a sole species.

History, general characters, anatomical and odontological features of S. kirchbergensis have extensively been discussed in previous works (Billia, 2008a, 2008b; Billia & Petronio, 2009). There is no doubt that S. kirchbergensis – among the Plio-Pleistocene rhinoceros species – is characterized by unique odonto-morphological traits and is therefore one of the most distinctive species. Unfortunately, very few well dated cranial and postcranial remains are elsewhere available.

Until to day, the area of origin of S. kirchbergensis has not been yet identified, even if in the author’s opinion the Central Asian one would seem fairly plausible.

In any case, it is useless to deny when faced with facts that S. kirchbergensis is a rhinoceros still scarcely investigated and consequently not well known yet.


E.M.E. Billia - Occurrences of Stephanorhinus kirchbergensis (Jäger, 1839) (Mammalia, Rhinocerotidae) in Eurasia

8

REFERENCES Billia E.M.E., 2008a. The skull of Stephanorhinus kirchbergensis (Jäger, 1839) (Mammalia,

Rhinocerotidae) from the Irkutsk region (Southwest Eastern Siberia). Quaternary International, 179 (1): 20-24. [http://dx.doi.org/10.1016/j.quaint.2007.08.034]

Billia E.M.E., 2008b. Revision of the fossil material attributed to Stephanorhinus kirchbergensis (Jäger, 1839) (Mammalia, Rhinocerotidae) preserved in the museum collections of the Russian Federation. Quaternary International, 179 (1): 25-37. [http://dx.doi.org/10.1016/j.quaint.2007.09.034].

Billia E.M.E. & Petronio C., 2009. Selected records of Stephanorhinus kirchbergensis (Jäger, 1839) (Mammalia, Rhinocerotidae) in Italy. Bollettino della Società Paleontologica Italiana, 48 (1):1-12, Modena.

Czyzewska T., 1962. Uzebienie górnej szczeki Dicerorhinus mercki (Jäger) ze Szczesliwice kolo Warszawy [Upper dentition of Dicerorhinus mercki (Jäger) from Szczesliwice near Warszawa (Poland)] [in Polish]. Acta Palaeontologica Polonica, 7 (1-2): 223, Warszawa.

Dubrovo I.A., 1957. Ob ostatkakh Parelephas wüsti (M. Pavl.) i Rhinoceros mercki Jäger iz Yakutii [On remains of Parelephas wüsti (M. Pavl.) and Rhinoceros mercki Jäger from Yakutya] [in Russian]. Byulleten’ Komissii po Izucheniyu Chetvertichnogo Perioda, 21: 97-104, Izd-vo AN SSSR, Moskva/Leningrad.

Distribution of heavy mineral assemblages in the Maastrichtian continental deposits of the Hateg basin, Romania: tectonic and

palaeogeographic implications

Ana-Voica BOJAR1, Hans-Peter BOJAR2, Franz OTTNER3 & Dan GRIGORESCU4

1 Institute of Earth Sciences, Geology and Palaeontology, Karl-Franzens University, Heinrichstrasse 26, A-8010 Graz, Austria, e-mail: [email protected] 2 Department of Mineralogy, Landesmuseum Joanneum, Raubergasse 10, A-8010 Graz, Austria 3 Institute for Applied Geology, University of Natural Resources and Applied Life Sciences, Peter Jordan Strasse 70, A-1190 Vienna, Austria 4 Department of Geology and Geophysics, Bucharest University, Bd. Bălcescu 1, RO-010041 Bucharest, Romania Keywords: eavy minerals, Maastrichtian, Haţeg Basin, Romania

The study represents the first extensive investigation on source-areas of the Maastrichtian continental deposits in the Haţeg basin using heavy mineral assemblages. Heavy mineral concentrates were performed on 11 samples (siltstones to sandstones) collected from different parts of the basin. The heavy mineral identification was done using a polarization microscope (transmitted and reflected light) and with the scanning electron microsocope. A minimum of 250 mineral grains were counted for each sample.

The heavy mineral associations consist of garnet, hematite, magnetite, ilmenite, rutile, staurolite, kyanite, epidote, apatite, titanite, tourmaline and zircon. Garnet, with its wide range of chemical compositions, is a standard tool for provenance studies of sandstones or river sediments (Morton et al., 2004; Mange and Morton, 2007). In order to constrain source areas, Morton et al. (2004) plotted garnet analyses from river sediments from the northern Scotland and Norway. They defined four type of fields (from A to D) within the ternary system Mg – Ca – Fe+Mn. Field A has low Ca-contents with variable XMg/XFe+Mn. Field B has low XMg and variable XFe+Mn/XCa. Field C covers the centre of the ternary. For the Haţeg basin, the summary diagram shows that more than 90% of the analyses plot within the two B fields. Based on these analyses the source of most garnets is an amphibolite-facies metasedimentary rock. Around 8 % of the analyses plot in the Ci field showing that these garnets are derived from high-grade metabasic rocks (Mange and Morton, 2007). The general pattern shows different source areas with contrasting metamorphic grades for the different parts of the basin. The sediments of the northern and central sectors of the basin show a high proportion of garnet, staurolite and kyanite and a low proportion of epidote, supporting an amphibolite-facies metamorphic source area, compatible with the lithology of the Getic upper plate on which the basin formed. The samples with abundant amphibolite-facies heavy mineral components have high proportions of magnetic Fe-Ti-oxides with complex exsolution/intergrowth features. These oxides belong to the hematite-ilmenite solid-solution series and are indicating a high-grade metamorphic and/or igneous source area. Southwards the heavy mineral spectra change to epidote-rich reflecting exhumation and erosion of the greenschist metamorphic rocks of the Danubian lower plate during updoming and core-complex formation.

MOEL/Österreichsiche Forschungsgemeinschaft is acknowledged for finnancial support.


A.-V. Bojar et al. - Distribution of heavy mineral assemblages in the Maastrichtian continental deposits of the Hateg basin

10

REFERENCES Mange, M.A., Morton, A.C., 2007. Geochemistry of Heavy Minerals: in Mange, M.A. & Writh, D.T.,

(Eds.) Heavy Mineral in Use, Developments in Sedimentology 58, 345-391. Morton, A.C., Hallsworth, C., Chalton, B., 2004. Garnet compositions in Scottish and Norwegian

basement terrains: a framework for interpretation of North Sea sandstone provenance. Marine and Petroleum Geology 21, 393–410.

Micropaleontological and paleofloristic content of Sarmatian from southern

Moldavian Platform – backbulge depozone

Mihai BRÂNZILĂ1, Gabriel CHIRILĂ1 & Mihaela JITARU1

1 “University Al. I. Cuza” Iaşi, Departament of Geology, Bd. Carol I, nr. 20A, 700505, Iasi, Romania, e-mail: [email protected], [email protected] Keywords: Miocene, Moldavian Platform, palynomorphs, microfauna

The southern part of the Moldavian Platform evolved under complex conditions, partly similar with those in the northern part, i.e. in a marine environment corresponding to the last stage of evolution of the foreland basin of the Eastern Carpathians, with an obvious tectonic control.

The investigated samples originate from Stăniţa – Vlădicele borehole (Neamţ County), located nearby the tectonic limit represented by the Fălciu – Plopana fault (Vaslui County), which separates the Moldavian Platform from the Bârlad Platform.

Only Sarmatian deposits have been intercepted along the whole borehole profile, from the limit with the Badenian anhydrite until the Cryptomactra clays (Lower Bessarabian and beginning of Upper Bessarabian). Deposits of this interval belong to the first stage of evolution of the foreland basin where the subsidence was polarized from east to west, being induced by the influence of the break-thrust.

Under such circumstances, an evolutionary trend of the microfauna and paleofloras associations typical to backbulge depozone can be noticed.

The following microfauna taxa have been identified: Articulina glabra, Articulina problema, Elphidium aculeatum, Elphidium macellum, Quinqueloculina reussi, Quinqueloculina consobrina, Cibicides badenensis, Ammonia beccarii, and Porosononion subgranosus confirming the presence of the Sarmatian, starting with the Buglovian, the Volhynian and most of the Bessarabian.

The identified palynomorphs are represented by taxa such as: Pityosporites labdacus, Pityosporites alatus, Pityosporites insignis, Pinuspollenites miocaenicus, Abiespollenites sp., Myricipites bituitus, Tricolpopollenites liblarensis, Tricolporopollenites henrici, Carpinipites carpinoides, Engelhardtioides microcoryphaeus, Leiotriletes sp. etc.

Bucur I.I. et al. (eds.) – 7th Romanian Symposium on Palaeontology-Abstracts. Cluj-Napoca, 2009, 11



Holocene paleobiotas in the NWrn Black Sea

Andrei BRICEAG1, Gheorghe OAIE1, Marius STOICA2 & Mihaela C. MELINTE-DOBRINESCU1

1 National Institute of Marine Geology and Geo-ecology, 23-25 Dimitrie Onciul Street, RO-024053 Bucharest, Romania; 2 University of Bucharest, Faculty of Geology and Geophysics, Bucharest, Romania; e-mail addresses: [email protected]; [email protected]; [email protected]; [email protected] Keywords: Romanian shelf: ostracods; foraminifera; calcareous nannoplankton; Holocene.

Our investigation focused on Holocene sediments recovered by a core placed in the southern Romanian Black Sea Shelf, in a shallow environment, at around 28 m water depth. From lithological point of view, in the interval 0-183 cm the investigated core is mainly characterized by the deposition of a grey mud, alternating with thin, centimetres in size, sands and coquina layers; mainly broken shells of mollusks, such as Modiolus and Mytilus, as well as small gastropods, are present.

The calcareous nannoplankton is represented by assemblages with Emiliania huxleyi and Braarudosphaera bigelowii. In the oldest sampled cores (15 cm), only reworked nannofossil taxa from Cretaceous, Paleogene and Neogene deposits are present.

The microfauna is dominated by brackish forams and ostracods that are still common in the actual Black Sea communities (at a salinity below18g/l). The forams’ assemblage is dominated by the important development of Ammnoia beccari that can be associated with scarce species belonging to Haynesina, Porosononion, Elphidium and Quinqueloculina genera.

Ostracods are represented by brackish taxa especially from the Cytheracea group, commonly containing Cyprideis littoralis (Brady), Leptocythere multipuncatata (Sequenza), L. devexa Schornikov, L. histriana Caraion, Amnicythere striatocostata (Schweyer), A. quinquetuerculata (Schveyer), A. reticulata (Schornikov), A. cymbula (Livental), A. olivina (Livental), Callistocythere diffusa (G.W. Müller), Cythereiss rubra pontica Dubovski, Heterocythereiss amnicola (G.O. Sars), Loxoconcha granulata G.O. Sars, L. gibboides (Livental), L. aestuarii Marinov, Limnocythere inopinata (Baird), Cytherura euxinica Caraion, Cytheroma variabilis G.W. Müller, Cytherois cepa, Paracytherois agigensis Caraion, Pontocythere bacescoi (Caraion), P. tchernjawskii Dubowski, Cytheroma variabilis G.W. Müller, Xestolebris decipiens G. W. Müller, X. corenelii Caraion, and X. chanakovi Livental. The Cypridacea taxa are very rare, being represented by ostracod species such as Paracandona albicans (Brady), Pseudocandona sp. and Ilyocypris gibba (Ramdohr). The vertical distribution of the microfauna suggests short-term variations concerning paleobathymetry and paleosalinity.







In Sahelo-Saharian Africa (Chad, Egypt, Libya) on the track of a new cradle of mankind

Michel BRUNET1, 2

1 Collège de France Chaire de Paléontologie humaine, 3 Rue d’Ulm, 75231 Paris Cedex 05. [email protected] Institut International de Paléoprimatologie et Paléontologie Humaine : Evolution & Paléoenvironnements (IPHEP, UMR CNRS 6046). Université de Poitiers F86022 Poitiers Cedex, FRANCE. [email protected] 2 The Mission Paléoanthropologique Franco-Tchadienne headed by Michel Brunet is an international scientific transdisciplinary collaboration between Collège de France (Paris), University of Poitiers, University of N’Djamena and CNAR (N’Djamena) including more than sixty researchers from ten countries.

Keywords: Early Hominids, Late Miocene, Early Pliocene, Sahelo-Saharian Africa

The idea of an ascendance for our species is quite recent (about 150 years ago). But which was our ancestral group, when and where did it arise? ... Even if these

questions entail more constraints, they are still currently unresolved. In the 80’s, early hominids identified in South and East Africa - the oldest being

found in East Africa, led to the elaboration of an “East Side Story», i.e. the bipedal hominid original savannah paleoscenario (Coppens, 1983).

Starting with 1994, the M.P.F.T.2 diggings in the Djurab desert (Northern Chad) successively unearthed a new australopithecine, Australopithecus bahrelghazali Brunet et al. 1996, nicknamed Abel and dated as 3.5 Ma old, the first ever found west of the Rift Valley (Brunet et al., 1995). Later, a new hominid - the earliest yet found (nicknamed Toumaï), Sahelanthropus tchadensis (Brunet et al., 2002) was recovered from late Miocene deposits and dated as 7 Ma old (Vignaud et al., 2002; Lebatard et al.,2008). This new milestone suggests that an exclusively southern or eastern African origin for the hominid clad is unlikely to be correct.

Since 1994, our roots went deeper, from 3.6 Ma to 7 Ma up to date, with three new Late Miocene species: Ardipithecus kadabba Haile-Selassie, 2001 (5.2–5.8 Ma, Middle Awash, Ethiopia), Orrorin tugenensis Senut et al., 2001 (ca. 6 Ma, Lukeino, Kenya) the oldest species ( 7 Ma) being the Chadian one. These discoveries have a scientific impact similar to that of A. africanus Dart, 1925.

S. tchadensis displays a unique combination of primitive and derived characters that clearly show no relationship with chimpanzees or gorillas, but obvious connections with later hominids and temporal links to the last common ancestor between chimpanzees and humans (Brunet et al., 2002 & 2005; C. P. E. Zollikofer & al., 2005). In Chad, the Late Miocene sedimentological and paleobiological data point to a mosaic-type landscape (Vignaud et al., 2002). Today, in Central Kalahari (Bostwana) the Okavango delta appears to be a good analog with such a mosaic of lacustrine and riparian waters, swamps, patches of forest, wooded islets, wooded savannah, grassland and desertic areas (Brunet et al., 2005). Within this mosaic landscape, the detailed features of the habitat where Toumaï lived are still to be defined; however, as in the case of other known late Miocene Hominids, we assume a wooded one. Moreover, these three late Miocene hominids were probably usual bipeds. Thus, models assuming a significant role of savannah habitats in the hominid origin must be reconsidered. Now, it appears that the earliest hominids inhabited wooded environments and were not restricted to Southern or Eastern Africa but were



M. Brunet - In Sahelo-Saharian Africa (Chad, Egypt, Libya) on the track of a new cradle of mankind

14

rather living in a wider geographic region, including also Sahelian Africa: at least Central Africa (Chad) and maybe also North Eastern Africa (Libya and Egypt) (Brunet, 2008) have to be taken into account.

Accordingly, the early hominid history must be reconsidered within completely new paradigms. SELECTED BIBLIOGRAPHIC REFERENCES Brunet, M. & al. (1995) The first australopithecine 2 500 kilometres west of the Rift Valley (Chad).

Nature 378: 273-274. Brunet M. et al. (1996) - Australopithecus bahrelghazali une nouvelle espèce d'Hominidé ancien de la région de Koro Toro (Tchad). C.R. Acad. Sc. Paris, 322, Iia: 907-913.

Brunet, M.& al. (2002) A new hominid from the Upper Miocene of Chad, Central Africa. Nature 418:145-151.

Brunet M. & al. (2005). New material of the Earliest Hominid from the Upper Miocene of Chad. Nature 434: 753-755.

Brunet M.(2006). D’Abel à Toumaï, Nomade Chercheur d’Os, Editions Odile Jacob, Paris. Brunet M; (2008) Origine et Histoire des Hominidés…Nouveaux paradigmes.Leçon inaugurale du

Collège de France, Editions Fayard Paris (in press). Coppens, Y. (1983) Le singe, l’Afrique et l’Homme. Jacob/Fayard Paris. Dart, R. (1925) Australopithecus africanus, the man-ape of South Africa. Nature 115: 195-199. Haile-Selassie, Y. (2001) Late Miocene hominids from the Middle Awash, Ethiopia. Nature 412: 178-

181. Lebatard A.E. & al (2008) Cosmogenic nuclide dating of Sahelanthropus tchadensis and

Australopithecus bahrelghazali: Mio-Pliocene hominids from Chad. PNAS 105 (9): 3226–3231. Senut, B. & al. (2001) First hominid from the Miocene (Lukeino formation, Kenya). C R Acad Sci

Paris 332: 137-144. Vignaud, P. & al. (2002) Geology and palaeontology of the Upper Miocene Toros-Menalla hominid

locality, Chad,Nature 418: 152-155. Zollikofer C.P.E. & al. (2005). Virtual Cranial Reconstruction of Sahelanthropus tchadensis. Nature 434: 755-759.

Green algae (Dasycladales, Bryopsidales) in the Middle Miocene deposits from Podeni (western border of the Transylvanian Basin).

Ioan I. BUCUR1, Jean-Paul SAINT MARTIN2, Emanoil SĂSĂRAN1

& Sorin FILIPESCU1

1 Babeş-Bolyai University, Department of Geology, str. M. Kogălniceanu nr.1, 400084 Cluj-Napoca, Romania. E-mails: [email protected]; [email protected]; [email protected] 2 Muséum National d’Histoire Naturelle, Département Histoire de la Terre, UMR CNRS 7207, 8 rue Buffon, Paris, France. [email protected] Keywords: Dasycladales, Bryopsidales, Miocene, Transylvanian Basin

Middle Miocene carbonate deposits on the western border of the Transylvanian Basin (Gârbova de Sus Formation) are well exposed at Gârbova de Sus, Lopadea Veche, Podeni and Moldoveneşti (Filipescu, 1996). The succession of lower Badenian carbonates is well opened by the Podeni quarry and the outcrop north-west of it. It begins with rhodoid wackestones, and continues with bioclastic grainstones, grainstones/packstones and packstones. Patch-reefs of coral and coralgal boundstone were reported in the middle part of the section (Saint Martin et al., 2007).

Bioclastic packstones and grainstones with fragments of bivalves, gastropods, annelids, beyozoans, echinoderms, foraminifera (frequently large calcareous benthics) and calcareous green algae (Halimeda sp. and Neomeris sp.) occur abobe the reef facies. Non-geniculate and geniculate corallinaceans (including Titanoderma sp. and Corallina sp.) have been occasionally identified.

Miocene halimedaceans and dasycladaceans seem to be more related to Recent than to fossil taxa. The different sections through Halimeda segments are comparable with sections of Recent Halimeda tuna (Ellis & Solander). Halimedaceans are also known as very important sediment producers in modern shallow-water carbonate environments. Moreover, since Miocene, Halimeda is building sometimes bioclastic mounds, as shown from Spain (Braga et al., 1996).

Regarding the dasycladaceans, it is important to point out that very few species of Neomeris were described from Neogene deposits: Neomeris ambigua Morellet, Neomeris ignota Morellet (both species discribed from the Miocene deposits of Coştei and Lăpugiu in Romania), Neomeris bowdenensis Racz and Neomeris venezuelensis Weisbord (the last two from the Pliocene of Jamaica and Venezuela, respectively). Also, seven Recent species of Neomeris are known. The specimens we found at Podeni seem to be the first report of Midle Miocene (Lower Badenian) Neomeris.

The green algae, and especially of dasycladaceans identified above the coral patch-reefs document a shallowing of the depositional environment. This hypothesis is also supported by the presence of beach-rock intercalations in the upper part of the sequence from Podeni. REFERENCES Braga J.C., Martin J.M. & Riding R., 996. Internal structure of segment reefs: Halimeda algal mounds

in the Mediterranean Miocene. Geology, 24/1, 35-38. Filipescu S., 1996. Stratigraphy of the Neogene from the western border of the Transylvanian Basin.

Studia Universitatis Babeş-Bolyai, Geologia, XLI/2, 3-77. Saint Martin J.-P., Merle D., Cornée J.-J., Filipescu S., Saint Martin S. & Bucur I.I. (2007) - Les

constructions coralliennes du Badénien (Miocéne moyen) de la bordure occidentale de la Dépression de Transylvanie (Roumanie). Comptes Rendus Palevol, 6, 37-46.



Microfacies and microfossils in a limestone sequence (Piatra Corbului) from the Meteş Formation (Metaliferi Mountains)

Camelia CATINCUŢ1 & Ioan I. BUCUR1

1 Babeş-Bolyai University, Department of Geology, 1, M. Kogălniceanu Str., 400084 Cluj-Napoca. E-mails: [email protected]; [email protected] Keywords: Microfossils, carbonates, wildflysch, Metaliferi Mountains

Piatra Corbului is a calcareous block located in the central-southern part of the

Metaliferi Mountains, on Ampoiului Valley, between Tăuţi and Meteş localities (east of Zlatna).

Piatra Corbului belongs to Meteş Formation (Lower Aptian-Middle Albian), one of the most studied geologic formations of the Feneş Unit (Metaliferi Mountains). The Meteş Formation (Bleahu & Dimian, 1967) has a typical wildflysch character. A marly-silty matrix embeds olistoliths consisting of ophiolites, Upper Jurassic massive limestones, granodiorites and Lower Cretaceous sandstones (Bleahu et al., 1981).

Piatra Corbului represents a calciruditic conglomerate bed caught within a wildflysch sequence (Gherman, 1943). In this area, because of tectonic events, the beds were straightened-up to the vertical. The erosion of the softer sediments surrounding the limestone led to its present-day appearance as a prominent rock wall, 9 meters in height and about 1.50 meters in width.

This calcareous body is composed of limestone and basic eruptive rocks (andesites, weathered basalts) blocks caught in carbonate cement. A closer look to the limestone blocks reveals their breccious nature given by the presence of Upper Jurassic and Lower Cretaceous limestone clasts. The carbonate cement may contain quartz grains and basic eruptive rocks. The matrix also contains orbitolinid foraminifera and algae.

The following microfacies types have been identified in the clasts forming the breccia: boundstone with corals and sponges, coral-microbial boundstone, bindstone (microbial crusts), bioclastic-peloidal grainstone, bioclastic wackstone/packstone. All microfacies types contain a large variety of bioclasts: corals, sponge, bryozoans, gastropods, echinoderms, foraminifers, calcareous algae, calpionellids and annelid worms.

The micropaleontological assemblage is relatively rich and consists of: foraminifera [Montseciella arabica (HENSON), Paracoskinolina sp., Protopeneroplis sp., Trocholina sp., Andersenolina sp., Charentia sp., Coscinophragma sp., Spirillinid foraminifera], algae [Griphoporella jurassica (ENDO), Neoteutloporella socialis (CAROZZI), Salpingoporella annulata CAROZZI, ?Salpingoporella genevensis (CONRAD), “Solenopora” sp., Nipponophycus ramosus YABE & TOYAMA, Thaumatoporella parvovesiculifera (RAINERI)), calpionellids (Calpionella alpina LORENZ), annelid worms (Mercierella dacica DRAGASTAN), microproblematic organisms [Crescentiella morronensis (CRESCENTI), Lithocodium aggregatum ELLIOTT, Koskinobulina socialis CHERCHI & SCHROEDER, Bacinella irregularis RADOIČIĆ, Labes atramentosa ELIAŠOVA, Radiomura cautica SENOWBARI-DARYAN & SCHAFFER, Iberopora bodeuri GRANIER & BERTHOU) and rivulariacean-type cyanobacteria (Diversocallis sp.).


C. Catincuţ & I.I. Bucur - Microfacies and microfossils in a limestone sequence (Piatra Corbului) from the Meteş Formation

17

The orbitolinid foraminifer Montseciella arabica (HENSON) identified in the sediment between the carbonate clasts points to an Upper Barremian-Lower Aptian age for the formation of the breccia.

Acknowledgements: This study is a contribution to the CNCSIS project BD 409. REFERENCES Bleahu, M. & Dimian, G., 1967. Studii stratigrafice şi tectonice în regiunea Feneş-Ighiel-Întregalde (M.

Metaliferi). Dări de Seamă ale Şedinţelor LIII/1 (1965-1966): 282-304. Bleahu, M., Lupu, M., Patrulius, D., Bordea, S., Ştefan, A. & Panin, S., 1981. The Structure of the

Apuseni Mountains. Guide to excursion B3, Asociaţia Geologică Carpato-Balkanică, Congresul XII, 107 p.

Gherman, I., 1943. Cercetări geologice în colţul de SV al Depresiunii Transilvaniei (între Valea Stremţului şi Valea Ampoiului). Revista Muzeul Mineralogic-Geologic al Universitatii din Cluj, VII (1-2). p. 1-110.

Paleogene-Neogene boundary in Bucovina, Romania: Raşca -Vatra Moldoviţei area

Carmen Mariana CHIRA1, Doru-Toader JURAVLE2 & Mirela Violetta POPA1

1 Babeş-Bolyai University, Faculty of Biology and Geology, Department of Geology, 1 Kogălniceanu St., Cluj-Napoca, 400084, Romania, [email protected] 2 Faculty of Geography and Geology, “Al. I. Cuza” University, 20A, Carol I Street, 700505-Iaşi, Romania, [email protected] Keywords: Pg/Ng boundary, flysch, Bucovina, Raşca-Vatra Moldoviţei, calcareous nannofossils.

The present study was realised in the area between the localities Raşca and Vatra

Moldoviţei. It focused especially on Raşca area, were the section from Loba Valley was studied concerning the calcareous nannofossils and compared with the previous studied section from Dumbravnic Brook, as well as with other sections.

Loba Valley is a left affluent of Moldoviţa Valley. The section was studied starting from the confluence of Loba and Moldoviţa valleys, which is located in Raşca locality (Fig. 1).

Fig. 1. Simplified geological map of the Raşca – Moldoviţa area (according to Joja et al., 1984; Juravle et al., 2008; Micu, 1981, and our own field data) with location of the studied logs.

In Moldoviţa Basin, the Paleogene/Neogene boundary was remarked in the

northern part of the Tarcǎu Nappe, in the Vineţişu Formation. The calcareous nannofossils from Izvor Brook, separated from the pelitic intervals of the limestones belonging to the Jaslo Limestone have been studied. The presence of the NP25 Biozone – with Sphenolithus ciperoensis was documented. In the succession from Izvor Brook that crosses the Dilma – Deia and Palamania – Ascuţita synclines, the



C.M. Chira et al. - Paleogene-Neogene boundary in Bucovina, Romania: Raşca -Vatra Moldoviţei area

19

subsequent biozone is represented by NN1 - with Triquetrorhabdulus carinatus (Ionesi & Meszaros, 1989, Juravle, 2007). The Oligocene – Miocene boundary was evidenced in the terminal part of the Lower Member of the Vineţişu Formation (Ionesi & Meszaros, 1989). The Vineţişu Formation represents the last term of the Moldoviţa Lithofacies and it consists of sandstones and clays, 100 – 120 m thick. The calcareous sandstones are disposed in beds with thicknesses of 30 – 40 cm (Grasu et al., 2007).

Previous studies were realised on Dumbravnic Brook, affluent of the Secrăieş Valley, which is the affluent of the Moldoviţa Valley, nearby Moldoviţa locality (Chira et al., 2008).

In the section from Dumbravnic Brook, which crosses the Dilma – Deia and Palamina – Ascuţita synclinal structures, the sediments belong to the Vineţişu Formation. In the second part of the section, the calcareous nannofossils assemblages contain species that are present also on the top of the Oligocene/Miocene boundary, which are frequent in the Lower Miocene: Helicosphaera scissura (NP24 – NN4), H. recta (NP24 – NN4), Discoaster deflandrei (NP11 – NN7), Sphenolithus moriformis (NP12 – NN9) etc.; also Paleogene species are present. The presence of Triquetrorhabdulus carinatus was remarked in the second part of the section; in the upper part, also Helicosphaera ampliaperta was identified. Thus, the presence of the Paleogene/Neogene boundary could be doubtlessly documented in the section from Dumbravnic Brook to Moldoviţa Basin (Chira et al., 2008).

About 68 samples were investigated from Loba Valley – Rasca concerning the calcareous nannofossils.

In the first part of the investigated section of Loba Brook, the nannofossil assemblages are rich in Upper Oligocene forms: reticulofenestrids, sphenoliths, Zygrablithus bijugatus etc.

The presence of Sphenolithus conicus (NP23-NN2) was until now remarked starting from the second part of the section, besides Helicosphaera scissura, Coccolithus pelagicus, Reticulofenestra spp. etc., which prove the presence of the Lower Miocene. Sometimes also coccospheres of Reticulofenestra were observed. Very frequent are ascidian spicules, and in some cases also thoracospheres. REFERENCES Chira C.M., Juravle D. T., Balc R., Igritan A. & Popa M.V., 2008. The Paleogene/Neogene Boundary

in northern Moldavia (Moldovita Basin, Romania). INA12 Abstracts, Lyon, France, p. 36. Grasu C., Miclaus, C., Florea, F. & Saramet M., 2007. Geologia si valorificarea economica a rocilor

bituminoase din Romania. Ed. Univ. “Alexandru Ioan Cuza”, Iasi: 5-253. Ionesi L., Meszaros N., 1989. Sur la limite Oligocene-Miocene dans le Flysch Externe Carpatique. In:

L. Ghergari, N. Meszaros, E. Nicorici, I. Petrescu (EDS.). The Oligocene from the Transylvanian Basin Romania. Univ. of Cluj Napoca, Cluj Napoca: 133-141.

Joja T., Alexandrescu Gr., Micu M., 1984. Geological map of Romania 1:50,000; Suceviţa Sheet. Geological and Geophysical Institute Bucharest.

Juravle D.T., 2007. Geologia regiunii dintre Valea Sucevei si Valea Putnei (Carpatii Orientali). Casa Editoriala Demiurg, Iasi: 6-319.

Juravle D-T., Florea F. F., Bogatu L., 2008. The importance of calcareous nannoplankton in establishing lithostratigraphic landmarks in the Eocene column of Tarcu Nappe in the Suceava River Basin (Obcina Mare). Acta Palaeontologica Romaniae, VI, Iaşi. Edited by: Ţabără D., Olaru L., University “Alexandru Ioan Cuza” Iaşi: 145-172.

Micu M., 1981. Nouvelles données sur la stratigraphie et la tectonique du flysch externe du bassin de la Suceviţa. Dări de Seamă ale şedintelor Comitetului Geologic., 64: 51-64.

Cretaceous-Paleogene nannoflora and the K/P boundary in Putna - Suceviţa area (Bucovina, Romania)

Carmen Mariana CHIRA1, Doru-Toader JURAVLE2,

Peter Zsolt FODOR1 & Mirela Violetta POPA1

1 Babeş-Bolyai University, Faculty of Biology and Geology, Department of Geology, 1 Kogălniceanu St., Cluj-Napoca, 400084, Romania, [email protected] 2 Faculty of Geography and Geology, “Al. I. Cuza” University, 20A, Carol I Street, 700505-Iaşi, Romania, [email protected] Keywords: K/P boundary, flysch, Bucovina, Putna - Steja Valley, Suceviţa, calcareous nannofossils.

New data in order to investigate the K/P boundary from northern Moldavia (Bucovina) are presented in this study. Two new sections from Putna area – Steja Valley (affluent of Putnişoara Valley, which is an affluent of Putna Valley) (Fig. 1) and a left affluent of Steja Valley, named here Brook 19 according to the forestry number, were investigated (Fig. 2).

About 55 samples were studied concerning the content of calcareous nannofossils.

These data were compared with those from previous studies from Putna area (Putna Valley) and Sucevi�a area (Bercheza and Rusca Valleys), concerning the Cretaceous and Paleogene nannoflora (Chira et al., 2007, 2008).

Previous studies on the K/P boundary were performed by Melinte (2000) and Bojar et al. (2007) in the southern part of Moldavia, which evidenced the presence of Upper Maastrichtian/Lower Paleocene deposits based on biozones Nephrolithus frequens, Micula prinsii, Biantholithus sparsus and Cruciplacolithus primus.

In the Sucevi�a Basin, previous research on flysch deposits has been carried out by

Ionesi & Florea (1984, 1996), Juravle (2007) etc. The K/P boundary was identified in the upper part of the Hangu Formation within the Tarcǎu Nappe. It follows the Izvor Formation, assigned to Paleocene and Lower Eocene.

Fig. 1. Steja Valley (Putna area).

The investigated content of calcareous nannofossils currently performed on the two sections from Putna area – Steja Valley and its affluent (Figs. 1, 2) proved the presence of a very rich and well-preserved Lower Paleocene calcareous nannofossil


C.M. Chira et al. - Cretaceous-Paleogene nannoflora and the K/P boundary in Putna - Suceviţa area (Bucovina)

assemblage, especially along Steja Valley. In the interval corresponding to samples 4 to 11 (Fig. 1), with few exceptions and especially in sample 5, the following forms were identified: Ericsonia subpertusa, E. starkeri, Lanternithus duocavus, Zeugrhabdotus sigmoides, Podorhabdus elkefensis, Chiasmolithus danicus, Markalius apertus, M. inversus, Cruciplacolithus primus, C. tenuis, Cyclagelosphaera alta, Prediscosphaera spinosa, and Rhagodiscus angustus. Seldom Upper Cretaceous forms were also recognized: Watznaueria barnesiae, Lucianorhabdus maleformis, Micula staurophora, M. prinsii, Eiffelithus turriseiffelii etc. Relatively frequent are thoracospheres.

This assemblage is characteristic for the K/P boundary, for the beginning of the Paleogene. At some levels, like in samples 1-3, and on the top of sample 11, the deposits are barren or very poor in calcareous nannofossils. More barren intervals were found in the section from the affluent of Steja Valley (Fig. 2). Only at some levels, like in sample 17, abundant Lower Paleogene calcareous nannofossils were identified.

Fig. 2. Affluent of Steja Valley –Brook 19.

REFERENCES Chira C., Balc R., Igritan A. & Florea, F., 2007. Cretaceous – Paleogene calcareous nannofossil

assemblages from Sucevita – Putna area: Bercheza, Rusca and Putna Valleys (northern Moldavia), and the problem of the Cretaceous/Paleogene Boundary. Abstract. Annual Scientific Session, Department of Geology, Cluj-Napoca.

Chira C., Balc R., Igritan A. & Florea F., 2008. Cretaceous and Paleogene calcareous nannofossils from northern Moldavia (Sucevita – Putna area, Romania) and the Cretaceous/Paleogene Boundary. Abstract, INA12 Lyon, France, p. 35.

Ionesi L. & Florea F., 1984. Quelques aspects concernant la lithostratigraphie et la structure du flysch externe du Bassin de la Sucevita. Analele stiintifice ale Universitatii Al. I. Cuza din Iasi, 30: 5 – 12.

Ionesi L. & Florea, F. (1996) - Contributii litostratigrafice si sedimentologice asupra Formatiunii cu Inocerami (Hangu s.s.). Studii si cercetari de geologie, 41:81 – 92.

Juravle D.T., 2007. Geologia regiunii dintre Valea Sucevei si Valea Putnei (Carpatii Orientali). Casa Editoriala Demiurg, Iasi: 6-319.

Melinte M., 2000. Cretaceous/Tertiary boundary in the East Carpathians, based on nannofloral evidence. Acta Paleontologica Romaniae, 2:269-273, Cluj-Napoca.

21

Biometrical quantitative analyses and taphonomy of the Upper Jurassic Lacunosella brachiopod assemblage from Hǎghimaş

Mountains (Eastern Carpathians, Romania)

Diana CIOBANETE1, Iuliana LAZAR1 & Andrei PANAIOTU1

1 University of Bucharest, Faculty of Geology and Geophysics, Department of Geology and Paleontology,1, N. Balcescu Ave., RO – 010041, Bucharest, [email protected] Keywords: biometry, quantitative analyses, Jurassic, rhynchonellid brachiopods, Carpathians.

The very rich Lacunosella brachiopod assemblage from Obârşia Fagul Oltului (north-eastern part of Hǎghimaş Mountains) is represented by an abundant oligospecific association, strongly dominated by rhynchonellid brachiopods.

The presence of this very rich level with Lacunosella in the area was previously mentioned by Pelin, 1965; Preda, 1967, 1973; and Grasu, 1971. However, this is the first study regarding the biometry of this impressive population. Observations on the taphonomy and the palaeoecology of this fossil assemblage have been also recorded.

The studied fauna was sampled from a rock sequence that consists of red limestones: mudstone and wackestone alternate with crinoidal limestone. The Lacunosella-rich horizon is 1.63 m thick and is abundant in rhynchonellid brachiopods (tens-of-thousands of specimens). The fauna is dominated by rhynchonellids: Lacunosella (>90 %), Septaliphoria, and Rhynchonella occurring within distal red crinoidal limestone (Saccocoma facies). The red limestone is generally dominated by a fine granular carbonatic matrix: bioclastic mudstone and wackestone in which the brachiopods represent the dominant group. The large brachiopods are associated with scattered forams, crinoid columnals, calcified sponges, dasycladal algae, planktonic bivalves, and some juvenile ammonites. Very specific is the presence of some oncolite-type structures which may be related to a long disputed form of Tubiphytes, now called Crescentiella morronensis (Senowbari-Daryan et al., 2008) - a form of tubular foraminifer encrusted by cyanobacteria.

The wide-range of shell sizes preserved point to the presence of a paleobiocoenosis. Specimens are fully of partially filled with matrix; geopetal infillings are common, marking the top of the unit and pointing to the fact that the specimens have not been transported. Hundreds of specimens are very well preserved; shells are not decorticated into the sediment, thus not eroded. The brachiopods show no evidence of being deformed by compaction.

Morphometric parameters such as the length and the height of the shell, the length and the height of the sinus and the number of ribs have been statistically-processed by using the method of bivariate analysis. The statistical analysis has been made on a number of 523 specimens out of 1200 fossil specimens (694 from the Preda collection, Department of Geology and Paleontology of the University of Bucharest, and 502 collected during field research).

In this way, some intraspecific different characteristics have been emphasized, which are the result of the ontogenetic processes. The biometrical analysis of specimens of Lacunosella showed that it is difficult to argument the definition of more than one species based only on the variability of external characters. The individuals show a normal growth series within a large population.


D. Ciobanete et al. - Biometrical quantitative analyses and taphonomy of the Upper Jurassic Lacunosella brachiopod

23

SELECTED REFERENCES Grasu, C. 1971, Recherches geologiques dans le sedimentaire Mesozoique du bassin superieur de Bicaz

(Carpates Orientales). Lucr. Staţiuni de Cercet.Biol., Geol., Geograf., “Stejarul”. Pelin, M., 1965. Asupra brachiopodelor portlandiene de pe Piriul Fagul Oltului – Culmea Piatra Rosie

(Masivul Haghimas). Analele Universitatii din Bucuresti, Seria Stiintele naturii, Geologie – Geografie,Bucuresti, nr. 2, p. 73-84.

Preda, I., 1973. Variatiile de facies si biosytratigrafia Jurasicului superior din Muntii Haghimas. Studii si Cercetari, Stratigrafie, vol. II, p. 12-21, pl. I – XIX.

Senowbari-Daryan, B., Bucur, I. I., Schlagintweit, F., Săsăran, E., Matyszkiewicz, J. 2008. Crescentiella, a new name for “Tubiphytes” morronensis CRESCENTI,1969: an enigmatic Jurassic –Cretaceous microfossil. Geologia Croatica 61/2–3 185–214 8 Figs. 8 Pls. Zagreb 2008.

New Upper Cretaceous (Maastrichtian) exposures in Haţeg Basin

Vlad A. CODREA1, Zoltan CSIKI2, Dan GRIGORESCU2, Matei VREMIR3, Emanoil SĂSĂRAN1 & Cătălin JIPA4

1 Babeş-Bolyai University, Faculty of Biology and Geology, Department of Geology-Paleontology, 1 Kogălniceanu Str., 400084 Cluj-Napoca, Rumania. E-mail: [email protected]; [email protected] 2 University of Bucharest, Faculty of Geology and Geophysics, Department of Geology and Paleontology, 1 N. Balcescu Blvd, 010041, Bucharest, Rumania, University of Bucarest. E-mail: [email protected]; [email protected] 3 Weatherford, Weatherford House, Lawson Drive, Dyce, AB21 ODR, Aberdeen, UK. E-mail: [email protected] 4 Babeş-Bolyai University, Faculty of Environment Science, Str.Fantanele 30, 400294 Cluj Napoca, Rumania. E-mail: [email protected] Keywords: Haţeg Basin, Maastrichtian, continental deposits

The Haţeg Basin is well known worldwide due to its peculiar small-sized

Maastrichtian dinosaurs, first reported by baron Nopcsa more than a century ago. The main dinosaur-bearing localities he discovered in Transylvania were marked on the geological map issued in 1905. After his death, for several decades vertebrate remains continued to be unearthed exclusively from these localities.

However, in the last decade some additional new Maastrichtian exposures have been reported either on the northern basin border at Tuştea, Budurone, Livezi (Grigorescu et al., 1990; Csiki et al., 2008; Grigorescu & Csiki, 2008), or along Râul Mare in Toteşti and Nalaţ-Vad areas (Codrea et al., 2002; Smith et al., 2002).

According to recent discoveries, some outcrops along Ruşor valley, previously mapped as Miocene (Nopcsa, 1905, Laufer, 1925; Stilla, 1985) are in fact Maastrichtian in age; this age is supported by the discovery of a large sauropod femur devoid of signs of reworking. Yellowish coarse and fine poorly cemented sands and microconglomerates (channel fill) and greenish silty mudstones with plant remains and mollusk fragments represent the dominating rocks.

The same age has to be assigned to the deposits exposed along the Râul Mare riverbed, upstream from the Pâclişa storage lake. These outcrops are continuing the ones from Toteşti, following the same direction and plunge, as well as showing a comparable lithology. The fossils are scarce; however, some dark-colored bone fragments could be observed. Towards the Râu de Mori dam, these deposits are covered by yellowish sands and clays, probably of Miocene age. The same overlapping relationships can be noticed on Sibişel valley, downstream of Sibişel village, between the upper part of the Sinpetru stratigraphic section and the overlying Miocene marine deposits.

The ongoing research, including palynological and microfaunistic study of these deposits, is aiming to definitively establish the Latest Cretaceous age of these deposits.

Moreover, under these circumstances, all the exposures once marked as Cenozoic should be carefully re-studied, because part of them could be older than previously presumed.








V.A. Codrea et al. - New Upper Cretaceous (Maastrichtian) exposures in Haţeg Basin

25

REFERENCES Codrea V., Smith T., Dica P., Folie A., Garcia G., Godefroit P. & Van Itterbeeck J., 2002. Dinosaur

egg nests, mammals and other vertebrates from a new Maastrichtian site of the Haţeg Basin (Romania). Comptes Rendus Palevol 1, 173-180.

Csiki Z. & Grigorescu D., 2008. The Budurone microvertebrate site from the Maastrichtian of the Haţeg Basin – flora, fauna, taphonomy and paleoenvironment. Acta Palaeontologica Romaniae, 6 : 49-66, Iaşi.

Grigorescu D., Şeclăman M., Norman B.D., Weishampel D.B., 1990. Dinosaur eggs from Romania. Nature 346, 6283, 417.

Grigorescu D. & Csiki Z., 2008. A new site with melaloolithid egg remains in the Maastrichtian of the Haţeg Basin. Acta Palaeontologica Romaniae, 6 : 115-121, Iaşi.

Laufer F., 1925. Contribuţiuni la studiul geologic al împrejurimilor oraşului Haţeg. Anuarul Institutului Geologic al României, 10: 301-333, / in German: 335-370/, Bucureşti.

Nopcsa F., 1905. A Gyulafehérvár, Déva, Ruszkabánya és a Romániai határ közé eső vidék geológiája. A magyar Királyi Földtani Intézet Évkönyve 14, 82-254. Budapest

Smith T., Codrea V., Săsăran E., Van Itterbeeck J., Bultynck P., Csiki Z., Dica P., Fărcaş C., Folie A., Garcia G. & Godefroit P., 2002. A new exceptional vertebrate site from the Late Cretaceous of the Haţeg Basin (Romania). Studia Universitatis Babeş-Bolyai, Geologia, Special issue 1, 321-330.

Stilla A., 1985. Géologie de la région de Haţeg-Cioclovina-Băniţa (Carpates Méridionales). Anuarul Institutului de Geologie şi Geofizică, 66: 91-179, Bucureşti.

The Upper Pliocene Bovidae Pliotragus ardeus (Croizet & Jobert, 1828) (Mammalia, Artiodactyla) at Colteşti (Dacic Basin)

Vlad A. CODREA1 & Ştefan V. FEIGI2

1 Babeş-Bolyai University, Faculty of Biology and Geology, Department of Geology-Paleontology, 1 Kogălniceanu Str., 400084 Cluj-Napoca, Rumania. E-mail: [email protected] 2Babeş-Bolyai University, Faculty of Environment Science, Str. Fantanele nr. 30, 400294, Cluj-Napoca, Rumania. E-mail: [email protected] Keywords: Vertebrate paleontology, Artiodactyla, Late Pliocene, Dacic Basin, Oltenia, Rumania.

The Dacic basin is the most outstanding area where Pliocene vertebrates have

been found in Rumania. Two main areas of interest for these fossils are known within this basin: i. northeastwards, at Măluşteni, Bereşti and Tuluceşti and ii. west from Olt River, in Oltenia, where the Pliocene localities are even more numerous (Slatina, Tetoiu, Irimeşti, Groşerea, Podari, Covrigi etc).

Three decades ago, during the rig-up works related to oil drilling at Colţeşti (Gorj County), a number of fossil bones was unearthed when the bulldozer dug the catch pit. Part of them was donated by the workers to Gorjului Museum in Târgu Jiu. Among these ones, some belong to an Upper Pliocene Bovidae, Pliotragus ardeus (CROIZET & JOBERT, 1828). The samples consist of a fairly-well preserved skull, a left complete humerus and fragments of radius and tibia. The horn shape, as well as other skull features is indicating an adult male. This large herbivore is rather rare for Rumania, but also for the whole Europe, only a few localities being known as bearing fossils indubitable referable to this species.

The deposits form Colţeşti, which aside from this Bovidae yielded also horse, rhinoceros, proboscidian, fallow-deer or bear remains, are Late Pliocene in age.




Cytological and morphological indices used in the study of vegetal fossil species and their actual correspondent species

Gabriel C. CORNEANU1 & Mihaela CORNEANU 2

1 University of Craiova, Biology-Genetics Dept., Str. A.I. Cuza 13, 200585-Craiova, e-mail: [email protected]; 2USAMVB Timisoara, Genetic Engineering Dept., Calea Aradului 119, 300645-Timisoara, e-mail: [email protected], Romania

Keywords: fossil vegetal species; actual correspondent species; cytological features.

Previous research pointed out the importance of the some cytological and morphological features in the taxonomical characterization of vegetal species (Sanda, 1972; Corneanu and Popescu, 1981 etc.). In previous papers, some cytological features of the leaves (size and shape of the epidermal cells, as well as size and features of the stomata cells), were used for comparing some vegetal fossil species with their actual correspondent species (Corneanu et al., 2004 etc.). In this paper, some fossil vegetal species and their actual correspondent species were analyzed, using several cytological features, the existence of some similar values being noted.

In this paper, the analysis of some cytotaxonomical features was performed on the following fossil vegetal species: Pseudocycas dunkeriana (Goeppert) Florin; Taxodium dubium (Sternberg) Heer; Sequoia abietina (Brngt.) Kn.; Juglans acuminata Braun; Tsuga europaea Menzel, Platanus leucophylla (Brngt.) Kn. etc. (Table 1). The cytological features that have been used were: size and shape of epidermal cells, size and type of stomata, as well as some morphological features (size and number of leaves’ folioles). The biometrical values for the fossil species were provided by the regretted Acad. Prof. Răzvan Givulescu. Table 1. Fossil vegetal species and their actual correspondents

Fossil species Actual species Genotype Geological age Deposit Pseudocycas dunkeriana Taxodium dubium Sequoia abietina Juglans acuminata Tsuga europaea Platanus leucophylla

Lower Jurassic Tertiary, Oligocene Tertiary, Miocene Tertiary, Miocene Tertiary, Miocene Tertiary, Miocene

Anina Petrosani Chiuzbaia- Bihor Borod - Bihor Chiuzbaia Chiuzbaia

Cycas revoluta Taxodium distichum Metasequoia glyptostroboides Juglans regia Tsuga canadiensis Platanus hybrida

The biometrical values of the actual correspondent species were established using

plants that were grown in the Alexandru Buia Botanical Garden of Craiova University (Table 1). These actual species were: Cycas revoluta Thumb., Taxodium distichum (L.) Rich, Metasequoia glyptostroboides Hu & Cheng, Juglans regia L., Tsuga canadensis Carrière, Platanus occidentalis L. etc. A number of 30 biometric observations were performed on mature plants (at flowering), for every feature. The size and shape of the epidermal cells and the stomata length were recorded, as well as the size of the leaves’ folioles. The biometrical values were statistically interpreted.

The comparative analysis of the recorded biometrical values of fossil species and their actual correspondent species evidenced the existence of some similar values




G.C. Corneanu & M. Corneanu - Cytological and morphological indices used in the study of vegetal fossil species

28

regarding the cytological features (size of epidermal cells and stomata, as well as those related to leaves’ folioles). Values recorded for the epidermal cells from the fossil species Pseudocycas dunkeriana as compared to the actual correspondent species Cycas revoluta (two old phylogenetic species) were relatively close (Table 2). The differences recorded for stomata sizes probably represent the consequences of an adaptation process, because of the different atmosphere composition during Jurassic as compared with the actual period. In the case of the other species, a larger difference was registered between the values recorded on fossil species vs. present species (length of epidermal cell size on abaxial epidermis: 19.7 – 40.0 µm in Taxodium dubium and 37.5 – 65.0 µm in Taxodium distichum). Table 2. The cytological features in fossil vs. actual correspondent species (size of the epidermal cells and stomata length)

Epidermis Feature Variability limits (in µm)

Mean (in µm)

Pseudocycas dunkeriana Upper Cell length

Cell wide 30.76 – 73.89 18.53 – 36.99

50.82 26.73

Lower Cell length Cell wide

Stomata length

30.80 – 55.44 18.48 – 36.96 30.80 – 55.44

41.07 27.72 41.07

Cycas revoluta Upper Cell length

Cell wide 32.50 – 67.50 12.50 – 37.50

50.20 22.16

Lower Cell length Cell wide

Stomata length

25.00 – 65.00 20.00 – 45.00 30.00 – 35.00

41.33 31.58 33.33

Conclusions The comparative analysis of some cytological and morphological features on

fossil vs. actual correspondent species, pointed out the following trends, at geological time scale: (a) a speciation process that conducted to the spring up of new species, and (b) the adaptation of the fossil species to the new environmental conditions. The two processes are supported by experimental values resulted from this research. Acknowledgements. This paper is constituted as homage in memoriam of Acad. Prof. Rǎzvan Givulescu, from Cluj-Napoca, who encouraged this research. REFERENCES Corneanu C.G. & Popescu G.G., 1981. Distributional and anatomical studies on Fritillaria (Liliaceae)

in Romania. Willdenowia, 11: 307-315. Berlin. Corneanu C.G., Corneanu M. & Bercu R., 2004. Comparison between some morpho-anatomical

features at fossil vegetal species and at their actual correspondent species. Studia Universitatis Babes-Bolyai, Geologia, XLIX (2): 77-84.

Givulescu R., 1990. Flora fosila a miocenului superior de la Chiuzbaia. Ed. Academiei Romane, Bucuresti.

Givulescu R., 1996. Flora oligocena superioara din bazinul Petrosani. Ed. Casa Cartii de Stiinta, Cluj-Napoca.

Givulescu R., 1998. Flora fosila a jurasicului inferior de la Anina. Ed. Academiei Romane, Bucuresti. Sanda V., 1972. Cercetari taxonomice in cadrul sectiei Carthusiani Bois a genului Dianthus L. Studii si

Comunicari, Muzeul Bruckenthal Sibiu, 17: 147-157.

Phylogeny and speciation in Quaternary cervid genera Eucladoceros and Praemegaceros (Cervidae, Mammalia)

Roman CROITOR1

1 Centre for Archaeology, Institute of Cultural Heritage, str. Stefan Cel Mare 1, Chişinău, MD-2001, Republic of Moldova, E-mail: [email protected]

Keywords: Phylogeny, Mammalia, Cervidae, Quaternary

Eucladoceros and Praemegaceros are closely-related genera of large-sized and giant deer that were widespread in Eurasia during the Quaternary. Eucladoceros is a primitive genus that contains two species from Europe (E. ctenoides with several subspecies, and E. dicranios) and two species from China (E. proboulei and E. boulei). E. proboulei is the most ancient and primitive species from the Early Pliocene of China, while the Late Pliocene–Early Pleistocene E. boulei displays some characters that reminds primitive Praemegaceros. Eucladoceros were red-deer sized species with rather primitive comb-like antlers with varying number of tines. Eucladoceros shares with Praemegaceros such characters as the broad bell-shaped basioccipitale; the position of the nasofrontal suture that does not go behind the anterior line of the orbits; the position of M3 shifted forward with respect to the orbit; and the general cranial proportions (relatively short braincase, long orbitofrontal part of skull). The cranial morphology may suggest a close relationship among those two genera. Unlike Eucladoceros, Praemegaceros completely lost the metameric pattern of the antlers, evolved giant body size, and developed complicate antler branches and palmations. The mosaic combination of morphological details of the antlers and teeth suggest that Praemegaceros is a paraphyletic group and it includes several lineages that developed from Asian Eucladoceros. Therefore, the application of subgeneric division of Praemegaceros is reasonable. The most ancient lineage is presented by the subgenus Praemegaceros with the late Villafranchian P. (Praemegaceros) obscurus and its stunted middle-Pleistocene descent P. (Praemegaceros) dawkinsi. The second subgenus Orthogonoceros includes a Galerian forerunner P. (Orthogonoceros) pliotarandoides and its Middle Pleistocene descent P. (Orthogonoceros) verticornis. These deer share with previous lineage the development of the dorsal and the high degree of P4 molarization. The third subgenus Nesoleipoceros includes two sister species P. (Nesoleipoceros) solilhacus (Middle Pleistocene of Europe) and P. (Nesoleipoceros) cazioti (Late Pleistocene of Corsica and Sardinia) with a primitive P4 (occasionally fully-molarized in P. solilhacus) and the particular antler morphology (Croitor, 2006).

The origin and the development of the Praemegaceros lineages probably took place in the Asian continent approximately at the same time when Eucladoceros ctenoides and E. dicranious evolved in Europe, ca. 2.5 Ma. The separation of European forms of Eucladoceros from Praemegaceros, apparently occurred due to the Late Pliocene transgression of Paratethys that caused a geographical isolation of European and Asian populations of the forerunner Eucladoceros form with a very vast area of distribution that ranged from China to Western Europe along the northern side of Alpine mountain chain. The subsequent fragmentation of European and Asian areas of distribution of the ancestral Eucladoceros-like forms gave birth to several lineages of Eucladoceros and Praemegaceros species. This divergence of Eucladoceros and Praemegaceros lineages took place ca. 2.5 Ma ago, when almost simultaneously E.



R. Croitor - Phylogeny and speciation in Quaternary cervid genera Eucladoceros and Praemegaceros (Cervidae)

30

ctenoides in Western Europe (HEINTZ, 1970), E. dicranios in Eastern Europe (Tesakov, 1995) occurred, and slightly later, 2.2 Ma, P. pliotarandoides appeared in the Prekups fauna (Tesakov, 1995). The divergence between Eucladoceros and Praemegaceros lineages may be explained by the difference in the evolutionary rate of the ancestral forms. Praemegaceros has evolved during the Middle and Late Villafranchian in the less-favourable dry continental climate conditions of Asia that caused higher rates of evolution and more advanced specialisations in antler and dental morphology, as well as the larger body size. Eucladoceros have maintained ancestral primitive characters in antler morphology and primitive dentition due to lower evolutionary rate in the conditions of comparatively mild European climate. The subsequent disappearance of Paratethys barrier and climate deterioration during the Early Pleistocene caused the migration of Asian cervid species towards Western Europe and the overlap of distribution areas of several Praemegaceros and Eucladoceros species.

Bone histology in the Ornithopods from the Maastrichtian of Haţeg Basin – were these dinosaurs really dwarfs?

Zoltan CSIKI1, Ragna REDELSTORFF2 & Dan GRIGORESCU3

1 Laboratory of Paleontology, Faculty of Geology and Geophysics, University of Bucharest; 1 N. Bǎlcescu Blvd, 010041 Bucharest, Romania; e-mail: [email protected] 2School of Geological Sciences, University College Dublin, Belfield, Dublin 4, Ireland; e-mail: [email protected] 3 Laboratory of Paleontology, Faculty of Geology and Geophysics, University of Bucharest; 1 N. Bǎlcescu Blvd, 010041 Bucharest, Romania; e-mail: [email protected] Keywords: Hateg; Maastrichtian; Ornithopoda; osteo-histology; paleobiology; dwarfism

The Late Cretaceous dinosaurs of Haţeg Basin, Romania, are often cited, beginning with the pioneering work of Nopcsa (1914), as representing dwarf dinosaurs, presumably as a result of their insular habitat. These inferences are mainly based on their small size compared to their relatives living on other landmasses. However, their dwarf status has yet to be supported by independent evidence, and was recently questioned on different grounds (e.g. Le Loeuff, 2005; Pereda-Suberbiola & Galton, in press).

The study of bone histology represents a method that has proven its usefulness for determining ontogenetic stages and growth strategies of fossil vertebrates, including dinosaurs (e.g. Horner et al., 2000; Erickson, 2005). Accordingly, it may be successfully used to discriminate between adult individuals of small-sized (thus conceivably dwarf) taxa and juvenile individuals of otherwise large-sized taxa. Moreover, contrasting bone histology features and patterns of change with a well-supported hypothesis of phylogenetic relationships between the taxa studied and their close relatives allows understanding the process that determined the presence of small size in certain taxa.

A series of long bones of the Haţeg ornithopods Zalmoxes and Telmatosaurus was sampled during this study, in order to reveal whether these represent true small-sized adults (i.e. dwarfed taxa) or juveniles of normal-sized taxa.

A complete ontogenetic series was available for the basal-most hadrosaurid Telmatosaurus, from hatchlings (femur length 38 mm) to large-sized specimens (femur length 464 mm); besides femora, other bones (tibiae) were also sampled, but these were normalized to femur length for easier comparisons. Long bone histology of adults shows an advanced remodelling by secondary osteons within the primary cortex, being dense in the inner and scattered close to the surface of the cortex. The absence of vascular canals open to the bone surface is an unequivocal feature of cessation of growth. Open vascular canals were merely found in the subadult specimen and the hatchlings. The high number of growth marks, 8 in the oldest specimens, supports the fully grown appearance. An external fundamental system (EFS), which indicates an unequivocal cessation of growth, could not be observed due to abrasion of bone surfaces. According to measured bone lengths, an adult, fully grown stage could be confirmed for the individuals represented by the longest bones of Telmatosaurus (femur length 46 cm), the taxon being thus significantly smaller than other adult hadrosaurs (Maiasaura peeblesorum: approximately 100 cm, Horner et al. 2000).

A poorer sample, including only juvenile to adult ontogenetic stages was available for sampling for the rhabdodontid Zalmoxes (femur lengths 164 - 355 mm). The bone


Z. Csiki et al. - Bone histology in the Ornithopods from the Maastrichtian of Haţeg Basin – were these dinosaurs really dwarfs?

32

histology of the sampled femora and humeri of ornithopod Zalmoxes strikes in terms of its remodelling. Dense remodelling is restricted to the inner cortex in the oldest specimens, isolated to scattered secondary osteons occurring in the middle cortex, while none are present in the outer cortex. This pattern of late remodelling starting at subadult stage also occurs within other ornithopods such as Maiasaura peeblesorum (Horner et al. 2000) - though an early EFS as it is developed in subadult stage in Maiasaura is absent in Zalmoxes. Additionally to the restricted remodelling in Zalmoxes, the observation of vascular canals still opening to the bone surface indicating active growth at the time of death implies that a fully grown stage has not been reached yet in the sampled specimens. The high number of growth marks though, being up to 13 in Zalmoxes robustus and 7 in Z. shqiperorum, reveals that a juvenile stage can also be excluded for Zalmoxes. According to bone histology, Zalmoxes robustus is smaller at the same age than Z. shqiperorum, as it has been assumed before based on its bone morphology.

The long bone histology of the Haţeg ornithopods reveals a slow growth rate in Zalmoxes, and a moderate rate in Telmatosaurus. According to the high number of lines of arrested growth (LAGs - up to eight), an external fundamental system is present in the largest specimens of Telmatosaurus, indicating cessation of growth. A slow growth rate in Zalmoxes is supported by the narrow-spaced LAGs, which occur in an extremely high number (up to 15) indicating an adult stage for most sampled specimens. In contrast to the high number of LAGs, bone histology of Zalmoxes shows vascular canals open to the bone surface indicating active growth at time of death.

Femur lengths of Zalmoxes were compared to other rhabdodontids and basal iguanodontians, and those of Telmatosaurus to basal hadrosauroids and derived hadrosaurids. These comparisons suggest reduced body size in both taxa, presumably caused by a slowdown of growth rate, which was taken to the extreme in Zalmoxes. However, its dwarfed status is less well supported, due to the smaller absolute size difference between this taxon and its close relatives.

The combination of extremely reduced growth rate and extended growth period, observed in Zalmoxes, contrasts with the conclusions of the only other study on rhabdodontid bone histology available (Company, 2006). These features are also unknown in any other ornithopod, and suggest a unique growth strategy in this taxon. REFERENCES Company J., 2006. Bone histology of the ornithopod dinosaur Rhabdodon from the Late Cretaceous of

the Iberian Peninsula. Preliminary data. Hantkeniana, 5: 82. Erickson G. M., 2005. Assessing dinosaur growth patterns: a microscopic revolution. TRENDS in

Ecology and Evolution, 20(12): 677-684. Horner J. R., de Ricqlès A. & Padian, K., 2000. Long bone histology of the hadrosaurid dinosaur

Maiasaura peeblesorum: growth dynamics and physiology based on an ontogenetic series of skeletal elements. Journal of Vertebrate Paleontology 20(1):115-129.

Le Loeuff J., 2005. Romanian Late Cretaceous dinosaurs: big dwarfs or small giants? Historical Biology, 17:15-17.

Nopcsa F. 1914. Über das Vorkommen der Dinosaurier in Siebenbürgen. Verhandlungen, Zool. Bot. Gesellschaft 54: 12-14.

Pereda Suberbiola X. & Galton P.M., (2009, in press). Dwarf dinosaurs in the latest Cretaceous of Europe? In: Colectivo Arqueológico-Paleontologógico de Salas (Ed.), IV Jornadas Internacionales sobre Paleontología de Dinosaurios y su Entorno, Salas de los Infantes (Burgos, Spain), Actas: 263-272.

Studies of some Late Turolian Lagomorpha from the Moldavian platform (Republic of Moldova)

Andrian DELINSCHI1 & Igor NICOARA1

1 National Museum of Ethnography and Natural History of Moldova, 82 Kogǎlniceanu str., Chişinǎu, MD 2009, [email protected] 2 Institute of Geology and Seismology of ASM, 3 Academiei str., Chişinǎu, MD 2009, [email protected] Keywords: Lagomorpha, Late Turolian, Moldavian Platform

The Upper Turolian localities bearing Hipparion faunas from the Republic of

Moldova yielded also small mammal assemblages. Among these representatives, a rich fauna of Lagomorpha has been collected, currently weakly studied. A lot of details concerning their systematic, phylogeny, or stratigraphy remained poorly-known.

From the Upper Turolian localities in the Republic of Moldova, two lagomorph families have to be mentioned: Leporidae and Ochotonidae.

Family Leporidae. The first representatives of this family appear at the beginning of Kersonian (in Cainari), belonging to Alilepus. These representatives are the same ones known from Maeotian (Cimişlia, MN 12/13) and Pontian (Balanesti, MN 13) assemblages. The Maeotian representatives are related to Alilepus lascarewi CHOMENKO.

Family Ochotonidae. During the Late Miocene, this family concerned Proochotona and Prolagus representatives.

Proochotona. During the Late Turolian, Proochotona eximia Chomenko (Leordoia, Veveriţa-2, Balanesti, MN 13) was widespread in the Moldavian Platform area. On the contrary, the Proochotona representatives seemed to be missing from the faunal assemblages located westwards of the Carpathians. Perhaps these mountains acted as a barrier for the species’ spreading in this direction.

Prolagus. This representantive of the Ochotonidae family is rarely recorded in the Miocene assemblages of Eastern Europe. However, Prolagus fossils have been collected in the Pontian localities Balanesti and Leordoaia and assigned to Prolagus cf. michauxi LOPEZ-MARTINEZ, a species known from the Turolian of Western Europe. Prolagus is a peculiar representative of the Miocene faunas in Mediterranean regions. It seems that these representatives intruded also the Eastern Europe areas, but there their presence remains rather rare.




Contribution concerning the Pontian flora in soutwest Oltenia

Florina DIACONU1

1 Iron Gates Region Museum, 2, Independentei Str, 1500 Drobeta Turnu Severin, Mehedinţi E-mail: [email protected] Keywords: Lower Pontian, macroflora, Oltenia, Romania

The paper deals with the paleoflora from a new site within Lower Pontian deposits cropping out at Crivina, in the vicinity of Drobeta Turnu Severin municipality (fig.1), SW Romania.

The deposits rich in fossil flora from Crivina are mainly represented by stratified clay with fossil plant remains, besides which siltic clays and sandy silts, including carbonate sandstone concretions - also containing plant impressions, occur.

The macroflora is allochthonous, partly hypautochthonous, and it has a special significance in understanding the evolution of the vegetation and climate of the Late Miocene.

The flora from Crivina is similar to the one identified at Batoţi site. The flora from Batoţi represented the only Lower Pontian assemblage described until now from Romania. Fig. 1 The geological map of Crivina site (after the geological map 1:200000, L-34-XXIX Turnu Severin)



Preliminary observations on Middle Triassic mud-mound limestones from Mahmudia (Tulcea unit, North Dobrogean Orogen)

Livia DOBRE1, Cristina PANAIOTU1 & Eugen GRADINARU1

1 Faculty of Geology and Geophysics, University of Bucharest, Romani. E-mails: [email protected]; [email protected]; [email protected] Keywords: Carbonates, methane, Triassic, microbial crusts

In the north-eastern part of Tulcea tectonic Unit belonging to the North

Dobrogean Orogen, around the Mahmudia village, Middle Triassic limestones are cropping out; they were described in the literature as the first occurrence of Middle Triassic mud mound deposits in Romania. Associated with the mottled structure and stromatactis, some structures resemble those generated by methane seeps: gas tubes, many calcite crusts, large voids filled with radiaxial calcite, specific mineralization and associated fauna etc.

We have initiated a detailed study of these limestones, which will include optical and electron microscopy, cathodoluminescence, UV fluorescence, microthermometry of fluid inclusions, stable isotopes (C, O and S) and biomarkers identification. Until now we applied mainly the optical methods: UV fluorescence, cathodoluminescence and peels on stained polished slabs, but also stable isotopes (O, C) measurements on a few samples.

In this preliminary stage of research we cannot yet assign the observed structures to a cold seep methane origin. The epifluorescence indicates probable bacterial remains and shows that organic matter played a role in the syndepositional precipitation of the crusts, while the dolomite crystals’ composition – a non-fluorescent and non-luminescent core with a highly fluorescent and luminescent thin, outer rim – indicates a potential methanogenetic origin of the overgrowth. Stable isotopes results did not reveal strongly negative values related to the reduced number of samples and low accuracy. In the next stages of this research we will sample all cement generations and dolomite zoning in order to discriminate inorganically- vs. organically-mediated precipitation.





Stromatolites and calcareous algae of Münder Formation (Tithonian-Berriasian) from NW Germany

Ovidiu N. DRAGASTAN1 & Detlev K. RICHTER2

1 University of Bucharest, Dept. of Geology & Paleontology, Bd. Nicolae Balcescu no.1, 010041 Bucharest, Romania. e-mail:[email protected] 2 Ruhr-Universität Bochum, Institut für Geologie, Mineralogie & Geophysik, Lehrstuhl für Sediment und Isotopen Geologie, Universitätstr.150, D-44801 Bochum, Germany. e-mail:[email protected] Keywords: Stromatolites, Calcareous Algae, New Taxa, Tithonian-Berriasian, environmental facies, NW Germany.

The Tithonian stromatolites of Münder Formation, from Thüste locality (Hils syncline), NW Germany were intensively investigated in the last years for their special environment of formation (Jahnke & Ritzkowski 1980, Dragastan & Richter 2001, Arp et al. 2008). Descriptions and interpretations in this paper focused on the stromatolites of the lowermost Katzberg Member in the uppermost Tithonian. The stromatolites developed in a moderately-high energy lagoon environment, between coastal sabkha (supratidal salt flat) facies and intertidal to subtidal facies including oolitic bars, like a “barrier island” interlayered with serpulid-reef banks (Dragastan & Richter 2001). Serpulid reef-banks are more or less an equivalent of oolitic bars, being composed of a mass of tiny (entire or fragmentary) tubes consisting up to 60 % of Serpula coacervata (Blumenbach 1803) Schönfeld 1979 as successive growth stages.

In several slabs, the stromatolite bioherms contain diverse morphologies and populations characterized by three growth stages or phases:

- growth phase 1, in the basal part composed of small (0.250-0.500 mm in diameter), spheroidal to ellipsoidal microbial oncolites with serpulid-tubes nuclei and a few, 2 up to 3, microbial laminae of reduced thickness. Rarely, Chlorellopsis coloniata Reis - in our opinion, a green alga that remains a debated organism concerning its origin and taxonomy, occurs as biofilms.

The initial substratum of the stromatolite bioherms was represented by serpulid-reef banks. The tubes of serpulids, transported selectively according to sizes, represent in most of the cases nuclei for microbial oncoids. On the other hand, it is interesting to specify that very few ooids were found in the stromatolite bioherms, suggesting that the oolitic bar was not in direct connection with the stromatolites and did not serve as substratum. Millimetre-sized biomats and oncolites are also present on large areas and in the channels’ floor.

- growth phase 2 contains, in the lower part, microbial macrooncoids (up to 2 cm in diameter) with serpulid-tubes nuclei fixed by the substratum and growing up to form microbial mounds or knolls. To the upper part, the microbial mounds compose up to 10 laminae, which are thinner in the lower part and thicker towards the top of this stage. Also during this stage, the green algae contributed to the edifice of stromatolites: Chlorellopsis coloniata Reis (rarely) and Brachydactylus reisi Dragastan & Richter 2001 (frequently). Sometimes between the knolls vertical “cracking-pockets” occur, filled up with reworked material, mat debris, and intraclasts, as well as “pockets” filled with coprolites of gastropods, ostracods, bivalves’ fragments and possibly caddisflies (as pupal larvae). This phase ends by a


O.N. Dragastan & D.K. Richter - Stromatolites and calcareous algae of Münder Formation from NW Germany

37

clear erosional surface impregnated with partly oxidized framboidal pyrite, possibly of bacterial origin, which also points to subaerial exposure;

- growth phase 3 begins with basal domal laterally-linked stromatolites, which in some areas more inwards in the lagoon turn into tabular stromatolitic structures composed more or less of horizontal parallel microbial laminae. To the top of this final phase, the stromatolites present only planar-pustular, wavy microbialites crossed by upward cracks filled with coarsely-crystalline calcite, rarely ostracod shells and irregular fenestral fabrics. This stage was built-up by microbial agglutinated-fine grained sediments and is well laminated.

Thus, it can be stated that the Tithonian stromatolites of Thüste were mainly built by microbial organisms, additionally with the contribution of green-algae: Chlorellopsis coloniata and Brachydactylus reisi (frequently) in a lagoon environment, under warm climate conditions showing only two seasonal periods (?).The growth phases 1 and 2 indicate an intertidal environmental facies, while growth phase 3 corresponds to supratidal facies. The facies model for Thüste stromatolites can be compared with the Recent facies model for the coastal sabkha (supratidal salt flat) of the Trucial Coast (Abu Dhabi) from the Arabian/ Persian Gulf.

The Berriasian deposits of Borberg Member (Münder Formation) contain marlstone, micritic limestone, bindstone, oncoids with serpulid-tubes nuclei, calcareous algae, serpulids and ostracods. The calcareous algae were described from the Deister area, near Springe. Thalli - fixed in some cases on serpulid tubes, have hemispheroidal and planar shapes and belong to the cyanophycean and chlorophycean algae.

The following taxa are redescribed and described: Springerella bifurcata Dragastan & Richter 2001, S. fuchtbaueri Dragastan & Richter 2001, S. westphalica n.sp., Deisterella germanica n.gen.n.sp. (Chlorophyta) and Rivularia lissaviensis (Bornemann) Dragastan 1985 (Cyanophyta).

In conlusion the calcareous algal assemblage corresponds to lacustrine-brackish marine environments: eulittoral, freshwater-oligohaline (Teriosynoecum ostracods association) with calcareous algae in lithofacies 4 (Springerella species, Rivularia lissaviensis) and sublittoral-miohaline (Mantelliana ostracods association) with Deisterella germanica n.gen.n.sp. in lithofacies 5, sensu Arp & Mennerich (2008). REFERENCES Arp G., Ostertag-Henning CH., Yucekent S., Reitner J. & Thiel V., 2008. Methane-related microbial

gypsum calcitization in stromatolites of marine evaporative setting (Munder Formation, Upper Jurassic, Hils Syncline, north Germany ). Sedimentology, 55:1227-1251

Arp G. & Mennerich G., 2008. Ostracod assemblages, palaeoenvironment and cyclicity of Purbeck-type sediments of Munder Formation (Lower Cretaceous, Hils Syncline, N-Germany). Palaeogeogr., Palaeoclimat. Palaeoecology, 264: 230 -249.

Blumenbach J.F., 1803. Specimen Archaeologiae telluris terranum-que imprimis Hannoveranarum.H.Dietrich, Gotti-ngen: 1-28.

Bornemann J.G., 1887. Geologische Algenstudien. Jahrb. der Konig. Preuss. geol. Landesanst. und Bergakademie., Berlin, fur das Jahr 1886: 116 - 134.

Dragastan O., 1985. Review of Tethyan Mesozoic Algae of Romania. ( In Palaeologology, Eds. Toomey D.F. & Nitecki N.H., V) :101-161.

Dragastan O. & Richter D.K., 2001. Non-marine calcareous algae of Upper Jurassic to Lower Cretaceous sequences from the Weserbergland (northwest Germany). Geologica Carpathica, 52: 301 - 318.

Jahnke H. & Ritzkowski S., 1980. Die Fazies - Abfolge in Munder Mergel der Steinbruche bei Thuste ( Ober Jura, Hilsmulde). Ber. Naturhist. Ges. Hannover, 123: 45 -67.

Schonfeld M., 1979. Stratigraphische, fazielle, palaogeographische und tektonische Untersuchungen in Obere Malm des Deisters, Osterwaldes und Suntels (NW- Deutschland). Clausthaler Geol. Abh., 35: 1 - 270.

Middle Jurassic (Bajocian) echinoids of Bucegi Mountains (Eastern Carpathians, Romania)

Jaume GALLEMÍ1 & Iuliana LAZĂR2

1 Museu de Geologia de Barcelona-MCNB, Parc de la Ciutadella s/n, 08003-Barcelona, SPAIN, [email protected] 2 University of Bucharest, Faculty of Geology and Geophysics, Department of Geology and Palaeontology, 1, N. Bǎlcescu Ave., RO-010041, Bucharest, ROMANIA, [email protected] Keywords: Middle Jurassic, Bajocian, echinoids, Bucegi Mountains, Eastern Carpathians.

The Middle Jurassic deposits that crop out along the western side of Bucegi Mountains (located in the southern extremity of the East Carpathians) are distinguished by the richness of their fauna. The most complete succession of Middle and Upper Jurassic deposits occurs in the Strunga Pass – Strunguliţa Pass – Obârşia Văii Tătarului area, confined northwards by Strunga Pass and southwards by Tǎtaru Valley. Lazăr (2006) presented an outline of the palaeontological research in the area and a general account on the local geology.

Many of the macrofaunal assemblages from this area, dominated by bivalves, also contain other groups such as corals, gastropods, nautiloids, belemnites, serpulids, arthropods, bryozoans, crinoids, echinoids and fish teeth. In the Middle Jurassic associations from Bucegi, these groups show both a reduced diversity, and are represented by few specimens.

During the extensive field work campaigns accomplished by Lazăr (1994-2000) in this area only a few well-preserved echinoid specimens, which will be described for the first time in the present paper, have been recovered. Sampling echinoid specimens is a difficult task because of the very high hardness of the host rocks. The specimens were collected from a section in Pasul Strunguliţa-Vârful Tătarul-Obârşia Văii Tătarului area, where a 6 meter- level of grey calcareous sandstones alternating with biocalcarenites, separated by centimetre-thick joints of pelites and siltites provided a rich fauna of molluscs, rare colonial corals and brachiopods, as well as the echinoids. These levels, formerly known as "the upper lumachellic level" and reputed as representative for the parkinsoni Zone, are considered to represent the uppermost part of a Lower to Middle Bajocian succession (Patrulius, 1969), i.e. the Strunguliţa Member of the Strunga Formation.

The recorded echinoids have been identified as Stomechinus longuemari Cotteau, 1867, Pygaster semisulcatus (Phillips, 1829), and Collyrites elliptica (Lamarck, 1816).

S. longuemari was erected for a single specimen (Cotteau, 1858-80) from the surroundings of Poitiers (Vienne, France), attributed to Bajocian and including Cotteau's indication "Very rare". The holotype is probably kept in the Collections de Paléontologie, Université C. Bernard-Lyon I, Villeurbanne, France as part of the former ENSM (École Nationale Supérieure des Mines, Paris) collection. This species, never quoted anywhere else, is now mentioned in Romania for the first time.

P. semisulcatus syntypes come from the Coralline Oolite (Oxfordian, plicatilis Zone) of Malton and Scarborough in North Yorkshire and from unspecified locations in Wiltshire (United Kingdom). It is also known from the Bajocian, Upper Bathonian, Lower, Middle and Upper Callovian, Middle and Upper Oxfordian and Lower


J. Gallemi & I. Lazăr - Middle Jurassic (Bajocian) echinoids of Bucegi Mountains (Eastern Carpathians, Romania)

39

Kimmeridgian of several localities in France (Barras, 2006). Our results represent the first record for the Carpathians.

C. elliptica is very abundant in the "Kelloway ferrugineux 1 et 2" (Callovian, macrocephalus and anceps zones) of France and in the "Cornbrash" (Bathonian, discus zone to Lower Callovian, macrocephalus zone) of Sarthe (France). Also quoted in many Callovian localities of France and Switzerland, this species has been reported from the "Inferior Oolite" (Lower to Middle Bajocian; West, 2008) of Bridport (Dorset, United Kigdom). SELECTED REFERENCES Barras C., 2006. British Jurassic irregular echinoids. Palaeontographical Society Monographs 159 (nº.

625). 273 pp. + 14 plates. The Palaeontographical Society, London. Cotteau G., 1858-80. Échinides nouveaux ou peu connus (1ère série). Extraits de la Revue et Magasin

de Zoologie, 230 pp, pls. 1-32. J.-B. Baillière, Paris. Lazăr I., 2006. Middle Jurassic from the Bucegi Mountains – Paleontology and Paleoecology (in

Romanian), Ed. Ars Docendi, Bucharest, 185 p., I – XL plates. Patrulius D., 1969 Geology of the Bucegi Massif and Damboviciara Basin (in Romanian). Academy

Printing House, R.S.R., Bucharest. West I. M., 2008. Burton Bradstock - Bridport Sands and Inferior Oolite. Geology of the Wessex

Coast. Internet site: http://www.soton.ac.uk/~imw/burton.htm. Version: 16th March 2008.

The Ruhr Basin in Central Germany - Review and Outlook

Hartwig GIELISCH1

1 DMT GmbH & Co. KG, Am Technologiepark 1, 45307 Essen, Germany. Email: [email protected] Keywords: Ruhr Basin, General Stratigraphy, German Coal mining industry, Future mining in the North

The Carboniferous Ruhr Basin is located in central-western Germany and it is part of the foreland basin of the Variscian Mountains of Central Europe. Similar coal de-posits occur in the Netherlands, France, Ireland, Belgium, Great Britain and the east-ern United States. During the Carboniferous, the Atlantic Ocean did not yet exist thus fauna and flora found in different coal deposits are comparable, allowing to verify the common development of the basins. Horizons of volcanic ash originate from volca-noes in the southern German Hunsrück area and altered into pyroclastic coaly ton-steins. These pyroclastic coaly tonsteins allow the correlation of nearly all North European coal deposits in terms of time.

The Carboniferous Ruhr coal deposit was affected by tectonic movements at the end of the variscian orogeny. The southern part of the deposit was intensely folded in the Late Carboniferous. These areas were mined out during the last 500 years. North-wards from the centre of the basin, the folding is tailing off and the strata of the actual mining front north of the “Ruhrgebiet” show syncline and anticline angles of 10° and lower. Here, long-wall operations are possible.

During the opening of the Atlantic Ocean, the so-called Saxonian tectonics af-fected the deposit by widening the European continent along west–east direction, re-sulting in normal faults of up to x 100 m displacement.

In these areas, the German Hard Coal Industry has been operating in the last 20 years. The times of mining in steep or semi-steep seams are over and long-wall opera-tions are mostly affected by major normal faults. The exploration of the northern parts of the deposit in order to find areas unaffected by structural deformation to allow hard coal mining using long-wall operations were terminated in 2004 due to a reorganisa-tion of the German Hard Coal Industry. Today, the deposit comprises explored hard coal resources for the next 400 years of mining operation in Germany.



Palynological study of the Pliocene deposits from Panga quarry (Vâlcea, Romania)

Elena GIUREA1, Ioan TANŢĂU2 & Mirela Violetta POPA2

1 "C. Brâncoveanu” High School Horezu, 1, Al. I. Cuza st., RO-245800 Horezu, Vâlcea, e-mail: [email protected] 2 Babes-Bolyai University, Department of Geology, 1 M. Kogălniceanu str., 400084 Cluj-Napoca, e-mail: [email protected]; [email protected]

Keywords: pollen analysis, vegetation, paleoclimate, Pliocene, Dacic Basin.

The Pliocene deposits of the Dacic Basin are characterized by specific continental

floras, with plant associations that are well-individualized and whose evolution was influenced by climate changes.

The palynological analyses on samples from Panga quarry were meant to evidence and investigate in detail some aspects on the vegetation and climate in the region, during the Upper Dacian and the Romanian period.

The main botanic groups that were identified (pteridophytes, gymnosperms, monocotyledonous and dicotyledonous angiosperms) present a relative homogeneity in their evolution through the whole Upper Dacian interval.

From paleoclimate point of view, we consider that during the Upper Dacian - Romanian interval warm and temperate stages succeeded one after the other.

The warmer stages are characterized by the presence of vegetation abounding in thermophile (Arecipites, Myrica) and intermediary (Cedrus, Abies, Carya, Pterocarya, Zelkova, Celtis, Tilia etc.) elements. The vegetation of the cooler periods was dominated by temperate elements (Pinus, Picea, Tsuga, Ulmus, Fagus etc.).

The warm temperate climate at the end of the Dacian allowed the development of mixed vegetation – with both angiosperms and coniferous elements. Dicotyledons were dominant, as shown by pollens of Ulmus, Zelkova, Pterocarya, Carya, and more seldom Salix, Betula, Alnus and Fagus, coniferous – represented by Pinus, Cedrus, and Picea being subordinate.

The palynological analysis of the Lower Romanian sediments pleads for the hypothesis of the continuation of favourable climate elements of the Dacian. Thus, the pollinic spectra are dominated by temperate elements (Pinus, Picea, Ulmus, Fagus), followed by the intermediary (Cedrus, Abies, Carya şi Pterocarya) and sporadically by thermophile (Arecipites, Myrica) ones.


Middle Jurassic Zoophycos in North Dobrogea: An early onshore/offshore migration

Eugen GRĂDINARU1 & Adolf SEILACHER2

1 University of Bucharest, Faculty of Geology and Geophysics, Bd. Bălcescu Nicolae 1, RO-010041 Bucharest, Romania, [email protected] 2 Tübingen and Yale Universities, Geologisches Institut, Sigwartstr.10, D-72076 Tübingen,Germany, [email protected] Keywords: Zoophycos, trace fossil, Middle Jurassic, North Dobrogea, Romania

The trace fossil Zoophycos is known in shallow-marine sequences from

Ordovician to Cretaceous times. Since the Cretaceous, it is also known from deep-sea environments, where it survived to the present day. In this new environment, the unknown trace markers developed highly complex behavioural programs. New discoveries in Middle Jurassic turbidites of North Dobrogea document a different behavioural specialization. Instead of lobes and flat, well-distanced helicospiral whorls, the new ichnospecies produced a backfilled spreite that bends down towards the margin. Also, whorls are so closely spaced that the marginal tube of the previous whorl is regularly erased by the following one. As the width of the spreite increased with the age of the animal, the resulting burrow resembled an ammonite or gastropod shell.

This discovery suggests that the onshore/offshore migration of Zoophycos happened more than once. In every case, however, it led to the evolution of complex behaviour programs that are not found in shallow-marine environments.




First discovery of Rhabdoceras suessi Hauer (Ammonoidea, Upper Triassic) in the exotic Triassic from the East Carpathians

Eugen GRĂDINARU1 & Evgeny SOBOLEV2

1 University of Bucharest, Faculty of Geology and Geophysics, Bd. Bălcescu Nicolae 1, RO-010041 Bucharest, Romania, [email protected] 2 Trofimuk Institute of Petroleum Geology and Geophysics, Siberian Branch of Russian Academy of Sciences, Akademgorodok, Koptyug Ave., 3, 630090 Novosibirsk, Russian Federation, [email protected] Keywords: Rhabdoceras suessi, Ammonoidea, Upper Triassic, Timon-Ciungi olistolith, Rarău Syncline, East Carpathians.

The occurrence of Rhabdoceras suessi Hauer is for the first time recorded in the Upper Triassic limestones that build the Timon-Ciungi olistolith, located in the Rarău Syncline, East Carpathians (Romania). The heteromorphic ammonoid Rhabdoceras suessi has a long range that covers the stratigraphic interval Upper Norian to Rhaetian. In the Timon-Ciungi olistoliths, Rhabdoceras suessi is occurring together with Monotis salinaria that constrains its appearance here to the Upper Norian (Sevatian). Rhabdoceras suessi is a cosmopolitan ammonoid being known from both Tethyan and Boreal ammonoid faunas.




Sedimentary patterns, carbonate diagenesis and geochemistry of the Jurassic hardgrounds from Bucegi Mountains

(Eastern Carpathians)

Mihaela GRǍDINARU1, Cristina PANAIOTU1, Lucian PETRESCU1

& Iuliana LAZǍR1

1 Faculty of Geology and Geophysics, University of Bucharest ([email protected]; [email protected]; [email protected]; [email protected]) Keywords: hardground formation, carbonate diagenesis, geochemistry, Jurassic, Carpathians.

In Bucegi Mountains, the occurrence of indurations surfaces - hardground type has been mentioned by Patrulius (1969, 1980), within the Middle Jurassic deposits that crop out in Strunga – Strunguliţa, Grohotişul Mountain area, at the confluence of the Tǎtarului and Ialomiţei Valleys. Lazǎr (2006) presented an extensive discussion on previous studies (from Suess, 1867, to Patrulius, 1969, 1980 and Neagu, 1996) concerning these condensation levels, heavily mineralized with ?”limonitic” crusts. The most interesting locations that have been studied are La Poliţie Pass, Gaura Valley, Grohotiş Mountain, the area between Strunga Pass and Strunguliţa Pass, and the upper part of the Tǎtarului Valley. The lithostratigraphic successions containing hardground-type discontinuity surfaces have been described; for each studied area, detailed taphonomical and paleoecological observations were recorded.

Carbonate diagenesis studies provide qualitative information about post-depositional evolution features of the sediments like burial rate, or fluid-rock interactions leading to peculiar mineral assemblages over time. Synsedimentary lithified carbonate sea-floors and mineralized surfaces have been formed under a fairly consistent set of physical parameters, thus we used them to estimate ancient sedimentation and erosion rates and to estimate the oceanic geochemistry, as well as tectonic and eustatic changes in the sea level. Intensive sediment’s cementation may represent intervals of exposure to meteoric waters, or burial or renewed sedimentation following an erosional event. The detailed study of cement textures and fabrics allowed us to identify the genuine hardgrounds, formed by synsedimentary submarine cementation.

X-ray diffraction and X-ray fluorescence analyses were used for the evaluation of the degree of crusts’ mineralization. Most of the Jurassic studied hardgrounds were formed on carbonate platforms, into shallow shelf environments with high hydrodynamic basin energy, and high faunal diversity; only a few if them (30 %) are mineralized. On the other hand, pelagic hardgrounds are heavily mineralized with crusts. Fürsich (1979) showed that there is a clear distinction concerning the composition of the crusts: shallow shelf hardgrounds are rich in Fe-hydroxides, while the pelagic ones in Mn-oxides. Rarely, glauconite is associated with the shallow shelf hardgrounds (Fürsich, 1971), while hematite and chamosite with the pelagic ones. When the hardgrounds are pyritized, this indicates strong reducing conditions during the formation process.

X-ray fluorescence spectrometry (XRF) has been used to obtain additional data on the hardgrounds’ depositional environment. A SRS3400 Bruker AXS unit was used, with glass discs (obtained by mixing the calcined samples with lithium nitrate anhydrous and lithium tetraborate and melting the mixture at 1100° C in a platinum crucible) for measuring major oxides.


M. Grădinaru et al. - Sedimentary patterns, carbonate diagenesis and geochemistry of the Jurassic hardgrounds

45

The composition (SiO2, TiO2, Al2O3, Fe2O3, MnO, MgO, CaO, Na2O, K2O, P2O5), in oxides %, was determined for a total of 10 representative hardground samples. In order to verify the accuracy of the resulted data, seven international standards for soil (SRM 2709, SRM 2710, SRM 2711 – National Institute of Standards and Technology, USA, NIST; SO-1, SO-2, SO-3, SO-4 – Canadian Certified Reference Materials Project, Canada, CCRMP) were also analyzed. The geochemical data reveal that the depositional environment was represented by a shelf area; titanium oxides are incorporated in the clay fraction.

The present study groups the preliminary results of an extensive project founded by CNCSIS, Romania (Project 1922 / 2009-2011) to one of the authors (I. Lazǎr), concerning biostratigraphy, genesis and paleoecology of the associated faunas for Jurassic hardgrounds from Romania. SELECTED REFERENCES Fürsich, F. T. 1979, Genesis, environments, and ecology of Jurassic hardgrounds. N. Jb. Paläont.

Abh., 158, 1, p. 1-63, Stuttgart. Lazar, I., 2006, Jurasicul mediu din Bucegi – Versantul Vestic – paleontologie si paleoecologie,

Ars Docendi, Bucuresti. Patrulius, D. 1969, Geologia Masivului Bucegi şi a Culoarului Dîmbovicioara. Editura Acad. R.S.R.,

Bucureşti.

Kimmeridgian – Lower Tithonian ammonite assemblages from Ghilcoş - Hăghimaş Massif (Eastern Carpathians – Romania)

Dan GRIGORE1

1 Geological Institute of Romania (GIR), Caransebeş 1st. Bucharest 012721, Romania, tel. 021-2128952, e-mail: [email protected]

Keywords: Ammonites, Biostratigraphy, Kimmeridgian, Ghilcoş, Romania

The rich ammonite fauna from Ghilcoş Mts. discovered by Franz Herbich in 1866, well scientifically-evaluated by M. Neumayr (1873) and later by other scientists (Vadasz, 1915, Jekelius, 1921, Preda, 1973, Turculeţ, 1980 and others) was considered as an important location for the Kimmeridgian Stageby Arkell (1956) in his “The Jurassic of the World”. In the last 20 years, this fauna was studied more systematically (Grigore, 1996, 2000 2002) and in a complex way (integrated studies) in the frame of the GEOBIOHAS Project by a working group including the author.

The exposures of the “Acanthicum Beds” rich in ammonites are located in the western and north-western side of Ghilcoş Mts. (Grigore 2002 and Grigore & al., in press).

One of the results of this research concerns the biostratigraphic distribution of the ammonites’ fauna, attesting the entire Kimmeridgian and the Lower Tithonian in part for these deposits. The ammonite assemblages confirm the zones Platynota, Hypselocyclum/Strombecki and Divisum for the Lower Kimmeridgian; Acanthicum, Eudoxus and Beckeri for the Upper Kimmeridgian and Hybonotum, Vimineus, Semiforme and Fallauxi for the Lower Tithonian (Grigore, 2000, 2002 Ph.D. thesis). Until now, it was possible to define as taxon ranges only the Platynota and Beckeri zones, while the others were defined as assemblage zones, some of them on partial range of their index. In this paper, each assemblage is detailed and the zones limit is argued. A new range and subzone – Spinata, in the base of Platynota Zone (i.e. of the Kimmeridgian) are also proposed. REFERENCES Arkell W.J., 1956. Jourassic geology of the World. Edinburgh, Oliver and Boyd: 806 pp. Grigore D., 1996. Date noi din regiunea Lacu-Roşu- Hăghimaş. Anuarul Institutului Geologic al

României, Bucureşti. 61/1: 71-74. Grigore D., 2000. Kimmeridgian and Lower Tithonian sequences from East and South Carpathians –

Romania. Anuarul Institutului Geologic al României, Bucureşti. 72 part II: 37-45. Grigore D., 2002. Formaţiunea cu Acanthicum din regiunea Lacu Roşu (Msv.Hăghimaş-Carpaţii

Orientali) - posibil hipostratotip al limitei Kimmeridgian – Tithonic. Stratigrafie.Paleontologie. Teză Doctorat, Univ. „Al.I.Cuza” Iaşi: 347 pp.

Grigore D., Stoica M., Sandy M, Lazar Iuliana, Gheuca I., (in press). Late Jurassic fossil assemblages from the Ghilcoş Mts-Eastern Carpathians-an exquisite paleontological site. The 8th Symposium of IGCP 506 on Marine and non-marine Jurassic. UB, Bucharest 2009.

Herbich F., 1866. Eine geologische Excursion von Bălan an den Vorosto, nach bekas, Zsedan Patak. Verhandlungen und Mittheilungen Siebeburger, verf. Naturwiss., Hermanstatd (Sibiu). 18/10: 80 pp.

Herbich, F. 1878. Das szeclerland mit Berucksichtigung der Angrezenden Landesteile. Mittheilungen aus dem Jahrbuch der Koeniglichen Ungarischen geologischen Reichsanstalt in Budapest. 5: 19-363.

Jekelius E., 1921. Der mittlere und obere Jura in Gebiet des Hăghimaşul Mare in Siebeburgen. Bulletin de la Section Scientifique de l’Academie Roumaine, Bucharest. 7/10.



D. Grigore - Kimmeridgian – Lower Tithonian ammonite assemblages from Ghilcoş - Hăghimaş Massif

47

D. Grigore - Kimmeridgian – Lower Tithonian ammonite assemblages from Ghilcoş - Hăghimaş Massif

48

Neumayr M., 1873. Die Fauna der Schichten mit Aspidoceras acanthicum. Abhandlungen der kaiserliche und koenigliche geologische Reichsanstalt, Wien. 5 (6): 141-257.

Preda I., 1973. Variaţiile de facies şi biostratigrafia Jurasicului superior din Munţii Hăghimaş. Studii şi Cercetări de Geologie, Geografie şi Biologie, Seria Geologie Geografie, Piatra Neamţ. 2: 11-21.

Turculeţ I., 1980. Stratele cu Acanthicum din M. Ghilcoş (Hăghimaş) – o excepţională rezervaţie paleontologică. Anuarul Muzeului Judeţean Suceava, Ştiinţele Naturii, Suceava. 6: 79 – 87.

Vadasz E., 1915. Geologische Beobachtungen im Persanyer und Nagyhagymas Gebirge. Sonderabdruck aus den Mitteilungen aus dem Jahresbericht der koeniglichen ungarischen Geologische Reichsanstalt, Budapest: 264-298.

Is “Pobitite kamani” a Petrified Forest of Varna?

Stănilă IAMANDEI1, Eugenia IAMANDEI2 & Vladimir BOZUKOV3

1 National Geological Museum (IGR),2nd, Kiseleff Ave., 011345 – Bucharest, Romania. 2 Geological Institute of Romania, 1st, Caransebeş Street, 012271 – Bucharest, Romania. 3 Institute of Botany, Bulgarian Academy of Science, Acad. G. Bonchev Street, 1113 - Sofia, Bulgaria. Keywords: Pobitite kamani, petrified forest, bioherms, bubbling reefs, seeping.

Developed on a large area, close to Varna (Bulgaria), there is a very interesting geological site named in Bulgarian “Pobitite kamani” (stones on the ground) or “Dikilitash” in Turkish (stone forest), constituted from numerous stone pillars as high as 10 m, shaped as hollow or solid cylinders, truncated cones, various bulging and single rocks and cliffs suggesting a petrified forest. In order to be protected, since 1937 the Pobitite Kamani area was designated a natural landmark. Previous visitors of this extended site described it as a petrified forest and some former studies and interpretations of Davitashvili & Zaharieva (1975) and others, tried to demonstrate this, based on geologic or geomorphologic arguments, lesser on paleobotanic studies. Nachev et al (1986) interpreted this phenomenon as huge algal bioherms. According to Jansen et al. (1992) the site could represent "bubbling reefs" chimneys of carbonate-cemented rocks supporting a diversified ecosystem at methane seeps. Botz et al. (1993) considered it as the result of late diagenesis in sediments at approximately 1300 m burial depth. After uplift, additionally the effect of percolating groundwaters might have been recorded, because calcium carbonates identified in these pillars show an isotopic composition characteristic for precipitation from meteoric waters under normal sedimentary temperatures, in isotopic equilibrium with 12C-enriched soil carbon dioxide. Other authors simply considered it of unknown origin (Walther, 1994). Recently, an international project was initiated for reviewing the site - currently considered as a result of fossil seeping (De Boever et al. 2002-2008). Recently we visited this extended site for geological observations and sampling; this study presents our recent results.


A carbonized fossil wood in Ocna-Mureş salt deposit

Stănilă IAMANDEI1, Eugenia IAMANDEI2 & Vlad CODREA3

1 National Geological Museum (IGR),2nd, Kiseleff Ave., 011345 – Bucharest, Romania. E-mail: [email protected] 2 Geological Institute of Romania, 1st, Caransebeş Street, 012271 – Bucharest. Romania. 3 “Babes-Bolyai” Univ. Cluj-Napoca, Faculty of Biology and Geology, Departm. of Geology and Paleontology, 44th, Bilascu street, 4000015 - Cluj-Napoca, Romania. E-mail: [email protected]

Keywords: charcoal, salt environment, paleoecology.

The Miocene salt deposits of Transylvania preserve a lot of poorly-studied vegetal remains, which can contribute to paleoclimatic and paleoecological reconstructions of their geological time. Salt rock provides a special type of fossilization environment, leading, e.g. to mummification. Large amounts of mummified woods can be found within “salt breccia” in the Subcarpathians; besides, also fruit and seeds, pollen and spores, and to a lesser extent leaves can be found. They have been transported there by wind or by water. A fragment of coalified wood found within the Miocene salt deposit of Ocna Mureş was studied, identified as a coniferous wood and is presented here. It is in the form of charcoal, which signifies that the wood was subject of a fire previous to reaching the salted basin as a piece of char; subsequently it was fossilized like that, and preserved by salt.




Fossil woods in the collection of Drobeta-Tr. Severin Museum

Eugenia IAMANDEI1, Stanila IAMANDEI2 & Florina DIACONU3 1 Geological Institute of Romania, 1st, Caransebeş Street, 012271 – Bucharest, Romania. E-mail: [email protected] 2 National Geological Museum (IGR),2nd, Kiseleff Ave., 011345 – Bucharest, Romania. 3 Museum of Iron Gates Region, 2nd, Independence street, 220160 - Drobeta-Turnu Severin, Romania. E-mail: [email protected] Keywords: “Iron Gates” Museum Collection, Pliocene petrified wood, paleoclimatic and paleoecologic significance

Our study concerned a small collection of Pliocene petrified wood coming from newly discovered locations like Bala and Marman (Mehedinţi County), currently hosted by the “Iron Gates” Museum in Drobeta-Tr. Severin. The paleoclimatic and paleoecologic significance of the identified taxa is discussed, especially in this region of the Dacic Basin where large Pliocene coal deposits are known, unfortunately less studied from wood species point of view. Following a difficult study on a badly preserved material, we can state that the newly identified vegetal taxa belong to Conifers and to Dicotyledons; it can be added to the previously known regional flora of similar age, in the frame of lowlands and related to the coal deposits. Further systematic research could enrich the collection of the “Iron Gates Region” Museum, as well as and also our knowledge on Pliocene paleobotany in the western part of the Dacic Basin.




Liassic Petrified Wood in the Carpathian Mountains

Eugenia IAMANDEI1, Stănilă IAMANDEI2 & Eugen GRĂDINARU3 1 Geological Institute of Romania, 1st, Caransebeş Street, 012271 – Bucharest. Romania. E-mail: [email protected] 2 National Geological Museum (IGR),2nd, Kiseleff Ave., 011345 – Bucharest, Romania. 3 University of Bucharest, Faculty of Geology and Geophysics, Departm. of Geology, 1st, Bălcescu Blvd., 010041 - Buharest, Romania. E-mail: [email protected]

Keywords: Carpathian Liassic Flora, petrified forest, Gymnosperms, new taxa

Liassic flora in the South Carpathian Mountains is especially known from the study of vegetal adpressions identified in the Liassic coaly deposits from the region (Ettinghausen, 1852; Stur, 1860-1872; Humml, 1957; Semaka, 1956-1962, Givulescu, 1990-2002). There were even some attempts to achieve a detailed Liassic phytostratigraphy (Semaka 1962; Popa, 2002). More recently, new studies and re-evaluations were performed by Popa, 1992-2005; Popa & Van Konijnenburg-Van Cittert, 2006). The identified flora belongs to Bryophytes, Pteridophytes, Pteridosperms, Cycads and Gymnosperms. However no systematic paleoxylotomical studies on the coalified trunks from the coal deposits were done till now. The newly collected petrified woods from Liassic deposits in Braşov region provided us the opportunity to start their systematic study. The first results indicate the presence of some Liassic morphotaxa, recorded for the first time in the Romanian Carpathians, such as Circoporoxylon, Gingkoxylon, Baieroxylon and diverse other Gymnosperms. The newly described Liassic lignoflora has interesting paleobiogeographic, paleoecologic and paleoclimatic significance, which will be discussed.




Petrified wood from Căprioara Valley, Feleac, Cluj

Stănilă IAMANDEI1, Eugenia IAMANDEI2 & Mirela SABĂU DUMITRESCU3

1 National Geological Museum (IGR),2nd, Kiseleff Ave., 011345 – Bucharest, Romania. E-mail: [email protected] 2 Geological Institute of Romania, 1st, Caransebeş Street, 012271 – Bucharest. Romania. 3 “Babes-Bolyai” Univ. Cluj-Napoca, Faculty of Biology and Geology, Departm. of Geology and Paleontology, Str. M. Kogălniceanu nr.1, 400084 - Cluj-Napoca, Romania. E-mail: [email protected] Keywords: Early Sarmatian, Feleac Flora, petrified wood, paleoclimatic significance

A new fragment of petrified wood represents a challenge. Especially if it comes from a new location and it is studied by a potential paleoxylologist to-be, currently a junior student. The fossiliferous source area is well known from the papers of Staub (1883, 1891), Szadeczky (1917) or Givulescu (1957-1997) which have described a small Early Sarmatian flora with Pinus felekiensis, Sequoia abietina, Quercus mediterranea, Daphnogene polymorpha, Platanus, Palaeocarya, Phragmites, Cyperites and others, indicating a mesophytic forested riverside vegetation growing under warm temperate climate conditions. The sample, consisting of several decimetre-long fragments coming from the same petrified trunk was described and some oriented thin sections have been studied under the optical microscope. The specific features point to a taxodiaceous wood, the identification being a good lesson for a new student in paleoxylology. The paper presents the detailed description of the new fossil wood and comparative structures of extant relatives.




New data regarding Congeria fauna from Bârnova-Muntele Formation

Viorel IONESI1 & Gabriel CHIRILĂ1

1 “Al. I. Cuza” University of Iaşi, Department of Geology, Bd. Carol I, no. 20A, 700505, Iaşi, Romania, e-mail: [email protected]; [email protected] Keywords: Ciortesti, Bârnova-Muntele Formation, Moldavian Platform, Congeria, Mactra.

The purpose of this paper was to present the paleontological association identified in Ciorteşti area (Vaslui County) belonging to the Bârnova-Muntele Formation (Moldavian Platform). This is the first mention of the studied outcrop. A similar outcrop was discovered at approx. 10 km north-eastwards by JEANRRENAUD (1971) near Răducăneni (Pârâul Pietrei). The fauna identified by JEANRRENAUD at Răducăneni was studied by IONESI and COCHIOR (1995). The fauna we have studied from Ciorteşti is very similar to that described by IONESI and COCHIOR (1995): Congeria taxa (Congeria neumayri moldavica, C. neumayri poenensis, C. tacutai, C. elongata, C. mediocarinata, C. zsigmondyi etc.) but also taxa of small Mactra (Mactra caspia acuminata, M. caspia caspia, M. (P) podolica naviculata), Hydrobia, Helix, Melanopsis, Planorbis. The above-mentioned brackish fauna forms a fosiliferous level. According to IONESI et al. (2005), congerias were contemporaneous with small mactras, but they inhabited waters with a reduced salinity, such as the outlet zones of some hydrographical distributaries or lagoon basins, separated by bars (with or without breaches).




The Formation with Cryptomactra in Palas area (Iaşi, Romania)

Viorel IONESI1 & Florentina PASCARIU1

1“Al. I. Cuza” University of Iaşi, Department of Geology, Bd. Carol I, no. 20A, 700505, Iasi, Romania, e-mail: [email protected]; [email protected] Keywords: foraminifera, Formation with Cryptomactra, Palas, Iaşi, Romania

During construction works in Palas area (Iaşi Municipality), several profiles were made available in deposits belonging to the Formation with Cryptomactra, at various locations. In these profiles, the following fauna was identified: Cryptomactra pesanseris, foraminifera taxons (Elphdium macellum converia, E. incertum, Nonion bogdanowiczi, Quinqueloculina akneriana, Q. cf. complanata), statoliths of Mysidae, ostracods etc. The identified fossil fauna was found in the yellow clays, located immediately below the foundations of the old buildings studied from archaeological point of view, but also in the underlying grey – greenish clays.

From geotechnical point of view, in Iaşi area there are two categories of rocks in which building foundations may be located: „bedrock” and „shallow deposits”. The „bedrock” is the correspondent of the Formation with Cryptomactra, while the „shallow deposits” are represented by Quaternary deposits. One of the most important criteria to separate these „soils” is colour: the „bedrock” is grey–greenish and the „shallow deposits” are mostly yellow. Our study points out that this criterion is not always valid.




Palaeoclimatic reconstructions for the Late Miocene in Southwest Bulgaria based on palynological data

Dimiter IVANOV1

1 Institute of Botany, Bulgarian Academy of Sciences, Acad. G. Bonchev Str., bl. 23; 1113 Sofia, Bulgaria; e-mail: [email protected] Keywords: palaeobotany, palynology, vegetation analysis, climate reconstructions, Upper Miocene, Bulgaria.

Lake and lake-and-marsh sediments are widely spread on the territory of South Bulgaria and they often contain various plant fossils: carpoids, leaf imprints, cuticles, as well as spores and pollen. In the last years, Neogene sediments from the Sandanski Basin have been palynologically studied, revealing new floristic data (Ivanov 2003). The present paper is a continuation of these studies and it offers a quantitative palaeoclimate analysis of the fossil pollen flora. The analyzed palynomorphs come from the Sandanski Formation, represented by irregularly layered whitish, yellowish and greyish-green conglomerates, sandstones, siltstones and clays, interbedded with fine-grained coal layers. According to finds of mammalian fauna (zones MN 11-12), the age of the formation is estimated as Turolian.

The Sandanski Basin (Fig. 1) is filled in with alluvial-proluvial, lake and lake-marsh sediments. Three sedimentation cycles were differentiated in the evolution of the basin and four lithostratigraphic units have been described (Kojumdgieva et al. 1982, Nedjalkov et al. 1986). More recent investigations suggest that the accumulation of upper Miocene terrigenous-continental (alluvial or alluvial-proluvial) deposits is related to active and inconstant river activity of “braided rivers”-type (Tzankov et al. 2005) This is characterized by rapid and very irregular sedimentation. Thus the lake/marsh sedimentation is limited only to small ponds in the southern part of the Sandanski Basin, from where originate the analyzed pollen samples (three cores drilled in the southern part of the basin).

Fig. 1. Geological map of the Neogene sediments in the Sandanski Graben. (Redrawn after Kojumdgieva et al. 1982). Legend: 1. Kalimantsi Formation: a) IInd cycle; b) IIIrd cycle. 2. Sandanski Formation: a) IInd cycle; b) IIIrd cycle. 3. Delchevo Formation. 4. Fault. 5. Position of the drill core.

Vegetation analysis. Paleoecological analysis of pollen flora led to inferences about the


D. Ivanov - Palaeoclimatic reconstructions for the Late Miocene in Southwest Bulgaria based on palynological data

character of the fossil vegetation. Swamp forests of Taxodiaceae (Glyptostrobus and Taxodium) were widest distributed. Alnus, Liquidambar, Myrica, Nyssa, and Itea contributed to these plant communities; they developed on permanently/temporary flooded terrains along the basin. The presence of Sparganium, Typha, Nuphar, and Pseudoeuryale, Ceratophyllum, Brasenia, Potamogeton, Stratiotes, Carex, Acorellus suggests the existence of communities of aquatic plants inhabiting the areas close to swamp forests and the shallow-water littoral zone of the basin.

A major role in the composition of mesophytic forest paleocoenoses was played by species of Quercus, Castanea, Ulmus, Pterocarya, and Carya, but representatives of Betula, Carpinus, Corylus, Castanopsis, Fagus, Juglans, Engelhardia, and Araliaceae were also common contributors. The mesophytic forests developed on relatively distant areas from the basin, on the hilly and mountainous terrains surrounding the paleobasin, without forming an integrally-developed mesophytic forest belt. Some xerophytic elements (Celtis, Pistacia, Berberis and Rubus) evidenced the existence of xeromesophilous shrub communities along stony slopes and in drier habitats.

The presence of a considerable number of herbaceous taxa (Chenopodiaceae, Artemisia, Centaurea, Asteroideae, Chichrioideae, Caryophyllaceae, Poaceae etc.) with relatively high abundance suggests distribution of herbaceous communities in open riverine valleys and on low-hill territories. Finds of Hipparion fauna related to open spaces and steppe (or savannah) communities (Kojumdjieva et. al. 1982) corroborate to this assumption. The herbaceous coenoses had played a significant role in the structure of vegetation.

Palaeoclimate analysis. In order to reconstruct palaeoclimate based on palynological record, the coexistence approach (CA) (Mosbrugger & Utescher 1997) was applied. In the present study, four climatic parameters were considered and discussed below, namely mean annual temperature (MAT), mean temperature of the coldest month (CMT), mean temperature of the warmest month (WMT), and mean annual precipitation (MAP). These are the parameters which most reliably record changes in palaeoclimatic conditions because their effect on plant distribution is most significant (Ivanov et al. 2002).

The results of palaeoclimate analysis point to dynamic climatic conditions during the sedimentation process. Intervals for mean annual temperature covered mainly the range 15.6–18.4° C, winter temperatures in most cases were 5 to 9.4° C. Most common intervals for summer temperatures were 25.6–27.5° C and 25.6–28.1° C (Fig. 2). The annual amount of precipitation represents a quite variable parameter. The highest intervals fall in the 1187–1322 mm range, while the lowest in the 512-741 mm one (in some cases even lower). Lower levels of rainfall probably reflect dry climate with seasonal distribution of rainfall. These values indicate that the climate was about 3-4 degrees warmer than today, and precipitation reached values exceeding more than twice the contemporary level.

The dynamics of climate variables in the sedimentary sequences revealed changes in climate conditions which are likely cyclical in nature, but fragmentarily presented. The oldest sediments of the drilling section C-554 show a pronounced tendency of transition from dry and cool climate to warmer and more humid one (Fig. 2), which was well-reflected in the CA-intervals for MAP, MAT and TWM. After the stabilization of the annual precipitation value at about 1000 mm and the installation of a relatively constant temperature, a tendency towards a dry and cool climate occurred, with two distinct intervals for rainfall and lower values for MAT and TCM (Fig. 2), which was followed by a new pulse towards increasing humidity (CA-intervals for

57

D. Ivanov - Palaeoclimatic reconstructions for the Late Miocene in Southwest Bulgaria based on palynological data

Fig. 2. Coexistence intervals (bars) for mean annual temperature (MAT), temperature of the coldest (CMT) and warmest month (WMT), and mean annual precipitation (MAP) based on pollen data from core C-554. The curve linking middle values of CA-intervals is shown to better express the overall trends of climate change.

annual rainfalls are 897-1322 mm and 1187-1322 mm), annual and summer temperatures. This period of more humid and warm climate turns again into a dry and cool period with reduction of precipitation and average annual temperature. Similar climate variations during the Maeotian were recorded by microfloristic complexes in the Forecarpathian Basin, NW Bulgaria (Ivanov et al. 2002). Acknowledgements: This work is a contribution to the Project B-1525 (NSF, Bulgaria). REFERENCES Ivanov D., 2003. Palynological data on the Miocene flora and vegetation of the Sandanski Graben.

Phytologia Balcanica, 9, 197-206. Ivanov D., Ashraf, A. R., Mosbrugger, V. & Palamarev, E., 2002. Palynological evidence for Miocene

climate change in the Forecarpathian Basin (Central Paratethys, NW Bulgaria). Palaeogeogr., Palaeoclimatol., Palaeoecol., 178, 19-37.

Kojumdgieva E., Nikolov I., Nedjalkov, P. & Busev, A., 1982. Stratigraphy of the Neogene in the Sandanski Graben. Geologica Balcanica, 12, 69-81.

Mosbrugger V.& Utescher T., 1997. The coexistence approach - a method for quantitative reconstructions of Tertiary terrestrial palaeoclimate data using plant fossils. Palaeogeogr., Palaeoclimatol., Palaeoecol., 134, 61-86.

Nedjalkov P., Tcheremisin, N., Kojumdgieva, E. , Tzatzev, B. & Busev, A., 1986. Facial and palaeogeographic features of Neogene deposits in the Sandanski graben. Geologica Balcanica, 16, 69-80.

Spassov N., Tzankov T. & Geraads, D., 2006. Late Neogene stratigraphy, biochronology, faunal diversity and environments of South-West Bulgaria (Struma River Valley). Geodiversitas, 28, 477-498.

Tzankov T., Spassov N. & Stoyanov, K., 2005. Neogene-Quaternary Paleogeography and Geodynamics of Middle Struma River Valley Area (S.-W. Bulgaria). South-West University “N. Rilski”, Blagoevgrad, 199 p. (English summary).

58

Correlation of Upper Jurassic-Lower Cretaceous carbonate platforms in Western Bulgaria and Eastern Serbia based on

foraminiferal record and microfacies

Daria IVANOVA1, Elena KOLEVA-REKALOVA2 & Nenad MALESEVIC3

1, 2 Geological Institute, Bulgarian Academy of Sciences, Acad. G. Bonchev Str., Bl. 24, 1113 Sofia, Bulgaria 3Department of Geology, Faculty of Mining and Geology, University of Belgrade, Kamenicka 6, P.O. Box 227, 11000 Belgrade, Serbia; [email protected]; [email protected]; [email protected] Keywords: Upper Jurassic, Lower Cretaceous, carbonate platform, microfossils, microfacies, correlation, W Bulgaria, E Serbia

The present study focuses on the correlation of Upper Jurassic–Lower Cretaceous carbonate platform sequences in Western Bulgaria and Eastern Serbia based on foraminiferal record and microfacies.

The Upper Jurassic and Lower Cretaceous systems are well presented in both West Bulgaria and East Serbia. The Upper Jurassic–Lowermost Cretaceous sediments were deposited in a bathymetrically-differentiated basin, associated with the gradual emergence of the southern landmass and the formation of the Central Moesian Basin. The West and East Moesian platforms were developed on both sides of the Central Moesian Basin. The sections under study are located in the south-western prolongation of the Western Moesian Carbonate Platform (Patrulius et al., 1976, fig. 4) and belong to the outcrops in the Dragoman positive block, according to Sapunov et al., 1985. Later, Tchoumatchenco et al. (2006a, b; 2008) introduced new palaeogeographic/paleotectonic units for Western Bulgaria and Eastern Serbia; accordingly, the studied sections belong to the Getic unit (Western Getic unit).

The main part of the studied sections is represented by the limestones of the Slivnitsa Formation (Western Bulgaria) and Crni Vrh Limestones (Eastern Serbia). Both formations are built-up by thick-bedded to massive, light gray to whitish organogenic - and less common micritic - limestones containing a large number of benthic foraminifers and massive alga, colonial corals, rudists, brachiopods, crinoids, gastropods and other benthic forms.

The taxonomic identification of the microfossils and the analysis of the benthic foraminifers for the Middle Callovian?–Hauterivian interval is a result of the investigation of more than 200 thin sections. The studied carbonate successions were mainly generated in a shallow marine environment. This environment can be divided into a deeper, and a shallower subtidal one. The shallower subtidal is represented by a deeper subtidal (with open platform development) and a shallow subtidal environment. A higher abundance of agglutinated foraminifers is connected with the shallow or very shallow marine (shallower subtidal) environment. In the carbonate platform sections, rich foraminiferal associations were determined, the biostratigraphic significance of some of the species being pointed out. From stratigraphical point of view, the most important species are: Globuligerina oxfordiana (Grigelis), Trocholina conica (Schlumberger), Ophthalmidium strumosum Gümbel, Paalzowella feifeli Paalzow, Ammobaculites irregularis Gümbel, Textularia jurassica Gümbel, Ammobaculites suprajurassicus (Schwager), Labyrinthina mirabilis Weynschenk, Mesoendothyra izjumiana Dain, Protopeneroplis striata





D. Ivanova et al. - Correlation of Upper Jurassic-Lower Cretaceous carbonate platforms in Western Bulgaria and Eastern Serbia

60

Weynschenk, Protopeneroplis ultragranulata (Gorbachik), Haghimashella arcuata (Haeusler), Pseudocyclammina lituus Yokoyama, Nautiloculina bronnimanni Arnaud-Vanneau & Peybernes, Charentia cuvillieri Neumann, Haplophragmoides joukowskyi (Charollais, Brönnimann & Zaninetti), Meandrospira favrei (Charollais, Brönnimann & Zaninetti), Patellina turriculata Dieni & Massari, Istriloculina eliptica (Iovcheva), Istriloculina emiliae Neagu, Quinqueloculina infravalanginiana Bartenstein, Quinqueloculina multicostata Neagu, Verneuilinoides neocomiensis (Mjatliuk), Protomarssonella kummi (Zedler), Montsalevia salevensis (Charollais, Brönnimann & Zaninetti), Valdanchella miliani Pfender, Pfenderina neocomiensis (Pfender), Pfenderina trochoidea Smout & Sugden, Paracoskinolina jourdanensis Foury & Moullade, Paracoskinolina tunesiana Peybernes, Paracoskinolina pfenderae Canerot & Moullade, as well as representatives of genus Trocholina.

Applying microfossil (mainly foraminifera) biostratigraphy and microfacies analysis allowed us to obtain more precise evidence on the age of the studied sequences and to correlate them in the area across the Bulgarian – Serbian border.

Acknowledgements. We thank all colleagues from the Bulgarian-Serbian bilateral joint project for field trip studies, for their kind advices on regional geology, and critical remarks on the text. This work was undertaken in the framework of the Joint Research Project “Transborder stratigraphic correlations in Western Stara Planina Mts between East Serbia and West Bulgaria” and was financially supported by the Project 1516/05 of the Bulgarian Scientific Fund. REFERENCES Patrulius D., Neagu T., Avram E. & Pop, G., 1976. The Jurassic – Cretaceous boundary beds in

Romania. An. Inst. Geol. Geof., 50: 71-125. Sapunov I., Tchoumatchenco P., Dodekova L. & Bakalova, D., 1985. Stratigraphy of the Callovian and

Upper Jurassic rocks in Southwestern Bulgaria. Geologica Balc., 15, 2: 3-61. Tchoumatchenco P., Rabrenović D., Radulović B. & Radulović, V., 2006a. Trans-border (east

Serbia/west Bulgaria) correlation of the Jurassic sediments: main Jurassic paleogeographic units. Annales Géologiques de la Péninsule Balkanique, 67; 13-17.

Tchoumatchenco P., Rabrenović D., Radulović B. & Radulović, V., 2006b. Trans-border (east Serbia/west Bulgaria) correlation of the Jurassic sediments:Infra-Geticum. Annales Géologiques de la Péninsule Balkanique, 67; 19-33.

Tchoumatchenco P., Rabrenovic D. Radulovic, V. Malesevic N. & Radulovic, B., 2008. Trans-border (South-Eastern Serbia/South-Western Bulgaria) correlations of the Jurassic sediments: the Getic and Supra-Getic units. Annales Géologiques de la Péninsule Balkanique, 69; 1-12.

Late Aptian planktonic foraminiferal biostratigraphy of the West Carpathian Pieniny Klippen Belt and Fatric units

(Choč Mts., Malá Fatra Mts.)

Štefan JÓZSA1

1 Department of Geology and Paleontology, Faculty of Natural Sciences, Comenius University, Mlynská dolina G-1, 842 15 Bratislava, [email protected]

Keywords: Late Aptian; Planktonic foraminifera; Biostratigraphy; Western Carpathians

Several profiles and localities have been studied to obtain data on the occurrence and distribution of Late Aptian planktonic foraminifera from Párnica Marl Formation, Nižná Limestone Formation and Rudina Marl Formation, of the Fatric and Pieniny Klippen Belt paleogeographic domains, in the Slovak part of the Western Carpathian area. Earlier studied associations belong to the Leupoldina cabri zone with scarce but diverse occurrence of morphotypes with spherical, elongate and radial chambers (Blefuscuiana / Hedbergella, Globigerinelloides, Liliputianella, Leupoldina, Schackoina, Pseudoschackoina). Morphotypes with elongate and radial chambers among abundant morphotypes with spherical chambers are common in black shales of the Nižna Limestone Formation (Leupoldina cabri zone). As for the Párnica Marl Formation, among common spherical-chambered planktonic foraminifera, scarce radial-chambered morphotypes have been observed (Leupoldina). Less typical, but present are forms with elongated chambers identified in the Párnica Marl Formation, Globigerinelloides ferreolensis zone, along with seldom booms with dominant Lilliputianella globulifera (KRETCHMAR and GORBACHIK). The total abundance of planktonic foraminifera increases starting with Globigerinelloides ferreolensis zone. Opposite to rather eupelagic character and rich associations in the Pieniny Klippen Belt (Rudina Marl Formation), the Fatric formations show originally rather hemipelagic (Párnica Marl Formation), and later on flysch features (Poruba Formation) with rather scarce microfossil content. Dominant in the associations of the Globigerinelloides ferreolensis and Globigerinelloides algerianus zones are morphotypes with spherical chambers (Blefuscuiana / Hedbergella, Globigerinelloides with typical larger, many-chambered globigerinelloids). Subsequently, an association with Blefuscuiana / Hedbergella, Globigerinelloides and scarce Pseudoplanomalina developed, which was assigned to Planomalina cheniourensis / Hedbergella trocoidea zone (Párnica Marl Formation). The latest association consists of larger spherical-chambered morphotypes (Blefuscuiana / Hedbergella, Ticinella, Globigerinelloides or Planohedbergella). This association is assigned to Ticinella bejaouensis zone (Rudina Marl Formation, Párnica Marl Formation). Acknowledgements. Financial support provided by the Slovak Research and Development Agency (project APVV-0280-07, and APVV-0571-06) is gratefully acknowledged.



Lithostratigraphical units of the external flysch of the Eastern Carpathians. Terminology issues

Doru-Toader JURAVLE1, Carmen Mariana CHIRA2, Crina MICLĂUŞ1,

Constantin GRASU1 & Angelica JURAVLE3

1 Faculty of Geography and Geology, “Al.I.Cuza” University, 20A, Carol I Street, 700505-Iaşi, Romania, [email protected] 2 Babes-Bolyai University, Faculty of Biology and Geology, Department of Geology, 1 Kogălniceanu St., Cluj-Napoca, 400084, Romania, [email protected] 3 SMARTCOM S.A., Iaşi, Romania, [email protected] Keywords: external flysch, petrographic type, lithostratigraphical units, lithofacies, terminology

When reviewing the history of the names used in references concerning the external flysch of the Eastern Carpathians for the lithostratigraphical units, one can notice that various schemes have been used that do not comply with the current regulations of the ICS and thus may lead to confusion. The main confusing aspects that were pointed out by references are related to the pre-requisite requirements when presenting lithostratigraphical aspects of areas within the Carpathian flysch region by constant use of lithological facies, characteristic lithostratigraphical units and petrographic types, as well as by relatively wide employment of informal names for these units. The aspects under debate mainly refer to: insufficiently-sensitive terms used for defining specific petrographic types and lithostratigraphic units; procedure used for naming lithofacies types for the Carpathian external flysch; and frequent usage of informal terms.

1. Using petrographic and lithostratigraphic terms The original definition of the lithostratigraphic units was mainly based on

petrographic and stratonomic features of the “rock volumes”. For example, in the western part of the Tarcău Nappe, Athanasiu (1908, in Grasu et al., 1988) described the stratotype of the lithostratigraphic unit known as “Tarcău Sandstone Formation”. Băncilă (1958), separated „the Tarcău sandstone horizon”. Than the petrographic meaning of the term „Tarcău sandstone” has been abandoned, this being used for defining the lithostratigraphic unit with typical lithological features as non-formal equivalent for the Tarcău Sandstone Formation (Grasu et al., 1988; Ionesi, 1968; Micu, 1981; Mutihac, 1990; Mutihac & Ionesi, 1974; Săndulescu, 1984). However, sometimes in the same paper the authors have used the term “Tarcău sandstone” in both its petrographical and lithostratigraphical meanings (Mutihac, 1990), generating confusion. Similar problems occurred also in the case of the usage of the following terms: „Scorbura sandstone”, „Doamna limestone”, „Lucăceşti sandstone”, „Tărcuţa sandstone”, „Kliwa sandstone”, „Vineţişu sandstone” [Grasu et al., 1988; Grasu et al., 2007; Mutihac & Ionesi, 1974; Săndulescu, 1984) etc.

2. Using lithofacies types for the external flysch units The situation in the field has imposed separation of areas of lithofacies variability

that reflect distinctive depositional environments within the flysch basin, as well as various relationships with their source areas. Ionesi (1968) considered that the geometric criterion used for the separation of tectonic units and lithofacies types induces a series of ambiguities related to their spatial distribution. The terms introduced by Ionesi, which subsequently become standard ones, concerned the



D.T. Juravle et al. - Lithostratigraphical units of the external flysch of the Eastern Carpathians. Terminology issues

Eocene lithofacies types of Tarcău, Tazlău and Doamna, as well as the Oligocene ones of Fusaru, Moldoviţa and Kliwa. These terms reflect petrofacial variations along the orogenic polarity (west-to-east). Ionesi’s lithofacial scheme has been completed by taking into account the longitudinal lithological variations within the basin, the following lithofacies types being subsequently separated: Scorbura - north from Moldova Valley (Eocene), as well as Leşunţ, Piepturi-Puica and Colţi (Eocene) and Pucioasa (Oligocene) – south from Trotuş Valley. The confusion arising from the usage of this terminology (items 1 and 2 above) in the references are related to the ambivalent meaning referring to both petrographic types (e.g. Kliwa quartzitic sandstone, Scorbura quartzitic sandstone, Lucăceşti quartzitic sandstone, Doamna limestone), and lithostratigraphic units (e.g. „Tarcău Sandstone”, „Doamna Limestone”, „Lucăceşti Sandstone”, „ Kliwa Sandstone”). In such cases, simple solutions could be represented by: a – the use of the term, e.g. „Tarcău sandstone” in its originary petrographic meaning (Băncilă, 1958); b – the use of names of lithostratigraphical units in agreement with the ICS regulations Filipescu (2002) (e.g. Tarcău Formation instead of the informal term „Tarcău Sandstone”); c – the use of the name of the formation that differentiates lithofacies types would not be confusing anymore if the recommendations presented above (items 1 and 2) would be implemented (e.g. the Eocene Tarcău lithofacies used as name for the rock volume corresponding to the Eocene series, clearly distinctive from the adjacent ones in Tarcău Formation). Thus, using terms following the algorithm: Tarcău sandstone (petrographic type) –Tarcău Formation (lithostratigraphic unit) – Eocene Tarcău lithofacies would prevent confusion in specialized references and would provide lithostratigraphic coherence in regional geological interpretations.

3. Using informal terms This aspect is typical for descriptions of areas showing transitions between

classical lithofacial domains. For example, for Suceviţa Basin, the term „Plopu-Bisericani Formation” was introduced (Micu, 1981), while for Suceava Basin „Scorbura-Tazlău Formation”, „Doamna-Viţeu Formation”, and „Sorbura-Doamna Lithofacies” were used (Juravle, 2007). Solving these issues implies two possibilities: a – if the lithostratigraphic information is presented in detail, and two distinctive lithostratigraphic units may be separated, this should be done (e.g. two lithostratigraphic units may be defined as formations: Scorbura Formation and Tazlău Formation within the lithological column corresponding to „Scorbura-Tazlău Formation”); b – if the description of the formation does not provide data for coherent interpretation of lithological variation along the lithological column, then the formation has to be revised only following mapping in the field (e.g. „Plopu-Bisericani Formation”).

REFERENCES Băncilă I. (1958) – Geologia Carpaţilor Orientali. Editura Ştiinţifică, Bucureşti, p. 249-254. Filipescu S. (2002) – Stratigrafie. Presa Universitară Clujeană, p. 125-166. Grasu C., Catană C., Grinea D. (1988) – Flişul carpatic. Petrografie şi consideraţii economice. Editura

Tehnică, Bucureşti, p. 71-73, 106, 133, 136. Grasu C., Miclăuş Crina, Florea F., Şaramet M. (2007) – Geologia şi valorificarea economică a rocilor

bituminoase din România. Editura Universităţii „Al. I. Cuza” Iaşi, Iaşi, p. 125-126, 144. Ionesi L. (1968) – Cu privire la nomenclatura utilizată în flişul Carpaţilor Orientali. An. şt. ale Univ. „

Al. I. Cuza” Iaşi, secţiunea II-b, Geol.-Geogr., T. XIV. Ionesi L. (1971) – Flişul paleogen din bazinul văii Moldovei. Editura Acad. R. S. R., Bucureşti, p. 71-

74, 83.

63

D.T. Juravle et al. - Lithostratigraphical units of the external flysch of the Eastern Carpathians. Terminology issues

64

Juravle D-T. (2007) – Geologia regiunii dintre Valea Sucevei şi Valea Putnei (Carpaţii Orientali). Casa Editorială Demiurg, Iaşi.

Micu M. (1981) – Nouvelles donnees sur la stratigraphie et la tectonique du flysch externe du bassin de la Suceviţa. D.S. Inst. Geol. Geof., vol. LXIV, Bucureşti, p. 51-65.

Mutihac V. (1990) – Structura geologică a teritoriului României. Editura Tehnică, Bucureşti, p. 179-181.

Mutihac V., Ionesi L. (1974) – Geologia României. Editura Tehnică, Bucureşti, p. 279, 282, 288, 299. Săndulescu M. (1984) – Geotectonica României. Editura Tehnică, Bucureşti, p. 266-267, 271-273.

The systematic position of the foraminiferal genus Cubanina Palmer, 1936 and its relationship to Columinella Popescu, 1998

Michael A. KAMINSKI1 & Gilberto SOTO2

1 Department of Earth Sciences, UCL, Gower Street, London, WC1E 6BT, U.K. E-mail: [email protected] 2 Centro de Micropaleontologia “Pedro Bermúdez”, INTEVEP, Los Teques, Venezuela Keywords: Foraminifera, systematics

The foraminiferal genus Cubanina Palmer, 1936 (type species Cubanina alavensis Palmer, 1936), first described from the Oligocene of Cuba, is characterised by its triserial to uniserial coiling and thick, coarsely agglutinated wall. The chambers are subdivided by vertical partitions that extend from the floor to the ceiling of the chambers. In the systematics of Loeblich & Tappan (1987) the genus was placed within the superfamily Ataxophragmiacea.

We examined topotype specimens of Cubanina that are preserved in the P.J. Bermúdez collection in INTEVEP, Los Teques, Venezuela. Specimens in the Bermúdez collection are from “Batey of Central Alava”, Matanzas Province, Cuba and are registered in slide BC836. These specimens may even be metatypes or paratypes, because Palmer and Bermúdez collaborated on the study of the Cuban Oligocene. Our examination of abraded and broken specimens reveals a regularly canaliculate wall structure, with pseudopores clearly visible under a binocular microscope as a regular pattern of small dark spots on the abraded test surface, owing to their pyrite infillings. We therefore transfer Cubanina Palmer, 1937 to the order Textulariida, subfamily Colominellinae Popescu, 1998.

The genus Colominella Popescu, 1998 (type species Textulariella paalzowi Cushman, 1936, described from Coştei in Transylvania) is similar to Cubanina in the fact that it possesses an identical coiling mode and internal vertical partitions, but differs in possessing a long biserial stage and lacking a terminal uniserial stage. Our finding of pseudopores in Cubanina means that the two genera may be closely related. In agglutinated foraminifera, the transition from a biserial stage to a uniserial stage is regarded to be a more advanced character state within a lineage. Terminally uniserial genera generally have a biserial ancestor. The fact that Cubanina is found at an older stratigraphical level than Colominella or the other genus in the subfamily (the terminally biserial genus Colomita Gonzalez-Donoso, 1968) presents an interesting evolutionary paradox that begs further investigation.

REFERENCES Loeblich A.R. & Tappan H., 1987. Foraminiferal Genera and their Classification. Van Nostrand

Reinhold. 970 pp + 847 pl. Palmer D.K., 1936. New genera and species of Cuban Oligocene foraminifera. Memorias de la

Sociedad Cubana de Historia Natural "Felipe Poey", 10, 123-128. Popescu G, Cicha I. & Rögl, F., 1998. Systematic Notes. In: Cicha, I., Rögl, F., Rupp, C., & Cytroka,

J. (eds), Oligocene – Miocene foraminifera of the Central Paratethys. Abhandlungen der senckenbergischen naturforschenden Gesellschaft, 549, 69-325.


Cathodoluminescence as a tool in foraminiferal studies: a case study from Oxfordian, southern Poland

Bogusław KOŁODZIEJ1, Agata JURKOWSKA1, Michał BANAŚ2 & Daria

IVANOVA3

1Institute of Geological Sciences, Jagiellonian University, Oleandry 2a, 30-063 Kraków, Poland [email protected]; [email protected] 2Institute of Geological Sciences, Polish Academy of Sciences, Senacka 3, 31-002 Kraków. Poland [email protected] 3Geological Institute, Bulgarian Academy of Sciences, Acad. G. Bonchev, 24, 1113 Sofia, Bulgaria [email protected] Keywords: Cathodoluminescence microscopy, foraminifera, glauconitic marls, Oxfordian, Cracow, Poland.

Cathodoluminescence (CL-microscopy) is a significant tool in geosciences. It is often used in petrology and sedimentology, however yet it is still not widely used by palaeontologists. This method can be applied in studies on biomineralization, environmental analyses of recent and fossil organisms and their diagenesis. CL is also useful in taxonomy, because it can reveal outlines and internal structures of fossils that are poorly-visible or invisible in transmitted light microscopy (e.g. Barbin, 2000). The luminescence intensity of carbonates is determined mainly by incorporation of Mn2+ (main activator element) and Fe2+ (quencher element).

Interesting results have been acquired during CL-studies of polished, uncovered thin sections of Oxfordian carbonate rocks from the Kraków (Cracow) Upland (southern Poland) representing deposits of an epicratonic basin located on the northern Tethyan shelf. Equipment employed in CL analyses was Carl Zeiss Jena JENAPOL microscope with Cambridge Image Technology (CITL) cold cathode instrument.

Particularly, cathodoluminescence observations of the Middle Oxfordian glauconitic marls (Podłęże, Młynka near Kraków) revealed foraminifera, which in transmitted light are invisible or preserved as “ghosts” structures (Fig. 1A). The abundant planktonic foraminifer Globuligerina oxfordiana (Grigyalis, 1958) exhibits bright red-orange luminescence (Fig. 1B). Other foraminifera: Nodosaria sp., Lenticulna sp. show similar luminescence. In other studied facies (grey marls, peloidal wackestones, sponge microbial-boundstones) foraminifera show weaker luminescence or do not show CL emission.

Although CL-microscopy was succesfuly applied to recent and fossil carbonate organisms, the literature review indicates that this method is still not widely used in micropalaeontological studies. Spectacular results have been received by Martini et al. (1987) in analysis of foraminifera from recrystallized Triassic limestones of SW Sardinia (Italy). CL observations revealed abundant monospecific assemblages of Agathammina? sp., which under transmitted light were preserved as “ghosts” only.

Both these cases studies indicate the great potential of cathodoluminescence in studies of foraminifera orginating from sediments of different depositional and diagenetic history.






B. Kolodziej et al. - Cathodoluminescence as a tool in foraminiferal studies: a case study from Oxfordian, southern Poland

Fig. 1. A. Glauconitic marls under normal light. Outlines of foraminfera are poorly visible. B. Tests of Globuligerina oxfordiana under cathodoluminescence light. In the original CL view, foraminifera are bright red-orange.

REFERENCES Barbin, V., 2000. Cathodoluminescence of carbonate shells: biochemical vs diagenetic process. In:

Pagel, M., Barbin, V., Blanc, P., Ohnenstetter, D. (Eds.), Cathodoluminescence in geosciences. Springer, Berlin Heidelberg New York Tokyo, pp. 303–329.

Martini, R., Amieux, P., Gandin, A., Zaninetti, L., 1987. Triassic foraminifers from Punta Tonnara (SW Sardinia) observed in cathodoluminescence. Rev. Paléobiol., 6: 3–27.

67

New turtle remains (Kallokibotionidae, Dortokidae) from the Upper Cretaceous of Transylvania (Romania)

France de LAPPARENT DE BROIN1, Vlad A. CODREA2, Thierry SMITH3

& Pascal GODEFROIT3

1 UMR 7207 du CNRS - USM 203, Département Histoire de la Terre, Muséum national d’Histoire naturelle, Paléobiodiversité, CP 38, 8, rue Buffon, 75231 Paris cedex 05, France, [email protected] 2 Catedra de Geologie–Paleontologie, Universitatea Babeş-Bolyai, Str. Kogălniceanu 1, 3400 Cluj-Napoca, Romania, [email protected] 3

Département de Paléontologie, Institut royal des Sciences naturelles de Belgique, rue Vautier 29, B- 1000 Bruxelles, Belgium.

Keywords. Chelonii - Kallokibotion - Dortokidae - Transylvania - Maastrichtian

Transylvania (Romania) has yielded a large number of Late Cretaceous

(Maastrichtian) fossils, including chelonians. Localities which provided turtles are distributed in river basins, southern tributaries of the Mureş River.

The first known area is Haţeg basin: localities are principally situated close to the margins of the affluents of Strei River. The only named form, up to now, is Kallokibotion bajazidi Nopcsa, 1923, originating from Sânpetru Valley, type locality of the Sânpetru Formation of Haţeg area: it is a primitive cryptodire, endemic of Transylvania during the Late Cretaceous. Further specimens from various Transylvanian localities have been attributed to this taxon after the type material, but without figuration and description, so that their determination needed confirmation. Other remains, previously presented as Pleurosternon sp., Pleurodira indet., cf. Polysternon, and Dortokidae?, have been mentioned in some localities, also without definition and figuration. We have examined some elements of all this material and not yet seen fragments attributable to Pleurosternon and Polysternon. In return, some of the specimens from Sânpetru Valley are enough well-preserved to be confirmed in their attribution to Kallokibotion. A part of the newly-collected specimens also belongs to Kallokibotion. It provides a new knowledge on some anatomical parts of this turtle, which were previously misunderstood. The best material comes from Toteşti baraj and Nălaţ-Vad areas, in the Râul Mare River basin. Both localities have been excavated, firstly in the scope of the Belgian-Romanian excavation campaigns in Transylvania, carried out by the Royal Belgian Institute of Natural Sciences and the University Babeş-Bolyai, from 2000 to 2005. Young specimens from Sânpetru Valley (Fig. 1) and from Nălaţ-Vad (Fig. 2) are particularly interesting because the sutures are visible. The shape of the nuchal and anterior peripherals is well visible at Nălaţ-Vad (Fig. 1): in previous works, this part was erroneously interpreted, based on the synostosis in the adults of the published type material. At Toteşti, a specimen is preserved with the partial head (Fig. 3), the plastron and some postcranial: anterior limb bones and girdle and amphicoelous vertebrae (Fig. 5), confirming the type material.

The second examined area is located between Alba-Iulia-Sebeş-Vinţu, in the Alba County (Metaliferi area), outside and north-eastwards from Haţeg basin, along Mureş River and some of its tributaries. Among the collected turtle fragments, Kallokibotion bajazidi has been clearly recognized previously from Râpa Roşie, and figured; its presence is also possible at Oarda de Jos.


F. de Lapparent de Broin et al. - New turtle remains (Kallokibotionidae, Dortokidae) from the Upper Cretaceous of Transylvania

A new taxon of the pleurodire Dortokidae was also recovered from the same Oarda de Jos locality (Alba County) (Fig. 6); it is represented by a few isolated elements and it might represent in part the “Dortokidae?” previously mentioned from some Transylvanian Cretaceous localities. A preliminary examination shows that it could be the most primitive member of the family, more closely related to the Palaeocene Ronella botanica from Jibou, Romania, than with the Cretaceous Dortoka line from the south of France-Iberian Peninsula. Its discovery fills a gap in the story of the group in these two countries. However, as the latter is present as soon as the Late Barremian in Spain, the origin of the family being an old one - toward the Jurassic–Cretaceous boundary, many steps are still lacking.

The turtle fauna of this part of Transylvania during the Late Cretaceous is confirmed as endemic, in spite of the presence of Dortokidae, shared only with the western Mediterranean area. Kallokibotionidae remain exclusively Romanian, with the single taxon Kallokibotion bajazidi.

Fig. 1. Kallokibotion bajazidi Nopcsa, 1923. 1, Sânpetru valley, juvenile, dorsal carapace, dorsal view. 2, Nălat-Vad, juvenile, anterior dorsal carapace, dorsal view. 3, Totesti, MTB ToK-1, skull with lower jaw, left lateral and dorsal views. 4, Totesti, MTB ToK-1, plastron, dorsal view; 5, Totesti, MTB ToK-1, cervical vertebra, lateral view. Dortokidae indet., 6, Oarda de Jos, right pleurals 1 and 2, dorsal view.

69

Data on Deinotherium Kaup in the Republic of Moldova

Alexandru LUNGU1 & Theodor OBADĂ2

1 Tiraspol State Pedagogical University, Iablockin 5 str., MD-2096, Chişinau, Republic of Moldova 2 Institute of Zoology of the Academy of Sciences of Moldova, Academiei 1 str., Chişinau, MD-2028, Republic of Moldova; e-mail: [email protected]

Keywords: Systematics, Deinotherium, Republic of Moldova

The palaeontological data of the latest decades have enabled to more precisely define the age of some Miocene sites from the Republic of Moldova where remains of the Deinotherium genus were found.

The remains of the largest-sized genus representative – D. gigantissimum Ştefănescu, 1892 (found in Codreanca, Pripicenii-Răzeşi and Peresecina localities) – are originating from Kersonian deposits (MN 10 unit), and not from Pontian (MN 14) ones, as it was reported earlier (David, Shushpanov, 1967, 1972; Tarabukin, 1968, 1969, 1974).

The large size of the individuals from these localities is similar to the one of those collected in Mânzaţi, Romania (Ştefănescu, 1910).

It is important to mention that remains of Chilotherium, a characteristic representative of Khersonian in Eastern Europe, were also found in all the above-mentioned sites.

The validity of D. gigantissimum Ştefănescu, 1892 requires confirmation. REFERENCES David A.I. & Shushpanov K.I., 1967. Novaya nahodka ostatkov dinoteriya v Moldavii. Materialy V

konferentsii molodyh ucenyh Moldavii. Kishinev, : 63-64. David A.I. & Shushpanov K.I., 1972. Ostatki mlekopitayushchih iz neogenovyh otlozheniy Moldavii.

Pozvonochnye neogena i pleistotsena Moldavii. Kishinev, „Shtiintsa” : 3-18. Ştefănescu Gr., 1910. Dinotherium gigantissimum. Anuarul Museului de Geologiă şi de Paleontologiă,

IV: 1-43. Tarabukin B.A., 1968. O raskopkah skeletal dinoteriya v Rezinskom raione Moldavskoi SSR, Izvestiya

AN Moldavsjkoi SSR, ser. biol. i him. Nauk, 3 : 37-42. Tarabukin B.A., 1969. Rod Deinotherium v SSSR. Trudy Gosudarstvennogo istoriko-kraevedcheskogo

muzeya MSSR, vyp. 2, Kishinev, „Kartea Moldoveneaske”:135-146. Tarabukin B.A., 1974. Novye dannye po sistematike, filogenii i ecologii podotryada Deinotherioidea

Osborn (1921). Mlekopitayushchie pozdnego kainozoya yugo-zapada SSSR, Kishinev, „Shtiintsa” : 77-90.



The residual colour patterns of the European Cenozoic molluscs: a new taxonomic tool

Didier MERLE1, Bruno CAZE1, Jean-Paul SAINT MARTIN1 & Jean-Michel

PACAUD1

1 Muséum National d’Histoire Naturelle, Département Histoire de la Terre, Centre de Recherches sur la Paléobiodiversité et les Paléoenvironnements (CR2P) UMR 7207 du CNRS, 8, rue Buffon, CP 38 – [email protected], [email protected], [email protected], [email protected] Keywords: residual colour patterns, molluscs, Cenozoic, Europe.

One of the features constituting the beauty of mollusc shells is that they arbour various colour patterns. From scientific point of view, these patterns often represent useful characters in order to identify species. Indeed, the use of shell characters only may not be sufficient, particularly when shells display little ornamentation as it is the case of naticids, conids or venerids. Records of preserved colour patterns in fossils remain exceptional and are regarded rather as anecdotic data than scientific observation of heuristic value. Therefore, fossil colour patterns are rarely regarded as a taxonomic tool by paleontologists. When fossil shells are not decalcified or recrystallized, they are not significantly transformed by diagenesis. Their colour patterns are lacking or poorly visible, but they can be revealed following exposition under UV light. A preliminary bath in sodium hypochlorite greatly increases the success of observations during the exposition under UV light. Investigations made by our team at the Muséum have shown first that, in using this approach, the residual colour patterns have been outlined for all Cenozoic stages, except the Danian (Early Paleocene). Furthermore, colour patterns can be revealed for fossiliferous remains from any ecosystem type (continental, lagoonal or marine). The second result concerns the distribution of residual patterns among molluscs. They have been found in many families of gastropods or bivalves, including recent ones. The third result concerns studies at specific level. The fact that numerous specimens reveal their colour pattern under UV light allows accessing the intraspecific variability, which represents a fundamental aspect of research at specific level. In conclusion, the major condition for an observation to be used for scientific investigations is its reproducibility. This condition is fulfilled in the case of the residual colour patterns.

Fig. 1 - The Veneridae Costacallista laevigata (Lamarck, 1806) in natural light left view) and under UV light (right view). Specimen from Grignon (Lutetian, Paris basin, France)






Microfacies and microfossils of the Upper Jurassic–Lower Cretaceous limestones from Vâlcan Mountains: an overview

Mihai MICHETIUC1 & Ioan I. BUCUR1

1Babeş-Bolyai University, Department of Geology, 1, M. Kogălniceanu Str., 400084 Cluj-Napoca. E-mails: [email protected]; [email protected]

Keywords: Carbonates, microfacies, foraminifera, dasycladalean algae, Vâlcan Mountains.

Vâlcan Mountains are located between Jiu Valley (to the east), Petroşani Basin (to the north), Motru Valley (to the west) and Getic Depression (to the south). Except for some thin strips belonging to the Getic Nappe, this area is dominated by crystalline and volcanic rocks of the Lower Danubian Napes (Berza et al., 1983), and by its Mesozoic cover. The Upper Jurassic–Lower Cretaceous deposits crop out on the southern border of Vâlcan Mountains and belong to the alpine cover of the Lainici Nappe (Berza in Balintoni et al., 1989). Drǎgǎnescu (in Berza et al., 1989) assigned the entire limestone succession from the Lainici Nappe to the Oslea-Polovragi Limestone Formation.

The studied limestones from the southern part of Vâlcan Mountains present six dominant facies (or facies association) types: 1) non-fossiliferous, fenestral, laminated mudstone; 2) fenestral wackestone/packstone-grainstone; 3) wackestone with algae and foraminifers; 4) peloidal bioclastic packstone/grainstone; 5) wackestone/packstone with cyanobacteria and bindstone (microbial crusts), and 6) bioclastic packstone/grainstone (bioclastic shoals). The five facies types are characteristic for carbonate platforms, respectively for environments ranging from shallow-subtidal, to inter- and supratidal

The flora and fauna are represented by gastropods, bivalve and brachiopod fragments, echinoderm plates, foraminifera, and dasycladalean algae. Besides, we have identified Rivularia-type cyanobacteria and microploblematic organisms such as Bacinella and Lithocodium.

Based on the micropaleontological results, the studied deposits were assigned to the Upper Jurassic and to the Berriasian-Valanginian (?Hauterivian) on the one side, and to the Barremian-Aptian (Urgonian facies) on the other. The Upper Jurassic age is justified by the presence of typical foraminifera [Protopeneroplis striata WEYSCHENK, Alveosepta jaccardi (SCHRODT), Kurnubia palastiniensis HENSON, and Kilianina sp.], and dasycladalean algae [Clypeina sulcata (ALTH) and Salpingoporlla annulata CAROZZI].

In the Berriasian-Valangian-?Hauterivian deposits, a micropaleontological association consisting of foraminifers [Haplophragmoides joukowskyi (CHAROLLAIS, BROENNIMANN & ZANINETTI), Bramkampella arabica REDMOND, Andrersenolina cherchiae ARNAUD-VANNEAU & BOISSEAU, Mohlerina basiliensis (Mohler), Nautiloculina broennimanni ARNAUD-VANNEAU & PEYBERNES, Vercorsella camposaurii (SARTONI & CRESCENTI), Mayncina sp., Montsalevia sp.] and calcareous algae [Clypeina parasolkani FARINACCI & RADOIČIĆ, Clypeina sp., Salpingoporella circassa (FARINACCI & RADOIČIĆ), Salpingoporella annulata CAROZZI, and ?Macroporella praturloni DRAGASTAN] has been identified.

The Barremian-Aptian association consists of the following foraminifers: Paracoskinolina? jourdanensis (FOURY & MOULLADE), Montseciella arabica


M. Michetiuc & I.I. Bucur - Microfacies and microfossils of the Upper Jurassic–Lower Cretaceous limestones

73

(HENSON), Orbitolinopsis sp.?, Palorbitolina sp., Palaeodyctioconus actinostoma ARNAUD-VANNEAU & SCHROEDER, Pseudolituonella gavonensis (FOURY), Debarina hahounerensis (FOURCADE, ROUL, VILA), Neotrocholina fribourgensis GUILLAUME & REICHEL, Sabaudia minuta (HOFKER), Pseudocyclammina lituus YOKOYAMA, Everticyclamina sp., Vercorsella sp., Nautiloculina sp., Charentia sp., Verneuillina sp.?, and Commaliama sp. The association of calcareous algae consists of: Salpingoporella melite RADOIČIĆ, Salpingoporella muehlbergii (LORENZ), Salpingoporella cf. cemi RADOIČIĆ, Salpingoporella sp., Clypeina solkani CONRAD & RADOIČIĆ, Clypeina cf. solkani (CONRAD & RADOIČIĆ), Suppiluliumaella tuberifera (SOKAĆ & NIKLER), Milanovicella sp., Clypeina sp., Pseudoactinoporella fragilis CONRAD, Similiclypeina conradi BUCUR, Salpingoporella urladanasi CONRAD & PEYBERNES, Salpingoporella heraldica SOKAC, and Salpingoporella cf. genevensis (CONRAD).

The above-mentioned micropaleontological assemblage is not only the richest one

currently identified in Vâlcan Mountains, but it also brings new arguments for dating the Upper Jurassic-Lower Cretaceous limestones in this area.

Acknowledgements: The study is a contribution to the CNCSIS project BD 413. REFERENCES Balintoni I., Berza T., Hann, H. P., Iancu V., Krautner H. G. & Udubasa A., 1989. Precambrian

Metamorphics in .the South Carpathians. Guide to excursion. 83 p., Inst. Geol. Geophys., Bucureşti.

Berza T., Krautner H. & Dimitrescu R., 1983. Nappe Strucutre in the Danubian Window of the Central -South Carpathians. An. Inst. Geol. Geofiz. Rom. 60/: 31-38.

Berza T., Draganescu A., Constantinescu A., Constantinescu D., Mateescu G. & Vajdea V., 1989. Studiul geologic-geofizic si prin teledetectie al masivului Vilcan in vederea evaluarii potentialului economic si orientarii activitatii de prospectiune. Raport arhiva I.G.R. Bucuresti.150 p.

Preliminary data on the microfauna from Vârciorog (Vad-Borod basin, Romania)

Angela MICLEA1 & Sorin FILIPESCU1

1Babeş-Bolyai University, Department of Geology. Kogălniceanu 1, 400084, Cluj-Napoca, Romania ([email protected], [email protected]) Keywords: foraminifera, Sarmatian, Vad-Borod Basin

A section in Sarmatian deposits has been investigated in Vad-Borod basin, on the

north-western border of Pădurea Craiului Mountains. The Sarmatian deposits occur transgressively over the unconformity from the top

of the Cretaceous. The succession starts with gravel lags followed by an alternation of mudstones and grainstones about 70 m thick. The fine sediments preserve a rich and quite diverse assemblage of macro- and microfossils.

Nicorici & Istocescu (1970) and Nicorici (1971) made the first estimations on the early Sarmatian age based on mollusk assemblages. Our goal was to get a better stratigraphic resolution and to have an image on the environmental distribution of the fossil foraminifera.

Foraminifera assemblages are dominated by species of Elphidium, Ammonia and miliolids, proving a shallow-water marine environment, typical for the margins of the rising mountains. The ostracod and gastropod assemblages were only used as support for our conclusions at this stage.

Based on the foraminifera, a more precise age could be assigned to the studied deposits, due to the separation of the Elphidium reginum Biozone of the late early Sarmatian.

In order to get a detailed image on the area, other interesting sections are still under study. REFERENCES Nicorici, E., 1971. Fauna sarmaţiană de la Vârciorog (Bazinul Vadului). Studii şi Cercetari – Geologie,

Geofizică, Geografie (Geologie), 16, 1: 215-232. Nicorici, E. & Istocescu, D., 1970. Cercetări biostratigrafice asupra Sarmaţianului de la Vârciorog

(Bazinul Vadului). Studia Universitatis “Babeş-Bolyai”, Geologie-Mineralogie, 2: 47-55.


De la Terre à la Mer, l’histoire évolutive des Cétacés From Earth to Sea, the evolutionary history of Cetaceans

Christian de MUIZON1

1Muséum National d’Histoire Naturelle, Département Histoire de la Terre, Centre de Recherches sur la Paléobiodiversité et les Paléoenvironnements (CR2P) UMR 7207 du CNRS, 8, rue Buffon, CP 38. [email protected] Mots-clés : Cétacés, origine, histoire évolutive, adaptation, nage Keywords: Cetaceans, origin, evolutionary history, adaptations, swimming

Les cétacés sont les plus modifiés des mammifères. Ils ont leur origine parmi des artiodactyles terrestres au début de l'Éocène. Le premier cétacé connu est Pakicetus une forme terrestre et coureuse de l'Éocène inférieur (50 Ma) qui pouvait sans doute entrer dans l'eau des rivières pour compléter son alimentation ou se protéger du soleil. Quelques millions d'années plus tard Ambulocetus est une forme amphibie capable de marcher sur la terre ferme mais nageant sans doute agilement à l'aide de ses membres postérieurs. Ambulocetus était un redoutable prédateur armé de puissantes dents. Les narines de Pakicetus et d'Ambulocetus étaient situées à l'apex du crâne. À l'Éocène supérieur apparaissent les premiers Cétacés totalement inféodés au milieu aquatique, les Basilosauridés. Leurs membres postérieurs sont totalement atrophiés et ne sont plus fonctionnels. Les narines se situent sur la face dorsale du rostre dans le tiers antérieur du crâne. Dès lors la voie vers les cétacés modernes est ouverte; les premiers mysticètes apparaissent à l'Éocène terminal et les premiers odontocètes à la fin de l'Oligocène inférieur.

Cetaceans are the most highly modified mammals. They originate among

terrestrial atrtiodactyles during the early Eocene. The oldest known cetacean is Pakicetus, a terrestrial and cursorial taxon of the early Eocene (50 Ma), which entered the water in search for food or, possibly, to protect its skin from the sun. A few million years later, Ambulocetus is an amphibious cetacean capable to move on land but also an agile swimmer using its hind limbs for propulsion. Ambulocetus was a formidable predator with powerful teeth. The nares of Pakicetus and Ambulocetus were anteriorly placed, at the apex of the snout. During the late Eocene, appear the first strictly aquatic cetaceans, the Basilosauridae. Their hind limbs are totally atrophied and are not functional. The nares are on the dorsal face of the rostrum on anterior third of the skull. From that time the way toward modern cetaceans is opened; the oldest mysticetes are from the latest Eocene and the oldest odontocetes from the early Oligocene.


Turonian marker Foraminifera associations from the southern part of the Eastern Carpathians: Valea Dambovitei - Intorsura Buzaului

area

Theodor NEAGU1 & Mihai DUMBRAVĂ2

1 University of Bucharest, Faculty of Geology and Geophysics, Department of Paleontology, Bd. Nicolae balcescu nr.1, 010041 Bucharest, Romania. E-mail: [email protected] 2 Petrom S.A, I.C.P.T. Campina, Department of Geology. E-mail: [email protected] Keywords : Biozone, Turonian, Dumbravioara formation, Flysch, Gura Beliei formation, Lithology

In the southern region of the Eastern Carpathians, between Valea Mare – Intorsura Buzaului to the north, and Valea Dambovitei to the west, the Turonian deposits which lie over the Dumbravioara formation (Vraconian – Cenomanian) comprise two completely different lithofacies types. In the area between Valea Dambovitei and Valea Prahovei, a complex of marls very similar to the Gura Beliei Formation is well developed.

In the region between Valea Teleajenului - Telejenel - Intorsura Buzaului - Valea Mare areas, the Turonian is represented by a stratified marly-sandy type facies, typically flysch like, black or blackish grey and rich in mica. In the upper part lies a pack of tawny bluish – red to black marls with one or two interlaced beds of white tuffs.

From both lithological and micropaleontological standpoints, the Dumbravioara Formation in the above mentioned region, belongs to the Vraconian - Cenomanian and begins with the Planomalina buxtorfi biozone, followed by the Rotalipora apenninica (terminal Vraconian), Thalmanninela brotzeni (lower Cenomanian), Thalmanninela reicheli (middle Cenomanian) and Rotalipora cushmani (upper Cenomanian) biozones. Beginning with the Cenomanian – Turonian, a profound differentiation occurs, both lithological and faunal. In the Valea Dambovitei – Valea Prahovei area, red and green marls, extremely rich in planktonic foraminifera are found, and the following biozones can be separated: Whiteinella arheocretacea biozone, Helvetoglobotruncana helvetica biozone, Marginotruncana sigali biozone and the Dicarinella primitiva biozone of the lower Coniacian. Clearly, the Dicarinella asymetrica biozone of the Santonian is missing, as is the Globotruncanella elevata biozone. The Gura Beliei formation begins with the Globotruncana ventricosa biozone.

In the Valea Teleajenului – Intorsura Buzaului area, the aforementioned Turonian series is totally devoid of planktonic foraminifera. In the tawny red interlacings a very rich fauna comprised of primitive agglutinated foraminifera with silicaceous cement and small size is well developed. This type of association was noted from the Turonian deposits of the DSDP drillings from the Atlantic Ocean and was thought at the time to be comprised of benthic foraminifera from below the CCD limit. The characteristic element of these associations is given by Uvigerinammina jankoi, Thalmannammina meandertornata, Recurvoides recurvoidiformis, Haplophragmoides herbichi, Gerochammina obesa, and Bulbobaculites problematicus. With the exception of Uvigerinammina and Thalmannammina, all the other genera in these associations are found alongside the aforementioned planktonic foraminifera but only in the finest samples.




T. Neagu & M. Dumbrava - Turonian marker Foraminifera associations from the southern part of the Eastern Carpathians

77

Beginning with the Campanian, a facies nearly identical with the Gura Beliei formation begins to be deposited once more. Biostratigraphically, these deposits comprise the biozones of the upper Campanian and Maastrichtian (Globotruncana ventricosa, Globotruncana calcarata, Globotruncanella havanensis, and Abathomphalus mayaroensis).

Fossil squirrels (Rodentia, Mammalia) from the late Miocene of

Republic of Moldova

Igor NICOARA1, Alexandru LUNGU2 & Andrian DELINSCHI3

Institute of Geology and Seismology of ASM, 3 Academiei str., Chisinau, MD 2009, Republic of Moldova, [email protected] Tiraspol State University (Chisinau), 5 Gh. Iablocichin str., Chisinau, MD 2009, Republic of Moldova National Museum of Ethnography and Natural History of Moldova, 82 Kogalniceanu str., Chisinau, MD 2009, [email protected] Keywords: Sciuroidea, Late Miocene, Vallesian, Turolian.

Ground and flying squirrels were recovered from Upper Miocene (MN 9-MN 13) Hipparion localities in Republic of Moldova. The study of the superfamily Sciuroidea allows to find answers to a series of systematic and phylogenetic questions, as well as to reconstruct the Upper Miocene geography and environments. These Miocene Sciuroidea are related to the families Scuiridae (genera Spermophilinus and Tamias) and Petauristidae (genera Miopetaurista, Pliopetaurista, Hylopetes and Blackia).




Dămuc series of Hăghimaş syncline from East Carpathians, Romania. New petrographical and palynostratigraphical data

Leonard OLARU1, Constantin GRASU1 & Marinela CHIHAIA1

1 Department of Geology, University “Al.I. Cuza” – Iaşi, 20A, Carol I Blvd., 700505, Iaşi, Romania, email: [email protected]. Keywords: Petrography, palynostratigraphy, Hăghimaş, East Carpathians, Romania

Dămuc Series, described by Mureşan et al. (1974) from the southern extremity of Dămuc „Ridge”, represents a monotonous succession of crystalline schists which include sericitous-muscovitic, weakly graphitous schists with biotite and garnets, representing the core of an anticline with a western overthrust, covered on both flanks by Triassic dolomites overlaying the Formation with Aptychus. The petrographic characteristics of these crystalline schists differentiate them from both the uncomformably overlaying mezometamorphites from Bretila-Rarău Group and from the epimetamorphites of Tulgheş Group, on the top of which they are together overthrusted.

Our investigations concerned the study of the geological sections which crop out along Arşiţa Almaşului Brook (Mâţului Brook), left tributary of Dămuc Valley. Here, the crystalline schists are characterized by advanced schistosity and black colour with metallic lustre. The quartz enrichment determines, at different levels, the separation of 1-m thick sequences with quartzitic character with higher hardness, which contrast with the plastic-schistous content of the rest of the lithological series.

The common presence a quartz-rich component with marked schistosity, conferring the rocks a granoblastic structure, was confirmed by optical microscopy. Schistosity is marked by the spatial arrangement of muscovite, biotite, sericite and chlorite, as well as that of the graphitous material. In the case of the granoblastic structure, the respective minerals do not show any preferred orientation.

The first palynological and palynostratigraphical observations on these deposits belong to Iliescu and Mureşan (1972); they assigned these rocks to Dămuc Series (Ordovician) and they concluded about a schematic palynological assemblage correlated with similar ones from the Russian Platform.

Our investigations were based on the study of 12 samples, yielded from all the petrographic types from Arşiţa Almaşului Valley (Mâţului Brook), where we separated two distinct palynological assemblages: an acritarch one (62 taxa), and a chitinozoan one (24 taxa).

Of the total palynomorphs identified, the acritarch assemblage includes 32.62 % typical for the Tremadocian-Arenigian (Lower Ordovician) period. In some cases, the acritarch category represents a larger stratigraphical extent, from the Middle Cambrian to the Upper Cambrian-Tremadocian, in some cases the upper limit being restricted to the Upper Cambrian only. These features point to the slow evolution of such planktonic microorganisms during a longer stratigraphical period as well as to the adaptation capacity and co-existence of some older and newer organisms, under various environmental conditions.

The second assemblage, of chitinozoans - including benthonic microorganisms, developed during a more compressed period, being dependent of the quality and the structure of the seafloor, of the thickness of the water layer, the quality of nutrients, the dynamics of marine streams etc. These microorganisms represent typical biozones


L. Olaru et al. - Dămuc series of Hăghimaş syncline from East Carpathians. New petrographical and palynostratigraphical data

80

that can be correlated with graptolites, trilobites and conodonts biozones. This allows us to combine the interpretation based on the acritarchs biozones with that using the chitinozoan ones, as well as with other faunistic biozones. The chitinozoan assemblage is characteristic for the Lower Arenigian-Upper Arenigian stratigraphical period, where 87.49 % from the determined taxa are specific for Lower Arenigian-Upper Arenigian stratigraphical period.

Based on these results, we defined the age of the deposits from Dămuc Series as Tremadocian-Arenigian (Lower Ordovician). Therefore, the initial depositional stage of the rocks that currently consist the crystalline component of the Dămuc Series was pre-Tremadocian-Upper Arenigian (Lower Ordovician) in age, according to the arguments brought by the study of the synsedimentary assemblages of acritarchs and chitinozoans included.

Subsequently, all these rocks were successively metamorphosed during the phases of Caledonian Orogenesis, starting with the Sardic, and continuing with the Taconic and probably Ardenian ones. The radiometric ages of 415 and 420 M.y., established by Mureşan et al. (1974), on samples yielded from Arşiţa Almaşului Valley (Mâţului Brook) are equivalent to the last phase of Caledonian Orogenesis (Ardenian phase) at the limit between the Upper Ordovician and the Silurian. However, Silurian deposits are missing on Arşiţa Almaşului Brook (Mâţului Brook), probably as a result of erosion. REFERENCES Achab, A., 1991. Biogeography of Ordovician chitinozoa - In: Barnes, C.R. & Williams, S.H. (Eds.)

Advances in Ordovician Geology, Papers Geological Survey, Canada, 90-9: 135-142. Iliescu, V., Mureşan, M., 1972. Asupra prezenţei Cambrianului inferior în Carpaţii Orientali. Seria

epimetamorfică de Tulgheş. D.S. Inst. Geol., Geof., 58, 4: 23-38. Mureşan, M., 1976. O nouă ipoteză privind pânzele bucovinice din partea sudică a zonei cristalino-

mezozoice a Carpaţilor Orientali - D.S. ale Şedinţelor Institutului de Geologie şi Geofizică, LXII, 5: 77-94.

Mureşan, M., 2000. Age des épimétamorphites du Grupe de Tulgheş (Carpates Orientales) - Romanian Journal of Mineral Deposits, 79, Suppl.: 66-68.

Mureşan, M., Ioncică, M., Tănăsescu, A., 1974. Asupra prezenţei metamorfitelor caledoniene în zona cristalino-mezozoică a Carpaţilor Orientali (Seria de Dămuc) - D.S. ale Şedinţelor Institutului Geologic, 5, LX, 47-54.

Olaru, L., 2005. Some problems of biostratigraphy and palynological correlation of Upper Formation (Tg. 4) from Tulgheş Group, East Carpathians (Romania), Acta Palaeontologica Romaniae, V : 351-366.

Paris, F., Mergl, M., 1984. Arenigian chitinozoans from Klabava Formation Bohemia - Review Paleobotany and Palynology, 43: 33-35.

Paleofloristic diversity of the Sarmatian deposits (Middle Miocene) from Oltenia province, southern Romania

Valentin PARASCHIV 1

1 Geological Institute of Romania, National Museum of Geology, Kiseleff Pavel Dimitrievici G-ral. Ave., No.2, Sct.1, P.O. Box 011345, Bucharest, Romania. E-mail: [email protected] Keywords: Paleoflora, Miocene (Sarmatian), Oltenia, Romania

The Sarmatian time interval is very rich in fossil plant records. The most representative Sarmatian sites with macroplant remains (primarily leaves) from the Dacian Basin (southern Romania) have been investigated. These fossiliferous sites are represented by the Morilor Valley flora, the Ciocadia flora, the Slǎtioara flora, the Rǎmeşti Valley flora, and the Sǎcelu flora. The floral assemblages are allochthonous s.l. and demonstrate a wide range of preservation states. They occur in several different facies types: braided-flood plain, shallow biogenic lacustrine, shallow volcanigenic lacustrine, shallow marine, all reflecting an ocean-marginal lowland environment (Central Paratethys) bordering the Southern Carpathians. The composition of the Sarmatian paleofloras indicates a strong floristic variability and mixtures of plants from habitats so widely different that an explanation is difficult to find. Brown algae like Cystoseirites partschi, Cystoseirites flagelliformis, Bifurcaria palaeobifurcata, Ascophyllum palaeonodosum are often found in some of these floras. A single rhodophytae thallus of Ceramium sp. was recognized from the Morilor Valley site. As a rare presence we notice fertile and sterile stems of Equisetum in the Slǎtioara and Morilor Valley outcrops. From the Morilor Valley and Ciocadia paleofloras, fern remains that belong to Osmundaceae and Schizaeaceae (Osmunda parschlugiana and Lygodium gaudini) are documented. The unexpected presence of the relict Eostangeria cf. ruzinciniana in the Ciocadia flora marks an extension of the distribution areal of this taxon. Gymnosperms are widely represented by 14 genera with numerous species. Taxodiaceae family is well represented in the composition of Sarmatian floras by Glyptostrobus europaeus, Sequoia abietina and Taxodium dubium. Tetraclinis salicornioides (Cupressaceae) was frequently found as twigs and seeds. Pinus was abundantly identified as seeds, needles, inflorescences and cones. Magnolia, Laurus, Daphnogene and Persea are floristic elements that habitually generate the under-canopy layer of the Sarmatian forests. Matudaea menzelii, an Oligocene relict hamamelidacean, was found in the Sarmatian deposits of Morilor Valley; its presence raises numerous questions about its paleoecological demands and migration routes. In the mesophytic associations, Ulmaceae (Ulmus, Zelkova, Cedrelospermum), Fagaceae (Fagus, Castanea, Quercus) and Juglandaceae (Juglans, Carya, Pterocarya and Engelhardia) predominate. These elements fall in the subtropical Evergreen Broad-leaved Forest category of vegetation. Also, the Fabaceae family is widely represented by the genera Robinia, Podocarpium and Leguminosites (riparian and/or sclerophyllous elements). Betulaceae (Betula, Alnus, Carpinus) are often found as leaves and fruits. The Aceraceae family is represented by numerous impressions of samaras (five morphotypes) and leaves. Rare monocotyledons, as Potamogeton, Phragmites, Typha indicate scarce pond-like habitats or proximity to some swamp forests.



Geology and palaeontology of Middle Eocene localities in Namibia

Martin PICKFORD1

1 Collège de France, and Département Histoire de la Terre, UMR 7207, CR2P du CNRS, Case postale 38, 8, rue Buffon, 75005, Paris. e-mail: [email protected]

Keywords: Africa, Namibia, Palaeogene, Mammals, Biochronology, Geology

African Palaeogene mammal faunas are known principally from the northern extremities of the continent, although there are a few poorly fossiliferous sites represented in the tropical areas. In 2008, fossiliferous freshwater carbonates infilling dolines were found in Sperrgebiet, Namibia, which yielded a rich and diverse vertebrate and invertebrate fauna as well as plants. A preliminary study of the mammals reveals a high level of endemicity, but with some taxa common to North African sites, and some even to Eurasia and possibly South America. Biostratigraphic correlation indicates an age equivalent to faunas in North Africa that are generally attributed to the Lutetian, although there is a possibility that they could be as old as Ypresian (Table 1). Table 1. Fauna from Palaeogene freshwater deposits in Sperrgebiet, Namibia. (CT – Chalcedon Tafelberg, EK – Eisenkieselklippenbake, SN – Silica North, SS – Silica South, BC – Black Crow, SK – Steffenkop, GM – Gamachab).

Taxon CT SN SS BC SK EK GM Ecological indications

Ostracoda - x x - - - - Freshwater Tomichia x x x x x x - Freshwater

snail Lymnaeidae x x x x - - - Freshwater

snail Planorbidae - - x - - x - Freshwater

snail Dorcasia sp. - x x x - - x Land snail,

summer rainfall Trigonephrus sp. - x x x - - - Land snail,

winter rainfall Xerocerastus sp. - x - - - - - Land snail,

summer rainfall Succinea - x x - - - - Land snail

(humid areas) Subulinidae - - - x - - - Land snail Pisces - x x - - - - Fresh water

fish Amphibian (Pipidae) - x - - - - - Clawed toad Amphibian (Ranoidea) - x x - - - - Frog Amphibian (Anuran indet.)

- x x - - - - Frog

Squamate (lizard) - x - - - - - Lizard Squamate (amphisbaenian)

- x - - - - - Burrowing lizard

Squamate (snake) - x - - - - - Snake Crocodilia - x x x - - - Crocodile,

subtropics to tropics

Aves - - x - - - - Bird Todralestidae Namalestes - - - x - - - Small carnivore Erinaceidae - - - x - - - Insectivore

(hedgehog)



M. Pickford - Geology and palaeontology of Middle Eocene localities in Namibia

83

Macroscelididae - x - - - - - Insectivore (elephant

shrew) Proviverrinae - - - x - - - Tiny

insectivorous(?) carnivore

Hyaenodontidae Pterodon - - - x - - - Medium-sized carnivore

Pholidota (or edentate) - - - x - - - Pangolin (or sloth)

Hyracoidea Namahyrax - x x x - - - Medium sized bunodont hyrax

Arsinoitheriidae Namatherium

- - - x - - - Large lophodont mammal

Primates Namaia - x - x - - - Small bundont primate, arboreal

Zegdoumyidae Glibia - - - x - - - Bundont rodent, maybe

arboreal Myophiomyidae Silicamys - x - - - - - Bunodont

rodent, granivore

Phiomyidae Apodecter - x - - - - - Brachyodont rodent

Phiomyidae Protophiomys - x x - - - - Brachyodont rodent

Diamantomyidae Prepomonomys

- x - - - - - Hypsodont rodent

Bathyergidae cf Bathyergoides

- x - - - - - Hypsodont, burrowing

rodent

Some of the mammals present in Namibia, such as the rodents and an erinaceid, represent descendents of lineages that entered Africa from Eurasia, whereas most of the others are endemic African elements, save perhaps for a phalanx that could belong to an edentate, and if so, signalling possible connections with South America. The admixture of endemic and Eurasian faunal elements suggests that there was an intercontinental faunal exchange some time prior to the deposition of the Sperrgebiet carbonates - a conclusion that is reinforced by the presence of African mammal types in Eurasia at the same epoch. Among these is the family Arsinoitheriidae described from the Eocene of Romania - Crivadiatherium, and Turkey - Palaeoamasia, both of which represent descendants of an immigrant from Africa. The timing of this faunal interchange is poorly constrained, partly because the African fossil record for the Palaeogene is still relatively poor, but mainly because of uncertainties in determining the precise ages of the African faunas. However, the faunal interchange was likely to have occurred during the Ypresian or early Lutetian. REFERENCE Pickford, M., Senut, B., Morales, J., Mein, P., and Sanchez, I.M., 2008 - Mammalia from the Lutetian

of Namibia. Memoir of the Geological Survey of Namibia, 20 : 465-514.

Valserina primitiva, orbitolinid (Framinifera) from the Upper Hauterivian of Eastern Serbia

Svetlana POLAVDER

1 & Svetlana FIŠTER1

1Faculty of Ecology and Environmental Sciences, The Union University, Belgrade, Serbia;

[email protected]; [email protected] Keywords: Valserina, Orbitolinids, Foraminifers, Upper Hauterivian, eastern Serbia.

The first find of orbitolinid foraminifera Valserina primitiva Schroeder, Charollais & Conrad, 1969 in Upper Hauterivian sediments of eastern Serbia is presented in this work. The discovery of this species represents the first micropaleontological evidence for the Upper Hauterivian in eastern Serbia.

Introduction The Lower Cretaceous sedimentary rocks between Sokobanja and Niš belong to

the western belt of the Carpato-Balkanides, eastern Serbia. In the mentioned region, the Lower Cretaceous deposits continuously overlay Jurassic carbonates and consist of: Valanginian-Hauterivian shallow-water limestones, as well as Barremian and Aptian sediments represented by shallow-water limestones in Urgonian facies (Krstić et al., 1980 and references herein).

Within the Lower Cretaceous series, in the area between Sokobanja and Niš, Polavder (2004) has designated Biosequence E, Upper Hauterivian in age. Upper Hauterivian was attributed based on the contained species Valserina primitiva, which is an index fossil for Upper Hauterivian stratigraphy.

The results of the present study agree with the stratigraphical data of the most recent integral study by a group of authors from several European countries (Clavel, et al., 2002).

Valserina primitiva in Eastern Serbia Valserina primitiva SCHROEDER, CHAROLLAIS & CONRAD, 1969 is

described as Valserina broennimanni primitiva from the Upper Hauterivian of French Pyrenees. It was later found also in the Upper Hauterivian of Spanish Pyrenees, Lerida province (Becker, 1999; Ullastre et al., 2002).

This species is presently reported from Upper Hauterivian shallow-water limestones of eastern Serbia in Kamenica, Prekonozi and Cerje localites (Fig. 1).

In all the mentioned localities it was found in bioclastic, more or less muddy limestones of packstone-floatstone-rudstone type.

These limestones contain numerous orbitolinids and other groups of foraminifers, algae and algal fragments, bryozoans, microgastropods and other metazoans. Besides the species Valserina primitiva, the microfossil assemblage includes: Orbitolinopsis debelmasi MOULLADE & THIEULOY, O. elongatus DIENI, MASSARI & MOULLADE, Paracoskinolina? jurdanensis FOURY & MOULLADE, P. sunnilandensis (MAYNC), Paleodictyoconus cuvillieri (FOURY), Pfenderina globosa FOURY, Mayncina bulgarica LAUG, PEYBERNES & REY, Charentia cuvillieri NEUMANN, Nautiloculina cretacea PEYBERNES and other foraminifers, as well as algae: Clypeina estevezii GRANIER, Salpingoporella af. S. steinhauseri CONRAD, PRATURLON & RADOIČIĆ, Rajkella laskarevi (RADOIČIĆ) and other species.




S. Polavder & S. Fišter - Valserina primitiva, orbitolinid (Framinifera) from the Upper Hauterivian of Eastern Serbia

Fig.1. Valserina primitiva SCHROEDER, CHAROLLAIS & CONRAD, 1969; 1-Prekonozi locality, 2, 3 - Kamenica locality; 1, 2- subaxial sections; 3-transverse section; All figures: 52 x.

The stratigraphic distribution of Valserina primitiva, according to the available

references, is restricted to the Upper Hauterivian. In the shallow-water limestones from Kamenica, Prekonozi and Cerje, Valserina primitiva is a species of high incidence. REFERENCES Becker E., 1999. Orbitoliniden-Biostratigraphie der Unterkreide (Hauterive-Barrême) in den

spanischen Pirenäen (Profil Org uanyà, prov. Lèrida). Revue de Paléobiol., 18 (2):359-489, Genève.

Clavel B, Schroeder R., Charollais J., Busnardo R., Closas M., Decrouy D., Sauvagnat J. & Cherchi A., 2002. Les „Couches inférieures à orbitolines“ (Chaînes subalpines septentrionales): mythe ou réalité?. Revue de Paléobiol., 21 (2): 865-871, Genève.

Krstić B., Veselinović M., Divljan M. & Rakić M., 1980. Explanatory booklet, Sheet Aleksinac 1: 100 000. Savezni geološki zavod, Beograd.

Polavder S., 2004. Lower Cretaceous microfossil and biostratigraphy of the Gornjak-Suva Planina Zone between Sokobanja and Niš, eastern Serbia. Unpublished Doctoral thesis, Univerzitet u Beogradu, 1-83 (in Serbian).

Schroeder R., Charollais J. & Conrad, A. M., 1969. Neunter beitrag über die Foraminiferen der Unterkreide der gegend von Genf. Weitere studien an Orbitoliniden des Urgons. Arch. Sc.: 22/1, 91-104, Genève.

Ullastre J., Schroeder R. & Masriera A., 2002. Sobre la estratigrafia del singular corte de la Roca de Nerieda (parte S de la serie del Cretácico inferior de Organyà). Pirineo catalán, España.Treb.Geol.: 67-95, Barcelona.

85

Badenian small gastropods from Borod Basin (NW Romania). Pyramidellidae family

Mirela Violetta POPA1

1”Babes-Bolyai” University, Department of Geology, 1, M. Kogalniceanu St., RO-400084, Cluj-Napoca, Romania. e-mail: [email protected] Keywords: gastropods, Pyramidellidae, Badenian, Borod Basin, Romania

Boreholes drilled in the eastern area of Borod Basin (NW Romania) have intercepted Badenian deposits assigned to Borod Formation (Popa, 2000). They consist of grey and blackish, sometimes green-violet siltic marls with interbedded silts, as well as sands and coals.

The deposits of Borod Formation include gastropods, bivalves, scaphopodes, foraminifera and calcareous nannoplankton. Malacofauna is abundant and very well-preserved.

Four mollusk assemblages have been previously defined (Popa & Chira, 2000; Filipescu & Popa, 2002). Small gastropods belonging to the Pyramidellidae Family are present in two of these associations, i.e. Turritella-Anadara, and Alvania-Ringicula-Pyramidella assemblages.

In Borod Formation deposits, this family of small gastropods shows the widest specific and quantitative spectrum.

More than that, the representatives of this family are dominant in all the occurrences where small gastropods have been identified in the western basins (Şimleu, Beiuş, Făget, Caransebeş), and in the Transylvanian Basin.

In the eastern part of Borod Depression, ten species assigned to Pyramidella, Ebala, Turbonilla, Chrysallida and Odostomia genera were determined and described.

REFERENCES Filipescu S. & Popa M., 2002. Biostratigraphic and paleoecologic significance of the macro-and

microfossil assemblages in the Borod Formation (eastern Borod Depression, north-west Romania). Acta Paleontologica Romaniae, 3 (2001), p. 135-148, 2 fig., 1 tab., 6 pl., Iaşi

Popa M., 2000. Lithostratigraphy of the Miocene deposits in the eastern part of Borod Basin (NW of Romania).Studia, Univ. Babes-Bolyai, XLV, 2, p. 93-103, 5 fig., Cluj-Napoca.

Popa M. & Chira C., 2000. Miocene mollusks and calcareous nannoplankton assemblages from the Borod Formation (Borod Basin, Romania), Acta Palaeontologica Romaniae, 2 (1999), p. 397-406, 2 fig., 1 tab., 4 pl., Cluj-Napoca.

.


Plant-insect interactions in the Lower Jurassic continental formations of the South Carpathians, Romania

Mihai E. POPA1 & Andreea ZAHARIA2

1, 2University of Bucharest, Faculty of Geology and Geophysics, Laboratory of Palaeontology, 1, N. Balcescu Ave., 010041, Bucharest, Romania. e-mail: [email protected] Keywords: Plant-insect interactions, Lower Jurassic, South Carpathians, Romania

Plant-insect interactions during Early Jurassic times in the South Carpathians were rarely reported previously by Givulescu and Popa (1994) and by Popa (2000, 2009). Recently, a large amount of fossil material was gathered from Reşiţa Basin (Getic Nappe) and from Sirinia Basin (Danubian Units), bearing various types of plant-insect interactions remains. Such material occurs following compression affecting the continental, coal bearing formations of both basins; it is usually well-preserved, although in some cases cuticles cannot be macerated. Such interactions are represented by the following morphological and behavioural types:

1. leaf cuttings, produced by herbivore insects, represented by cutting traces of

all shapes and sizes, in both Pteridophyte and Gymnosperm foliage. They have been recorded from both Reşiţa and Sirinia Basins;

2. leaf mining, also produced by herbivore insects, represented by borrows produced by insects, of various diameters and shapes of tunnels, in Pteridophytes and Gymnosperms, recorded mainly from the Sirinia Basin;

3. leaf galls, produced by insects infesting the leaf mesophyll with germs, thus producing individual or grouped swellings in various Gymnosperm foliage, reported from the Reşiţa Basin, Steierdorf Formation;

4. ovipositorial remains, represented by single or grouped egg traces, produced by insects depositing their eggs for hatching on the leaf surface of Gymnosperms, reported from the Sirinia Basin.

Such interactions are described and discussed for the first time on Lower Jurassic

leaf material collected from the South Carpathians, their paleoecological and stratigraphical significance, as well as their relationships with coeval cases described outside the South Carpathians being addressed in detail. REFERENCES Givulescu R. & Popa M.E., 1994. Eine neue Dictyophyllum - Art aus dem unteren Lias von Anina

(Rumanien). Documenta Naturae, 84: 42-46. Popa M.E., 2000. Early Jurassic land flora of the Getic Nappe, University of Bucharest, PhD thesis,

Bucharest, 258 pp. Popa M.E., 2009. Late Palaeozoic and Early Mesozoic continental formations of the Resita Basin.

Editura Universitatii din Bucuresti, Bucharest, 197 pp.


Miocene globigerinas from Romania

Gheorghe POPESCU1 & Ileana-Monica CRIHAN2

1 Str. Arh. Petre Antonescu nr. 4, bl. 29, apt. 14, sector 3, 023591 Bucharest, e-mail: [email protected] 2 University Petrol-Gaze, Department Geology-Geophisics, Bd. Bucuresti nr. 39, 100680 Ploiesti, e-mail: [email protected] Keywords: globigerinas, Romania, Miocene

The paper is an attempt to outline an inventory of planktonic foraminifera from the Miocene deposits from Romania. The studied geological sections are situated in the strongly-deformed deposits of the Subcarpathians, the Getic Depression, Transylvania and connected basins, e.g. Haţeg Basin, and the Neogene basins from the eastern border of the Pannonian Depression, e.g. Caransebeş, Bega, and Zarand Basins.

More than 40 species belonging to 13 genera of planktonic foraminifera were described, of which one new genus and species (Globospinina banatica).

The descriptions are accompanied by remarks on the stratigraphic range, many times different from their range in open seas.


Microbial structures in Triassic carbonate deposits from the Eastern Carpathians (northern compartment of the Crystalline

Mesozoic Area)

Daniela Alexandra POPESCU1 & Liviu Gheorghe POPESCU1

1 University „Ştefan cel Mare” Suceava, Department of Geography, University Street, Nr. 13, 720 229, Suceava, [email protected] Keywords: microbialites, microencrusters, carbonates, Triassic, Eastern Carpathians.

The Triassic sedimentary deposits from the northern compartment of the Crystalline Mesozoic Area of the Eastern Carpathians are developed in two main lithofacies types: terrigenous (Induan) and carbonatic (Olenekian-Rhaetian).

These Triassic lithofacies types of the Central East Carpathian Nappe System (the Median Dacides) are represented by the Infrabucovinian Nappes, the Subbucovinian Nappe, the Bucovinian Nappe and the Transilvanian Nappes.

The carbonate facies that consists of limestones and dolomites has a wide spreading in the Bucovinian and Transylvanian sedimentation domains.

Microbial activity developed in the Triassic carbonate deposits has generated several types of microbialitic structures: microbial peloids, micritic crusts, laminate and undulated micritic structures, Tubiphytes- and Baccanella-type structures, Cayeuxia-type structures, microbial oncoids and agglutinated microbialites. The latter three types are less abundant.

Microbialites are built through the combined effect of biota (bacteria, algae, calcimicrobes), sedimentation and diagenetic processes.

The microencrusters association includes „Tubiphytes”, Baccanella floriformis, Ladinella porata, and Cayeuxia.

The intense microorganisms’ activity resulted in the formation of microbial and peloidal micrites in shallow marine environments, characterised by low energy in subtidal protected facies.


Middle Triassic cyamodontoid reptiles from Romania

Erika POSMOŞANU1

1 Muzeul Ţării Crişurilor, B-ul Dacia nr. 1-3, 410464 Oradea; e-mail: [email protected]

Keywords: Reptiles, Middle Triassic, Romania The Middle Triassic sites Lugaşu de Sus and Peştiş near Aleşd, north-western

Romania, have produced hundreds of marine vertebrate bones over the last 40 years. Jurcsak described a new species of Tanystropheus, Tanystropheus biharicus JURCSAK 1975, based on a cervical vertebra from Lugaşu de Sus and a new species of Nothosaurid, namely Nothosaurus transsylvanicus JURCSAK 1976, based on a skull fragment from Peştiş, formerly mentioned as Nothosaurus cf. procerus (Jurcsak, 1973).

Among Placodontia, Jurcsak (1976, 1977, 1978) identified specimens as belonging to non-armored placodonts (Placodontoidea), namely the genera Placodus and Paraplacodus, as well as armored placodonts (Cyamodontoidea), mentioning the genera Psephoderma, Placochelys and Psephosaurus. Jurcsak (1976) described a right lower jaw fragment from Peştiş (MTCO 7339), as belonging to genus Placodus, referring it in the figure caption as “Placodus gracilis” n.sp. Later, Jurcsak (1978) considered Placodus gracilis as a form close to Paraplacodus broilii PEYER. Rieppel (1995) discussed the figured lower jaw of Placodus gracilis and considered that the specimen does not represent Placodus, moreover not even a placodont; therefore Placodus gracilis became a nomen dubium, pending a revision of the original material. Jurcsak has referred a maxillary fragment from Lugaşu de Sus (in Huza et. al, 1987), to “Placodus gracilis” or to a form close to Paraplacodus broilii Meyer and figured it as “Placodus gracilis”. Re-examination of the cast of the maxillary (Posmoşanu, 2008) has revealed that this specimen was not Placodus or any other non-armored placodont, which was thus assigned to the armored placodonts, Cyamodontoidea. Further study of the original specimen, which is hold at the National Geological Museum Bucharest, will allow generic identification.

The formerly described cyamodontoids from Romania were based on fragmentary isolated osteoderms. The validity of these genera is pending on the question whether isolated osteoderms or carapace fragments can be used as a diagnostic character at generic level. Rieppel (2002) described in detail the morphology of the dermal armor of cyamodontoid placodonts and their systematic value, aspects that support the further evaluation of the Romanian cyamodontoid osteoderms and carapace fragments.

A detailed analysis of the osteoderms from the Middle Triassic sites Lugaşu de Sus and Peştiş concludes that all the remains of placodontian reptiles currently found in Romania belong to the armored placodonts - Cyamodontoidea. REFERENCES Jurcsak T. 1973. Date noi asupra reptilelor fosile de vârstă mezozoică din Transilvania, Nymphaea, I,

Oradea, 245-261. Jurcsak T., 1975. Tanystropheus biharicus n.sp. (Reptilia, Squamata) o nouă specie pentru fauna

triasică a României, Nymphaea, III, Oradea, 45-52. Jurcsak T., 1976. Noi descoperiri de reptile în Triasicul de la Aleşd, Nymphaea, IV, Oradea, 67-105.



E. Posmoşanu - Middle Triassic cyamodontoid reptiles from Romania

91

Jurcsak T., 1977. Contribuţii noi privind placodontele şi sauropterygienii din Triasicul de la Aleşd (Bihor, Romania), Nymphaea, V, Oradea, 5-30.

Jurcsak T. 1978. Rezultate noi în studiul saurienilor fosili de la Aleşd, Nymphaea, VI., Oradea, 15-60. Posmoşanu E. 2008. Notes on a Cyamodontoid maxillary from the Middle Triassic site Lugaşu de Sus

(W.Romania), Nymphaea, Folia Naturae Bihariae, XXXV, Oradea, 27-34. Rieppel O. 1995. The genus Placodus: Systematics, Morphology, Paleobiogeography, and

Paleobiology, Fieldiana, Geology NS., 31,Chicago, pp. 1-44. Rieppel O., 2002. The Dermal Armor of the Cyamodontoid Placodonts (Reptilia, Sauropterygia):

Morphology and Systematic Value, Fieldiana, Geology, N.S., 46, Chicago, 1-41.

Upper Pleistocene Panthera leo spelaea (Goldfuss, 1810) skeleton from Urşilor Cave, Romania

Marius ROBU1, Emanoil ŞTIUCĂ1, Virgil DRĂGUŞIN1 & Cajus DIEDRICH1

1 “Emil Racoviţă” Institute of Speleology, Romanian Academy, Calea 13 Septembrie 13 , Bucuresti. Keywords: Upper Pleistocene, Panthera leo spelaea, Urşilor Cave, taphonomy, Romania

This study is reporting the discovery of new skeleton remains of a cave lion from the western part of Romania.

A nearly complete skull, many forelimb and hindlimb bones, two vertebrae, five metapodials - all belonging to Panthera leo spelaea (Goldfuss, 1810), are described. Fossil remains were discovered inside Urşilor Cave, for the first time in the Lower passage, within a Ursus spelaeus (Rosenmuller & Heinroth, 1794) typical site.

Both the proportions and the morphological cranial and postcranial features of the remains point to a subadult male. Forelimb and hindlimb bones (two humeri, one ulna and one femur) and the skull present severe bite and gnawing marks, made by a large carnivore, probably by Crocuta crocuta spelaea (Goldfuss, 1823), species already recorded in the Quaternary fauna from Urşilor Cave.

In assessing the weathering degree of the fossils from the karstic environment, Behrensmayer’ methodology for assessing the bone weathering degree for the open-air site was adapted.

Introduction The first reference on cave lion rests in Urşilor Cave belongs to Terzea (1979),

recording fossils both on the cave floor and in a section (made at 40 m from the cave entrance) in the upper 30–40 cm of the stratigraphical section. The second record is that of Jurcsak et al. (1981): a cave lion scapula and tibia, with bite and gnawing marks, situated close to the entrance, on the cave floor.

The aim of our study is to report the discovery of new cave lion remains, to define their morphometrical characters and to expose some taphonomical considerations.

Materials and methods Urşilor Cave from Chişcău is located in the western part of Romania, in Bihor

County. It is situated on the left slope of Crăiasa Valley, south-eastern part of Beiuş Depression, at 482 m AMSL.

The cave is roughly developed on two carstification levels – the upper one is fossil and is used as show cave, while the lower one is active and represents the place where the cave lion remains were discovered.

The sediments in the Lower passage have a very different facies as compared to the upper carstification level. The underground river is limited throughout the entire passageway by clay-cut alluvial terraces, with slopes affected by small slides as a result of river undercutting; on their plateau lay Ursus spelaeus beds and fossil remains.

Cave lion remains discovered by one of us (C.G. Diedrich, December 2008) in the Lower passage of Urşilor Cave, represent the first record for this species found within this cave sector. Our reported materials are: a nearly complete skull, two humeri, two ulnae, a femur, a radius, two vertebrae, five metapodials, all belonging to Panthera leo spelaea and derived from the same individual.

The evaluation of principal cranial and post-cranial features of the remains and their identification as P. l. spelaea is based on Terzea (1965), Samson & Kovacs (1967), Sala (1990), Guzvica, (1998), Ştiucă (2000), Sotnikova & Nikolskiy (2006) and Diedrich (2007, 2008). The main cranial measurements were plotted on the ratio


M. Robu et al. - Upper Pleistocene Panthera leo spelaea (Goldfuss, 1810) skeleton from Urşilor Cave, Romania

diagram of Sotnikova & Nikolskiy (2006), according to G.G. Simpson’s method (1941).

Fig 1. Urşilor Cave map (redrawn after Rusu & Racoviţă, 1981)

For a better comparison with cave lions from other palaeontological sites, we performed the dentition measurements according to Turner (1984) and Sotnikova & Nicolskyi (2006), at the alveoli, excepting the canines. The upper and lower canines were measured and plotted on the scatter diagrams of Turner (1984), for having a better image concerning the dimension and sex of our material.

All measurements are in millimetres. For comparison, a recently discovered cave lion female skull (PSS 007/10, “Emil Racoviţă” Institute of Speleology collection; Ştiucă, 2000) was also plotted in the ratio diagram and in the scatter diagrams.

Fig. 2. The cave lion remains from Bears Cave, Lower passageway, plateau 5.

93


Results and discussion Weathering stages. Our fossil rests (which belong to a single specimen) present

different stages of weathering. The differences within the weathering stages of the bones of a skeleton are due to various degrees of exposure to the taphonomic agents. It is known that buried bones are better preserved than those exposed (Lyman, 2004), a fact emphasized as well by the P.l.spelaea fossils discovered by us.

Excepting the skull, found in a plateau microdepression covered by a thin clay layer, all the bones collected from the surface have degrees of weathering between 3 and 5 (see tab. 1). The other bones, which were half-buried, are much better preserved. Metapodials, metatarsals and phalanges are the best preserved pieces due to their small size and robustness: “…small, compact bones, such as podials and phalanges weather more slowly than other elements of the same skeleton” (Behrensmeyer, 1978).

Tab.1. Weathering morphological stages in large mammals from open-air sites adapted for large mammals from cave sites (Behrensmeyer, 1978 cited by Lyman 2004).

Large mammals Weathering stages

Description

0 No cracking or flaking bone. 1 Cracking parallel to fiber structure (longitudinal). 2

Flacking of outer surface (exfoliation), cracks are present, crack edge is angular.

3 Rough homogeneously altered compact bone, resulting in fibrous texture.

4

Coarsely fibrous and rough surface; splinters of bone loose on surface, with weathering penetrating inner cavities; open cracks.

5 Bone falling apart in situ , large splinters present, bone material very fragile

In assessing the weathering degrees of fossils from karst environments, the

Behrensmayer’ (1978) methodology for the open-air sites was adapted. Obviously, this raises a few methodological problems stemming from the differences between the climate of subterranean environment vs. the open-air sites, as well as between subaerial vs. subsurface weathering. Our assessment of the bones’ weathering stages in karst environment is only a morphologically-based one.

Bite and gnawing marks. The presence of tooth marks indicates that a large carnivore had access to the bones (Lyman, 2004). According to Haynes (1983a, cited by Lyman, 2004), tooth marking may allow more precise identification of the carnivore taxon responsible, if the bones are not exclusively gnawed. Although we identified a polygonal hole on the PU/0006 at the fossa radialis, we interpreted it like a non-ursid bite mark, because the bone’s width is very small thus it could be damaged very easily only following a hyenid bite-mark coupled with weathering, or only due to weathering. Although the scavenge behaviour of cave bear was discussed previously by Pinto & Andrews (2004), the bite and gnawing marks are belonging, most probably, to Hyenid genus.

Graphics. The ratio diagram (fig. 3) points to a proximity of our material towards the cave lioness from Scocu Scorotei Cave for LBa - basal cranial length, LPN - length from prosthion to the posterior end of nasals, LPO - length from prosthion to the anterior margin of orbit, WCa - greatest base canine width. Measurements performed for WBu - bulla width, show that there is a minimal difference between the analysed cave lions. WIO - minimum infraorbital width, Win - width across incisors row, Wma - greatest mastoid width, and WP2 - palate width between show an evident

94


similarity with the cave lion male group. The incomplete fused sutures, and the visible morphometric differences between the cave lion female from Scocu Scorotei Cave point out that PU/0001 belongs, most probably, to a subadult male.

Fig. 4. represents a scatter diagram of upper C length and width measurements. Our upper canine measurement was plotted in the Turner’s scatter diagram (1984), where the modern lion samples were used for comparison and for sex determination among the Panthera genus. The sexual dimorphism is obvious between both males and females of P.leo and Panthera leo spelaea. The cave lion from Urşilor Cave falls almost clearly into the female group, at its upper limit, indicating a large cave lioness or a subadult male.

The next scatter diagram (fig. 5) plots the length and width measurements for the lower canine. The distinction between males and females is almost clear and our material’s lower canine falls into the female cloud, at its upper part.

From these three above-mentioned graphics emerge the possibility that our material belongs to a large-size cave lion female, or to a medium-sized subadult cave lion male.

Fig. 3. Ratio diagram for the main craniometrical measurements.

60

65

70

75

80

85

90

95

100

105

110

115

120

Lba LPN LPO Wca WIO Win Wma Wbu WP2

%

PU/0001 Urşilor Cave

Scocu Scorotei Cave

K-1, Kondakovka, Kolyma*

GIN-1123, Smolensk, Russian Plain*

P.leo ZMSU S-1639*

Fig. 4. Scatter diagram of lion upper canine and width (after Turner, 1984, Sotnikova & Nicolskiy,

2006, with additions).

95


Fig. 5. Scatter diagram of lion lower canine and width (after Turner, 1984, with additions).

Conclusions The Panthera leo spelaea remains found, for the first time, within the Lower

passage of Urşilor Cave from Chişcău belong, according to the morphometrical analysis and to the scatter and ratio diagrams interpretation, to a subadult cave lion male.

It is a rare situation when cave lion remains are recorded so deep (~ 850 m) within a cave. It is very possible that during the Upper Pleistocene the Urşilor Cave had another entrance, used by these felids and not only, which was blocked after this period.

Most probably, the responsible species for the bite and gnawing marks presented on the cranial and postcranial material is the Ice Age spotted hyena. The morphological analysis of the bite marks and the study of the faunal association sustain the theory of Crocuta crocuta spelaea scavenging the cave lion skeleton. It was impossible to determine if the cave lion carcass was imported or scavenged in situ. A future stratigraphical section will explain this.

The weathering stages, adapted from Behrensmeyer (1978) for the karst environment, represent a method that indicates roughly the preservation degree of bones; our results could be, however, the starting point for future research. Aknowledgements. We are grateful to Dr. Oana Teodora Moldovan for assisting this paper from its beginnings, as well as to the Apuseni Mountains National Park management, who allowed us to start this research. REFERENCES Bocherens H., Drucker D., Billiou D., Geneste J.M. & Kervazo B., 2008. Grotte Chauvet (Ardeche,

France): A “natural experiment” for bone diagenesis in karstic context. Paleogeography, Palaeoclimatology, Palaeoecology, 266 (2008) 220-226.

Diedrich C. G., 2007c. Upper Pleistocene Panthera leo spelaea (Goldfuss 1810) skeleton remains from Praha-Podbaba and contribution to other lion finds from loess and river terrace sites in Central Bohemia (Czech Republic). Bulletin of Geosciences 82: 99–117.

Diedrich C. G., 2008. The holotypes of the upper Pleistocene Crocuta crocuta spelaea (Goldfuss, 1823: Hyaenidae) and Panthera leo spelaea (Goldfuss, 1823: Felidae) of the Zoolithen Cave hyena den (South Germany) and their palaeo-ecological interpretation. Zoological Journal of the Linnean Society, 2008, 154, 822-831, London.

Guzvica G., 1998. Panthera spelaea (GOLDFUSS 1810) from North_Western Croatia. Geol.Croat. 51/1. 7-14. Zagreb.

Hadnagy A., 1977. Studiu micromineralogic şi rolul mineralelor grele în corelarea sedimentelor de peşteră. Nymphaea, vol V, p. 107-128, Oradea.

96


97

Jurcsak T., Plopiş R., Ignat D., Şerban M. & Popa E., 1981. Date privind fauna fosila a Peşterii Urşilor (Munţii Bihor) Nymphaea- folia naturae Bihariae, t. VIII-IX, 161-257, Oradea, 1980-1981.

Lyman R. L., 2004. Vertebrate Taphonomy. Cambridge University Press. Moldovan O. T., Viehman I. & Onac B. P., 2007. Bear’Cave of Chişcău. „ Emil Racoviţă” Speology

Institute, Cluj-Napoca Compartiment. Onac B.P., Constantin S., Lundberg J. & Lauritzen S., 2002. Isotopic climate record in a Holocene

stalagmite from Ursilor Cave (Romania). Journal of Quaternary Science 17, 319–327. Pinto A. C.& Andrews P. J. (2004). Scavenging behaviour in Cave Bear, Ursus spelaeus. Revue de

Paleobilogie, Geneve, (decembre, 2004) 23 (2): 845-853. Rusu T. & Racoviţă Gh., 1981. Peştera Urşilor de la Chişcău. Ocrot. nat. med. înconj., t. 25, nr.1, p. 57-

71, 1981. Sala B., 1990. Panthera leo fossilis (v. Reich., 1906) (Felidae) de Isernia la Pineta (Ple´istoce`ne moyen

infe´rieur d’Italie). Geobios 23 (2), 189–194. Samson P. & Kovacs A., 1967. Felis spelaea în pleistocenul superior al Bazinului Sf.Gheorghe

(depresiunea Braşov). Lucr. Inst.de speol. “Emil Racoviţă”, t. VI, p.211-220, Bucureşti. Simpson G.G., 1941. Large Pleistocene felines of North America.American Museum Novitates 1136,

1–27. Sotnikova M. & Nikolskiy P., 2005. Systematic position of the cave lion Panthera spelaea (Goldfuss)

based on cranial and dental characters. Quaternary International 142–143 (2006), 218–228. Ştiucă E., 2000. Câteva aspecte privind morfologia şi afinităţile leului de peşteră din România (Leo

spelaea Goldfuss). Oltenia.Studii şi Comunicări. Ştiinţele Naturii. XVI. 2000. Craiova. Terzea E., 1965. Panthera spelaea (Goldf.) în pleistocenul superior din România. Lucr. Inst.de speol.

“Emil Racoviţă”, t. IV, p.251-283, Bucureşti. Terzea E., 1978. Depot de remplisage et mammiferes quaternaires de “Peştera Urşilor” de Chişcău,

departament de Bihor (note preliminaire). Trav. Inst. Speol. “Emile Racovitza”, t XVII, p. 139-144, Bucurest, 1978.

Terzea E., 1989. Les Arvicolides (Rodentia, Mammalia) du Pleistocene Moyen de Chişcău-1 (Depart. De Bihor, Roumanie). Trav. Inst. Speol. “Emile Racovitza”, t. XXVIII, 57-72, Bucurest, 1989.

Turner, A., 1984. Dental sex dimorphism in European lions (Panthera leo L.) of the Upper Pleistocene: palaeoecological and palaeoethological implications. Annales Zoologici Fennici 21, 1–8.

Vălenaş L., 1979. Studiu complex al zonei Valea Crăiasa-Valea Vârtoape, cu referire specială la Peştera Urşilor (Munţii Bihor). Nymphaea- folia naturae Bihariae, t. VII, 139-176, Oradea.

Von den Driesch A., 1976. A guide to the measurement of animal bones from archaeological sites. Peabody Museum of Archaeology end Ethnology, Harvard University.

Bioconstructions and crusts in Sarmatian carbonate platforms of Hungary

Jean-Paul SAINT MARTIN1, Ioan I. BUCUR2, Pierre MOISSETTE3, Jean-

Jacques CORNÉE4, Miklos KAZMER5 & Alfred DULAI6

1 Muséum National d’Histoire Naturelle, Département Histoire de la Terre, UMR CNRS 7207, 8 rue Buffon, Paris, France. [email protected] 2 Universitatea Babes-Bolyai, Department of Geology, Str. M. Kogalniceanu nr.1, 400084 Cluj-

Napoca. România. [email protected] 3 Université Claude Bernard Lyon 1, UMR CNRS 5125, Campus de la Doua, 69622 Villeurbanne

cedex , France. [email protected] 4 Géosciences Montpellier UMR 5243 - CC 60, Université Montpellier 2, Montpellier, France.

[email protected] 5 Eötvös University, Department of Palaeontology, P.O. Box 120, H-1518 Budapest, Hungary.

[email protected] 6 Hungarian Natural History Museum, Department of Geology and Palaeontology, P.O. Box 137, H-

1431 Budapest, Hungary. [email protected] Keywords: Middle Miocene, Sarmatian, Hungary, carbonate platform, algae, microbialite

During the Sarmatian, ooidic-bioclastic systems developed at the margin of the semi-enclosed Zsámbék basin (Hungary). The foraminifer and ostracod associations indicate that the carbonate systems are latest Badenian to Late Sarmatian in age. From the Early Sarmatian to the Early-Late Sarmatian, the deposits are organized in superimposed dunes prograding towards the basin on a low-angle ramp (Cornée et al., 2009). In the Late Sarmatian lagoonal deposits, numerous build-ups and crusts exhibit various composition, dimensions and shapes: domes with a flat base, about a decimetre high and up to one metre wide; centimetre- to decimetre-wide nodules or bindstones around pebbles, centimetre-thick carpets etc. They are associated generally with diversified mollusc shell accumulations.

The build-ups and crusts contain macro-builders represented especially by omnipresent serpulid worms and bryozoans and, also, a variable content of coralline algae, encrusting foraminifers (nubeculariids) and microbialitic material.

Among the coralline algae, several genera and species were identified: Lithoporella minus of little dimensions with small-sized cells developing mono- or pluristromate thallus; Titanoderma ucrainica with higher and larger cells; melobesioidae of ?Mesophyllum/?Neogoniolithon sp. type with apparently coaxial core and ovoid-trapezoid conceptacles, probably monoporate. Frequently, coralline algae occur as more or less thick crusts, sometimes reduced to a line of cells, or they may develop nodules, sometimes branched. Green algae are also present with fertile caps of Polyphysaceae (Génot et al., 2008) and abundant fragments of halimedaceans.

Locally abundant tubular structures with diameter of appreciatively 100 µm could be interpreted as remains of the lacustrine green algae Cladophorites.

Various types of microbialites were observed: peloidal stromatolitic crusts, thrombolitic masses and joined hemispheric domes, sometimes encrusted by algae (Lithoporella). The latter clearly exhibit filaments (approx. 0.03–0.04 mm in diameter) forming fan structures like Rivularia.

The presence of probable paleosols and pendular cements indicates a shallow environment subject to temporary emersive episodes. The participation of reputed freshwater organisms as Rivularia and Cladophorites allows discussing about the true nature of the Sarmatian waters.


J.-P. Saint Martin et al. - Bioconstructions and crusts in Sarmatian carbonate platforms of Hungary

99

REFERENCES Génot P., Saint Martin J.P. & Bucur I.I., 2008. Polyphysaceae fertile caps in Hungarian Sarmatian

sediments. Geologia Croatica, 61, 2-3, p. 341-344. Cornée J.J., Moissette P., Saint Martin J.P., Kázmér M., Tóth E., Görög Á., Dulai A. & Müller P.,

2009. Marine carbonate systems in the Sarmatian of the Central Paratethys: the Zsámbék Basin of Hungary. Sedimentology, Published Online: Mar 24 2009, DOI: 10.1111/j.1365-3091.2009.01055.x

The Middle Eocene Climatic Event (MECO) revealed by siliceous phytoplankton

Simona SAINT-MARTIN1,2, Johan RENAUDIE3 & Taniel DANELIAN4

1 Universitatea din Bucuresti, Facultatea de Geologie-Geofizica, Bulevard N. Balcescu No. 1,

Bucuresti, Romania. [email protected] 2 Muséum National d'Histoire Naturelle, Département Histoire de la Terre, 8 rue Buffon, 75005 Paris,

France. [email protected] 3 Université Pierre-et-Marie-Curie, CNRS-UMR 5143 Paléobiodiversité et Paléoenvironnements, 4

place Jussieu, 75005 Paris, France. [email protected] 4 Université Lille 1, UMR CNRS 8157 Géosystèmes, bâtiment SN5, 59655 Villeneuve d'Ascq cedex,

France. [email protected]

Keywords: Middle Eocene, Atlantic, Diatoms, Productivity

Middle Eocene (Lutetian and Bartonian) represented a period of climatic transition, characterized by a progressive drop of global temperatures, between the Early Eocene Climatic Optimum and the Antarctic glaciations at the Eocene/Oligocene transition. The presence of well-preserved diatom assemblages in Middle Eocene chalk recovered from Demerara Rise (equatorial Atlantic) offers the opportunity to explore, for the first time, the response of the siliceous phytoplankton (mainly diatoms, but also silicoflagellates) in relation to the Middle Eocene Climatic Event (MECO) event. Based on a quantitative micropalaeontological analytical approach, the aim of the study is to describe the changes recorded in the structure of the siliceous floristic assemblages in relation to the environmental changes. We thus also contribute to improving the understanding on the palaeoenvironmental conditions that prevailed during the Middle Eocene in the western part of the equatorial Atlantic. We established that the pre-MECO diatom assemblages were dominated by cosmopolitan species of genus Triceratium, and that they were replaced within the MECO interval by a new assemblage essentially characterized by two endemic species of genus Hemiaulus. Diatom assemblages within the MECO event contain taxa that could be considered as indicative of higher levels of productivity. Although the floral response is clearly established, the nature of the underlying causes for this profound change in the structure of the phytoplankton community is currently unclear.


Sedimentological and paleoecological study of rudist deposits in Gosau facies from Valea Neagra de Criş (Borod Depression)

Liana SASARAN1, Emanoil SASARAN1 & Ioan I. BUCUR1

1Babeş-Bolyai University, Department of geology, Str, M. Kogălniceanu nr.1, 400084 Cluj-Napoca. E-mails: [email protected]; esasaran&bioge.ubbcluj.ro; [email protected] Keywords: rudists, sedimentology, paleoecology, Upper Cretaceous, Borod Basin, Romania

The studied deposits are located along the eastern extremity of Borod Depression,

close to Valea Neagră de Criş locality, more precisely on the right flank of Pietrelor de Moară Brook. According to Lupu (1976), the Upper Cretaceous deposits from Valea Neagra are comparable with the middle (Upper Santonian–Lower Campanian) and upper (Upper Campanian–Maastrichtian) Gosau deposits, as evidenced by specific rudist associations identified and descibedd by the author. The Upper Cretaceous deposits in Gosau facies along the right flank of Pietrelor de Moară Brook crop out along a stratigraphical succession of several tens of meters thick. These deposits consist of terrigeneous rocks interlayered at several levels with bioconstructed limestones with rudists.

The carbonate deposits are represented by bioaccumulated and bioconstructed (the latter by the contribution of both rudists and corals) limestones. The identified rudists belong to the Hipuritidae, Radiolitidae and Plagioptychidae families. These specimens have been identified in situ and in living position, showing elevator growth orientation; they sometimes build-up bioconstructions (build-ups), clearly differentiated from the neighbouring facies. Rudists occur either as isolated individuals (Plagioptychus sp.) at the base of the bioconstruction, or as “bush”-like associations of tens of speciments, as typical feature for the stage following the bioconstruction’ consolidation. From rock fragments in slope aggregates in the same area, Şuraru (1972) has mentioned a coral fauna including: Actinastrea cf. octolamellosa, Columnastrea striata, Heterocoenia verrucosa, Cunnolites cf. barrerei, Plesiocunnolites macrostoma, and Diplocterium sp.

The siliciclastic deposits within the succession represent submarine fan deltas accumulated in the marginal areas of the basin. These siliciclastic bodies built-up highland areas at the basin margins, providing proper conditions for the subsequent accumulation of carbonate deposits. On the top of these high areas, bioconstructions and open shelf carbonate deposits formed. This normal shallow marine environment with low hydrodynamics and favourable bioclastic substrate small bioconstructions initiated by rudists as well as corals - as solitary specimens or as small-size clusters, could develop. Acknowledgements. The paper is a contribution to the project granted by CNCSIS, grant ID-95.

REFERENCES Şuraru M., 1972. Studiul coralierilor senonieni din Bazinul Borod. Teză de doctorat, Universitatea din

Bucuresti, 340 p., 67 pls., Bucureşti. Lupu D., 1976. Contributions á l’étude des rudistes sennoniens des Monts Apuseni. Mémoires de

l”Institut de Géologie et Géophysique, XXIV, p. 83-152, Bucureşti.




La paléontologie: de la science à l’éducation

Brigitte SENUT1

1 Muséum National d’Histoire Naturelle, Département Histoire de la Terre, USM 203 MNHN, UMR 7207 CR2P CNRS, CP 38, 8, rue Buffon, 75005 Paris ; [email protected] Mots-clés: Paléontologie, Musée, Education

En géosciences et en particulier en paléontologie, la récolte de spécimens s’effectue sur des terrains en général communaux, privés ou autres. Si dans les pays occidentaux, l’accès à ces terrains est assez bien réglementé, que se passe-t-il dans les nations émergentes? Le temps où les chercheurs arrivaient dans un pays pour collecter et repartir avec le matériel sans rien laisser derrière eux est aujourd’hui révolu. Les pays s’approprient leur patrimoine et développement également leurs propres centres culturels.

Aujourd’hui, la responsabilité du chercheur est engagée : le savoir est universel et le transfert des savoirs est une nécessité et un devoir vis-à-vis de la société. N’oublions pas que l’éducation est un droit inscrit dans l’article 26 de la Déclaration Universelle des Droits de l’Homme.

Fig. 1 - Musée de Paléontologie du Geological Survey of Namibia à Windhoek réalisé par la Namibia Palaeontology Expedition. La Namibie est un des pays d’Afrique où la séquence paléontologique est une des plus complètes du Protérozoïque au Quaternaire.

Et de fait, de plus en plus de scientifiques naturalistes réalisent des expositions permanentes ou itinérantes, comme en témoigne la réalisation du Musée de Paléontologie du Geological Survey of Namibia (Fig.1) ou l’exposition itinérante «20 millions d’années avant l’homme » disponible sur CD-Rom (Fig. 2).

Fig. 2 CD-ROM de l’exposition itinérante « 20 millions d’années avant l’homme » (MNHN-MAE)

Toutefois, au cours de nos travaux de paléontologie en Afrique, nous avons été confrontés à un problème tout à fait particulier. La médiatisation de certains aspects de la discipline a engendré dans certains cas la frustration des gens qui vivent près de ces patrimoines ensevelis : ils ont été des « oubliés » de la science et du



B. Senut - La paléontologie: de la science à l’éducation

développement.

Fig. 3 - Musée de Kipsaraman au Kenya.

De plus, les communautés avec lesquelles nous travaillons s’inquiètent du fait qu’isolées de la capitale et du Musée National, elles n’ont pratiquement aucune chance d’avoir accès à l’histoire de leurs régions et/ou de leurs racines.

C’est ainsi que nous avons été sollicités pour monter des musées locaux (Collines Tugen au Kenya ou Karamoja en Ouganda) pour éduquer les enfants et exposer au grand public l’intérêt des terrains locaux pour comprendre l’évolution. Au Kenya, un premier musée a été réalisé en 2000-2001 pour exposer en trois langues (anglais, français, kiswahili) les principales découvertes dans leur contexte environnemental (Fig. 3, 4) et notamment celles d’Orrorin tugenensis. Aujourd’hui, dans le Karamoja, un musée de la culture Karimojong est en cours de réalisation à Moroto (Fig. 5) dédié en grande partie à l’ethnographie de la région, mais ce sera aussi l’occasion de parler de son histoire paléontologique.

Parallèlement à ces actions de muséologie, des formations ont été faites sur place ou en France à des niveaux variés. Mais au-delà de la connaissance, c’est aussi, grâce aux musées une sensibilisation à la conservation des patrimoines locaux et donc mondiaux.

Fig. 4 - Musée de Kipsaraman (Kenya) : vitrine consacrée aux méthodes de terrain.

Fig. 5 - Musée de la culture Karimojong à Moroto (Ouganda).

103

Middle Miocene (Late Sarmatian) foraminifera and ostracoda from the western part of the Transylvanian Basin

Lóránd SILYE1, Botond SZABÓ1, Sorin FILIPESCU1 & Franz WANEK2

1 Department of Geology, Babeş-Bolyai University, M. Kogălniceanu 1, 400084 Cluj-Napoca. E-mails: [email protected], ro; [email protected]; [email protected]; 2 Sapientia – Hungarian Science University of Transylvania, Matei Corvin 4, 400112, Cluj-Napoca. Email: [email protected]

Keywords: Sarmatian, foraminifera, ostracoda, Transylvanian Basin, palaeoecology

The Sarmatian formations of the Transylvanian Basin are well-developed and known in Cluj-Napoca area (see Filipescu, 1999; Kovács, 2001; Suciu, 2005), although the evolution and palaeoecology of the late Sarmatian foraminifera assemblages of the area are still poorly understood.

Therefore, we studied with quantitative methods foraminifera of the Sarmatian sediments cropping out in the northern part of Aiton village (N 46.690227, E 23.735914). In order to get better constrains on the evolution and palaeoecological significance of the studied assemblages, the outcrop was described in sedimentological details, and the ostracods accompanying the foraminifera were also studied.

The studied assemblages are Late Sarmatian (Bessarabian) in age, as proven by the presence of evolved Porosononion species throughout the section. This age assumption is supported by the presence the ostracod Euxinocythere egregia MÉHES in the topmost part of the section.

Within the foraminifera fauna, two assemblages were distinguished: Elphidium–Ammonia, and Porosononion–Nonion–Bolivina. Their alternations within the sedimentary record in the Aiton section point out rhythmic palaeoenvironmental changes from shallow water with decreased salinity (slightly hyposaline) to deep-water, normal marine environment throughout the section.

In the topmost part of the section, the presence of Xestoleberis sp., Leptocythere sp., Candona ?praesarmatica KRISTIĆ, 1972, Euxinocythere egregia (MÉHES, 1908), Loxoconcha sp., and Candona sp., and the reduced foraminifera population argue for an environment with decreased salinity (hyposaline), largely influenced by fresh-water input. In contrast, Argilloecia sarmatica JIŘÍČEK, Loxoconcha sp. present in the samples demonstrates the existence of deep shelf marine environment close to the Sarmatian/Pannonian boundary. REFERENCES Filipescu S., 1999. The significance of foraminifera fauna from the Feleac Formation (Transylvanian

Basin, Romania). Studia Universitatis Babeş-Bolyai, Geologia, v. 44, 2, p. 125-131. Kovács Z., 2001. A Kolozsvár környéki bádeni és szarmata üledékek biosztratigráfiája. Collegium

Geologicum, v. 2, p. 67-97. Suciu A.-A., 2005. Preliminary data on the Sarmatian deposits from Lombi Hill (Popeşti locality)

northwest from Cluj-Napoca. Analele Ştiinţifice ale Universităţii "Al. I. Cuza" din Iaşi, Geologie, v. 51, p. 121-132.


Darwin, the amphibians, and the natural selection

Jean Sébastien STEYER1

1 UMR 5143 « Paléobiodiversité et Paléoenvironnements » et Département Histoire de la Terre du Muséum national d’Histoire naturelle, CP 38, 8 rue Buffon, 75005 Paris cedex, [email protected] Keywords –history of science, lissamphibians, evolution, stegocephalians, Lamarck, ontogeny

A critical review of the Darwin’s publications shows that he did not dissert a lot about amphibians by comparison with other tetrapods. However, in “A Naturalist’s Voyage round the World”, Darwin described for the first time several amphibian species and he was surprised by their peculiar, terrestrial or euryhaline, way of life. These amphibian observations around the world led Darwin to discuss about evolutionary notions, like developmental heterochronies or evolving convergences, and later to illustrate his famous natural selection theory.

This is confirmed for example by the publication of “On the Origin of Species” where Darwin ironically questioned the creation theory, trying to explain the absence of amphibians on oceanic islands. Lamarck also considered amphibians as relevant material to illustrate his theory on acquired character heredity. These historical uses of lissamphibians as evolutionary models have been mostly realized prior to any fossil amphibian discovery, i.e. out of a palaeontological context.

Fig.1 - Amphibian specimens collected by Darwin, [4] Plate 20, the “Darwin’s taod” (“Phryniscus nigricans”) centre of the Plate. It is interesting to note that this plate is titled “Reptiles” (up right corner).



Middle Jurassic microfaunal assamblages from Bucegi mountains (Strunga – Strunguliţa area)

Marius STOICA1 & Iuliana LAZĂR2

1 University of Bucharest, Faculty of Geology and Geophysics, Laboratory of Palaeontology, 1, N. Balcescu Ave., RO-010041, Bucharest, Romania. [email protected]; [email protected]

Keywords: Middle Jurassic, Ostracoda, Foraminifera, Bucegi Mountains

The microfaunal assemblages described in the present paper are recorded from Middle Jurassic (Bajocian) deposits that crop out along the western flank of Bucegi Mountains (East Carpathians). Previous research concerning the micropaleontology of the Mesozoic deposits from these outcrops was accomplished by Patrulius (1957 - 1980), Stoica et al. (1982), and Neagu et al. (1983).

The micropaleontological samples described in this paper were collected from two main locations: Strunga Pass and Strunguliţa Pass that are the best outcrops for the Middle Jurassic succession in this area. One of the described assemblages was recorded from the lower part of the Bajocian deposits, from a 3.5 m thick bed represented by pelites alternating with silts, and limonitic concretions. The microfauna is dominated by forams: Epistomina nuda, E. steligera and Lenticulina quenstedti are the most abundant; with moderate frequency: Lenticulina calva, L. ovatoacuminata, Citharina citharella, Spiroohtalmidium clarum and Recorvoides pygmaeus were noticed. From the same assemblages, ostracods were recorded: Parashuleridea sp., Cytherella sp., Lophocythere propinqua, Monoceratina unguliana and other microfossils like bivalves and brachiopods juveniles, planorbide microgastropods, spines and calcitic echinoid plates, crinoid stem columnals, holothurid sclerites, otholites, teeth fish, and coprolites. The other microfaunal assemblages were sampled from the middle part of the Bajocian succession, from very thin silty marl levels. The microfauna is very poorly-preserved and it is represented by forams: Lenticulina quenstedti and Citharina citharella, bryozoans (with moderate frequency), echinoid spines and plates, as well as crinoid columnals.




Pollen analysis in Maramureşului Mountains

Ioan TANŢĂU1, Sorina FĂRCAŞ2, Marcel MÎNDRESCU3 & Bogdan HURDU2

1 Babeş-Bolyai University, Department of Geology, 1 Kogălniceanu Str., Cluj-Napoca, Romania, RO-400084, [email protected] 2 Institute of Biological Research Cluj-Napoca, 48 Republicii Str., Cluj-Napoca, Romania, RO-400015, [email protected] 3 Ştefan cel Mare University, 9 Universitatii Str, Suceava, Romania, RO-720225, marcel.mindrescu @gmail.com Keywords: Pollen analysis, radiocarbon dating, vegetation history, Holocene, “Natura 2000” site, Maramureşului Mountains, Romanian Carpathians

Maramureşului Mountains are, by their location at the northern border of Romania, their vastitude, their complex geomorphology with traces of glaciations and their biodiversity, an extremely interesting area from the scientific point of view, which resulted in their recent inclusion in the "Natura 2000" sites list.

The current biodiversity of flora and fauna of Maramureşului Mountains is well known, but their paleobiodiversity and development is still insufficiently studied. This is one of the reasons for selecting some peat bogs and ponds for palynological analysis.

This study presents the results of pollen analysis carried on two peat bogs from Maramureşului Mountains, developed in ancient glacial cirques: Tăul Mare - Bardău (1850 m altitude) and Cristina (1573 m altitude).

The vegetation record, which is supported by six 14C dates (four from Bardău and two from Cristina), starts in the Atlantic period. The vegetation of this period was represented by dense forests dominated by Corylus, Alnus, Picea, Ulmus and Betula.

Mixed oak elements (Quercetum mixtum) appear under-represented in the pollen diagrams because of the high altitude of the sites. Elm curve (Ulmus) is higher in the base of the sequences, while the other elements of the mixed oak (Quercus, Tilia, Acer, Fraxinus) are poorly represented.

The establishment of Carpinus occurred at about 5900 yr BP, with a maximum at about 3500 yr BP.

Fagus pollen is regularly recorded after 5000 yr BP and became dominant at about 3000 yr BP.



Early Badenian mollusk fauna from Bahna Basin (Southern Carpathians)

Rodica TIŢĂ1

1 Geological Institute of Romania, Str. Caransebeş nr.1, Bucharest 012721, Romania; E-mail: [email protected]

Keywords: Mollusks, Badenian, Bahna basin, Romania

This study focused on mollusks species from Bahna Basin (Southern Carpathians), sampled from Curchia limestone, component of Curchia Formation (Marinescu et al. 1998). Mollusk taxa from two old collections of Macovei (1909) and Stancu (1961) have been also revised. In the same time, mollusk species from the author’s personal collection have been identified as taxa belonging to the following families: Turritellidae, Cerithiidae, Naticidae, Cymatiidae, Turridae, Olividae, Arcidae, Glycymerididae, Pectinidae etc. This fauna point to a reef-type association with foraminifera, corals and echinids, all being forms identified by the authors. This represents a contribution to a better characterisation of the Curchia Formation as a marine one, locally showing reef-type features.



Upper Jurassic – Lower Cretaceous limestone from Hodobana-Gârda Seacă area (Bihor Mountains)

Valentin TURI1,2, Emanoil SĂSĂRAN2 & Ioan I. BUCUR2

1 Petrom S.A. Member of OMV Group, E&P, Exploration Division, Piaţa Eroilor nr.1 A, 100316 Ploieşti, Romania. Email: [email protected] 2 Babeş-Bolyai University, Department of Geology, Str. M. Kogălniceanu nr.1, 400084 Cluj-Napoca, Romania. E-mail: [email protected]; [email protected].

Keywords: Limestone, Upper Jurassic-Lower Cretaceous, Bihor Mountains, Romania

The calcareous deposits from Hodobana-Gârda Seacă region are located in the Bihor Mountains, and are very well exposed along the Gârda Seacă Valley. Triassic, Jurassic and Lower Cretaceous deposits belonging to the Bihor Unit crop out in this region. The limestones have been studied in Gârda Seacă, Sohodoale, Hoanca Fileştilor Valleys, as well as on Vârtopaşului, Crestătura and Chicera Hills.

From field observations, as well as from thin sections and polished slabs analyses we conclude that a part of the outcroping Triasic (Ladinian) and Lower Cretaceous limestones from Gârda Seacă-Hodobana region, delimited on the Geological Maps 1:50 000, Sheets b, d (Poiana Horea and Avram Iancu) (Bleahu et al., 1980; Dimitrescu et al., 1977), belong in fact to the Upper Jurassic carbonate succesion.

Kimmeridgian-Tithonian limestones are cropping out on Sohodoale Valley on aproximately 1 km upstream from the confluence with Hodobana Valley. These limestones are deposited in a high energy subtidal environment, as well as, most probably, in a shallow-water intertidal environment. The succesion continues with Barremian-Aptian limestones developed in Urgonian facies, with different organisms generating bioclasts. The rudists are important bioclasts producers, in comparisons with corals and sclerosponges. The last two groups generated bioconstructions, but these are not important elements of the Urgonian limestones..

The samples colected from Hoanca Fileştilor and Gârda Seacă Valleys contain a micropaleontological assemblage that points to the Kimmeridgian-Tithonian age, with reef bioconstructions, oncoidic limestones and their associated facies, typical for Crişanului Valley Formation (nom. corr.) and Albioara Formation (sensu Dragastan et al., 1986).

The age of the limestones was established based on micropaleontological assemblages. The Upper Jurassic limestones from Hodobana-Gârda Seacă area contain the following foraminifera [?Alveosepta sp., Andersenolina alpina (LEUPOLD), Andersenolina sp., ?Charentia sp., Coscinophragma sp., ?Everticyclammina sp., Kurnubia palastiniensis HENSON, ?Kurnubia sp., Labyrinthina mirabilis WEYNSCHENK, Mohlerina basiliensis (MOHLER), Neokilianina rahonensis (FOURY & VINCENT), Parurgonina caelinensis CUVILLIER, FOURY & PIGNATTI MORANO, ?Parurgonina sp., Pseudocyclammina lituus YOKOYAMA, ?Pseudocyclammina sp., Redmondoides lugeoni (SEPTFONTAINE)], dasycladalean and other green algae [Campbelliella striata CAROZZI, Clypeina sulcata (ALTH), Salpingoporella annulata CAROZZI, Salpingoporella pygmaea (GÜMBEL), Salpingoporella sp., Nipponophycus ramosus YABE & TOYAMA, Thaumatoporella parvovesiculifera RAINERI], rhodophyta (?Solenopora sp.), rivulariacean-type cyanobacteria, and microproblematica



V. Turi et al. - Upper Jurassic – Lower Cretaceous limestone from Hodobana-Gârda Seacă area (Bihor Mountains)

110

[Bacinella irregularis RADOIČIĆ, Lithocodium aggregatum ELLIOTT and Crescentiella morronensis (CRESCENTI)].

The Lower Cretaceous limestones from Hodobana contain a micropaleontological assemblage with foraminifera [Coscinophragma sp., Charentia cuvillieri NEUMANN, Everticyclammina hedbergi (MAYNC), Everticyclammina sp., Neotrocholina sp., Nezzazatinella sp., Montseciella arabica (HENSON), Paleodictyoconus sp., Palorbitolina lenticularis (BLUMENBACH), ?Palorbitolina sp., Paracoskinolina? jourdanensis FOURY & MOULLADE, Pseudolituonella gavonensis FOURY, Sabaudia minuta (HOFKER), Trocholina sp., Troglotella incrustans WERNLI & FOOKES and Vercorsella sp.], dasycladalean algae [Falsolikanella danilovae (RADOIČIĆ), ?Linoporella sp., Neomeris cretacea STEINMANN, Neomeris sp., Salpingoporella melitae RADOIČIĆ, Salpingoporella muehlbergii (LORENZ), Salpingoporella pygmaea (GÜMBEL), Suppiluliumaella elliotti BAKALOVA, Suppiluliumaella sp. and Terquemella sp.], rivulariacean-type cyanobacteria, rhodophyta (Marinella lugeoni PFENDER and ?Solenopora sp.), and microproblematica (Bacinella irregularis RADOIČIĆ and Lithocodium aggregatum ELLIOTT). Acknowledgements: The study is a contribution to the research project founded by CNCSIS, grant ID 561

REFERENCES Bleahu M., Bordea S., Bordea Josefina, Mantea Gh., Dimitrescu R. (1980) - Harta Geologică 1:50

000, Foaia 56b, Poiana Horea. Editura Institutului Geologic. Dimitrescu, R., Bleahu, M. & Lupu, M. (1977) - Harta Geologică 1:50 000, Foaia 56d, Avram Iancu.

Editura Institutului Geologic. Dragastan O., Purecel R. & Brustur T. (1986) – The Upper Jurassic and Lower Cretaceous formations

from the Bihor Mts. – central-southern sector (Northern Apuseni). Analele Universităţii Bucureşti, Geologie, XXXV, p.57-70, Bucureşti

Palaeoclimatic and palaeoenvironmental interpretation of the Sarmatian deposits of Şupanu Formation from Comăneşti Basin

(Bacău County)

Daniel ŢABĂRĂ1 & Gabriel CHIRILĂ1

1“Al. I. Cuza” University of Iaşi, Department of Geology, Bd. Carol I, no. 20A, 700505, Iasi, Romania, e-mail: [email protected]; [email protected] Keywords: Comăneşti Basin, Şupanu Formation, Sarmatian, palaeoflora, palaeoclima, palaeoenvironment.

Comăneşti Basin represents a subsidence area which acted as sedimentary basin

with mollase character during the Sarmatian and the Maeotian. Occasionally these deposits contain coal layers. First studies regarding macroflora associations from this area have been made by Barbu (1934), followed by Ciocârdel (1943), Givulescu (1957, 1963, 1968) and Micu et al. (1985). Palynological investigations on Sarmatian and Maeotian deposits have been performed by Lubenescu et al. (1986), Nicolaescu et al. (1984) and Horaicu (1989).

We have studied palaeofloral associations hosted by clay deposits of Şupanu Formation which crop out on the western part of the Lăloaia – Galeon and Asău basins. The following taxa have been identified: Glyptostrobus europaeus, Typha latissima, Taxodium dubium, Salix varians, Byttneriophyllum tiliaefolium etc.; additionally, palynological forms such as: Inaperturopollenites concedipites, Myricipites bituitus, Pterocaryapollenites stellatus, Tricolporopollenites henrici, Zonalapollenites rueterbergensis, Polypodiaceoisporites gracillimus etc. have been described.

Palaeoclimatic calculations (MAT – mean annual temperature, MAP – mean annual precipitations, WMT - mean temperature of the warmest mounth, CMT - mean annual temperature of the couldest mounth) have been performed using the „Coexistence Approach” method (Mosburgger and Utescher, 1997). Finally, this paper also presents the results of palynofacies analysis based on the organic matter content.

REFERENCES Barbu I. Z., 1934. Contribuţii la cunoaşterea florei fosile din Podişul Moldovei şi Basarabiei. Acad.

Rom Mem. Sect. Şt. s III, X/5: 105 - 135. Ciocîrdel R., 1943. Daten über das Alter des Beckens von Comăneşti (Bezirk Bacău – Rumänien).

Monit. de Petrole Roumain, LXIV/1-2. Givulescu R., 1957. Note botanice (III). St. Şi Cercet. Şt., 8/3-4: 46 - 50. Givulescu R., 1963. Acer ezoanum Oishi et Huzioka în Miocenul din RPR. Com. Acad. RPR, 13/5: 445

- 448. Givulescu R., 1968. Date noi privind flora fosilă a Bazinului Comăneşti. St. Cerc. geol. geof. geogr., s.

Geol., 13/1: 285-288. Horaicu C., 1989. Palynologic considerations on the coal formation in the Comăneşti Basin, Romania.

Anal. Şt. Univ. „Al. I. Cuza” Iaşi, s IIb, geol.-geogr., 35: 30 - 33. Lubenescu V., Balteş N., Manolescu C. & Balteş C., 1986. Considérations biostratigraphiques sur les

dépôts néogènes du Bassin de Comăneşti. D. S. Inst. Geol., 70 – 71: 128 - 143. Micu M., Ţicleanu N., Andreescu I., Jipa D., Popescu A., Rădan S., Anghel S., Iva M. & Căuş C.,

1985. Geologia Bazinului Comăneşti. D. S. Inst. Geol. şi Geofiz., LXIX/4 (1982): 194 - 244.




D. Ţabără & G. Chirilă - Palaeoclimatic and palaeoenvironmental interpretation of the Sarmatian deposits of Şupanu Formation

112

Mosbrugger V. & Utescher T., 1997. The coexistence approach - a method for quantitative reconstructions of Tertiary terrestrial palaeoclimate data using plant fossils. Palaeogeography, Palaeoclimatology, Palaeoecology, 134: 61-86.

Nicolaescu V., Lubenescu V., Cibotaru T., Nichiforescu H., Ciupu F. & Neacşu F., 1984. Bazinul Comăneşti. Consideraţii geologice. St. şi cercet. de geol., geofiz. şi geogr., seria geol., T. 29: 112 - 153.

First records of nautilids in the Lower Jurassic klippe of Praşca Peak (Rarău Syncline, Eastern Carpathians, Romania)

Paul ŢIBULEAC1

1 „Alexandru Ioan Cuza” University Iaşi, Department of Geology, Carol I Avenue, nr 20 A, 700506, Iaşi; [email protected] Keywords: Nautilids, first records, Rarău Syncline, Lower Jurassic

Introduction Nautilids have been usually encountered in Lower Jurassic strata with an abundant

ammonite fauna, but they are characterized by scarcity in taxonomic diversity and frequency of records as compared to those documented by ammonoids.

During the last diggings in the klippe of Praşca Peak, several nautilids were collected for the first time.

Geological framework Near to Praşca Peak, a large „ammonitico rosso” block occurs in the Cretaceous

Wildflysch of the Rarău Syncline. In the previous papers it was considered either klippe, or olistolith due to misunderstandings related to these terms or in respect with different models for the Alpine evolution of the Eastern Carpathians. Nowadays, in agreement with Săndulescu’s model (1984), we considered it as a klippe belonging to the Olt Nappe (Transylvanian Nappes).

The klippe is built by regular beds consisting of red nodular/pseudonodular limestones, limestones and marls into a facies assigned to „Adnet region” by Uhlig (1900); subsequent researchers considered it a transitional facies between Adnet and Hierlatz (Atanasiu and Răileanu, 1950; Turculeţ, 1965). It has an upside-down inclination within the Cretaceous Wildflysch, demonstrated by the relative position of in situ fossiliferous beds. The diggings show beds yielding ammonites from the Arnioceras semicostatum T.-r. Zone, occurring up-slope from beds yielding ammonites of the Echioceras raricostatum T.-r. Zone. The continuity of sedimentation was argued by several in situ ammonites taxa-index encountered between these zones.

Material The nautilids described herein (9 specimens) were mostly collected from the

extreme zones of the klippe, respectively from the Arnioceras semicostatum and Echioceras raricostatum T.-r. Zones. Only one was found in the soil, near of the middle height of the strata succession.

All specimens are internal moulds, few of them being affected by erosion or distortion of the shell cast. The specimen found in the Euagassiceras sauzeanum/resupinatum T.-r.Subzone, respectively Cenoceras (Hemicenoceras) cf. semistriatus (d’ORBIGNY, 1843) shows larger dimensions than the rest of nautilids; it preserves the phragmocon and body chamber, while the others have normal sizes; they represent the phragmocons only.

The absence of shell wall and sculpture is a disadvantage in the identification, because the morphology of the moulds and the suture line do not always show very distinctive features.

The following taxa were been identified: Cenoceras striatus (SOWERBY 1817), C. cf. striatus SOWERBY, 1817) C. intermedius (SOWERBY, 1816), and C. (Hemicenoceras) cf. semistriatus (d’ORBIGNY, 1843).



P. Ţibuleac - First records of nautilids in the Lower Jurassic klippe of Praşca Peak (Rarău Syncline, Eastern Carpathians)

114

The nautilids occur together with frequent ammonites (phylloceratids and ammonitids, few lytoceratids), then aulacocerids, brachiopods, rare bivalves and crinoids; in the klippe, foraminifers, alga, gastropods, ostracods, echinids, fish teeth etc. were also documented.

Correlations and discussion In the Eastern Carpathians, nautilids have been already documented in two areas

with Early Jurassic sediments. In the Hăghimaş Mountains, they were recorded from both autochthonous and

allochtonous nappes: Atanasiu and Răileanu (1950) mentioned Nautilus striatus Sow. and Nautilius sp. along Ghilcoş stream (Bucovinian Nappe), while Grasu (1970) described Nautilus austriacus HAUER and Cenoceras, striatus SOW. at Curmătura (Transylvanian Nappes).

In Perşani Mountains, records were frequent in the klippen of the Transylvanian Nappes: Nautilus austriacus Hau., N. cfr. Sturi Hau. N. Sturi var., N. striatus Sow., N. intermedius Sow, Nautilis sp., N. semistriatus d’Orb. were quoted by Herbich (1878), Vadàsz (1907, 1908, 1915), Preda and Răileanu (1960).

Nautilids were also documented in the Early Jurassic of Yorkshire, Dorset Coast, then Jura Mountains, Lyon environs, Lombardie, Central Apennine Mountains, Adnet and Enzesfeld regions, Bakony Mountains etc.

Cenoceras striatus and C. intermedius are common species in the Sinemurian rocks, while C. (H.) semistriatus was recorded from Toarcian rocks (Hildoceras bifrons T.r. Zone) in the Western Europe. Further more, Meneghini (1867-81, p. 128) noted that Dumortier (1869) signaled a specimen of C. semistriatus in beds older than Middle Liassic. As we already noted above, Vadàsz (1915, p. 279) also signaled the presence of this species in the Sinemurian of Perşani Mountains. Further data on more abundant faunas could bring new arguments to explain this uncommon record.

REFERENCES Atanasiu I. & Răileanu Gr., 1950. Contribuţii la cunoaşterea Liasicului din Munţii Hăghimaş. Buletin

ştiinţific, seria Geologie, Geografie, Biologie, Ştiinţe tehnice şi agricole, II/5: 275-289 Grasu C., 1970. Observaţii asupra Liasicului de Adneth de la Curmătura (Hăghimaş). Lucrările

Staţiunii de cercetări biologice, geologice şi geografice “Stejarul”, Piatra Neamţ : 7-12. Herbich F., 1878. Das Szeklerland. Mitteilungen des Jahrbuches der. k. Ungar. Geol. Anstalt, 363 p. Meneghini J., 1867-81. Monographie des fossils du calcaire rouge ammonitique (Lias supérieur) de

Lombardie et de l’Apennin Central. Imprimerie Bernadoni de C. Rebeschini & C.e. Milan D’Orbigny A., 1842-1849. Description des mollusques et rayonnés fossils. Terrains jurassiques, I-

Céphalopodes, 254 pl. Preda D. M. & Răileanu, Gr., 1960. Contributions à la connaissance du Lias de Mont Perşani. Annuaire

du Comité Géologique, XXVI – XXVIII: 53 – 67. Săndulescu M., 1984. Geotectonica României. Ed. Tehnică, 336 p. Turculeţ I., 1965. Câteva date privind Liasicul din dealul Praşca. Analele ştiinţifice ale Universităţii

“Al. I. Cuza” Iaşi, s. II/b, XI: 203-204. Uhlig V., 1900. Üeber eine unterliasische Fauna aus der Bukowina. Abhandlungen des deutschen

naturwissenschaftlich-medicinischen Vereins für Böhmen “Lotos”. II/1, 31 p. Vadász E. M., 1907. Über die Fauna der Unterrliassischen Schichten von Alsórákos (Persánygebirge).

Földtani Közlöny, XXXVII: 406 – 410. Vadász E. M. 1908. Die Unterliassische Fauna von Alsórákos in Komität Nagyküküllö. Mitteilungen aus dem

Jahrbuche der kgl. Ungarischen Geologischen Reichsanstalt, XVI/5: 309-406. Vadász E. M., 1915, Geologische Beobachtungen im Persány – und Nagyhagymás-Gebirge. Sonderabdruck aus

dem Jahresbericht der kgl. Ungar. Geologischen Reichsanstalt für 1914, Budapest, Buchdruckerei Ármin Fritz : 265 – 298.

Upper Jurassic spongolithic atolls in Central Dobrogea

Daniel UNGUREANU1 & Eugen BARBU2

1 Mihaela Ruxandra Marcu st. Nr.5, C7 Bl., Apt. 24, 061524 Bucharest 6, Romania; E-mail: [email protected] 2 1 Decembrie 1918 Ave.nr.31, Apt. 62, 900162 Constanta, Constanta; E-mail: [email protected] Keywords: Jurassic, Romania, Dobrogea, paleontology, sponge, atoll, reef

During the Upper Jurassic, a huge reefal belt developed across the Earth. It was spread over more than 7000 km in length and it represented the largest structure ever built by living organisms on the planet. Its' remains can be found in Europe from Por-tugal, through Spain, France, Switzerland, Germany, Poland, to Romania. There is also information about the presence of the Upper Jurassic Sponge Megafacies from Oklahoma, off Newfoundland, to Georgia and India in the east, imprinting the sponge reef belt a worldwide extent (Pisera, 1997; Mehl et Fursich, 1997; Krautter, 2003). All European occurrences are dated in the Upper Jurassic, but not precisely in the same time span. However, in most locations the reef was already developed and living dur-ing the Oxfordian. The studied Romanian occurrence represents the easternmost one in Europe and it has a very peculiar feature: here, Jurassic sponges developed reefs in atoll shape like nowhere in the world. They are such odd geological buildings that never repeated, either before or after that time. Noticed in the early second half of last century, the spongolithic atolls are clearly visible in the Northern part of Casimcea Syncline (Western Central Dobrogea), along the so called Cheile Dobrogei (Dobrogea Gorges) area. Actually, they border a part of the Canara-Cheia Valley, where in time the water stream eroded the soil and washed the rubble, revealing the buried reefs. They were studied by several researchers along decades.

The present work follows up the previous studies and adds some new data that change our picture on spongolithic deposits in Central Dobrogea. We are introducing the atoll structure as major pattern in the siliceous sponge reef facies. Arguments for paleoenvironmental reconstructions are also included, as well as some stratigraphic correlations, aiming to allow a clearer image of the living world 155 m. y. ago. REFERENCES Krautter M., 2003. Research of Bio-CenterLMU members highlighted – GeoBio-CenterLMU - News

Flash. Mehl D. & Fürsich F. T., 1997. Middle Jurassic Porifera from Kachchh, western India. Paläontolo-

gische Zeitschrift ,71/1,2: 19-33. Pisera A., 1997. Upper Jurassic Siliceous Sponges from the Swabian Alb: Taxonomy and Paleoecol-

ogy. Palaeontologia Polonica, 57.




Reassessment of the spatial extent of the fossil-bearing Maastrichtian middle member, Densus-Ciula formation (Hateg Basin, Romania)

Stefan VASILE1, Zoltan CSIKI1 & Dan GRIGORESCU1

1Laboratory of Paleontology, Faculty of Geology and Geophysics, University of Bucharest; 1 N. Balcescu Blvd, 010041 Bucharest, Romania; e-mails: [email protected]; [email protected]; [email protected] Keywords: Hateg Basin; Maastrichtian; lithostratigraphy; eggs

The Middle Member of the Densus-Ciula Formation (Maastrichtian-Lower Paleogene; Grigorescu, 1992) was defined based on its typical Latest Cretaceous fossil content (including dinosaur remains) and the occurrence of disperse volcanoclastic material within the coarser-grained deposits. It is considered to be overlain by the Upper Member of the formation, devoid both of Cretaceous vertebrates and volcanoclastic material. The presumptive boundary between the two members was suggested to occur eastward, but in the close proximity, of Farcadin village (Weishampel et al., 1991: Fig. 5). This uncertainty is due to the absence of a visible contact between the two subunits in this heavily vegetated area, as well as that of typical features (Maastrichtian vertebrate remains, volcanoclasts), previously not reported in the areas lying east of this line.

Recent fieldwork in the hilly region lying north of the Galbena Valley revealed the presence of several small-sized outcrops north of the General Berthelot (formerly known as Unirea) village church with a lithology markedly reminiscent of that known from the dinosaur nesting site of Oltoane Hill, Tustea locality (Grigorescu et al., 1994). Here, at least two sequences of red silty mudstones overlain by light grey sandstones were encountered. The sandstones contain disperse ruditic clasts, including altered cm-sized andesitic volcanoclasts, of the same type as those reported from the Tustea nesting site. Unfortunately, the restricted outcropping conditions, along a footpath, do not allow the assessment of the bed thickness and lateral development, neither the exact number of the repetitive sequences; however, apparently the thickness of the sandstone beds is less than at Tustea.

Further research at these new sites revealed another distinctive feature of the Densus-Ciula Formation Middle Member: the presence of dinosaurian eggshell fragments in the red silty mudstones underlying the volcanoclast-bearing sandstones. The eggshells are also similar to those reported from Tustea (Grigorescu et al., 1994), Totesti (Codrea et al., 2002), Nalat-Vad (Smith et al., 2002) and more recently from Livezi (Grigorescu and Csiki, 2008), belonging to the Megaloolithidae oofamily. Although only isolated fragments were found up to date, their large number, good preservation and sometimes large size suggest these are not reworked from stratigraphically older beds, although probably does not represent in situ, autochtonous remains representing a nesting ground, either.

The occurrence of lithological and paleontological features characterizing the Middle, Maastrichtian member of the Densus-Ciula Formation in the neighbourhood of General Berthelot locality supports the eastward extension of this lithostratigraphic entity. The eastern boundary of the subunit remains, however, hidden from direct observation, due to poor outcropping conditions in this area.




S. Vasile et al. - Reassessment of the spatial extent of the fossil-bearing Maastrichtian middle member, Densus-Ciula formation

117

REFERENCES Codrea V., Smith T., Dica P., Folie A., Garcia G., Godefroit P., Van Itterbeeck J., 2002. Dinosaur egg

nests, mammals and other vertebrates from a new Maastrichtian site of the Haţeg Basin (Romania). Comptes-Rendus Palevol 1 : 173–180.

Grigorescu D., 1992. Nonmarine Cretaceous formations of Romania. In: Matter, N.J., Chen, P.-J. (Eds.), Aspects of Nonmarine Cretaceous Geology, Special vol., ICGP Project 245, China Ocean Press, Beijing, pp. 142-164.

Grigorescu D. & Csiki Z., 2008. A new site with megaloolithid egg remains in the Maastrichtian of the Haţeg Basin. Acta Palaeontologica Romaniae 6: 115–121.

Grigorescu D., Weishampel D., Norman D., Şeclăman M., Rusu M., Baltreş A. & Teodorescu V., 1994. Late Maastrichtian dinosaur eggs from the Haţeg Basin (Romania). In: Carpenter, K., Hirsch, K.F., Horner, J.R. (Eds.), Dinosaur Eggs and Babies. Cambridge University Press, Cambridge, pp. 75–87.

Smith T., Codrea V., Săsăran E., Van Itterbeeck J., Bultynck P., Csiki Z., Dica P., Fărcaş C., Folie A., Garcia G. & Godefroit P., 2002.A new exceptional vertebrate site from the Late Cretaceous of the Haţeg Basin (Romania). Studia Universitatis Babeş-Bolyai, Geologia, Special issue 1: 321–330.

Weishampel D.B, Grigorescu D. & Norman D.B., 1991. The Dinosaurs of Transylvania. National Geographic - Research and Exploration, 7: 196–215.

Middle–Late Miocene snakes from the Pannonian Basin

Marton VENCZEL1

1 Ţării Crişurilor Museum, B-dul Dacia 1-3, RO-410464 Oradea, Romania, e-mail: [email protected] Keywords: Serpentes, Miocene, Fossil record, Pannonian Basin

The fossil localities included in this study are situated on or adjacent to the former Pannonian Sea margins: Sámsonháza (MN 6), Mátraszőlős 1 and 2 (MN 7+8), Felsőtárkány-Felnémet (MN 7+8), Felsőtárkány 1, 2, 3/2, 3/8, 3/10 (MN 9) (N-Hungary), Subpiatră 2/1 (MN 6), Subpiatră 2/2 (MN 7+8), Tăşad 1 (MN 7+8) and Tauţ (MN 7+8) (W Romania). The fossil record of snakes from these deposits included both Scolecophidia and Alethinophidia (Boidae, Colubridae, Elapidae, Viperidae).

Indeterminable Scolecophidia were present in most localities, their remains consisting of trunk vertebrae only. They could probably belong to a single taxon which presumably was not very different from the only extant European component of this group, Typhlops vermicularis.

The only Boidae recorded from the studied localities is a small-sized Erycinae snake from Felsőtárkány 2 (Albaneryx volynicus). Biogeographically, the presence of the latter form in the Pannonian Basin represents an important link between the West-European and East-European members of the genus.

Colubridae is the most diversified group from the studied deposits, which includes a series of modern genera (e.g. Coronella, Elaphe, Hierophis and Natrix). ‘Coluber’ poucheti, a member of the “large-sized colubrines”, described for the first time from the Middle Miocene of Sansan (MN 6), apparently was largely distributed stratigraphically and geographically in both the western and eastern European areas as indicated by its presence in Felsőtárkány 3/2 and 3/10. On the contrary, Coronella sp., Hierophis cf. hungaricus and Natrix cf. rudabanyaensis were possibly newcomers from the Asiatic continent.

Within Elapidae only small members, resembling the North-American genus Micrurus, were recorded on the basis of vertebrae only.

Viperidae were documented most frequently by indeterminable venom fangs. The only member of the Oriental ‘vipers’ group (Macrovipera sp.), recorded on the base of a single large-sized vertebra, is known from Tauţ locality. The first occurrence of the genus Vipera from the ‘berus’ group is known from Felsőtárkány 1, 2 and 3/10 localities.

The snake faunas from the Middle–Late Miocene of the Pannonian Basin were already dominated by modern colubrids (Natricinae and Colubrinae). Apparently, the Scolecophidia and the vipers were constantly present in most deposits (even if less frequent, when compared to colubrids), whereas the Erycinae boids and elapids became extremely rare onward Late Miocene.



Insect-related traces associated to the Maastrichtian vertebrate assemblages of Alba-Iulia and Haţeg areas (Romania)

Matei M. VREMIR1

1 Weatherford, Weatherford House, Lawson Drive, Dyce, AB21 ODR, Aberdeen, UK ([email protected]) Keywords: Maastrichtian, Romania, terrestrial environments, insect traces

Insect body-fossils were not previously known from Maastrichtian deposits of Transylvania. Indirect evidence of insects’ activities associated to Late Cretaceous vertebrate assemblages are scarce and not well documented, the only such find being reported from the Middle Maastrichtian of Sânpetru, Haţeg Basin. The plain burrow within a sauropod dermal scute was interpreted as Dermestid-like larvae trace, the palaeoecological and taphonomical interpretation being made in analogy with recent Dermestidae. The problem risen by such simple morphology is that traces can be produced by a wide range of invertebrates, not always comparable with modern ones, sometimes leading to false paleoenvironmental interpretations.

Our procedure is based on analyses of a variety of insect traces, all associated within the same tapho-faciesal context. The combination of various insect traces and their comparison in analogy (when exists) with recent ones could improve the paleoecological and taphonomical interpretation; however the very limited knowledge on recent insect-related bone modifications (particularly in tropical environments), still render difficult an accurate explanation of the nature of the trace-markers and their physiological and ecological demands.

Some of the possible track marker saprophagous and osteophagous insects are represented by:

Lepidopteres (Tienidae moths) known from the Early Jurassic, some of the extant species being cherativorous (hair, feathers, carcasses or bird nests). They are present on carcasses in the late stage of decomposition (stage 5), having the ability to make shallow grooves on bones, immediately before the pupation stage. The marks are represented by 15 mm-long and up to 4 mm-wide trails.

Coleopteres (Dermestidae) known from the Late Eocene. The extant representatives have a saprophagous feeding habit on various substrates, including vertebrate carcasses and even living bird hatchlings. The larvae are burrowing in pupation chambers in sizes similar to the larva (up to 31 mm in length and slightly wider than the larva diameter). In the fossil record, numerous Dermestid-like traces were described world-wide, from Jurassic till the Pliocene.

Isopteres (Termites), known as body fossils from the Early Cretaceous. Generally, termites are not osteophagous, but in nutrient-poor environments they can suply their phosphorous-nitrogen and calcium demands from bones, leaving shallow-sinuous trails, surface-scretches, star-shape pit marks and sometimes subcortical cavities. Such behaviour is characteristic for subtropical nitrogene-poor carbonatic soil substrates.

Various insect-traces are now reported from Maastrichtian bone-assemblages of Alba Iulia-Sebeş and Haţeg area. Their main occurrence is within attritional assemblages, mainly in mature paleosols (in the calcic horizon), being always associated to other bioturbations. The frequency of such bone modifications is very



M.M. Vremir - Insect-related traces associated to the Maastrichtian vertebrate assemblages of Alba-Iulia and Haţeg areas

high compared to other assemblages, up to 20-30 % at Vurpăr, Dealul Cuptorului, Sebeş-Glod and Pui. The traces indicate both coleopteran dermestid-like, and isopteran termite-like markers, mainly feeding-traces but also pupation chambers. The main similarity in all reported vertebrate sites is the litho-faciesal and fossil assemblage where they occur, indicating similar conditions (long-term subaerial exposure; attritional-trempled taphocoenosis; low water table; not densly-vegetated environment, dry conditions etc.). Vurpăr site is a special case: insect traces are common in certain paleosol horizons, but they are missing from the pedogenised floodplains were partial dinosaur carcasses occur, suggesting rapid burial (flood) of skeletons and sediment-protection against necrophagous insects. One exception was recored at Oarda de Jos, where insect traces are associated to partially-destroyed Enanthiornithid bird nests. In this case, the ground nests were washed together within a small pond, where eggs, embryos, hatchlings and even adult birds were mixed into the fine calcareous-muddy sediment. The high organic content immediately attracted a large number of saprophagous insects, which consumed mainly the soft tissues and feathers (bones remain unaltered). The recognition of the trace-marker in this case is not very easy, both certain extant coleopterans and lepidopterans colonizing bird nests or even living heatchlings.

As preliminary conclusion, we have to note the limited applicability of insect-trace analyses in paleoenvironmental and/or taphonomical interpretations mainly because of the lack of consistent knowledge on extant analogies. A large variety of traces in the same context could help the better understanding of the processes and environment in which they were produced. The only chance to use such informations is to utilise them in agreement with all other available evidences gathered from tapho-faciesal analysis. REFERENCES Bahrensmeyer R. J., 1978. Taphonomic and ecologic informations from bone weathering.

Paleobiology, 4/2: 25-37. Csiki Z., 2006. Insect borings in dinosaur bones from the Maastrichtian of Hateg basin, Romania –

Paleoecologic and Paleoclimatic interpretation. In Z. Csiki (ed.). Mesozoic and Cenozoic Vertebrates and Paleoenvironments. Ed. Ars Docendi: 95-104.

Derry D. E., 1911.: Damage done to skulls and bones by termites. Nature, 86: 245-246. Fejer O. & Kaiser M, T., 2005. Insect Bone-Modification and Paleoecology of Oligocene Mammal-

Bearing sites in the Doupov Mountains, Western Bohemia. Paleontologia Electronica, 8/1, 8A: 1-11.

Kaiser M. T., 2000. Proposed Fossil Insect Modification to Fossil Mammalian Bone from Plio-Pleistocene Hominid bearing Deposits of Laetoli (Northern Tanzania). Annales of the Entomological Society of America, 93/4: 693-700.

Laudet F. & Antoine, P-O., 2004. Dermestidae (Insecta: Coleoptera) pupal chambers from Tertiary mammal bone (Phosphorites of Quercy): taphonomic and paleoenvironmental implications. Geobios 37: 376-381.

Martin L. D. & West D. L., 1995. The recognition and use of dermestid (Insecta, Coleoptera) pupation chambers in paleoecology. Palaeogeography, Palaeoclimatology, Palaeoecology, 113: 303-310.

Paik I. S., 2000. Bone chip-filled burrows associated with bored dinosaur bone in floodplain paleosols of Cretaceous Hasandong Formation, Korea. Palaeogeography, Palaeoclimatology, Palaeoecology, 157: 213-225.

Retallack G. J., 1984. Trace fossils of burrowing beetles and bees in an Oligocene Paleosol, Badlands National Park, South Dakota. Journal of Paleontology, 58/2: 571-592.

Roberts E. M., Rogers R. R. & Foreman B. Z., 2007. Continental insect borings in dinosaur bone: examples from the late cretaceous of Madagascar and Utah. Journal of Paleontology, 81/1: 201-208.

120

M.M. Vremir - Insect-related traces associated to the Maastrichtian vertebrate assemblages of Alba-Iulia and Haţeg areas

121

Rogers R. R., 1990. Taphonomy of three dinosaur bone beds in the Upper Cretaceous Two medicine Formation of northwestern Montana: evidence of drought related mortality. Palaios, 5: 394-413.

Rogers R. R., 1994. Non-marine borings in dinosaur bones from the Upper Cretaceous Two Medicine Formation, Northwest Montana. Journal of Vertebrate Paleontology, 12: 528-531.

Tappen M., 1994. Bone weathering in tropical rain forest. J. Archeol. Sci., 21: 667-673. Therrien F., 2005. Paleoenvironments of the Late Cretaceous (Maastrichtian) dinosaurs of Romania:

insights from fluvial deposits and paleosols of the Transylvanian and Hateg basins. Palaeogeography, Palaeoclimatology, Palaeoecology. 218/1-2: 15-56.

Late Cretaceous turtle diversity in Transylvanian and Haţeg basins (Romania)

Matei M. VREMIR1 & Vlad A. CODREA2

1 Weatherford, Weatherford House, Lawson Drive, Dyce, AB21 ODR, Aberdeen, UK ([email protected]) 2 Babes-Bolyai University, Department of Geology-Paleontology, 1 Kogǎlniceanu Str. 400084, Cluj-Napoca, Romania ([email protected]) Keywords: Maastrichtian, Transylvania, continental turtles

Late Cretaceous terrestrial turtle remains from Haţeg Basin (SW Rumania), had been reported for more than a century. A large number of specimens were mainly collected from the Lower-Middle Maastrichtian vertebrate localities Sânpetru and Vălioara (Kadic, 1916; Nopcsa, 1923a; Szalai 1934). Based on these discoveries, a distinct primitive and endemic taxon was described in detail (Nopcsa, 1923a, b, Gaffney & Meylan, 1992). Up to recently, it concerned a single genus, Kallokibotion NOPCSA, 1923. In the last decades, new sites had been found and this genus was reported outside the Haţeg Basin too, in the Maastrichtian deposits of Sebeş-Alba, Rusca Montană and possibly, Jibou area (Codrea & Vremir, 1997; Vremir, 2004, Codrea & Godefroit, 2008).

The most recent research, based on older and new fossils, suggested also the presence of some additional turtle taxa, including a pleurodiran too (Vremir, 2001, 2004). Such “non-kallokibotionid” materials were unearthed from various Maastrichtian localities, from the Haţeg Basin (Pui, Sânpetru, Vălioara), and particularly from Sebeş-Alba area (Vurpăr, Teleac, Oarda de Jos, Lancrăm, etc.).

According to the current state of knowledge, at least three different turtle taxa can be reported from the Late Cretaceous (Campano-Maastrichtian) deposits from Transylvania.

1. The most widespread and well documented species is Kallokibotion bajazidi NOPCSA, 1923A, a primitive crypto Iran. In his second contribution on this topic, Nopcsa (1923b) already distinguished two species: K. bajazidi and K. magnificum. The later one differs from the type species by its narrow nuchal, narrower vertebral scutes, rather short intergulars and midline-connected mesoplastra. According to Gaffney & Meylan (1992), such differences (if they really exist) have to be considered as intraspecific variations. Thus, K. magnificum was considered a junior synonym of K. bajazidi. However, these conclusions were based only on the fossil rests curated at the British Museum (Natural History collection). These specimens are dissociated and most of them poorly-preserved - particularly the exoskeletal parts, therefore important features remained not revealed. In such circumstances, it was impossible to observe the differences between the two species, even on the type materials. New articulated and well preserved specimens were recently collected from Haţeg Basin (Toteşti, Nălaţ-Vad, Sânpetru areas). The endemic cryptodiran Kallokibotion was a medium- to large-sized (shell length up to 60 cm) semiaquatic-terrestrial form, widely spread during the whole Maastrichtian, being reported from several localities and stratigraphic units in Haţeg, Rusca Montană and Transylvanian basins. Its presence outside Romania is not supported yet, it still represents a rather enigmatic component of the Maastrichtian terrestrial vertebrate faunas of Europe.



M.M. Vremir & V.A. Codrea - Late Cretaceous turtle diversity in Transylvanian and Haţeg basins (Romania)

2. A new Upper Cretaceous fresh-water Dortokid-pleurodiran turtle is reported from the continental deposits of SW Transylvania and Haţeg basin. The first presence of a Dortokid-like taxon was recorded by Vremir (2001, 2004) from Vurpăr (Sebeş-Alba). Scarce, but rather well-preserved specimens were also collected from several other Lower-Middle Maastrichtian vertebrate localities of Alba Iulia and Sebeş region (i.e. Oarda de Jos, Lancrăm, Teleac etc.) as well as from Pui, in Haţeg Basin. This small-sized pleurodire is now assigned to a new dortokid species: Muehlbachia nopcsai (type: partial plastron with associated carapace fragments from Vurpăr), exposing a mixture of morphological features placing it between the Upper Cretaceous south-western European genus Dortoka LAPPARENT DE BROIN & MURELEGA, 1996 and the Romanian Upper Paleocene genus Ronella LAPPARENT DE BROIN, 2000. The family Dortokidae is an exclusive European endemic group of Pleurodires, exposing a series of morphologic features discussed in detail by Lapparent de Broin & Murelaga (1999) and Lapparent de Broin et al. (2004). The new taxon Muehlbachia nopcsai is a small-sized aquatic pleurodiran form, which is rather common in the Lower-Middle Maastrichtian fluvio-lacustrine deposits of Sebeş-Alba, but excepting Pui unknown from the other localities of the Haţeg Basin. This new taxon is of particular interest from paleobiogeographical viewpoint. During the Maastrichtian-Paleocene/Early Eocene, the Trasylvanian landmass acted as refuge area for this peculiar group of European endemic fresh-water pleurodiran turtles.

3. A second small-sized form is reported from the Lower-Middle Maastrichtian deposits of Sânpetru (Haţeg Basin), a fossil probably collected by Nopcsa himself in 1904 (MAFI Ob. 1949/1). This small specimen (shell length approx. 12-13 cm) was previously described and illustrated by Mlynarski (1966) as belonging to genus Pleurosternon Owen, 1853. However, in his description (op. cit. p. 241), the carapace fragment was inversed in antero-posterior direction, exposing neurals 1-8, a fragment of preneural and pleurals 1-7. Actually, the specimen lacks the anterior part, exhibiting neurals 2-8, two suprapygals (2nd one incomplete), and pleurals 1-8 (the 1st

preserved in a small section only). This specimen is characterised by reversed anterior neurals (Ne 2-4), which represent a primitive and homoplastic character (Lapparent de Broin & Murelega, 1999) known in primitive pleurodires and some cryptodires (e.g. Helochleydra). However, the bony sutures are well-expressed, the scutes are more obscured, chiefly because part of the carapace is eroded or preserved only as internal mould. On the caudal part of the carapace, at the level of the 6th neural, the very long intervertebral suture (V 3-4) can be noticed, suggesting wide vertebral scutes (like on Hylaeochelys, unlike Pleurosternon, both from the Purbeck of England). The possible juvenile stage, some of the morphological features and the very peculiar microreticulated-tuberculed decoration of the carapace, marked also by a longitudinal ridge on the wide neural series, suggest the assignment to the family Solemydidae LAPPARENT DE BROIN & MURELEGA, 1996, rather primitive aquatic cryptodires. The Solemydids are well-documented from the Late Cretaceous of Western Europe (Lapparent de Broin & Murelega, 1999; Milner, 2004). Certainly we have to deal with a peculiar form close to the Purbeckian Helochelydra NOPCSA, 1928; however, the lack of plastral remains makes difficult any further comparison. Some Solemydid-like decorated fragments were collected from the Maastrichtian of Pui and Sebeş-Alba as well. We have to notice the presence of similar finds from Santonian terrestrial deposits of Iharkut-Hungary and Campanian of Gosau-Austria (Rabi Marton, ELTE Budapest, written communication). Allocation to Solemydidae indet. (aff. Helochelydra sp.) is appropriate, since the closely-related Pleurosternidae are known from the Late Jurassic-Early Cretaceous only. All other Pleurosternon specimens

123

M.M. Vremir & V.A. Codrea - Late Cretaceous turtle diversity in Transylvanian and Haţeg basins (Romania)

124

described by Mlynarski (1966) from the Maastrichtian of Sânpetru (MAFI Ob.1949/2, Ob.4007-4008 and Ob.3142,), belong to Kallokibotion. REFERENCES

Codrea V. & Vremir M., 1997. Kallokibotion bajazidi Nopcsa (Testudines, Kallokibotidae) in the Red

Strata of Râpa Roşie – Sebeş (Alba county). Sargetia, Acta Musei Devensis, ser. Sci. nat., 17: 233–8.

Codrea V. & Godefroit, P., 2008. New Late Cretaceous dinosaur findings from northwestern Transylvania (Romania). C. R. Palevol, 7: 189-295.

Gaffney, E. S. & Meylan, P. A., 1992. The Transylvanian turtle Kallokibotion, a primitive Cryptodire of Cretaceous age. American Museum Novitates, 3040: 1-37.

Kadic O., 1916. Jelentés az 1915, évben végzett ásatásaimról: II A valiorai dinosaurusok gyűjtése. A Magyar Kiralyi Földtani Intezet Évi jelentése 1915: 573–576.

Koch A., 1900. A Magyar Korona országainak kövült gerincesállat maradványainak rendszeres átnézete. A Magyar Orvosi és Természettudományi Vizsgálatok Munkálatai : 1-538.

Λαππαρεντ δε Βροιν Φ. & Μυρελεγα Ξ., 1999. Τυρτλεσ φρομ τηε Υππερ Χρεταχεουσ οφ Λανο (Ιβεριαν πενινσυλα). Εστ. Μυσ. Χιενχ. νατ. δε Αλαϖα, 14 νομ. σπεχ. 1: 135−211.

Λαππαρεντ δε Βροιν, Φ., Μυρελεγα Βερεικυα, Ξ. & Χοδρεα, ς., 2004. Πρεσενχε οφ Δορτοκιδαε (Χηελονιι, Πλευροδιρα) ιν τηε εαρλιεστ Τερτιαρψ οφ τηε ϑιβου Φορματιον, Ρομανια: παλαεοβιογεογραπηιχαλ ιμπλιχατιονσ. Αχτα Παλαεοντολογιχα Ρομανιε, 4: 203−215.

Μιλλνερ Α. Ρ., 2004. Τηε Τυρτλεσ οφ τηε Πυρβεχκ Λιμεστονε Γρουπ οφ Δορσετ, Σουτηερν Ενγλανδ. Παλαεοντολογψ, 47 /6: 1441−1467.

Mlynarski M., 1966. Die fossilen Schildkröten in dem Ungarischen Sammlungen. Acta Zoologica Cracoviensia, 11/8: 223–88.

Nopcsa F. von, 1897. Vorlaufiger Bericht über das Auftreten oberer Kreide im Hatszeger Tale in Siebenbürgen. Verheindlung der Kaiserlischen und Königlischen Geologischen Reichs Anstalt, 1-247.

Nopcsa F. von, 1923a. On the geological importance of the primitive reptilian fauna in the Uppermost Cretaceous: with a description of a new tortoise (Kallokibotion). Quarterly Journal of the Geological Society, 79/1: 100–116.

Nopcsa F. von, 1923b: Kallokibotion, a primitive amphychelidean tortoise from the uppermost Cretaceous of Hungary. Paleontologia Hungarica, 1/1, pp. 1–34, Budapest.

Νοπχσα Φ. ϖον, 1928. Ηελοχηελψδρα ανδ Ηψλαεοχηελψσ, τωο λιττλε κνοων τορτοισεσ φρομ τηε Ωεαλδεν ανδ Πυρβεχκ Φορματιονσ. Γεολογιχα Ηυνγαριχα, σερ. Παλαεοντολογια, 1 /1: 44−50.

Szalai T., 1934. Die fossilen schildkröten Ungarns. Folia Zoologica et Hydrobiologica, 6/2: 97–192. Vremir M., 2001. Palaeontology, Palaeoecology and Taphonomy of the Late Cretaceous

macrovertebrates of Alba Iulia – Sebes area (Transilvania). Babes Bolyai University, Cluj-Napoca; MSc Thesis (in Romanian, unpublished).

Vremir M., 2004. Fossil Turtle found in Romania - overview. A Magyar Földtani Intézet Évi Jelentése, 2002 (2004): 143-152.

A giant Azhdarchid (Reptilia, Pterosauria) and other Upper Cretaceous reptiles from Râpa Roşie - Sebeş (Transylvanian basin, Romania) with a reassessment of the age of the “Sebeş Formation”

Matei M. VREMIR1, Dave M. UNWIN2 & Vlad A. CODREA3

1 Weatherford, Weatherford House, Lawson Drive, Dyce, AB21 ODR, Aberdeen, UK ([email protected]) 2 University of Leichester, 103-105 Princess Road, East Leichester LE1 7LG, UK ([email protected]) 3 Babeş-Bolyai University, Dept. Geology-Palaeontology, 1 Kogălniceanu Str., 400086 Cluj-Napoca, ([email protected])

Keywords: Maastrichtian, Transylvania, Azhdarchid, vertebrate assemblage, stratigraphy

Cretaceous pterosaur remains are extremely scarce in Romania. Lower Cretaceous

(Berriasian-Valanginian) fossils (mainly limb bones) were found at Cornet (Bihor district) belonging mainly to Ornithocheiridae indet. and to a small Dsungaripterid (Jurcsák & Popa 1984; Benton et al, 1997). The finds in Late Cretaceous (Maastrichtian) are even rarer. Few Ornithocheirid remains (notaria, humerus, femur) are reported from the early-middle Maastrichtian of Sânpetru in Haţeg basin (Nopcsa 1914, 1923; Jianu et al. 1997). A new giant Azhdarchid (Hatzegopteryx thambema) was described from the Middle? Maastrichtian of Vălioara in Haţeg basin (Buffetaut et al. 2002). An incomplete small sized wing-phalang (wp2?) was recently unearthed from the Maastrichtian of Boiţa (Haţeg) too (VM unpubl.). In Sebeş-Alba region, only two remains can be assigned to pterosaurians: an incomplete and heavily crushed forelimb bone fragment (possibly the ? IVth Metacarpus shaft) belonging to a large-sized form originating from the Upper Campanian/Lower Maastrichtian brackish-coastal facies of Petreşti-Sebeş, but also a very large cervical vertebra from the Middle-Late Maastrichtian of Râpa Roşie-Sebeş.

An almost complete vertebra of a giant pterosaur is reported now, originating from the so-called “Sebeş Formation” (informal name) at Râpa Roşie (Alba district, Transylvania). The specimen is identified as third cervical, and was found in situ and associated with other well-preserved vertebrate remains, including hadrosaurs (Telmatosaurus), sauropods, turtles (Kallokibotion) and crocodiles. The bones were collected from chanell-fill deposits (coarse sand and gravel), located in the upper section of the outcrop. Their para-autochtonous status is demonstrated by the reasonably good state of preservation and completeness, particularly of the pterosaur vertebra which is delicate and has very thin compacta. Any possibility of reworking from older formations (e.g. Vurpar or Şard Formations) is therefore excluded. In such circumstances, the Oligo-Miocene age of the “Sebeş Formation” cannot be supported and this sediment accumulation must be redated as Maastrichtian.

The cervical vertebra is largely complete and distinguished by its very large size. The remarkably thin cortical bone and general anatomy of the specimen clearly demonstrate that this is a pterosaur vertebra; comparison with other Late Cretaceous pterosaurs: Phosphatodraco (Pereda-Suberbiola et al. 2003); Azhdarcho (Nesov 1984; Bakhurina & Unwin 1995) and Zhejiangopterus (Cai & Wei 1994) indicate that it is most likely the third cervical. The vertebra is uncrushed and largely undistorted, but lacks the dorsal tip of the neural spine, the terminus of the left prezygapophysis, the entire left postzygapophysis and the condylar region. The neural spine appears to have been robust, but relatively low and divided into anterior and posterior portions




M.M. Vremir et al. - A giant Azhdarchid (Reptilia, Pterosauria) and other Upper Cretaceous reptiles from Râpa Roşie - Sebeş

by a distinct mid-length gap. The zygapophyses are short and remarkably stout. The prezygapophysial facet is oval, gently convex and faces dorsally and somewhat anteriorly. The postzygapophysial facet is more sub-circular and faces posteriorly and slightly ventrad. The neural arch is confluent with the centrum throughout its length. The transverse foraminae are well developed and enclosed ventrally by vestigial cervical ribs. These are completely fused to the centrum indicating that this individual had reached osteological maturity. The neural canal consists of an ossified tube suspended within a web of cancellous bone. The anterior opening of the neural canal is flanked on either side by a sub-circular pneumatic foramen. The general similarity of this vertebra to the third cervical of azhdarchids and the presence of characters (confluency of the neural arch and centrum) unique to, or almost exclusive (pneumatic foraminae flanking the neural canal, neural spine subdivided into cranial and caudal portions) to Azhdarchidae provide strong support for the assignment of the specimen to this family (Witton 2008; Witton & Naish 2009). The absence of comparative material does not allow us to determine whether this specimen belongs to the giant pterosaur Hatzegopteryx (Buffetaut et al., 2002, 2003), also known from the Late Cretaceous of Romania, although we note that the Sebeş azhdarchid seems to be quite distinct from Quetzalcoatlus (DMU pers obs), Phosphatodraco (Pereda-Suberbiola et al. 2003) and Zhejiangopterus (DMU pers obs).

With an estimated original length of 0.3 m and a maximum width, measured across the prezygapophyses, of 0.226m, this is the most massive vertebra known for any pterosaur. Preliminary comparative studies suggest that it was substantially larger than either of the giant individuals of Quetzalcoatlus (Lawson 1975; Langston 1981) and Hatzegopteryx (Buffetaut et al. 2002, 2003) which have an estimated forelimb length (x2) + body-width of around 10 m (Witton & Naish 2008). Combined with other finds from Romania, Spain (Company et al. 2001) and the USA, the Sebeş azhdarchid provides further support for the idea that these giant pterosaurs were not accidental freaks that achieved exceptionally large size, but were typical components of Latest Cretaceous vertebrate biotas. This new record is also consistent with the observation that azhdarchids completely dominated Campanian-Maastrichtian pterosaur faunas (Unwin 2005) and achieved considerable taxonomical, morphological (and possibly) ecological diversity (Witton 2008; Witton & Naish 2009).

From a geological point of view, the continental “red beds” exposed in the Alba Iulia – Sebeş area, belong to several distinct lithostratigraphic units. The main exposures can be followed between Şard-Teleac (North) and Vurpăr-Petreşti-Cacova (South) in the Mureş valley (Alba district). Since the end of the 19th century, the age of the red beds was controversial. Their age has been reported to be either Oligo-Miocene (Koch 1894; Palfy 1902, 1905; Roth 1904; Halavats 1906), or Late Cretaceous (Nopcsa 1905, 1909). Until recently, few studies have succeeded in solving this stratigraphical problem (for an overview see Codrea et al. 2003, 2008b). Grigorescu (1987) conducted a paleontological and taphonomical analysis on a few vertebrate remains that originated from the red beds of this area, and proposed a Late Cretaceous age for the lowermost section of the continental deposits in the Vurpar area, and Oligocene up to Lower Miocene age for the “Sebeş Formation” on the left flank of Mureş Valley. Later, conclusive evidence for an Upper Cretaceous age of the “lower red-beds” on the left side of Mureş river was issued by Codrea et al. (2001) and Vremir & Codrea (2002).

126


Two recent studies (Codrea et al. 2003; Codrea & Dica 2005), proposed a new stratigraphical scheme. According to this new model, two Late Cretaceous (Maastrichtian) continental formations can be recognized in the area, both of them yielding vertebrate remains. The underlying unit is represented by the Vurpăr Formation (VPF), which is lowermost Maastrichtian, while the overlying unit is represented by the Şard Formation (SDF), which is Middle Maastrichtian up to (?)Priabonian. In addition, two other red bed formations were redefined in Alba Iulia - Sebeş area: the Barabanţ Formation (BTF) - named by Koch (1894) as the “Sard-Borband red clays”, Oligocene in age and exposed N-NW of Alba Iulia; and the Sebeş Formation (SBF) dated as Upper Oligocene to Middle Miocene in age (Grigorescu 1992; Givulescu et al. 1996; Codrea & Dica 2005, Codrea et al. 2008a), and well developed between Teleac and Sebeş localities on the left side of the Mureş Valley. However the BTF lacks any fossils, while the SBF is long-known (Koch, 1894; Nopcsa, 1905) for fossil vertebrates belonging exclusively to supposedly reworked Late Cretaceous reptiles (Grigorescu 1987; Codrea & Vremir 1997; Jianu et al. 1997a; Codrea et al. 2008a).

In the light of the most recent field investigations and new data acquisition, this current stratigraphic model also requires revision, in particular regarding the relationship between the Maastrichtian VPF-SDF complex, and the “Oligo-Miocene” SBF. Investigation and collection of new outcrops that yielded well preserved vertebrate fossils suggest, in contrast to all previous oppinions, a Maastrichtian age for the Sebeş Formation. In this respect, the informal “Sebeş Formation” must be distinguished within the newly-defined Şard Formation as a more energetic alluvial facies, however with a different source area. REFERENCES

Antonescu E., 1973. Asociaţii palinologice caracteristice unor formaţiuni cretacice din Munţii

Metaliferi. Dări de seamă ale şedinţelor, LIX (1973), 3. Paleontologie: 115-169. Antonescu E., Lupu D., Lupu M., 1983. Corrélation palynologique du Crétacé terminal du Sud-Est des

Monts Metaliferi et des depressions de Haţeg et de Rusca Montană. Anuarul Institutului de Geologie şi Geofizică, LIX: 71-77.

Bakhurina N. N. & Unwin, D., M. 1995. A survey of pterosaurs from the Jurassic and Cretaceous of the former Soviet Union and Mongolia. Historical Biology, 10: 197-245.

Buffetaut E., Grigorescu D. & Csiki Z., 2002. A new giant pterosaur with a robust skull from the latest Cretaceous of Romania. Naturwissenschaften, (2002.) 89: 180-184.

Buffetaut E.,Grigorescu D. & Csiki, Z., 2003. Giant azhdarchid pterosaurs from the terminal Cretaceous of Transylvania (western Romania). In: Buffetaut, E. & Mazin, J.-M. (eds), Evolution and Palaeobiology of Pterosaurs. Geological Society of London, Special Publication, 217: 91-104.

Zhenquan C. & Feng W., 1994. On a new pterosaur (Zhejiangopterus linhaiensis gen. et sp. nov.) from Upper Cretaceous in Linhai, Zhejiang, China. Vertebrata Palasiatica, 32: 181-194.

Codrea V. & Vremir M., 1997. Kallokibotion bajazidi Nopcsa (Testudines, Kallokibotidae) in the red strata of Râpa Roşie (Alba County). Sargetia 17: 233-238.

Codrea V., Hosu Al., Filipescu S., Vremir M., Dica P., Săsăran E. & Tanţău I., 2001. Aspecte ale sedimentaţiei cretacic superioare din aria Alba-Iulia – Sebeş (jud. Alba). Complexul Muzeal judeţean Bistriţa-Năsăud, Studii şi cercetări, Geologie-Geografie, 6: 63-68.

Codrea V., Dica P., Fărcaş C. & Barbu O., 2003. Late Cretaceous-Early Miocene formations from Alba Iulia – Sebeş area (Transylvanian Depression, Alba district). Oltenia, Studii şi comunicări, Ştiinţele naturii, XIX: 22-27.

Company J., Unwin D.M., Ruiz-Omenaca J.I. & Pereda-Suberbiola, X., 2001. A giant azhdarchid pterosaur from the latest Cretaceous of Valencia, Spain - the largest flying creature ever? Journal of Vertebrate Paleontology, 21 (Suppl. to 3), 41A-42A.

127


128

Dimian M.& Popa-Dimian E., 1963. Date stratigrafice şi sedimentologice privind formaţiunile cretacice dintre Valea Mureşului şi Valea Ampoiului. Dări de Seamă ale Şedinţelor, L/1 (1962-1963): 107-130.

Gherman I., 1943. Cercetări geologice în colţul de SW al Depresiunii Transilvaniei (între Valea Stremţului şi Valea Ampoiului). Revista Muzeul Mineralogic-Geologic al Universităţii din Cluj la Timişoara, VII, 1-2: 1-110, Sibiu.

Grigorescu D., 1987. Considerations on the age of the “Red Beds” continental formations in SW Transylvanian Depression. In : The Eocene from the Transylvanian Basin (I. Petrescu, L. Ghergari, N. Mészáros, E. Nicorici Eds.): 189-196, Cluj-Napoca.

Grigorescu D., 1992. Nonmarine Cretaceous formations of Romania. In: Aspects of Nonmarine Cretaceous Geology (Mater N.J. & Chen P.-J. eds): 142-164.

Ilie M., 1943. Asupra răspîndirii depozitelor eocene în vecinătatea oraşului Alba-Iulia. Revista Fundaţiei Adamachi, XXXIX/3-4: 305-306.

Ilie M., 1959. Recherches géologiques dans le Bassin de Transylvanie (II. Région Alba Iulia-Sibiu Făgăraş-Rupea). Annuaire du Comité géologique, XXVI-XXVIII: 269-292.

Jianu C. M., Mészàros N. & Codrea V., 1997. A new collection of Haţeg and Râpa Roşie material (Dinosauria, Crocodilia, Chelonia) in the Cluj-Napoca University. Sargetia 17: 219-232, Deva.

Koch A., 1894., Die Tertiärbildungen des Beckens der Siebenbürgischen Landestheile. I. Paläogene Abtheilung. Mitteilungen aus den Jahrbuch der Kön. Ungarische Geologischen Anstalt, X, 6: 177-399.

Koch A., 1900. Az Erdélyrészi medencze harmadkori képződményei. II. Neogen csoport. Fóldtani Intezet Évkonyve, 329 p.

Lawson D. A., 1975. Pterosaur from the latest Cretaceous of West Texas: discovery of the largest flying creature. Science, 187: 947-948.

Langston W. Jr., 1981. Pterosaurs. Scientific American, 244(2): 122-136. Mészáros N., Băluţă C. & Speck, R., 1969. Stratigrafia şi fauna de moluşte a depozitelor paleogene din

regiunea Alba Iulia. Buletinul Societăţii de Ştiinţe Geologice din R.S. România, XI: 311-320. Nopcsa F. von, 1905. A Gyulafehérvár, Déva, Ruszkabánya és a Romániai határ közé eső vidék

geológiája. A magyar Királyi földtáni Intézet Évkonyve., XIV: 82-254. Pálfy M., 1902. Die oberen Kreideschichten in der Umgebung von Alvincz. Mitteilungen aus dem

Jahrbuche der Königliche Ungarischen Geologischen Anstalt, XXIII, 6: 243-348. Nesov L. A., 1984. Pterozavryi i ptitsyi pozdnyevo myela sryednyei Azii. Paleontologicheskii Zhurnal

1984, 47-57. [Pterosaurs and birds from the Late Cretaceous of central Asia. Paleontology Journal pp. 38-49.]

Pereda-Suberbiola X., Bardet N., Jouve S., Iarochène M., Bouya B. & Amaghzaz M. 2003. A new azhdarchid pterosaur from the Late Cretaceous phosphates of Marocco. In: Buffetaut, E. and Mazin, J.-M. (eds), Evolution and Palaeobiology of Pterosaurs. Geological Society of London, Special Publication, 217: 79-90.

Unwin D. M., 2005. The Pterosaurs from Deep Time. Pi Press, New York, 347pp. Witton M. P., 2007. Titans of the skies: azhdarchid pterosaurs. Geology Today, 23(1): 33-38. Witton M. P. & Naish D. 2008. A reappraisal of azhdarchid pterosaur functional morphology and

paleoecology. PLoS ONE 3(5): e2271 doi:10.1371/journal.pone.0002271. Vremir M. & Codrea, A., V., 2002. The first Late Cretaceous (Maastrichtian) dinosaur footprints from

Transylvania (Romania). Studia Universitatis Babeş-Bolyai, Geologia, 2: 27-36.

MIDDLE MIIOCENE RED ALGAE FROM THE WESTERN BORDER OF THE TRANSYLVANIAN BASIN

1

STOP 1

MIDDLE MIOCENE RED ALGAE FROM THE WESTERN BORDER OF THE

TRANSYLVANIAN BASIN

Ioan I. BUCUR1 & Sorin FILIPESCU

1

The sedimentary formations from the western part of the Transylvanian Basin

consist of Badenian (Middle Miocene) marine formations. The Lower Badenian

predominantly carbonate deposits were separated as Gârbova de Sus Formation

(Filipescu, 1996; Filipescu & Gârbacea, 1997). At Lopadea Veche, the largest part

of this carbonate sequence has a nodular aspect due to the fine sediment in which

most of the algal crusts are included.

LOCATION: Buhii Creek, near Lopadea Veche village, about 5 km west of the

European road E60, between Turda and Aiud (Fig.1).

1 “Babeş-Bolyai” University, Department of Geology. Str. Kogălniceanu 1, RO-3400 Cluj-Napoca,

Romania

Figure 1 – Location of the stop 11 (Lopadea Veche). 1. Jurassic volcanics; 2. Garbova de Sus Formation (Early - Middle Badenian); 3. Cheia Formation (Middle Badenian); 4. Mahaceni Formation (Sarmatian); 5. Lopadea Formation (Pannonian); 6. Quaternary deposits

FIELD TRIP A

IOAN I. BUCUR & SORIN FILIPESCU

2

Figure 2 – Succession of the Garbova de Sus Formation on Buhii Creek (Lopade Veche); 1. “Ophiolithe” (?) complex; 2. Conglomerates; 3. Nodular limestones; 4. Bioclastic limestones; 5. Rhodolithic bearing levels; 5. Large rhodoids.

SUCCESSION AND FACIES: The whole succession

consists of about 30 m nodular limestones, with

intercalations of bioclastic, more compact

limestone banks (Fig.2). At the upper part, a

distinct level of large (10-15 cm in diameter)

rhodoliths is present. The nodules are

predominantly made of lamellar, mamelonar or

spheroidal crusts of red algae within the whole

succession. Beside algae, bryozoans and

encrusting foraminifera of Miniacina type also

contribute to the crust formation. Branch

fragments of coralline algae of variable size, from

a few mm to 1 or 2 cm length, can be observed in

relative abundance within the marly

intercalations.

The stop focus on the rhodolithic level in the

upper part of the succesiion (Fig.3), about 1,5 m

thick. The rhodoliths are considered good

paleoenvironmental indicators. Montaggioni

(1979) defined some characteristics for rhodoliths

formed in shallow and/or calm waters, as well as

for rhodoliths in deep and/or high-energy waters.

The same principles were used by Braga &

Martin (1988) in the study of some Miocene

rhodoliths from Spain. Rhodoliths from Lopadea

section consists of crusts developed around a

nucleus. Several algal genera and species

contribute to their formation, but bryozoans and

encrusting foraminifera are also present. These

features are, according to Montaggioni (1979),

characteristic for deep-water rhodoliths. For

similar deposits, Studencki (1988) acknowledges

a maximum depth of 50 to 80 m, emphasising

that the greatest part of the rhodolith algal-

bryozoan facies were situated at depths around

MIDDLE MIIOCENE RED ALGAE FROM THE WESTERN BORDER OF THE TRANSYLVANIAN BASIN

3

Figure 3 – Detailed succession near the top of the Garbova de Sus Formation on Buhii Creek. 1. shales; 2. nodular limestones; 3. sandy-limestones; 4. rhodoliths-bearing bioclastic limestones; 5. large rhodoids

30 m. In Lopadea section the

foraminifera assemblages suggest

only shallow waters, with a

maximum depth of several metres."

ALGAL ASSEMBLAGE: Bucur &

Filipescu (1994) determined the

following species of red algae from

Garbova de Sus Formation:

Sporolithon lvovicum MASLOV,

Palaeothamnium archaeotypum

CONTI, Lithothamnion moretti

LEMOINE, Lithothamnion

praefruticulosum MASLOV,

Lithothamnion cf. gaviense

FRAVEGA et al., Lithothamnion cf.

lacroixi LEMOINE, Mesophyllum

roveretoi CONTI, Mesophyllum cf.

koritzae LEMOINE, Mesophyllum cf.

vaughani (HAWE), Lithophyllum

ramoississimum (REUSS),

Lithophyllum cf. praelichenoides

LEMOINE and Spongites albanense (LEMOINE).

As many discussions arose in the literature regarding the specific determination

of the Tertiary red algae species, we think that a genus level identification would be

generally enough for our purposes. Plates 3 to 5 illustrate the most significant red

algae recorded in the Lopadea Veche section: Sporolithon sp., Peyssonnelia sp.,

Mesophyllum sp., Lithoporella sp, Lithothamnion sp., Lithophyllum sp.,

Palaeothamnium sp., Spongites sp.. The rhodoliths from the upper part of the

section are made up of successive crusts of red algae, bryozoans and Miniacina

forams. The specific variety of algae participating to a rhodolith construction is not

very large. Mostly, two or three species, belonging frequently also to different

genera, produced each rhodolith. Lithothamnion, Mesophyllum and Spongites are

the main participants.

IOAN I. BUCUR & SORIN FILIPESCU

4

REFERENCES

Braga, J.C. & Martin, J.M (1988) – Neogene coralline-algal growth forms and their

paleoenvironments in the Almanzora River Valley (Almeira, SE Spain). Paleogeogr., Paleoclimatol., Paleoecol., 67, p.285-303, Amsterdam.

Bucur, I.I. & Filipescu, S. (1994) – Middle Miocene red algae from the Transylvanian Basin (Romania). Beiträge zur Paläontologie, 19, p.39-47, Wien.

Filipescu, S. (1996) – Stratigraphy of the neogene from the western border of the Transylvanian Basin. Studia Univ. babeş-Bolyai, Geologia, 41/2, p.3-77, Cluj-Napoca.

Filipescu, S., Gîrbacea, R. (1997) - Stratigraphic Remarks on the Middle Miocene deposits from Gârbova de Sus (Transylvanian Basin, Romania). Studia Univ. Babeş - Bolyai, Ser. Geologia - Geographia, 1-2/1994, 275 -286. Cluj-Napoca.

Montaggioni, L.F. (1979) – Environmental significance of rhodolites from the Mascarene reef province, Western Indian Ocean. Bull. Centr, Rech. Explor. Peod. Elf-Auitaine, 3/2,

p.713-723, Pau.

Studencki (1988) – Red algae from the Pinczow limestones (Middle Miocene, Swietokrzyskie Mountains, Poland). Acta Palaeontologica Polonica, 33/1, p.3-57, Warszawa.

MICROBIALITES AND CALCAREOUS ALGAE FROM CHEILE TURZII AREA

5

STOP 2

UPPER JURASSIC-LOWER CRETACEOUS MICROBIALITES AND CALCAREOUS

ALGAE FROM THE STRAMBERK-LIKE LIMESTONES IN CHEILE TURZII AREA

Emanoil SĂSĂRAN1 & Ioan I. BUCUR

1

The limestones in Cheile Turzii area belong to the Bedeleu Nappe, which is a

component of the Transylvanides. The Bedeleu Nappe consists of a basal

“ophiolitic” complex (keratophires and calkalkaline rocks associated with jaspers)

belonging to the tehyan suture. This complex is averlayed by carbonate rocks of

Oxfordian-Tithonian age, locally followed by Neocomian limestones. For geological

setting see p. 29

The “ophiolitic” complex in Cheile Turzii area is represented by pyroclastites

(breccias, rhyolitic agglomerates and tuffs), alternating with lava flows. The Upper

Jurassic-Lower Cretaceous limestones represent the northern ending of the

Trascău Mountains. In Cheile Turzii area these limestones overlies a magmatic arc

and were separated into two units (Dragastan et al., 1987): Sănduleşti Formation

and Petridu Formation (Fig.1)

2A

LOCATION: Cheile Turzii (Trascău Mountains) in the basal part of the Stramberk-

type limestones

AGE: Late Jurassic.

SUCCESSION AND FACIES. Overlaying the island arc complex, a ruditic melange of

limestone and “ophiolite” fragments develops 6 to 8 meters in thickness. The

limestone pebbles are subangular to subrounded and are up to 20-25 cm in size,

while the “ophiolite” pebbles are dominant subangular. The matrix contains

1 “Babeş-Bolyai” University, Department of Geology. Str. Kogălniceanu 1, RO-3400 Cluj-Napoca,

Romania

EMANOIL SĂSĂRAN & IOAN I. BUCUR

6

subangular to subrounded carbonate fragments, coral, mollusc, and echinoderm

bioclasts as well as extraclasts represented by “ophiolite” fragments, quarz and

feldspar.

Figure 1 – Sedimentological log through the limestones in Cheile Turzii area.


7

Figure 2 – Sedimentological log of the lower part of Sănduleşti Formation in stop 12 A.

The first deposits in the succession accumulated directly on the top of the island

arc, as a consequence of a significant decrease in the accomodation space This

context favoured the erosion of a pre-existing carbonate platform, including its

substrate represented by the island arc. The result was the formation of an

unconformity (SB1). Thus, a large amount of clastic carbonate and magmatic

material was reworked and transferred towards the basin. The material

accumulated as slope facies attributed to the lowstand fan. The reduced degree of

reworking of the magmatic clasts and the abundance of fresh feldspars, in

comparison with the well-rounded, platy sedimentary pebbles, as well as the

presence of small patch reefs suggest the accumulation of the fans in the vecinity

of the platform margin.

Two main microfacies were identified within the carbonate pebbles:

1. Coralgal boundstones with

algae, forams (Troglotella incrustans

WERNLI & FOOKES), and crusts of

probably microbial origin. The

sediment between the corals contains

sponges, mollusc and echinoderm

fragments, agglutinated forams and

miliolids.

2. Bioclastic peloidal

grainstone/packstone with forams

(Mohlerina basiliensis (MOHLER),

Andersenolina sp., miliolids), coral and

echinoderm fragments. (Săsăran et

al., 2000)

A succession of about 15 m thick

bioacumulated limestone formed on

the top of the submersed fans (Fig.2).

The lower part of the deposit is

characterized by bioclastic facies,

while towards the upper third the

oolitic one becomes dominant. Bodies

of bioclastic grainstones/packstones

with algae, forams, fragments of


8

corals echinoderms and molluscs and very numerous milimetric ophiolite fragments

and quartz clasts develop in the lower section. The grains are well-sorted, the

carbonate intraclasts are rounded, while the ophiolite fragments and quartz clasts

are angular to subangular.

The bodies show lens-shaped and rarely nappe-type geometries, with a slightly

erosional base, meters to tens of meters lateral extensions and decimetric to metric

thicknesses. They are erosionally overlapping and gradually pass to ooidic bodies

towards the median and upper part. Progressively, a decrease of the amount of

ophiolite fragments and quartz clasts and their replacement with ooids could be

noticed.

Interlayers of bioclastic wackestones/ mudstones formed within the succession.

They become more frequent and more diversified towards the top. The rapid

change of facies from ooidic-bioclastic grainstone/packestone to bioclastic

wackestone/mudstone was accompanied by the decrease of the diversity of clastic

material and by the dominant presence of ripples.

The abundance of oblique structures and ripples as well as the frequence of

erosional surfaces indicates a high energy environment located above the FWB

The gradual increasing participation of bioclastic wackestones/mudstones

interlayers, the accompanying reduced degree of diversity of the clastic material,

as well as the decreasing amount of oblique structures indicate a progressive

decrease of the environment dynamics, and a depositional environment below, or

near FWB (James and Desrochers, 1992; Einsele, 1992).

ALGAL ASSEMBLAGE: Encrusting and nodular structures probably of microbial origin

(Lithocodium aggregatum ELLIOTT, Bacinella irregularis RADOIČIĆ, “Tubiphytes”

morronensis CRESCENTI) are present in the coralgal boundstones, and

rivulariaceans in the bioclastic peloidal grainstones/packstones.

2B

LOCATION: On the top of the carbonate massif in Cheile Turzii area.

AGE: Upper Jurassic

SUCCESSION AND FACIES: The succession consists of peloidal - oncoidic - bioclastic

wackestones / packestones interlayered with progressively more abundant


9

oncoidic-bioclastic grainstones, that become dominant in the top of the section

(Fig. 3). The wackestones/packestones contain milimetric to centimetric oncoids

and granular aggregates in micritic matrix, associated with dasyclads,

rivulariaceeans, Bacinella, foraminifera and gastropods. The lens-shaped oncoidic

bodies show limited lateral extensions and metric thickness, they are well-sorted

and reworked. The dominant clastic features of the overlaying limestone, the high

frequency of the erosional surfaces and oblique structures at small and medium

scales, as well as the presence of fragmented oncoids and bioclasts indicated a

bioclastic-oncoidal shoal.

Quartz clasts and rock fragments belonging to the island arc, as components of

an oncoidic-bioclastic grainstone level were noticed in the succession near to the

Upper Jurassic-Lower Cretaceous boundary, indicating the proximity of the coastal

environment. Emmersion of the top of the platform occurs, as indicated by the

increased terrigenous input and the vadouse diagenesis. This environment

favoured the accumulation of charopphytes limestones. The transition from the

environment of formation of the oncoidic deposits to lacustrine environments

suggests the gradual decrease of the accomodation space. This lead to the

progradation of the coastal facies on the top of the marine facies, and to the

emmersion of the latter ones.

ALGAL ASSEMBLAGE. A relative rich assemblage of dasyclads, halimedaceans and

cyanobacteria occurs inside the oncoidal limestone sequence: Salpingoporella

annulata CAROZZI., Salpingoporella ettaloni BERNIER, Salpingoporella pygmaea

(GÜMBEL), Salpingoporella enayi BERNIER, Clypeina sulcata (ALTH),

Campbeliella striata (CAROZZI), Nipponophycus ramosus YABE & TOYAMA.,

Lithocodium aggregatum ELLIOTT.


10

Figure 3 – Sedimentological log of the upper part of Sănduleşti Formation and lower part of

Petridu Formation in stop 12 B-C.


11

2C

LOCATION: On the top of the carbonate massif in Cheile Turzii area.

Age: Lower Cretaceous (Berriasian)

SUCCESSION AND FACIES: At the upper part of the carbonate succession in Cheile

Turzii, banks of decimetric to metric limestone, about 70 m thick, accumulated. The

facies indicate shallow-subtidal, intertidal and supratidal depositional environments,

comprising marine and restricted lagoons, beaches and sand bars, tidal flats, algal

marshes, freshwater lakes and land. Many elementary sequences display a

shallowing-upward trend which is expressed by a gradual change from deeper to

shallower facies, or by intertidal to supratidal overprinting of subtidal facies.

Continuous shallowing-upward from deeper to shallower facies can be explained

by progradation or lateral migration of the depositional system.

Elementary sequence boundaries commonly correspond to the upper bedding

surfaces and are characterized by erosion, pedogenetic brecciation, root traces, or

desiccation polygons. These features occured during a drop of the relative sea

level. The overlying deposits are represented by sandstones and marls.

Charophytes, ostracods and gastropods identified in the marls or sandstones point

to the presence of freshwater lakes.

The marine transgression surfaces are marked by a basal lag containing

lithoclasts reworked from the subjacent beds. A gradual transition to peloidal -

oncoidic - bioclastic wackestones - packestones with algae (dasyclads,

rivulariaceeans), and foraminifera was noticed.

ALGAL ASSEMBLAGE. Except characean gyogonites from the fresh water deposit

intercalations the Lower Cretaceous limestones contain rivulariacean-type

cyanobacteria, and scarce dasyclads: Clypeina catinula CAROZZI and Seliporella

neocomiensis (RADOIČIĆ)

REFERENCES

Dragastan, O., Ciubotaru, T., Brustur, T. -1987 - Neoteutloporella socialis (Praturlon), algue

“recifale” du domaine tethysien. Revue du Paleobiologie, vol. 6, N1, p.143-149, Genève.

Einsele, G., 1992 – Costal and Shallow Sea Sediments (including Carbonates). In: Einsele G., (ed), Sedimentary Basins. Springer- Verlag Berlin, p. 94-155.


12

Gili, E., Masse, J-P., Skelton, P. W., - 1995- Rudists as gregarious sediment-dwellers, not reef-builders, on Cretaceous carbonate platforms. Paleogeogr., Paleoclimatol., Paleoclimatol., 118, p. 245-267.

Insalaco, 1998 – The descriptive nomenclature and classification of growth fabrics in fossil scleractinion reefs. Sedimentary Geology, 118, p. 159-186.

James, B., Desrochers, A., 1992 – Shallow Platform Carbonates. In: Walker R. G. and James N. P. (eds.), Facies Models. Geolog. Assoc. Canada, p. 277-303.

Leinfelder, R. R., Krouther, M., Laternser, R., Nose, M., Schmid, D., Scheigert, G., Werner, W., Keupp, H., Brugger, H., Herrmann, R., Rehfeld-Keifer, U., Schroeder, R., Reinhold, C., Koch, R., Zeiss, A., Schweizer, V., Christman, H., Menges, G., Luterbacher, H.,- 1994- The origin of Jurassic reefs: current research developments and results. Facies 31, p. 1-56.

Miall, A. D., 1978 – Facies types and vertical profile models in braided river deposits: a summary, in Miall, A. D., ed., Fluvial sedimentology. Canadian Society of Petroleum Geologists, Memoir 5, p. 597-604.

Riding, R., -1991- Classification of microbial carbonates: in Riding, R., ed., Calcareous algae and stromatolites: Springer-Verlag, p. 21-51.

Riding, R., -2000- Microbial carbonates: the geological record of calcified bacterial-algal mots and biofilms. Sedimentology, 47 (suppl. 1), p. 179-214.

Shapiro, R. S., -2000- A comment on the systematic confusion of thrombolites. Palaios, V.15, p. 166-169.

Schmid, D., -1996- Marine microbiolites and micro-encrusters from the Upper Jurassic. Profil, 9, p. 101-251.

Săsăran, E., Hosu, A., Spălnăcan, R., Bucur, I.I, (2000) Microfacies, microfosils and sedimentary evolution of the Sănduleşti limestone Formation in Cheile Turzii (Apuseni Mountains, Romania). Acta Paleontologica Romaniae, v. 2, p. 453-462.

GUIDE TO EXCURSION (POST – SYMPOSIUM)

STRATIGRAPHY AND FACIES OF THE MAASTRICHTIAN DINOSAUR

BEARING FORMATIONS FROM ALBA IULIA – VURPĂR – SEBEŞ AREA

(ALBA DISTRICT)

Vlad A. Codrea, Cătălin Jipa, Matei Vremir, Ştefan Feigi

THE LATE CRETACEOUS FROM THE SOUTHWESTERN SIDE OF THE

TRANSYLVANIAN BASIN

On its southwestern side the Transylvanian Basin exposes an embayment insinuating

between the South Carpathians and Apuseni mountains. On the geological map 1 :

200 000 published by the Geological Institute of Romania, this area exposes mainly

Oligocene formations, but as a matter of fact the largest part of these deposits belong to

the Late Cretaceous, when a transition from marine to terrestrial environments occurred

(Fig. 1).

Fig. 1: Geologic map and geographic location within Romania of the Alba Iulia - Sebeş

area (modified after Codrea and Dica, 2005). Legend : 1. Alluvia; 2. Lower terrace; 3.

Pannonian s.s.; 4. Badenian; 5. Sebeş Formation; 6. Sântimbru Formation; 7. Bărăbanţ

Formation; 8. Ighiu Formation; 9. Şard Formation; 10. Vurpăr Formation; 11. Bozeş

Formation; 12. Aptian – Albian; 13. Barremian – Aptian; 14. Fossil-bearing sites

The terrestrial environments are peculiar for the Maastricthian, but this kind of

sedimentation continuated in Paleogene too. In the inner Carpathian areas, apart the

Haţeg Basin this is the main region where dinosaur remains occur most frequently.

Codrea & Dica (2005) named it the “Metaliferi area”, as a distinct sedimentary realm

(Fig. 2). It includes the Alba Iulia – Vurpăr – Sebeş – Pianu area (Basin of Transylvania)

and possibly, the Zlatna Basin too.

Fig. 2 : Late Cretaceous and Cenozoic formations from Metaliferi area and NW

Transylvania. Stars are indicating dinosaur remains.

The Maastrichtian terrestrial environments concern fluvial system deposits, with red silty

clay originating from overbanks and conglomerate and sand as channel fills. The

lithology of clasts indicates two main source areas, drained by different trended streams:

one which flowed from Apuseni area, where clasts of sedimentary origin are frequent

(mainly different Mesozoic limestones), and another one which yielded mainly

metamorphic clasts originating from South Carpathians.

Description of the itinerary and outcrops

The field-trip starts from Cluj Napoca, city located on the northwestern side of the

Transylvanian Depression. To Alba Iulia, the road follows the limit between the

Transylvanian Depression and the Apuseni Mountains. Two old Transylvanian towns

will be crossed (Turda – the ancient Roman Potaissa – and Aiud also named Enyed or

Strassburg am Mieresch, with the oldest Natural Science Museum in Romania ).

1-st Stop: Şard : Fluvial Maastrichtian deposits originating from Apuseni source-area

Location: on the road Alba Iulia – Zlatna, on the right bank of Ampoiului River.

Facies. The sequence, first exposed at the bridge crossing the valley, along the road

linking Alba Iulia to Ighiu, can be followed upstream in two additional outcrops. It is

represented mainly by coarse siliciclastic rocks (conglomerates, micro-conglomerates,

sandstones, but also minor red silty clays) originating from repetitive superposed

channels of the Şard Formation. Large alluvial fans, medium to high energy braided

rivers, a very dynamic environment with pronounced erosional and depositional

processes can be presumed. In a few cases, undercut sections of riverbanks and

floodplains are preserved, indicating a very sinuous water-course characterized by coarse

loads, fast erosion/deposition and frequent changes in flow direction

(superposed/overlapping channels), a generally unstable environment.

Fig. 3: Alluvial fans in Şard

Faunal assemblage: Only scarce vertebrate fossils (a femur of a small-sized sauropod

and an ?ornithopod limb bone shaft, as well as several other unidentifiable reptilian

bones) have been found in these deposits; some of these show signs of reworking. These

few fossils are para-autochthonous or even allochthonous.

2-nd Stop Vurpăr : Basal Maastrichtian fluvial deposits from Apuseni source-area

Location: Sequences of fluvial origin (Codrea et al., 2001, 2003) are exposed north of

the village in “Râpele din susul Dumbrăvii”, midway Vurpăr and Câmpuţ.

Facies: The continental succession occurs on a single restricted surface (several square

meters) as a monocline dipping 20–35o to the NNE. Red and brown overbank mudstones

and siltstones dominate, interbedded with a few lens-like (0.5 to 3 m thick) beds of

yellowish sand, sandstone and microconglomerate channel fills. The majority of the

channel fills are exposing internal architecture specific for braided flows, with numerous

internal bars (SB, GB, LA elements) that temporarily stocked the sediments. The

downstream migration of the sand and gravel bars lead to dominating oblique-conchoidal

lamination. The instability of the channels led to the formation of fining-upward type

channel-fill sequences, few meters in width. The channels are flanked by crevasse cones,

sand/silt levees and floodplain silty clays (OF). Paleosols are frequent with pedogenic

processes indicated by root-marks or centimeter-sized carbonate nodular concentrations,

very specific for the Bk horizon. Frequently root traces may be preserved within the

nodules. This kind of paleosol containing caliche nodules is indicative of climatic

seasonality. A dry subtropical climate is presumed. All these deposits accumulated in a

high-sinuosity fluvial system that carried a significant suspended solid load.

Faunal assemblage: The majority of the fossils were found in the basal sequence of the

Şard Formation, nearly 30–50 m above the boundary with the Vurpăr Formation. The

finds are mainly disarticulated teeth and bones, but some incomplete skeletons preserving

bones still in connection are also known (occurring in red silty clays: young and adult

Zalmoxes as well as Struthiosaurus). The dominance of young and subadult individuals

could be indicative for periodic causes (e.g. droughts) of death, the carcasses and partially

disturbed skeletons subsequently being buried relatively rapidly by very fine floodplain

deposits. The isolated white bones remained exposed for longer time intervals under

subaerial conditions, being later reworked by the streams then buried. The vertebrate

faunal list at Vurpăr includes so far: two turtle taxa (Kallokibotion and probably a

?Dortokiidae representative), a large crocodilian (Allodaposuchus), two euornithopod

species (Zalmoxes shqiperorum, Z. robustus – very frequent), one hadrosaur

(Telmatosaurus transsylvanicus - rare) and one ankylosaur (Struthiosaurus

transylvanicus – common).

3-rd Stop: Râpa Roşie: Maastrichtian fluvial deposits, South Carpatinans source-area.

Location: The red beds from Râpa Roşie are exposed on the right bank of the Secaş

River, nearby Sebeş borough.

Facies: it exposes a facies dominated by several generations of superposed channel fills,

with reworked coarse lithoclasts, interbedded with silty clays of fluvial origin. One can

distinguish two main sequences: a basal coarse one, and a superposed finer one

dominated by red silty clay.

Faunal assemblage: Several reptile bones had been found in Râpa Roşie. The majority

concerns the dinosaurs already mentioned in Vurpăr. Besides dinosaurs, turtles

(Kallokibotion), crocodilians and a giant pterosaur are reported from this locality. Once,

al these bones had been considered reworked and the bearing deposits to belong to the

Paleogene or even to the Early Miocene. The new discovered bones originating from the

upper sequence reject this supposition: these bones bear not any mark of reworking. In

these circumstances, this succession could not be separate as a distinct formation (“Sebeş

Formation”) as once presumed, but as part of Şard Formation.

References Codrea, V., Dica, P., 2005. Upper Cretaceous–lowermost Miocene lithostratigraphic units exposed in Alba

Iulia-Sebeş-Vinţu de Jos area (SW Transylvanian basin). Studia Universitatis Babeş-Bolyai, Geologia

50, 19–26.

Codrea, V., Hosu, Al., Filipescu, S., Vremir, M., Dica, P., Săsăran, E, Tanţău, I., 2001. Aspecte ale

sedimentaţiei cretacic superioare din aria Alba-Iulia – Sebeş (jud. Alba). Studii şi cercetări, Geologie-

Geografie 6, 63–68.

Codrea, V., Dica, P., Fărcaş, C., Barbu, O., 2003. Late Cretaceous–Early Miocene formations from Alba

Iulia – Sebeş area (Transylvanian Depression, Alba district). Oltenia, Studii şi comunicări, Ştiinţele

naturii 19, 22–27.

Documents

Babeş-Bolyai University, Department of Geology€¦ · Middle Jurassic (Bajocian) echinoids of Bucegi Mountains (Eastern Carpathians, Romania ... Oxfordian, southern Poland ... Microfacies