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Background: During the SARS-CoV-2 pandemic period, in the treatment approved by the WHO, along with antivirals, antibiotics, nonsteroidal anti-inflammatory drugs and anticoagulants, dexamethasone was always used. This study started from the professional concern related to the vasopressor effect of cortisone on blood pressure (BP). Methods: The study group was achieved by selecting, from a total of 356 patients hospitalized in the clinic, the patients with known hypertensive status at admission for SARS-CoV-2. Dexamethasone was part of the anti-COVID-19 treatment, with an administration of 4–6–8 mg/day, depending on bodyweight, for 10 days. All patients with hypertension received antihypertensive treatment in adjusted doses according to the recorded BP values. Results: Monitoring of BP in hospitalized patients was performed daily, in the morning and evening. If on the 2nd day of treatment, 84% of the patients partially responded to the treatment with a moderate decrease in BP, on the 3rd therapy day, the situation clearly improved: more than 75% of the patients had values of BP that can be classified as high-normal (38.23%) and normal (40.03%). Conclusions: Dexamethasone for treatment of SARS-CoV-2 infection did not have a notable influence on increasing BP, because the doses were low–moderate and prescribed for a short time.

This paper presents the interpretation of the field investigations carried out in the southern part of the Eastern Carpathians, aiming to obtain a drainage model of the B��sca Rozilei, the left tributary of the Buz��u River. For achieving the drainage pattern, we have correlated the geomorphological, topographical and geological features of the studied area. We found that B��sca Rozilei is a 6th order stream, being a young basin, which shows a high degree of branching of the hydrographic network and a torrential character., {"references":["Agarwal P., de Berg, M., Bose, P., Dobrint, K., van Kreveld, D., Overmars, M., de Groot, M., Ross, T., Snoeyink, J., Yu, S. (1996). The Complexity of Rivers in Triangulated Terrains. Proceedings of the 8th Canadian Conference on Computational Geometry: 325-330.","Cebotarev, A.I. (1957). Hidrologia uscatului și calculul scurgerii rîurilor. Editura Tehnică, 259 p.","Chendeș, V. (2011). Resursele de apă din Subcarpații de la curbură. Evaluări geospațiale. Editura Academiei Române, 339 p.","Chorley, R. (1962). Geomorphology and general systems theory. U.S. Geological Survey Press Professional Paper 500-B, 10 p.","Comănescu, L. (2004). Bazinul morfohidrografic Casimcea-studiu geomorfologic. Editura Universității din București, 252 p.","Dumitrescu, I., Săndulescu, M., Bandrabur, T., Săndulescu, J. (1968). Geological Map Covasna Sheet, scale 1:200 000. Printed by the Geological Institute of Romania.","Ene, M. (2004). Bazinul hidrografic Râmnicu Sărat. Dinamica reliefului în sectoarele montan şi subcarpatic. Editura Universitară, 178 p.","Frunzescu, D., Brănoiu, G. (2004). Monografia geologică a Bazinului râului Buzău. Editura Universității din Ploiești, 428 p.","Gherghe, A., Nedelea, A., Briceag, A., Ion, G., Melinte Dobrinescu, M.C. (2020). Linking geological and geomorphological features. Case study: Slănicul de Buzău Valley. Geo-Eco-Marina 26: 135-156.","Grecu, F., Zăvoianu, I. (1997). Morphohydrographic basins. Revista de Geomorfologie, 1: 99-106.","Grecu, F., Palmentola G. (2003). Geomorfologie dinamică. Editura Tehnică, 392 p.","Horton, R.E. (1945). Erosional development of streams and their drainage basins: hydro-physical approach to quantitative morphology. Geological Society of America Bulletin, 56(3): 275–370.","Ielenicz, M. (1984). Munții Ciucaș – Buzău, Studiu geomorfologic. Editura Academiei RSR, București, 174 p.","Ielenicz, M., Comănescu, L (2003). Geografie generală. Editura Credis Bucureşti, 136 p.","Melinte-Dobrinescu, M.C., Brustur, T., Macaleț, R., Jipa , D., Ion, G., Popa , A., Ion, E., Briceag, A. (2017). The Geological and Paleontological Heritage and the Potential for the Geotourism Development in the Buzău Land Geopark (Romania). Geoheritage, 9(2): 225-236.","Minea, G. (2013). Assessment of the Flash Flood Potential of Bâsca River Catchment (Romania) Based on Physiographic Factors. Cent. Eur. J. Geosci. 5(3): 344-353.","Morariu, T., Pișota, I., Buta, I. (1962). Hidrologie generală. Editura Didactică și Pedagogică, 462 p.","O'Callaghan, J.M., Mark, D.F. (1984). The extraction of drainage networks from digital elevation data. Computer Vision, Graphics, and Image Processing, 28(3): 323-344.","Posea, G, Grigore, M., Popescu, N., Ielenicz, M. (1976). Geomorfologie. Editura Didactică și Pedagocică, 534 p.","Posea, G, Badea, I. (1984). România - unitățile de relief – harta scara 1:750.000. Editura Științifică și Enciclopedică București.","Posea, G, Cioac ă, A. (2003). Cartografierea Geomorfologică. Editura Fundației România de Mâine, 208 p.","Săndulescu, M. (1984). Geotectonica României. Editura Tehnică Bucureşti, 336 p.","Săndulescu, M. (1995). Overview on Romanian geology. Romanian Journal of Tectonic and Regional Geology, 75(2): 3-15.","Strahler, A.N. (1952). Hypsometric (area-altitude) analysis of erosional topology. Geological Society of America Bulletin, 63(11): 1117- 1142.","Strahler, A.N. (1957). Quantitative analysis of watershed geomorphology. Transactions of the American Geophysical Union, 38(6): 913-920.","Ştefănescu, M.O., Popescu, I., Melinte-Dobrinescu, M., Ivan, V, Ştefănescu, M., Papaianopol, I., Popescu, G., Dumitrică, P. (1993). Geological Map Sheet Nehoiu, scale 1: 50,000. Printed by the Geological Institute of Romania","Zăvoianu, I. (1978). Morfometria bazinelor hidrografice. Editura Academiei RSR, 174 p."]}

This work presents the calcareous nannofossils assemblages identified in samples recovered from 5 boreholes, drilled on the western side of the Olt River, in the B��beni area. These boreholes crossed the Lower Oligocene-Lower Miocene sedimentary successions. The identified assemblages were included in the following intervals: (i) upper part of NP21 calcareous nannofossil zone to the lower part of NP23 biozone, corresponding to the early Rupelian, (ii) upper part of NP23 biozone up to NP25 biozone, spanning the late Rupelian-Chattian interval, and (iii) NN1 up to NN3 biozones, covering the Aquitanian and Burdigalian stages. The diversity and abundance of the identified nannofossil assemblages allow paleoenvironmental reconstructions., {"references":["Aubry, M.P. (1992). Late Paleogene calcareous nannoplankton evolution: A tale of climatic deterioration. In: D. R. Prothero, D.R., and W. A. Berggren, W.A. (Eds.), Eocene/Oligocene Climatic and Biotic Evolution, Princeton Univ. Press, Princeton: 272-309.","Auer, G., Piller, W.E., Harzhauser, M. (2014). High resolution calcareous nannoplankton palaeoecology as a proxy for small scale environmental changes in the Early Miocene. Marine Micropaleontology, 111: 53-65.","Báldi-Beke, M. (1984).The nannoplankton of the Transdanubian Paleogene formations. Geologica Hungarica, Series palaeontologica, 43: 1-307.","Bąk, K. (1999). Late Oligocene foraminifera from the Krosno Beds in the San valley Section (Bieszczady Mountains); Silesian Unit, Polish Outer Carpathians. Annales Societatis Geologorum Poloniae, 69: 195–217.","Bergen, J.A., de Kaenel, E., Blair, S.A., Boesiger, T.M., Browning, E. (2017). Oligocene-Pliocene taxonomy and stratigraphy of the genus Sphenolithus in the circum North Atlantic Basin: Gulf of Mexico and ODP Leg 154. Journal of Nannoplankton Research. 37(2-3): 77-112.","Berggren, W.A., Kent, D.V., Swisher, C.C., Aubry, M.P. (1995). A revised Cenozoic geochronology and chronostratigraphy. Society of Economics Paleontologist and Mineralogists Special Publication, 54: 129-212.","Bombiță, G., Bratu, E., Gheța N., Ion, J. (1980). Foraminiferele mari din Depresiunea Getică. Anuarul Institutului de Geologie și Geofizică, LV: 45-95.","Bossio, A., Mazzei, R., Monteforti, B., Salvatorini, G. (2005). Stratigrafia del Neogene e Quaternario del Salento Sud-Orientale (Con Rilevamento Geologico alla scala 1:25.000). Geologica Romana, 38: 31-60.","Boroși, V., Ghiță, D., Olaru-Florea, R.F. (2003). O nouă abordare biostratigrafică a secvențelor oligocene si miocene din sectorul central estic al avanfosei Carpaților Meridionali. Revista Română de Petrol, Serie Nouă, 10(4): 1-16.","Bown, P.R., Dunkley Jones, T. (2012). Calcareous nannofossils from the Paleogene equatorial Pacific (IODP Expedition 320 Sites U1331- 1334). Journal of Nannoplankton Research. 32(2): 3-51.","Chira, C. (2004). Early Miocene calcareous nannofossils assemblages from Transylvania. Acta Palaeontologica Romaniae, 4: 81-88.","Chira, C.M., Igrițan, A., Juravle, D.-T., Florea, F., Popa , M.V. (2011). Calcareous Nannoplankton across the Paleogeoene-Neogene Boundary in the Moldovița-Paltinu area (Bucovina, Romania). Acta Palaeontologica Romaniae, 7: 93-101.","Ćorić, S., Hohenegger, J. (2008). Quantitative analyzes of calcareous nannoplankton assemblages from the Baden-Sooss section (Middle Miocene of Vienna Basin, Austria). Geologica Carpathica, 59: 447-460.","De Kaenel, E., Villa, G. (1996). Oligocene-Miocene calcareous nannofossil biostratigraphy and paleoeecology from the Iberian Abyssal Plain. Proceedings of the Ocean Drilling Program, Scientific Results, 149: 79-145.","Dicea, O., Dicea, M. (1979). Stratigraphic correlation on nannoplankton basis in the external flysch of East Carpathians. Dări de Seamă ale Institutului de Geologie și Geofizică, 65(4): 111-126.","Dunkley Jones, T., Bown, P.R., Pearson, P.N., Wade, B.S., Coxall, H.K., Lear, C.H. (2008). Major shifts in calcareous phytoplankton assemblages through the Eocene-Oligocene transition of Tanzania and their implications for low-latitude primary production. Paleoceanography, 23: PA4204, doi:10.1029/2008PA001640.","Garecka, M. (2012). Record of changes in the Oligocene – Miocene sediments of the Menilite-Krosno series of the Skole Unit based on calcareous nannoplankton studies – biostratigraphy and palaeogeographical implications (Polish Outer Carpathians). Biuletyn Państwowego Instytutu Geologicznego, 453: 1-22.","Gheța, N., Popescu, G., Leu, M. (1976). Reticulofenestra ornata Müller, a marker nannoplankton species in the Middle Oligocene. Revue Roumaine de Geologie, 20(1): 143-145.","Gradstein, F., Ogg, J.G., Schmitz, M.D., Ogg, G. (Eds.) (2012). The Geological Time Scale. Boston, Elsevier, 1129 p.","Haczewski, G. (1989). Coccolith limestone horizons in the Menilite – Krosno Series (Oligocene, Carpathians) – identification, correlation and origin. Annales Societatis Geologorum Poloniae, 59: 435-523 [In Polish with English summary].","Haq, B.U. (1980). Biogeographic history of Miocene calcareous nannoplankton and paleoceanography of the Atlantic Ocean. Micropaleontology, 26: 414-443.","Haq, B.U., J. Hardenbol, J., Vail, P.R. (1987). Chronology of fluctuating sea levels since the Triassic (250 million years ago to present). Science, 235: 1156–1167.","Holcová, K. (2002): Calcareous nannoplankton from the Eggenburgian stratotypes (Lower Miocene, Central Paratethys). Geologica Carpathica, 53(6): 381-390.","Holcová, K. (2013). Morphological variability of the Paratethyan Oligocene-Miocene small reticulofenestrids coccolites and its paleoecological and paleogeographical implications. Acta Palaeontologica Polonica, 58(3): 651-668.","Kallanxhi, M.-E., Bălc R., Ćorić, S., Székely, S.F., Filipescu, S. (2018). The Rupelian-Chattian transition in the north-western Transylvanian Basin (Romania) revealed by calcareous nannofossils: implications for biostratigraphy and palaeoenvironment reconstruction. Geologica Carpathica, 69(3): 264-282.","Krhovský, J., Adamová, J., Hladíková, J., Maslowská, H. (1992). Palaeo environmental changes across the Eocene/Oligocene boundary in the Ždánice and Pouzdřany Units (Western Carpathians, Czechoslovakia): The long–term trend and orbitally forced changes in calcareous nannofossil assemblages. In: Hamršmíd, B., Young, J. (Eds.): Nannoplankton Research. Proceedings of Fourth INA Conference, Prague, 1991. Knihovnička ZPN, 14b(2): 105-187.","Martini, E. (1971). Standard Tertiary and Quaternary Calcareous Nannoplankton Zonation. Proceedings of the 2nd Planktonic Conference, Roma, 1970, Editura Tecnoscienza: 739-785.","Mațenco, L., Bertott i, G., Dinu, C., C!oetingh, S. (1997). Tertiary tectonic evolution of the external South Carpathians and the adjacent Moesian platform (Romania). Tectonics, 16(6): 896-911.","Mărunțeanu, M. (1992). Distribution of the Miocene calcareous nannofossils in the Intra- and Extra- Carpathian areas of Romania. Knihovnička ZPN: 14b(2): 247-261.","Mărunțeanu, M. (1999). Litho- and biostratigraphy (calcareous nannoplankton) of the Miocene deposits from the Outer Moldavides. Geologica Carpathica, 50(4): 313-324.","Melinte, M.C. (1993). Contributions at the establishment of the Oligocene/Miocene boundary in the Tarcău Nappe from the Buzău Valley based on calcareous nannoplankton associations (in Romania). Romanian Journal of Stratigraphy, 75: 91-96.","Melinte, M.C. (2005). Oligocene palaeoenvironmental changes in the Romanian Carpathians, revealed by calcareous nannofossils. Studia Geologica Polonica, 124: 341-352.","Melinte-Dobrinescu, M.C., Brustur, T. (2008). Oligocene-Lower Miocene events in Romania. Acta Palaeontologica Romaniae, 6: 203-215.","Mészáros, N., Ianoliu, C. (1989). Nannoplankton zones in the Oligocene deposits in the north-western Transylvanian Basin. In: Petrescu I. (Ed.), The Oligocene from the Transylvanian Basin, Romania. Univ. of Cluj-Napoca, Geology-Mineralogy Department, Special Issue, Cluj-Napoca: 157-162.","Mészáros, N. (1991). Nannofossil Zones in the Paleogene and Miocene Deposits of the Transylvanian Basin. Proceedings of the 4th INA (International Nannoplankton Association) Conference, Knihovnicka ZPN, 14b(2): 87-92.","Micu, M., Gheța, N. (1986). Eocene-Oligocene boundary in Romania on calcareous nannoplankton. Dări de Seamă ale Institutului de Geologie și Geofizică, 70-71(4): 289-307.","Mihăilă, N., Stancu, J., Codarcea, M., Bombiță, G., Lupu, M. (1967). Harta geologică 1:200.000, Foaia L -34 - XXV, Pitești. Imprimeria Institutului Geologic, București.","Motaș, C., Nicolae, E., Tudoran, C., Horia, G., Carp, V., Giuglan, F., Mihai, S., Mihalache, M. (1995). Reconstituirea evoluției geologice a Depresiunii Getice, în vederea evaluării calitative a potențialului petroligen și precizării zonelor optime de acumulare a hidrocarburilor. Raport Arhiva OMV – PETROM S.A., 45 p.","Mutihac , V., Stratulat M.I., Fechet R.M. (2004). Geologia României. Editura didactică și pedagogică, 419 p.","Nagymarosy, A., Voronina, A.A. (1992). Calcareous nannoplankton from the Lower Maikopian beds (Early Oligocene, Union of Independent States). In: Hamršmíd, B., Young, J.R. (Eds.): Nannoplankton Research. Proceedingd of the 4th INA Conference, Prague 1991. Knihovnička ZPN, 14b(2): 187-221.","Nagymarosy, A. (2000). Lower Oligocene nannoplankton in anoxic deposits of the Central Paratethys. The 8th International Nannoplankton Association Conference, Bremen. Journal of Nannoplankton Research, 22: 128-129.","Oszczypko-Clowes, M., Źydek, B. (2012). Paleontology of Upper Eocene – Lower Oligocene Malcov Basin based on the calcareous nannofossils: a case study of the Leluchów section (Krynica Zone, Magura Nappe, Polish Outer Carpathians). Geologica Carpathica, 63(2): 149- 164.","Ozdínová, S., Soták, J. (2014). Oligocene-Early Miocene planktonic microbiostratigraphy and paleoenvironments of the South Slovakian Basin (Lučenec Depression). Geologica Carpathica, 65: 451-470.","Perch-Nielsen, K. (1985). Cenozoic calcareous nannofossils. In: Bolli, H.M., Saunders, J B., Perch-Nielsen, K. (Eds.), Plankton Stratigraphy. Cambridge University Press, Cambridge: 427-555.","Popescu, B., Bratu, E., Gheța, N., Popescu, D. (1976). Contribuții la cunoastera stratigrafiei formațiunilor paleogene dintre Olt si Olănești (Depresiunea Getica). Dări de Seamă ale Institutului de Geologie și Geofizică, LXII: 265-278.","Popov, S.V., Rögl, F., Rozanov, A.Y., Steininger, F.F., Scherba, I.G., Kováč M. (2004). Lithological-Paleogeographic maps of Paratethys. 10 Maps Late Eocene to Pliocene. Courier Research Institute Senckenberg, 250: 1-46.","Raffi, I., Backman, J., Fornaciari, E., Päliko, H., Rio, D., Lourens, L., Hilgen, F. (2006). A review of calcareous nannofossil astrobiochronology encompassing the past 25 million years. Quaternary Science Reviews, 25: 3113-3137","Roban, R.-D., Melinte, C.M. (2005). Paleogene litho-and biostratigraphy of the NE Getic Depression (Romania). Acta Palaeontologica Romaniae, 5: 423-439.","Rögl, F. (1998). Paleogeographic Considerations for Mediterranean and Paratethys Seaways (Oligocene to Miocene). Annalen des Naturhistorischen Museums in Wien, 99A: 279-310.","Rögl, F. (1999). Mediteranean and Paratethys. Facts and hypothesis of Oligocene to Miocene paleogeography (short overview). Geologica Carpathica, 50: 339-349.","Rusu, A. (1988). Oligocene events in Transylvania (Romania) and the first separation of Paratethys. Dări de Seamă ale Institutului de Geologie și Geofizică, 72-73: 207-223.","Săndulescu, M. (1984). Geotectonica României. Editura Tehnică, 334 p.","Steiniger, F. F., Aubry, M. P., Berggren, W. A., Biolzi, M., Borsetti, A. M., Cartlidge, J. E., Cati, F., Corfield, R., Gelati, R., Iaccarino, S., Napoleone, C., Ottner, F., Roegl, F., Roetzel, R., Erri, S., Tateo, F., Villa, G., Zevenboom, D. (1997). The Global Stratotype Section and Point (GSSP) for the Base of the Neogene. Episodes, 20(1): 23-28.","Švábenická, L. (2002). Calcareous nannofossils of the upper Karpatian and lower Badenian deposits in the Carpathian Foredeep, Moravia (Czech Republic). Geologica Carpathica, 53: 197-210.","Stradner, H., Aubry, M. P., Bonnemaison, M. (2010). Calcareous nannofossil type specimens in the collection of the Geological Survey of Austria: A taxonomic and stratigraphic update. Jahrbuch der Geologischen Bundesanstalt, 150(1-2): 9-84.","Theodoridis, S. (1984). Calcareous Nannofossil Biozonation of the Miocene and Revision of the helicoliths and discoasters. Utrecht micropaleontological bulletins, 32: 1-271.","Varol, O. (1998). Palaeogene. In: Bown, P. R. (Ed.) Calcareous Nannofossil Biostratigraphy. British Micropalaeontological Society Publication Series: 200-224.","Villa, G., Fioroni, C., Pea, L., Bohat y, S., Persico D. (2008). Middle Eocene–late Oligocene climate variability: calcareous nannofossil response at Kerguelen Plateau, Site 748. Marine Micropaleontology, 69: 173-192.","Wade, B.S., Bown, P.R. (2006). Calcareous nannofossils in extreme environments: the Messinian salinity crisis, Polemi Basin, Cyprus. Palaeogeography, Palaeoclimatology, Palaeoecology, 233: 271- 286.","Wagreich, M., Krenmayr, H.-G. (1993). Nannofossil biostratigraphy of the Late Cretaceous Nierental Formation, Northern Calcareous Alps (Bavaria, Austria). Zitteliana, 20: 67-77.","Young, J.R. (1998). Neogene. In: Bown, P.R. (Ed.), Calcareous Nannofossil Biostratigraphy. British Micropalaeontological Society Publication Series: 225-265.","Zachos, J.C., Shackleton, N.J., Revenaugh, J.S., Palike, H., Flower, B.P. (2001). Climate response to orbital forcing across the Oligocene/ Miocene boundary. Science, 292: 274-278."]}

International audience; Unlike most Neogene basins of the Betic Cordillera where the Salinity Crisis is dated to the Messinian, a contradictory Tortonian dating was proposed for evaporites of the Lorca Basin. As a consequence, complex structural models have been proposed in the literature to explain this discrepancy in the timing of evaporites. In order to integrate the Lorca Basin into the geological context of the western Mediterranean domain during the Late Miocene, new sedimentological and stratigraphical studies coupled with new dating were performed, which allow us to propose a Messinian age for both diatomite-bearing deposits and evaporites of the Lorca Basin. These new ages challenge the idea of a Tortonian salinity crisis in the Lorca Basin. Three main events of base-level drop were evidenced during the Messinian. Each event is correlated with successive steps of basin restriction. Shallow salina evaporites were deposited after a base-level fall during the Messinian before a final base-level drop, which led to the entire exposure of the basin. This last exposure is interpreted as coeval with the deposition of first evaporites and halite in the deep Mediterranean basins. The reflooding which allowed the deposition of brackish deposits and a short-lived marine incursion occurred at the end of the Messinian. Base-level drops occurred during eustatic falls amplified by the gradual uplift of the Betic Cordillera. The exhumation of the Tercia ridge along the strike-slip Alhama de Murcia fault system during the Messinian probably favoured the gradual restriction of the basin. A discussion on correlations of main unconformities between several Neogene basins of the Betics is proposed, suggesting a similar structural evolution at the regional scale.

The goal of pleural fluid assessment is to establish with certainty its etiology and major challenge is the etiologic diagnosis precocity. Pleural effusion as the first and the only event in the onset of non-Hodgkin lymphoma is atypically in the absence of other signs and symptoms. Follicular lymphoma (FL) also called indolent lymphoma the most frequent is a low-grade non-Hodgkin�s lymphoma (NHL). In patients with indolent lymphoma affecting the pleura and pericardium is atypical and appears only in aggressive forms, so the onset with pleural effusion is unusual. Serous effusions may occur from onset or during evolution of various subtypes of T cell originated lymphomas or high-grade B cell lymphomas. Primary pleural lymphomas (PPL) have been described at patients with human immunodeficiency virus infection; tuberculosis complicated with chronic pyothorax or after exposure to asbestos. Compared to other similar cases previously reported in the medical literature, the novelty of this case is the atypical onset of low grade of indolent B-cells non-Hodgkin with primary pleural effusion in the absence of personal history as well as of another clinical, laboratory and pleural changes.

The historical province of Dobruja, located in southeastern Romania, has experienced intense human population movement, invasions, and conflictual episodes during the Middle Ages, being an important intersection point between Asia and Europe. The most informative source of maternal population histories is the complete mitochondrial genome of archaeological specimens, but currently, there is insufficient ancient DNA data available for the medieval period in this geographical region to complement the archaeological findings. In this study, we reconstructed, by using Next Generation Sequencing, the entire mitochondrial genomes (mitogenomes) of six medieval individuals neglectfully buried in a multiple burial from Capidava necropolis (Dobruja), some presenting signs of a violent death. Six distinct maternal lineages (H11a1, U4d2, J1c15, U6a1a1, T2b, and N1a3a) with different phylogenetic background were identified, pointing out the heterogeneous genetic aspect of the analyzed medieval group. Using population genetic analysis based on high-resolution mitochondrial data, we inferred the genetic affinities of the available medieval dataset from Capidava to other ancient Eurasian populations. The genetic data were integrated with the archaeological and anthropological information in order to sketch a small, local piece of the mosaic that is the image of medieval European population history.

Our study aims to reconstruct the palaeogeography of the northern part of the Lesser Antilles in order to analyse whether emerged areas might have existed during the Cenozoic, favouring terrestrial faunal dispersals between South America and the Greater Antilles along the present-day Lesser Antilles arc. The stratigraphy and depositional environments of the islands of Anguilla, St Martin, Tintamarre, St Barthélemy, Barbuda and Antigua are reviewed in association with multichannel reflection seismic data acquired offshore since the 80's in the Saba, Anguilla and Antigua Banks and in the Kalinago Basin, including the most recent academic and industrial surveys. Seven seismic megasequences and seven regional unconformities are defined, and calibrated from deep wells on the Saba Bank and various dredges performed during marine cruises since the 70's in the vicinity of the islands. Onshore and offshore correlations allow us to depict an updated and detailed sedimentary organisation of the northern part of the Lesser Antilles from the late Eocene to the late Pleistocene. Paleogeographic reconstructions reveal sequences of uplift and emergence across hundredswide areas during the late Eocene, the late Oligocene, the early middle-Miocene and the latest Miocene-earliest Pliocene, interspersed by drowning episodes. The ∼200 km-long and ∼20 km-wide Kalinago Basin opened as an intra-arc basin during the late Eocene - early Oligocene. These periods of emergence may have favoured the existence of episodic mega-islands and transient terrestrial connections between the Greater Antilles, the Lesser Antilles and the northern part of the Aves Ridge (Saba Bank). During the Pleistocene, archipelagos and mega-islands formed repeatedly during glacial maximum episodes.

This paper summarizes the results of a sedimentologic investigation of Albian sandstones and conglomerates from the eastern extremity of the Southern Carpathians, the area between the Ialomița and Dâmbovița rivers. Lithofacies analysis, paleotransport, provenance and paleoenvironment of these clastic sediments are the main focus of the paper. An important component of the study is the part played by Ialomița-Dâmbovița Albian sediment accumulation in the Albian sedimentary history of the Carpathian Bend zone. Two major lithofacies occur in the Ialomița-Dâmbovița Albian sedimentary succession: medium- and coarse-grained sandstones and sandstones with conglomerate interbeds. These deposits are intercalated with a third significant lithofacies, rhythmic finer grained deposits of silty clay and silty and finegrained sandstones. Some of the coarser grained Albian sediments (both sandstones and conglomerates) are structureless, poorly sorted, have a relatively large amount of sandy matrix and include oversize clasts, features indicative of accumulation by sediment gravity flow. The normal graded sandstones and the conglomerates with poor sorting, abundant matrix and oversize clasts suggest sediment transport by high density turbidity currents. The accumulation of the rhythmic, alternating silty clay and silty fine-grained arenite sediments is ascribed to low density turbidity currents. According to their relationship with the underlying, younger deposits, the monocline structure and their presence within a succession of clastic sediments forming a coarsening-upward stacking pattern, it is proposed here that the Albian deposits in the Ialomița-Dâmbovița area were involved in a very active, large-scale progradation process, with deposition occurring on the continental rise. The Albian deposits in the Ialomița-Dâmbovița area are genetically and stratigraphically correlated with the deposits of the Babele Sandstone and the Scropoasa-Lăptici Sandstone units in the Bucegi Mountains. The Babele-Dâmbovița sedimentary basin is distinct and different from the depositional basin of the deep-water Albian conglomerate fan from the Carpathian Bend zone.

This paper presents the correlation between the geomorphological features of the Sl��nicul de Buz��u Valley and the geological ones, such as the tectonic regime and the type of rocks. We are pointing out that the geomorphology of the valley and the change of the flow direction are linked to the type of rocks and tectonic elements of traversed geological structures. The change of the upper course of the river from NS to WE upstream the Lop��tari locality coincides with a major tectonic element, a digitation occurring in the deposits formed by hard compact Paleogene rocks. The upper course deep valley is replaced by a larger one in the sector that exposed Miocene and Pliocene deposits, showing a W-E direction. The lower course of the river shows again a change in the course direction from N towards S, up to its confluence with the Buz��u River. This modification corresponds to the occurrence of the friable Pliocene, Pleistocene and Holocene deposits, such as sandstones, clays, marls and weakly consolidated ones, i.e., sands and loess., {"references":["Chendeș V. (2011). Resursele de apă din Subcarpații de la Curbură. Evaluări geospațiale. Ed. Academiei Române, 339 p.","Dumitrescu I., Săndulescu M., Bandrabur T., Săndulescu M. (1968). Covasna Sheet, scale 1:200,000. Printed by the Geological Institute of Romania.","Grecu F., Comănescu L. (2006). The morphometric analysis of the gravels from the Slănic of Buzău bed – preliminary considerations. Revista de geomorfologie, 8: 45-52.","Jipa D., Olariu C. (2009). Dacian Basin: Depositional Architecture and Sedimentary History of a Paratethys Sea. Geo-Eco-Marina Special Publication, 3, 264 p.","Melinte M. (2005). Oligocene palaeoenvironmental changes in the Romanian Carpathians, revealed by calcareous nannofossil fluctuation. In Tyszka, J., Oliwkiewicz-Miklasinska M., Gedl P., Kaminski M.A. (Eds.), Methods and Application in Micropalaeontology. Studia Geologica Polonica, 124: 15-27.","Melinte-Dobrinescu M.C., Stoica M. (2013). Badenian Calcareous Nannofossil Fluctuation in the Eastern Carpathians: Palaeoenvironmental significance. Acta Palaeontologica Romaniae, 9 (2): 47-56.","Melinte-Dobrinescu M.C., Brustur T., Jipa D.C., Ion G., Macaleţ R., Briceag A., Ion E., Popa A., Rotaru S. (2017). Geological Investigations and mapping in the Buzau Land Geopark. State of the art. Geoheritage, 9: 225-236.","Motaş I., Bandrabur T., Ghenea C., Săndulescu M. (1967). Geological maps of Romania, scale 1:200,000, Sheet Ploieşti. Printed by the Geological Institute of Romania.","Murgeanu G., Dumitrescu I., Săndulescu M., Bandrabur T., Săndulescu J. (1968). Geological maps of Romania scale 1:200,000, Sheet Covasna. Printed by the Geological Institute of Romania.","Pătroescu M. (1996). Subcarpaţii dintre Râmnicu Sărat şi Buzău - Potenţial ecologic şi exploatare biologică. Editura Carro, 125 p.","Piller W.E, Harzhauser M., Mandic O. (2007). Miocene Central Paratethys stratigraphy – current status and future directions. Stratigraphy, 4: 151-168.","Popov S.V., Rögl F., Rozanov A.Y., Steininger F.F., Shcherba I.G., Kováč M. (2004). Lithological-Paleogeographic maps of Paratethys. 10 Maps Late Eocene to Pliocene. Cour Forsch Senck, 250: 1-46.","Posea G., Badea L. (1984). România - unitățile de relief – harta scara 1:750,000 Ed. Științifică și Enciclopedică București.","Săndulescu M. (1984). Geotectonica României. Editura Tehnică București, 334 p.","Săndulescu M. (1994). Overview on Romanian Geology. Romanian Journal of Tectonics and Regional Geology, 75: 3-15.","Stoica M., Melinte-Dobrinescu M., Palcu, D. (2012). Neogene deposits in the South-Eastern Carpathians. Field trip guide. Editura Amanda, 48 pp.","Ştefănescu M., Melinte M. (1992). New data on the Eocene/Oligocene boundary in the Outer Flysch Zone of the Buzău Valley Basin on the basis of the nannoplankton. Romanian Journal of Stratigraphy, 76: 61-68.","Ştefănescu M., Popescu I., Ştefănescu M., Melinte M., Ivan V., Stănescu V. (1989). Aspects of the possibilities of the lithological correlations of the Oligocene/Miocene Boundary in the Buzău Valley. Romanian Journal of Stratigraphy, 75(4): 83-91.","Ştefănescu, M., Popescu, I., Melinte, M., Ivan, V., Ştefănescu, M, Papaianopol, I., Popescu, G., Dumitrică, R. (1993). Sheet Nehoiu, scale 1:50,000. Printed by the Geological Institute of Romania.","Tufescu V. (1966). Délimitations phytoclimatiques dans les régions montagneuses et sousmontagneuses de Roumanie. RRGGGGéogr., X: 39-46.","van Baak, C., Mandic O., Lazăr I., Stoica M., Krijgsman W. (2015). The Slanicul de Buzău section, a unit stratotype for the Romanian stage of the Dacian Basin (Plio-Pleistocene, Eastern Paratethys). Palaeogeography Palaeoclimatology Palaeoecology, 440: 594-613.","Visarion M., Săndulescu M., Drăgoescu I., Drăghici M., Cornea I., Popescu M. (1977). Harta mişcărilor crustale verticale recente, 1:100,000.","Republica Socialistă România. Institutul de Geologie şi Geofizică, Bucureşti.","Zăvoianu I., Herișanu G., Marin C. (2005). Legătura dintre altitudinea medie și rezistența la eroziune a rocilor din bazinul Slănicul Buzăului. Analele Universităţii Spiru Haret, Seria Geografie, 8: 69-74."]}

This paper presents the microfaunal assemblages of lower Sarmatian (Volhynian) deposits intercepted by 10 hydrocarbon wells from the Bleje��ti hydrocarbon field, S Romania. The identified microfaunas are typically for two Volhynian foraminifera zones: Varidentella reussi Zone and Elphidium reginum Zone. At the contact with the underlying Cretaceous or Middle Miocene (= Badenian) units, the Sarmatian studied samples, containing foraminiferal assemblages with abundant Ammonia beccarri, may not be assigned to a certain biozone. Besides, the identified ostracod assemblages were assigned to the NO 11 Cytheridea hungarica ��� Aurila mehesi. The composition and the abundance of microfaunal assemblages allow us to advance paleoecological considerations for the lower Sarmatian deposition interval of the studied area., {"references":["Andrusov N. (1917). Pontice skijjarus. Trudy Geol. Com. 4 (2).","Beca C., Prodan D. (1983). Geologia zacămintelor de hidrocarburi. Editura didactică şi pedagogică, Bucureşti.","Brânzilă M., Chira C. (2005). Sarmatian boundary in boreholes of the Moldavian Platform. Acta Palaeontologica Romaniae 5: 17-26.","Briceag A., Yanchilina A., Ryan W.B.F., Oaie G., Melinte-Dobrinescu M.C. (2016a). Late Pleistocene - Holocene paleoenvironmental changes from the Romanian Black Sea shelf inferred by microfaunal and isotope fluctuations. International Multidisciplinary Scientific Geoconference SGEM, 1: 305-312, doi: 10.5593/sgem2016B11.","Briceag A., Melinte-Dobrinescu M.C., Ion G., Balan S. (2016b). Reoccurrence of Phyllophora red algal genus on the Romanian Black Sea shelf. International Multidisciplinary Scientific Geoconference SGEM, 2(3): 813-819, doi: 10.5593/sgem2016B32.","Briceag A., Macaleţ R., Melinte-Dobrinescu M.C. (2018). Sarmatian palaeoenvironment and bioevents in the Dobrogea region (SE Romania). Geo-Eco-Marina 24: 81-91.","Briceag A., Yanchilina A., Ryan W., Stoica M., Melinte-Dobrinescu M. (2019). Late Pleistocene to Holocene paleoenvironmental changes in the NW Black Sea. Journal of Quaternary Science, 34 (2): 87-100.","Cornée J.-J., Moisette P., Saint-Martin J.-P, Kázmér M., Toth E., Görög A., Dulai A., Müller P. (2009). Marine carbonate systems in the Sarmatian (Middle Miocene) of the Central Paratethys: the Zsambek Basin of Hungary. Sedimentology 56(6): 1728-1750.","Dumitriu S.D., Longhin S., Dubicka Z., Melinte-Dobrinescu M, Paruch- Kulczycka J., Ionesi V. (2017). Foraminiferal, ostracod, and calcareous nannofossil biostratigraphy of the latest Badenian – Sarmatian interval (Middle Miocene, Paratethys) from Poland, Romania and the Republic of Moldova. Geologica Carpathica, 68(5): 419-444.","Debenay J.P., Beneteau E., Zhang J., Stouff V., Geslin E., Redois F., Fernandez Gonzalez M. (1998). Ammonia beccarii and Ammonia tepida (foraminifera): Morphofunctional arguments for their distinction. Marine Micropaleontology, 34: 235-244.","Filipescu S., Silye L. (2008). New Paratethyan biozones of planktonic foraminifera described from the Middle Miocene of the Transylvanian Basin (Romania). Geologica Carpathica, 59: 537-544.","Filipescu S., Miclea, A., Gross, MJ., Harzhauser, M., Zágoršek, K., Jipa , C., 2014. Early Sarmatian paleoenvironments in the easternmost Pannonian Basin (Borod Depression, Romania) revealed by the micropaleontological data. Geol. Carpat. 65 (1): 67–81.","Gebhardt H., Zorn I., Roetzel R. (2009). The initial phase of the early Sarmatian (Middle Miocene) transgression. Foraminiferal and ostracod assemblages from an incised valley fill in the Molasse Basin of Lower Austria. Austrian Journal of Earth Science, 102: 100-119.","Gross M. (2002). Middle Miocene ostracods from the Vienna Basin (Badenian/Sarmatian, Austria). Dissertation, Institüt für Geologie und Paläontologie Karl-Franzens-Universität Graz, 343 p.","Görög A. (1992). Sarmatian foraminifera of the Zambek Basin, Hungary. Annales Universitatis Scientiarum Budapestinensisde Rolando Eötvös Nominatae, XXIX: 31-153.","Hanganu E., Grigorescu D. (1981). Asupra ostracofaunei din nisipurile sarmatiene ale Dobrogei de Sud (Sectorul Cobadin – Cotu Văii). Studii si cercetari de geologie, geofizica si geografie, 26 (2): 309-313.","Harzhauser M., Piller W.E. (2004). Integrated stratigraphy of the Sarmatian (Upper Middle Miocene) in the western Central Paratethys. Stratigraphy, 1: 65-86.","Ionesi B. (1968). Stratigrafia depozitelor miocene de platform dintre Valea Siretului şi Valea Moldovei. Editura Academiei RSR, 396 pp.","Ionesi B., Guevara I. (1993). Studiul depozitelor sarmaţiene din forajul 1002 Bădeuţi (NV Platformei Moldoveneşti. Geological Bulletin of Romanian Society, 14: 79-87.","Ionesi B., Ionesi L. (1968). Contributions to the knowledge of theIoniţă C., Ghiţă D., Limberea L., Şindilar V., 2016. The first mention of Badenian in Cartojani (Central-Southern area of the Moesian Platform) based on biostratigraphical analyses (microfauna and nannoplankton). AAPG European Regional Conference & Exhibition, Bucharest, May 2016. Abstract Book, 56 p.","Jipa D.C., Olariu C. (2009). Dacian Basin: Depositional Architecture and Sedimentary History of a Paratethys Sea. Geo-Eco-Marina Special Edition 3, 268 p.","Jipa D.C., Olariu C. (2009). Sediment routing in a semi-enclosed epicontinental sea: Dacian Basin, Paratethys Domain, Late Neogene, Romania. Global and Planetary Change, 103: 193-206.","Jiŕíček R. (1985). Die Ostracoden des Pannonien. In: Chronostratigraphie und Neostratotypen Miozän der Zentralen Paratethys. Bd. VII. M6. Pannonien (Slavonien und Serbien): 378-425.","Jiŕíček R., Říha J. (1991). Correlation of Ostracod Zones in the Paratethys and Tethys. Saito Ho–on Kai Special Publications (Proceedings of Shallow Tethys) 3: 435-457.","Koubová, I., Hudáčková, N. (2010). Foraminiferal successions in the shallow water Sarmatian sediments from the MZ 93 borehole (Vienna Basin, Slovak part). Acta Geologica Slovaca, Ročník 2(1): 47-58.","Marinescu F. (1978). Stratigrafia Neogenului superior din sectorul vestic al Bazinului Dacic. Ed. Acad RSR, București, 155 p.","Melinte-Dobrinescu M., Ion G. (2013). Emiliania huxleyi fluctuations and associated microalgae in superficial sediments of the Romanian Black Sea shelf. Geo-Eco-Marina 19: 129-135.","Murray J.W. (1991). Ecology and paleoecology of benthic foraminifera. New York, John Wiley & Sons, 397 p.","Olteanu R., Jipa D. (2006). Dacian basin environmental evolution during Upper Neogene within the Paratethys domain. Geo-Eco-Marina 12: 91-105.","Papp A., Marinescu F., Seneš J. (1974). M5 - Sarmatien (sensu E. SUESS, 1866). Die Sarmatische Schichten gruppe und ihr Stratotypus. Chronostratigraphie und Neostratotypen. Miozän der Zentralen Paratethys. Slowak Akad Wissensch Bratislava, 4.","Piller W.E., Harzhauser M., Mandic O. (2007). Miocene Central Paratethys stratigraphy – current status and future directions. Stratigraphy, 4: 151-168.","Popescu G. (1995). Contribution to the knowledge of the Sarmatian foraminifera of Romania. Romanian Journal of Paleontology, 76: 85-98.","Popov N., Kojumdgieva E. (1987). The Miocene in Northeastern Bulgaria (Lithostratigraphic subdivision and geological evolution) [in Bulgarian with English abstract]. Rev. Bulg. Geol. Soc. 48 (3): 15-33.","Popov S.V., Rögl F., Rozanov A.Y., Steininger F.F., ShcherbaI. G., Kováč M. (2004). Lithological–Paleogeographic maps of Paratethys. 10 Maps Late Eocene to Pliocene. Cour Forsch Senck 250: 1-46.","Paraschiv D. (1979). Platforma Moesică şi zăcămintele ei de hidrocarburi. Editura Academiei RSR Bucureşti,195 p.","Reinhardt E.G., Patterson R.T., Schröder Adams C.J. (1994). Geoarcheology of the ancient harbor site of Caesarea Maritima, Israel: Evidence from sedimentology and paleoecology of benthic foraminifera. Journal of Foraminiferal Research 24 (1): 37-48.","Royden L., Horváth F., Burchfiel B.C. (1982). Transform faulting, extension and subduction in the Carpathian Pannonian region. Geological Society of America Bulletin, 93: 717-725.","Saint Martin, J.P., Pestrea, S. (1999). Les constructions à serpules et microbialites du Sarmatien de Moldavie. Acta Palaeontol. Rom., 2: 463-469.","Săndulescu M. (1984). Geotectonica României. Editura Tehnică Bucureşti.","Schmid S.M., Bernoulli D., Fügenschuh B., Maţenco L., Schefer S., Schuster R., Tischler M., Ustaszewski R. (2008). The Alpine-Carpathian-Dinaridic orogenic system: correlation and evolution of tectonic units. Swiss J. Geosci., 101: 139-183.","Short F.T., Neckles H.A. (1999). The effects of global climate change on sea grasses. Aquatic Botany 63 (3-4): 169-196.","Steininger F.F., Wessely G. (2000). From the Tethyan Ocean to the Paratethys Sea: Oligocene to Neogene stratigraphy, paleogeography and paleobiogeography of the circum-Mediterranean region and the Oligocene to Neogene Basin evolution in Austria. Mitt. Österr. Geol. Ges. 92: 95-116.","Ter Borgh M., Stoica M., Donsellar M., Maţenco L., Krijgsman W. (2014). Miocene connectivity between the Central and Eastern Paratethys: Constraints from the western Dacian Basin. Palaeogeogr., Palaeoclim., Palaeoecol. 412: 45-67.","Zelenka J. (1990). A review of the Sarmatian Ostracoda of the Vienna. Basin. In: Whatley R., Maybury C. (Eds.): Ostracoda and global events. Chapman & Hall: 263-270."]}

Seven Middle Miocene (Upper Badenian to Lower Sarmatian) sedimentary sections of the Central Paratethys, two from the Polish Carpathian Foredeep Basin (PCFB) and five from the Eastern Carpathian Foreland Basin (ECFB) of Romania and the Republic of Moldova have been analysed micropalaeontologically to better constrain the Badenian-Sarmatian Extinction Event, characterized by significant taxonomic impoverishment of both foraminifers and ostracods. Our studies show significant palaeoenvironmental changes in the basin including depth, salinity, oxygenation, and organic matter flux. The occurrence of moderately diverse planktonic foraminifera (Globigerina, Globigerinita, Globorotalia, Trilobatus, Orbulina, Velapertina) in the Upper Badenian deposits of the PCFB as well as in the ECFB and their rarity in the lowermost Sarmatian indicate an almost fully marine environment during the latest Badenian, followed by a significant regression and possible appearance of much more restricted marine conditions across the boundary. The taxonomic composition of the Sarmatian foraminifera, ostracoda and calcareous nannofossils indicate that during this interval the salinity fluctuated strongly, with the water regime varying from brackish to normal marine. In addition, the identified micropalaeontological assemblages identified show palaeoenvironmental similarity across different basins of the Central Paratethys. This supports a hypothesis of possible connections during the latest Badenian between different areas of the Central Paratethys, as well as of the existence of a gateway between the Central Paratethys and the Mediterranean realm

Reconstructing orogenic systems made up dominantly by sediments accreted in trenches is challenging because of the incomplete lithological record of the subducted oceanic domain and its attached passive continental margin thrusted by collisional processes. In this respect, the remarkable ~600 km long continuity of sediments exposed in the Eastern Carpathian thin-skinned thrust and fold belt and the availability of quantitative reconstructions for adjacent continental units provide excellent conditions for a paleogeographical study by provenance and sedimentological techniques constraining sediment routing and depositional systems. These sediments were deposited in the Ceahl?u-Severin branch of the Alpine Tethys Ocean and over its European passive continental margin. We report sedimentological, paleomagnetic, petrographic, and detrital zircon U-Pb data of Lower Cretaceous sediments from several thin-skinned tectonic units presumably deposited in the Moldavides domain of the Eastern Carpathians. Sedimentological observations in the innermost studied unit demonstrate that deposition took place in a deepwater basin floor sheets to sandy turbidite system. Detrital zircon age data demonstrate sourcing from internal Carpathian basement units. The sediment routing changes in more external units, where black shales basin floor sheets to sandy mud turbidites were sourced from an external, European continental area. Although some degree of mixing between sources located on both margins of the ocean occurred, constraining a relatively narrow width of the deep oceanic basin, these results demonstrate that the internal-most studied unit was deposited near an Early Cretaceous accretionary wedge, located on the opposite internal side relative to the passive continental margin domain of other Moldavides units.

Reconstructing orogenic systems made up dominantly by sediments accreted in trenches is challenging because of the incomplete lithological record of the subducted oceanic domain and its attached passive continental margin thrusted by collisional processes. In this respect, the remarkable ~600 km long continuity of sediments exposed in the Eastern Carpathian thin-skinned thrust and fold belt and the availability of quantitative reconstructions for adjacent continental units provide excellent conditions for a paleogeographical study by provenance and sedimentological techniques constraining sediment routing and depositional systems. These sediments were deposited in the Ceahl?u-Severin branch of the Alpine Tethys Ocean and over its European passive continental margin. We report sedimentological, paleomagnetic, petrographic, and detrital zircon U-Pb data of Lower Cretaceous sediments from several thin-skinned tectonic units presumably deposited in the Moldavides domain of the Eastern Carpathians. Sedimentological observations in the innermost studied unit demonstrate that deposition took place in a deepwater basin floor sheets to sandy turbidite system. Detrital zircon age data demonstrate sourcing from internal Carpathian basement units. The sediment routing changes in more external units, where black shales basin floor sheets to sandy mud turbidites were sourced from an external, European continental area. Although some degree of mixing between sources located on both margins of the ocean occurred, constraining a relatively narrow width of the deep oceanic basin, these results demonstrate that the internal-most studied unit was deposited near an Early Cretaceous accretionary wedge, located on the opposite internal side relative to the passive continental margin domain of other Moldavides units.

International audience; The phosphate series of the Moroccan High Atlas accumulated during the Upper Cretaceous-Paleogene phosphogenic period, on a biologically-productive shallow-water platform. These phosphate-rich sediments were deposited during a relative sea-level cycle generating major stratigraphic surfaces. Five different types of phosphatic lithofacies are recognized based on their petrographic and sedimentologic features. The pristine phosphate lithofacies corresponds to phosphatic marls formed by francolite authigenesis within the outer platform domain below the storm wave-base (primary phosphogenesis zone). This primary phosphatic lithofacies can be differentiated as a result of the interaction between hydrodynamic autocyclic processes and allocyclic forcing. Accordingly, the granular phosphate lithofacies was formed by in-situ storm and bottom currents that winnowed the pristine phosphate. This winnowed lithofacies, composed of densely-packed peloids, shows relatively high P2O5 concentrations. The turbiditic phosphate resulted from the basinward transport and deposition of other phosphate types by gravity flows leading to normally-graded phosphatic sediment. The phosphatic lags were formed by wave reworking and transporting of pristine and associated granular facies within the inner platform. The karst-filling phosphate corresponds to former phosphate types transported by early transgressive currents and trapped within karstic pockets as phospharudites. The distribution of the different phosphate types across the margin and within the depositional sequences is controlled by the effects of relative sea-level changes. The pristine phosphate and associated winnowed facies are found above the major maximum flooding surface, which is dated by nannoflora to the Selandian-Thanetian transition. The phosphatic turbidites occurred during periods of high sea-level. The karst-related phosphatic facies accumulated during early transgressive stages. The phosphatic lags accumulated mainly during the regressive phases of third and fourth-order sequences. The accumulation processes of the different phosphatic lithofacies control the ore grade of the phosphatic sediments: repeated storm-induced winnowing of pristine phosphate contributes to the enrichment of the phosphate ore grade.

We provide new data on the Black Sea evolution during the preconnection and reconnection stages with the Mediterranean, based on sedimentology, geochemistry, calcareous nannoplankton and ostracods analysis, in 13 cores placed between 141 m and 1315 m water depths. Unit 1 – The Coccolith Mud, Unit 2 - The Sapropel Mud and Unit 3 – The Lacustrine Lutite, including red-brownish depositional intervals, were identified in all studied deep-water cores. These units are not present in a shallow setting, i.e., above 166.7 m water depth, being replaced by sandy levels and shell debris. The red-brownish layers are interpreted as hyperpycnites, but some of the red successions show turbidite features, especially the ones situated on canyon sides, at a water depth below 600 m. In the oldest intercepted Unit 3 of the Neoeuxinian lake, CaCO3 values are constantly low, but towards the top of this unit they show two distinct peaks, interpreted as signals of Bolling–Allerod and Preboreal interstadials. In between, a significant decrease in CaCO3 values, linked to the setting of the Younger Dryas, is coincident in the deep cores with diatom blooms and high frequency of ostracods related to cooler waters. The scarce but continuous occurrence of Emiliania huxleyi nannoplankton species from the top of Unit 3 indicates that the salinity was at least 10–11‰ prior the Sapropel Mud deposition and increase at a least 17‰ within the lower part of Unit. 2. In the same interval, the Ponto-Caspian ostracods are still present. The Mediterranean ostracods consistently occur from the top of Unit 2, when bottom water salinity reached values for allowing their survival. The first bloom of E. huxleyi is placed at the base of Unit 2, where coccolith laminae occur, while the second bloom is placed in Unit 1 that contains exclusively Mediterranean ostracods and consistent assemblages of benthonic foraminifers, similar with the ones present today.

The Paleocene–Eocene Thermal Maximum (PETM) event was a dramatic global warming ∼55.93 Ma ago that resulted in biological extinction events, lithological changes, and major deviations in δ13C and δ18O. The southwestern Tarim Basin of China exposes successive Paleogene strata as a result of Tethys evolution and is considered an ideal region for PETM research.Based on calcareous nannoplankton biostratigraphy, we also used stable isotopes and XRD to analyse the Paleocene–Eocene transition in the Tarim Basin. At the Bashibulake Section, the PETM interval is characterized by (1) an abrupt negative shifts in δ13Corg, δ13Ccarb and δ18O (−3‰, −4.5‰ and −3‰ respectively); (2) an obvious negative correlation between the K-mode (Discoaster, Fasciculithus, Ericsonia, Sphenolithus and Rhomboaster) and r-mode (Biscutum, Chiasmolithus, Toweius) nannofossil taxa coincident with a robust Rhomboaster-Discoaster assemblage; and (3) a significant increase in the percentage of detrital input along with an increase in gypsum content. In the upper part of the Qimugen Formation Micrantholithus and Braarudosphaera are commonly found right up to the top where most of the nannofloras suffer a sharp decrease. In the overlying Gaijitage Formation, calcareous nannofossils disappear completely. These events indicate that the southwestern Tarim Basin was a warm shallow continental shelf during the deposition of the Qimugen Formation. From the early Eocene, the environment changed conspicuously. Evaporation increased and sea level fell, which led to an acid climate. This climate mode continued within the youngest unit studied, the Gaijitage Formation, characterized by the deposition of thick evaporates. Consequently, most of the marine plankton, i.e. calcareous nannoplankton, became disappear, because of the significant climate shift. Keywords: Calcareous nannofossil, Biostratigraphy, Paleocene–Eocene Thermal Maximum (PETM), Tarim Basin

This study presents detailed foraminiferal, ostracod, and calcareous nannofossil analyses of five Middle Miocene sections located in the Central Paratethyan realm, namely in Poland, Romania and the Republic of Moldova. Based on foraminiferal distribution, five biostratigraphically important assemblages (labelled A-E) are distinguished. Foraminifera data combined with ostracoda and nannofossil evidence allowed correlation between the studied sections, and a comparison with the deposits of similar age from the Transylvanian, Vienna and Pannonian basins, as well as with the Transcarpathian regions. The micropaleontological record across the Badenian-Sarmatian boundary interval is also presented.

The sediments brought by several left tributaries of the Lower Danube, such as Cerna, Topolnița, Jiu, Olt, Argeș, Ialomița and Siret were sampled close to their confluence. An overview of the rock provenance is presented, taking into account the identified mineralogical feature based on the mineralogical observations, two heavy mineral associations were identified, having, in general, a clearly provenance signature from lower to medium grade metamorphic units. Other sources of the sampled sediments are represented by the igneous bodies, high grade metamorphics, as well the sedimentary rocks of the external nappes from the Carpathian belt. Besides, the Carpathian surrounding platforms, such as Moesian and Moldavian ones, contribute to the sedimentary input of Danube River. Additional to the mineralogical data, geochemical analysis show a medium maturity grade of the sampled sediments., {"references":["Bădescu D. (2005). Evoluția tectono-stratigrafică a Carpaților Orientali în decursul Mesozoicului și Neozoicului. Editura Economică București.","Balintoni I., Balica C., Ducea M.N., Chen F.K., Hann H.P., Sabliovschi V. (2009). Late Cambrian-Early Ordovician Gondwanan terranes in the Romanian Carpathians: a zircon U-Pb provenance study. Gondwana Research 16: 119–133.","Balintoni I., Balica C., Ducea M., Stremțan C. (2011). Peri-Amazonian, Avalonian-type and Ganderian-type terranes in the South Carpathians, Romania: The Danubian domain basement. Gondwana Research 19: 945–957.","Balintoni I., Balica C. (2012). Avalonian, Ganderian and East Cadomian terranes in South Carpathians, Romania, and Pan-African events recorded in their basement. Mineralogy and Petrology 107/5: 709–725.","Balintoni I., Balica C. (2013). Carpathian peri-Gondwanan terranes in the East Carpathians (Romania): a testimony of an Ordovician, North-African orogeny. Gondwana Research 23: 1053–1070.","Balintoni I., Balica C., Ducea M.N., Hann H.P. (2014). Peri-Gondwanan terranes in the Romanian Carpathians: A review of their spatial distribution, origin, provenance and evolution. Geoscience Frontiers 5: 395–411.","Băncilă I. (1958). Geologia Carpaților Orientali, 367 p, Ed. Științifică București.","Berza T., Balintoni I., Iancu V., Seghedi A., Hann H.P. (1994). South Carpathians. ALCAPA II Field Guidebook, Romanian Journal of Tectonics and Regional Geology, Suppl. 2: 37–50.","Cascalho J., Fradique C. (2007). The sources and hydraulic sorting of heavy minerals on the northern Portuguese continental margin. Developments in Sedimentology 58: 75–110.","Dill H.G., Skoda R. (2019). Provenance analysis of heavy minerals in beach sands (Falkland Islands/Islas Malvinas) – A view to mineral deposits and the geodynamics of the South Atlantic Ocean. Journal of South American Earth Sciences 78: 17–37.","Dimitrescu R. (1978). Structure géologique du massif cristallin Fagăraș-Ezer-Leaota. Rev. Roum. Géol. 22: 43–51.","Dinu C. (1985). Geologic study of the Cretaceous flysch deposits in the upper course of the Trotus Valley (East Carpathians). Anuarul Institutului de Geologie si Geofizica LXV: 5–142.","Duchesne J.-C., Laurent O., Gerdes A., Bonin B., Tatu M., Berza T. (2017). Source constraints on the genesis of Danubian granites in the South Carpathians Alpine Belt Romania. Lithos, 294-295: 198– 221.","Dumitrescu I., Săndulescu M. (1968). Problèmes structuraux fondamentaux des Carpates roumaines et de leur avant-pays. Anuarul Comitetului Geologic 36: 195–218.","Gheucă I. (1988). Versantul sudic al Muntilor Făgăraș, litostratigrafe și tectonică. D. S. Inst. Geol. Geofiz. 72-73/5: 187–205.","Gheucă I., Dinică I. (1986). Litostratigraphie et tectonique du crystalline de Leaota entre Albești-Vallee et Ghimbav Vallee de Bădeanca. D. S. Inst. Geol. Geofz. 70-71/5: 87–95.","Hann H.P., Balintoni C. (1988). Geological Structure of the Olt Valley between Rășinari and Cîineni (South Carpathians), D.S. Șed. Inst. Geol. Geofiz. 72‐73/5:119–128","Hann H.P., Szasz L. (1984) Geological structure of the Olt valley between Câineni and Brezoi (South Carpathians), D. S. Inst. Geol. Geofiz. 68: 23–39.","Hubert J.T. (1962). Zircon-tourmaline-rutile maturity index and interdependence of the composition of heavy minerals assemblages with the gross composition and texture of sandstones. Journal of Sedimentary Petrology 32: 440–450.","Iancu V., Axente V., Bindea G., Ledru P., Maluski H. (1997). HT/LP and MT/MP mylonites related to nappe emplacement in a Palaeozoic convergent plate boundary in the Danubian Units, South Carpathians. Intern. symposium \"Geology in the Danube Gorges\", Belgrad-Bucharest Geoinstitut, Special Edition 25: 289–290.","Iancu V., Berza T., Seghedi A., Gheuca I., Hann H-P. (2005a). Alpine polyphase tectono-metamorphic evolution of the South Carpathians: a new overview. Tectonophysics 410: 337–365.","Iancu V., Berza T., Seghedi A., Mărunțiu M. (2005b). Palaeozoic rock assemblages incorporated in the South Carpathian Alpine thrust belt (Romania and Serbia): a review. Geologica Belgica 8/4: 48–68.","Iancu V., Seghedi A. (2017). The South Carpathians: Tectono-metamorphic units related to Variscan and Pan-African inheritance. Geo-Eco-Marina 23: 245–262.","Mange M.A., Maurer H.F.W. (1992). Heavy minerals in colour. Ed. Chapman & Hall, London, 148 p.","Mațenco L., Bertotti G. (2000). Tertiary tectonic evolution of the external East Carpathians (Romania). Tectonophysics 316: 255–286.","Mațenco L., Bertotti G., Cloetingh S., Dinu C. (2003). Subsidence analysis and tectonic evolution of the external Carpathian - Moesian platform region during Neogene times. Sedimentary Geology 156: 71–94.","Medaris G.Jr., Ducea M., Ghent E.D., Iancu V. (2003). Conditions and timing of high-pressure metamorphism in the South Carpathians, Romania. Lithos 70: 141–161.","Melinte-Dobrinescu M.C., Jipa D. (2008). Stratigraphy of the Lower Cretaceous sediments from the Romanian Carpathian Bend area. Acta Geologica Sinica, English Edition 81/6: 949–956.","Melinte-Dobrinescu M.C., Jipa D., Brustur T., Szobotka S. (2009). Eastern Carpathian Cretaceous oceanic red beds: lithofacies, biostratigraphy and paleoenvironment. In: Hu X., Wang C., Scott R.W., Wagreich M. & Jansa L. (eds.), Cretaceous Oceanic Red Beds: Stratigraphy, Composition, Origins and Paleoceanographic/Paleoclimatic Significance. SEPM Special Publication (Tulsa, OK), 91: 111–119.","Morton A.C. (1985). Heavy minerals in provenance studies. In: Zuffa, G.G. (Ed.), Provenanceof Arenites. Reidel, Dordrecht: 249–277.","Oaie G., Seghedi A., Rădan S., Vaida M. (2005). Sedimentology and surce area composition for the Neoproterozoic - Eocambrian turbidites from East Moesia. Geologica Belgica 8/4: 78–105.","Panin N. (1996). Danube Delta: Genesis, evolution, geological setting and sedimentology, Geo-Eco-Marina 9: 7–23.","Plimer I.R., Elliott S.M. (1979). The use of Rb/Sr ratios as a guide to mineralization. Journal of Geochemical Exploration 12: 21–34.","Săbău G., Massonne H-J. (2003). Relationship among eclogite bodies and host rocks in the Lotru Metamorphic Suite (South Carpathians, Romania): Petrological evidence for multistage tectonic emplacement of eclogites in a medium pressure terrain. International Geology Review 45: 225–262.","Săbãu G., Negulescu E. (2006). Metamorphic forming and evolution conditions of the eclogites in the Topolog Complex, Făgăraș Mountains. Romanian Journal of Petrology 78: 39–46.","Săndulescu M., Kräutner H.G., Balintoni I., Russo-Săndulescu M., Micu M. (1981). The Structure of the East Carpathians (Moldavia - Maramures Area) Guide Exc. B1, Carp.-Balk. Geol. Assoc., XII Congr. Inst. Geol. Geophys., 92 p, Bucuresti.","Săndulescu M. (1984). Geotectonica României. Ed. Tehnică București.","Sandulescu M. (1994) Overview on Romanian Geology, Rom. Journ. Tect. Reg. Geol., 75, Suppl. 2, 3-15.","Săndulescu M. (1988). Cenozoic tectonic history of the Carpathians. In: Royden L.H., Horvath F. (eds.), The Pannonian basin, a study in basin evolution. AAPG Memoir 45: 17–25.","Săndulescu M., Visarion M. (1988). La structure des plate – formes situées dans l´avant - paysetau - des sous des nappes du flysch des Carpathes orientales. Studii tehnico-economice, Seria Geofizica 15: 62–67.","Săndulescu M. (1996). Overview on Romanian Geology. Romanian Journal of Tectonics and Regional Geology 75/2: 3–15.","Seghedi A., Berza T., Iancu V., Mărunțiu M., Oaie G. (2005). Neoproterozoic terranes in the Moesian basement and in the Alpine Danubian nappes of the South Carpathians. Geologica Belgica 8/4:4–19.","Seghedi A., Oaie G. (1995). Palaeozoic evolution of North Dobrogea, 5-15. In: Săndulescu M., Seghedi A., Oaie G., Grădinaru E. & Rădan S. (eds), Field Guidebook, Central and North Dobrogea. IGCP Project no. 369 'Comparative evolution of PeriTethyan Rif Basins', Mamaia 1995, 75 p.","Seghedi A. (2012). Palaeozoic formations from Dobrogea and Pre-Dobrogea – An overview. Turkish Journal of Earth Sciences 21: 669– 721 [in Turkish, with English summary].","Schuller V., Frisch W. (2006). Heavy mineral provenance and paleocurrent data of the Upper Cretaceous Gosau succession of the Apuseni Mountains (Romania). Geologica Carpathica 57/1: 29–39.","Ștefănescu M., Hann H. P., Gheuca I., Szasz L., Ștefănescu M. (1982). Harta geologică a României, scara 1:50000, foaia Titești. Institutul Geologic al României. București.","Ștefănescu M. (1995). Stratigraphy and structure of Cretaceous and Paleogene flysch deposits between Prahova and Ialomița valleys. Romanian Journal of Tectonics and Regional Geology 76 (Supplement): 1–49.","Wang K., Shi X., Yao Z., Liu J., Liu J., Xu T. (2019). Heavy-mineral-based provenance and environment analysis of a Pliocene series marking a prominent transgression in the south Yellow Sea. Sedimentary Geology 382: 25–35."]}

This study aims to bring new constraints on the Eocene stratigraphy of the northern edge of Istria Basin, located in Western Black Sea. For achieving our goal, we have studied several core reports containing the description of the lithology and microfossils assemblages (foraminifera, ostracods and calcareous nannofossils) from 3 wells drilled in the northern Istria Basin. Thus, we were able to identify lithological and biostratigraphic constraints, allowing to generate a coherent correlation scheme for the Eocene deposits, with precise age assignment and advanced models of the IB evolution during the Eocene. The lithology of the 3 wells, situated in the Sinoe, Lebăda West and Lebăda East areas, is mainly represented by calcareous sandstones and siliciclastic ones. The biostratigraphy indicates that the deposits of the Sinoe and Lebăda West wells are Middle Eocene in age (mostly the upper part), while in the Lebăda East well a late Early to Middle Eocene age was assigned., {"references":["Agnini C., Muttoni G., Kent D.V., Rio D., 2006. Eocene biostratigraphy and magnetic stratigraphy from Possagno, Italy: The calcareous nannofossil response to climate variability. Earth and Planetary Science Letters, 2241: 815-830.","Allen A.P., Allen R.J., 2005. Basin Analysis: Principles and Applications. The 2nd Edition. Blackwell Publishing, Malden.","Belousov V.V., Volvovsky B.S., Arkhipov I.V., Buryanov V.B., Evsyukov Y.D., Goncharov V.P., Gordienko V.V., Ismagilov D.F., Kislov G.K., Kogan L.I., Kondyurin A.V., Kozlov V.N., Lebedev L.I., Lokholatnikov V.M., Malovitsky Y.P., Moskalenko V.N., Neprochnov Y.P., Ostisty B.K., Rusakov O.M., Shimkus K.M., Shlezinger A.E., Sochelnikov V.V., Sollogub V.B., Solovyen V.D., Starostenko V.I., Starovoitov A.F., Terenkov A.A., Volvovsky I.S., Zhigunov A.S., Zolorarev V.G., 1988. Structure and evolution of the earth's crust and upper mantle of the Black Sea. In: Finetti, I. (Ed.), Monograph of the Black Sea. Bolletino di geofisica teoretica ed applicata, Trieste, 109-196.","Berggren W.A., Van Couvering J.A., 1974. The Late Neogene Biostratigraphy, geochronology and paleoclimatology of the last 15 million years in marine and continental sequences Palaeogeogr. Palaeoclimatol. Palaeoecol.16 (1-2): 1-215.","Berggren W.A., Kent D.V, Swisher III C.C., Aubry M.-P., 1995. A revised Cenozoic geochronology and chronostratigraphy. In: Berggren W.A., Kent D.V, Swisher C.C. III, Aubry M.-P., Hardenbol J., (Eds.), 1995. Geochronology, Time Scales and Global Stratigraphic Correlation. SEPM (Society for Sedimentary Geology) Special Publication 54: 129-212.","Bindiu R., 2013. Fossil agglutinated foraminifera and their relationship to the depositional environments in the Northern part of the Eastern Carpathians, Romania [in Romanian], Ph.D. Thesis, Babes-Bolyai University, Cluj-Napoca","Blow W.H., 1969. Late Middle Eocene to recent planktonic foraminiferal biostratigraphy. Proceedings of the First International Conference on Planktonic Microfossils, Geneva, 1967, 1: 199-422.","Blow W.H., 1979. The Cainozoic Foraminifera. Vols 1-3. E.J. Brill., Leiden, 1413 p.","Bolli H.M., Saunders J.B., Perc h-Nielsen K. (eds), 1985. Plankton Stratigraphy. Cambridge University Press, Cambridge, 407 p.","Bombiţă G., 1963. Contribuţii la corelarea Eocenului epicontinental din R.P. România. Edit. Acad. R.P.R., Bucharest, 113 p.","Boote R.D., 2017. The geological history of the Istria 'Depression', Romanian Black Sea shelf: tectonic controls on second-/third order sequence architecture. Geological Society London, Special Publications, 464: 169-209.","Bown P.R., Dunkley Jones T. 2012. Calcareous nannofossils from the Paleogene equatorial Pacific (IODP Expedition 320 Sites U1331- 1334). Journal of Nannoplankton Research, 32(2): 3-51.","Chaisson W.P., Pearson P.N., 1997. Planktonic foraminifer biostratigraphy at Site 925: middle Miocene - Pleistocene, Proceedings of the Ocean Drilling Program: Scientific Results, 154: 3-32.","Dinu C., Wong H.K., Țambrea D., Mațenco L., 2005. Stratigraphic and structural characteristics of the Romanian Black Sea shelf. Tectonophysics, 410: 417-435.","Folk R.L., 1974. Petrology of Sedimentary Rocks. Hemphill Publishing Co., Austin,170 p.","Görür N., 1988. Timing of opening of the Black Sea basin. Tectonophysics, 147: 247-262.","Görür N., 1997. Cretaceous Syn- to Postrift Sedimentation on the Southern Margin of the Western Black Sea Basin, Regional and Petroleum Geology of the Black Sea, AAPG Memoire, 68: 227-240","Gebhardt H., Ćorić S., Darga R., Briguglio A., Schenk B., Werner W., Andersen N., Sames B., 2013. Middle to Late Eocene paleoenvironmental changes in a marine transgressive sequence from the northern Tethyan margin (Adelholzen, Germany). Austrian Journal of Earth Sciences,106(2): 45-72.","Georgiev G., 2012. Geology and Hydrocarbon Systems in the Western Black Sea. Turkish Journal of Earth Sciences, 21: 723-754.","Gradstein F.M., 2012. The Geologic Time Scale. Elsevier, Amsterdam,1176 p.","Hippolyte J.C. Müller C., Kaymakçi N., Sangu E., 2010. Dating of the Black Sea Basin: new nannoplankton ages from its inverted margin in the Central Pontides (Turkey). Geological Society, London, Special Publications, 340: 113-136.","Holbourn D.A., Henderson A.S., Macleod N., 2013. Atlas of Benthic Foraminifera, Wiley-Blackwell, London, 634 p.","Ionescu A.L., 2006. Formation evaluation by integrated analysis of geological and borhole geophysics data. Case study, stuctures from the Romanian Black Sea continental platform [in Romanian]. PhD Thesis, Faculty of Geology and Geophysics. University of Bucharest, Bucharest, 68 p.","Ionescu G., 2000. Facies architecture of the Paleogene Formations of the NW shelf of the Black Sea (in Romanian). PhD Thesis, Faculty of Geology and Geophysics. University of Bucharest, Bucharest, 133 p.","Ionescu G., 2002. Facies architecture and sequence stratigraphy of the Black Sea offshore Romania. In: Dinu C., Mocanu V. (Eds.), Geology and Tectonics of the Romanian Black Sea Shelf and its Hydrocarbon Potential 2: 43-51.","Kaminski M.A., Gradstein F.M., 2006. Atlas of Paleogene Cosmopolitan Deep-Water Agglutinated Foraminifera. Grzybowski Foundation Special Publication, 10: 547 p.","Kennet J.P., Srinivasan M.S., 1983. Neogene planktonic foraminifera - A phyllogenetic atlas, Hutchinson Ross Publishing Company, 265 p.","Krezsek C., Bercea R.-I., Tari G., Ionescu G. 2017. Cretaceous sedimentation along the Romanian margin of the Black Sea: inferences from onshore to offshore correlations. In: Simmons M.D., Tari G.C. & Okay A.I. (Eds.), Petroleum Geology of the Black Sea. Geological Society, London, Special Publications, 464","Martini E. 1971. Standard Tertiary and Quaternary calcareous nannoplankton zonation. Proceedings of the Second International Conference on Planktonic Microfossils, Rome 1970 2: 739-785.","Munteanu I., 2012. Evolution of the western Black Sea: Kinematic and sedimentological inferences from geological observations and analogue modelling. Utrecht Studies in Earth Sciences, 16, 169 p.","Munteanu I., Maţenco L., Dinu C., Cloetingh S., 2011. Kinematics of backarc inversion of the Western Black Sea Basin. Tectonics, 30: 1-21.","Murray J.W., 2006. Ecology and applications of benthic foraminifera. Cambridge University Press, New York, 440 p.","Nikishin A.M, Korotaev M.V., Ershov A.V., Brunet M.-F., 2003. The Black Sea basin: tectonic history and Neogene-Quaternary rapid subsidence modelling.Sedimentary Geology, 1-4: 149-168","Nikishin A.M., Okay A., Tüysüz O., Demirer A., Wannier M., Amelin N., Petrov E., 2015. The Black Sea basins structure and history: New model based on new deep penetration regional seismic data. Part 2: Tectonic history and paleogeography. Marine and Petroleum Geology, 59: 656-670.","Okay A.I., Şengör A.M.C., Görür N., 1994. Kinematic history of the opening of the Black Sea and its effect on the surrounding regions. Geology, 22: 267-270.","Okay A.I., Tüysüz O., 1999. Tethyan sutures of northern Turkey. Geological Society, London, Special Publications,156: 475-515.","Olsson R.K., Hemleben C., Huber B.T. & Berggren W.A., 2006. Taxonomy, biostratigraphy, and phylogeny of Eocene Globigerina, Globoturborotalita, Subbotina, and Turborotalita. In: Pearson, P. N., Olsson, R. K., Hemleben, C., Huber, B. T. & Berggren, W. A. (eds) Atlas of Eocene Planktonic Foraminifera. Cushman Foundation for Foraminiferal Research, Special Publication. 41: 111-168.","Pearson P.N., Chaisson W.P., 1997. Late Paleocene to middle Miocene planktonic foraminifer biostratigraphy of the Ceara Rise. In: Shackleton, N.J., Curry, W.B., Richter, C., Bralower, T.J. (Eds.), Proceeding of the Ocean Drilling Program: Scientific Results, 154, 33-68.","Pearson P.N., Berggren W.A., 2006. Taxonomy, biostratigraphy and phylogeny of Morozovelloides N. Gen. In: Pearson P.N., Olsson R.K., Huber B.T., Hemleben C., Berggren, W.A. (Eds.), Atlas of Eocene Planktonic Foraminifera, 327-342. Cushman Foundation Special Publication, 41, Fredericksburg, USA.","Perch-Nielsen K., 1985. Cenozoic calcareous nannofossils. In: Bolli H.M., Saunders J.B., Perch-Nielsen K. (Eds.), Plankton Stratigraphy. Cambridge University Press, Cambridge, 427-555.","Popescu I., Lericolais G., Panin N., Wong, H. K., Droz L., 2001. Late Quaternary Channel avulsions on the Danube Deep-Sea Fan, Black Sea. Marine Geology, 179 (1-2): 25-37.","Popov S.V., Akhmetiev M.A., Zaporozhets N.I., Voronina A.A., Stolyarov A.S., 1993. Evolution of the eastern Paratethys in the Late Eocene-Early Miocene: The type section of the Maikop Group (Oligocene–lower Miocene) at the Belaya River (North Caucasus). Depositional environment and hydrocarbon potential. Stratigraphy and Geological Correlation, 1: 10-39.","Popov S.V., Rögl F., Rozanov A.V., Steininger F., Shcherba I.G., Kovač M., 2004. Lithological-Paleogeographic maps of Paratethys 10 maps Late Eocene to Pliocene, In: Senckenberg, C.F. (Ed.). Schweizerbart Science Publishers, Sttutgart.","Schmiedl G., Mackensen A., 1993. Cornuspiroides striolatus (Brady) and C. rotundus nov. spec.: large miliolid foraminifera from Arctic and Antarctic oceans. Journal of Foraminiferal Research, 23: 221-230.","Schnitker D., 2007. Cenozoic deep water benthic foraminifers, Bay of Biscay, DSDP Initial reports, 48: 37.","Tappan, H. 1980: The paleobiology of plant protists. Freeman & Co., 678- 803.","Toumarkine M., Luterbacher H.P., 1985. Paleocene and Eocene Planktic Foraminifera. In: Bolli H.M., Saunders J.B., Perch-Nielsen K., (Eds.), Plankton Stratigraphy. Cambridge University Press, Cambridge, 87-154.","Tucker M.E., 2001. Sedimentary Petrology: An introduction to the Origin of Sedimentary Rocks. 3rd Ed., Blackwell Publishing, 291 p.","Țambrea D., 2007. Subsidence analysis and thermo-tectonic evolution of Histria Depression (Black Sea). Implications in hydrocarbon generation [in Romanian], Ph.D. Thesis, Faculty of Geology and Geophysics. University of Bucharest, Bucharest, 165 p.","Țambrea D., Răileanu A., Boroși V., 2002. Seismic facies and depositional framework in central Romanian Black Sea offshore. Implications for hydrocarbon exploration. In: Dinu C., Mocanu V. (Eds.), Geology and Tectonics of the Romanian Black Sea shelf and its Hydrocarbon Potential. BGF Special Volume, 2: 85-100.","Vincent S.J., Morton A.C., Carter A., Gibbs S., Barabadze T.G., 2007. Oligocene uplift of the Western Greater Caucasus: an effect of initial Arabia–Eurasia collision. Terra Nova, 19: 160-166.","Wade B.S., Olsson R.K., Pearson P.N., Edgar K.M., Premoli Silva I., 2018. Taxonomy, biostratigraphy, and phylogeny of Oligocene Subbotina. In: Wade B.S., Olsson R.K., Pearson P.N., Huber B.T., Berggren W.A. (Eds.), Atlas of Oligocene Planktonic Foraminifera. Cushman Foundation for Foraminiferal Research, Special Publication,46: 307-330.","Wade B.S., Pearson P.N., Berggren W.A., Palike H., 2011. Review and revision of Cenozoic tropical planktonic foraminiferal biostratigraphy and calibration to the geomagnetic polarity and astronomical time scale. Earth-Science Reviews, 104: 111-142","Wang P., Li C-F., Li Q., 2014. Geology of the China Seas, Volume 6, Elsevier, Amsterdam, 702 p.","Yilmaz Y., Tüysüz O., Yigitbas E., Gen, S.C, Şengör A.M.C., 1997. Geology and Tectonic Evolution of the Pontides. In: Robinson, A.G. (Ed.), Regional and Petroleum Geology of the Black Sea and Surrounding Region. AAPG Memoirs, 68: 183-226.","Young J.R., 1998. Neogene. In: Bown, P.R. (Ed.), Calcareous Nannofossil Biostratigraphy. British Micropalaeontological Society Publication Series, Chapman & Hall/Kluwer Academic Publishing, London, 225-265.","https://www.gebco.net/","https://mikrotax.org","www.foraminifera.eu","www.marinespecies.org"]}

The Black Sea is a semi-enclosed marginal basin, which connects with the Mediterranean Sea through the Bosphorus Strait, Marmara Sea and Dardanelles Strait. Beside the connection with the Mediterranean Sea, in the Late Pliocene-Pleistocene times the Black Sea experienced a period of connection with the Caspian Sea through the Manych Corridor due to the melt waters from the Scandinavian ice sheets (Fedorov, 1977; Major et al., 2006). In the deeper parts of the Black Sea basin, i.e., below 200 m water depth, Ross and Degens (1974) identified three litho-stratigraphic units (from young to old): Unit 1 (the microlaminated coccolith ooze, deposited under marine conditions), Unit 2 (the sapropel mud, corresponding to an anoxic phase), and Unit 3 (the lacustrine lutite deposited during the freshwater or oligohaline stage). In the early Holocene, water composition in the Black Sea evolved from brackish to marine; biotical turnover mirrors this change. The transition of the Black Sea from an inland lake to a marine basin during the last glacial/deglacial episode is still generating discussion in the scientific community. In this study, high resolution microfaunal analyses coupled with isotopic and calcium carbonate performed on an AMS 14C dated core, 09 SG 13, revealed changes that occur in the Black Sea from the Last Glacial Maximum through the transition to the present day semi-enclosed marine basin. In the sedimentary record this deglaciation accumulated allochthonous continentally derived red sediments, simultaneous with the global Heinrich Event 1, 18 to 15 kyr BP., {"references":["Fedorov P.V. (1977). Late Quaternary history of the Black Sea and southern seas of Europe. In: Kaplinand, P.A., Shcherbakov, F.A. (Eds.), Paleogeografiia i otlozheniia pleistotsena iuzhnykh morei SSSR [Paleogeography and Deposits of the Pleistocene of the Southern Seas of the USSR]. Nauka, Moscow, pp. 25-32 (in Russian)","Major C.O., Goldstein S.L., Ryan W.B.F., Lericolais G., Piotrowski A.M., Hajdas I. (2006). The co-evolution of Black Sea level and composition through the last Deglaciation and its paleoclimatic significance. Quaternary Science Reviews 25: 2031-2047","Ross D.A., Degens E.T. (1974). Recent sediments of the Black Sea. In: Degens E.T. and Ross D.A. (Eds.), The Black Sea: Geology, Chemistry, and Biology. American Association of Petroleum Geologists, Tulsa, USA: 183–199"]}

The sedimentary model of coastal deposits in eastern Rhodes over the last 2 Ma is refined and improved in accuracy. New field investigations and U/Th dating of Spondylus bivalve shells, combined with micropalaeontological and sedimentological data, allow the recognition of four synthems separated by major erosional surfaces. We present here evidence for two of these erosional surfaces. This new model allows the identification and quantification of the vertical movements recorded by the studied exposures. The history of these vertical motions is characterized by two periods of uplift and two periods of subsidence. Such an evolution is unique at the regional scale in the eastern Hellenic forearc. We interpret these results as reflecting the individualization of Rhodes as a single tectonic block during increasing trench bending. This trench bending is accommodated by an increase in the curvature of the forearc during the last 2 Ma. © 2018 The Author(s).

Since Antiquity, when the Greek colonization of Pontus Euxinus started in the 7th century BC, the Black Sea area was the scene of diverse human activities, among which the most important was the trading navigation. Most of the colonies and settlements founded by the ancient Greek colonists comming from Megara, Milet, Corinth or Heraclea Pontica were located along the coast and were connected to each other and also to the metropolis of origin mainly by nautical trade routes running along the shores. Over millennia, the navigation along Black Sea maritime routes has intensified and diversified, many military confrontations have also taken place, all these leading to the accumulation on the seabed of numerous shipwrecks. Although the history of navigation and its associated activities along the western coast of the Black Sea is over 25 centuries old, paradoxically, the number of shipwrecks discovered until now, especially from the ancient and medieval periods, is unnaturally low. However, if such discoveries have been made in the Bulgarian coastal waters at Kitten (e.g. Batchvarov, 2014) and Ropotamo (e.g. Pachero-Ruiz et al., 2018, Sturt et al., 2018), in Bulgarian deep waters (see the fabulous results of Black Sea Maritime Archaeology Project, 2017-2018), in Ukrainean and Turkish waters at Chersonesos (Brennan et al., 2011) and respectively off Sinop Peninsula (Piechota et al., 2010, Brennan et al., 2011, Sahin et al., 2016), until recently such information regarding findings of interest for the submerged cultural heritage (e.g. Scarlat, 1973; 1975, Munteanu & Vochițu, 2009, Atanasiu-Croitoru, 2015) made in Romanian waters were very few and only published in Romanian. Recent findings of researches carried out during the few last years (e.g. Caraivan et al., 2015, Pflederer et al., 2016, Dimitriu et al., 2018), as well as synthesis (e.g. Custurea et al., 2007, Munteanu, 2016, Dobre, 2016, Dimitriu et al., 2019), of the archaeological discoveries made over the last decades in the coastal waters provide information that clearly invalidate the false impression regarding a poor submarine cultural heritage off Romanian coast. Thus, the synthesis of all available data and information regarding the geo-archaeological findings made in Romanian waters indicate until present the certain existence of over 120 shipwrecks (Fig. 1), among which 15 belong to former wooden ships, whose ages range from Antiquity to the beginning of 20th c. BC. Within the paper, the authors focus exclusively on the southern half of the Romanian coastal zone. When assessing the potential of the marine shallow waters off the southern Romanian coast, from the perspective of its submerged cultural heritage, we must consider at least the following essential aspects: (1) – the entire coastal zone is subsiding by 1-2 mm/y to 3-4 mm/y (e.g. Popescu & Drăgoescu, 1986, Dimitriu et al., 2017, etc.) and (2) – the secular mean sea level rise is about 0.5-1 mm/y. Combined, these two processes determine the sinking of the site located in ancient times at the sea level, to 6 m or more bellow the curent mean sea level., {"references":["Atanasiu-Croitoru A. (2015). Ancore antice și medievale de pe epavele Mării Negre. Descoperiri recente. Collegium Mediense, V, Comunicări Științifice, XIV, 36-41","Batchvarov K. (2014). The Hull Remains of a Post Medieval Black Sea Merchantman from Kitten, Bulgaria. The International Journal of Nautical Archaeology, 43.2, 397-412, doi: 10.1111/1095-9270.12057","Brennan M.L., Ballard L.D., Bell K.L.C. (2011). Archaeological oceanography and environmental characterization of shipwrecks in the Black Sea. The Geological Society of America, Special Paper 473, 179-188","Caraivan G., Oaie G., Bujini J., Seghedi A., Bosneagu R., Chera C., Voinea V., Palazov A., Stancheva M., Shtirkov H., Peev P., Krastev A., Mircheva D., Popa M., Stanica A., Ion G., Dimitriu R., Sava C.S., Popa A., Dutu F., Anghel S., Opreanu G., Vasiliu D., Balan S., Teaca A., Pop C., Pojar I., Scrieciu A., Iordache G., Slavova K., Hristova R., Tasev V. (2015). HERAS Book - Submarine Archaeological Heritage of the Western Black Sea Shelf. GeoEcoMar Constanta, 51 pp","Custurea G., Dima M., Talmațchi G., Velter A.M. (2007). Coin hoards of Dobrudja I. Ex Ponto, Constanța, ISBN: 978-973-644-709-9, 297 pp","Dimitriu R.G., Stanciu I.M., Barbu M.-B., Dobrev N., Dumitru P.D. (2017). First results on the western Black Sea coastal geodynamics resulted from GeoPontica permanent GNSS stations network data processing. 17th International Multidisciplinary Scientific GeoConference SGEM2017, Conference Proceedings, 17, 11, 149-158, ISSN 1314-2704, DOI: 10.5593/sgem2017/11/S01.019","Dimitriu R.G., Nuțu G., Popa A., Barbu M.-B. (2018). High resolution geophysics off Danube delta's shore line for the evaluation of its cultural heritage load. Case study: the mouth of New Dunavăț paleo-distributary. 18th International Multidisciplinary Scientific GeoConference SGEM2018, Conference Proceedings, 18, 1.1, 855-862, ISSN 1314-2704, ISBN 978-619-7408-35-5, DOI: 10.5593/SGEM2018/1.1/S05.106","Dimitriu R.G., Dobrinescu C., Nuțu G., Caraivan G., Barbu M.B., Bodolică V. (2019). New steps towards revealing the true extension of the submarine cultural heritage off Romanian coast. 27th Assembly of Advanced Materials Congress, Symposium on Archaeology & Cultural Heritage, 11-14 August 2019, Stockholm, Sweden, Proceedings & Abstracts Book, 2 pp, ISBN: 978-91-88252-20-3, DOI: 10.5185/eamc2019","Dobre L.M. (2016). Underwater archaeology. Wooden shipwrecks discovered in Romania between 1989-2015 (in Romanian). in Current Trends in the protection of archaeological heritage in Romania and the Republic of Moldova (ed. Mustatea, S.), Ed. Arc, Chisinau-Iasi, 191-209","Munteanu C., Vochițu A. (2009). Țigle și olane de pe epava antică Mangalia B. Pontica, 42, 117-132","Munteanu C. (2016). Ancient navigation and underwater research in Romania: A selective bibliography. Brukenthal Acta Musei, XI, 1, 33-39","Pachero-Ruiz R., Adams J., Pedrotti F. (2018). 4D modelling of low visibility Underwater Archaeological excavations using multi-source photogrammetry in the Bulgarian Black Sea. Journal of Archaeological Science, 100, 120-129","Piechota D., Ballard R.D., Buxton B., Brennan M. (2010) In situ preservation of a deep-sea wreck site: Sinop D in the Black Sea. Studies in Conservation, 6-11, DOI: 10.1179/sic.2010.55.Supplement-2.6","Pflederer T., Fiederling M., Ahl M. (2016). Scwarzes Meer, Rumänien. Das römerzeitliche Wrack \"Rusu\". Jahresbericht der Bayerischen Gesellschaft für Unterwasserarchäologie e. V. 17, 5-6","Popescu M.N., Drăgoescu I. (1986). The new map of recent vertical crustal movements in Romania - scale 1:1,000,000. Rev. Roum. Geol. Geophys. Geogr., s. Geophysique, 30, 3-10","Sahin D., Tarakci Y., Karsli Z., Eyubogly B., Aslan O.S. (2016). Inner harbour wrecks of Sinop. Rapp. Comm int. Mer Medit., 41, 21","Scarlat C. (1973). Portul antic Callatis. Cercetări de arheologie submarină. Acta Mvsei Napocensis, Cluj, X, 529-540","Scarlat C. (1975). Portul antic Tomis și peninsula submersă Tomis, o așezare geto-dacică anterioară sosirii navigatorilor greci. Cercetări de arheologie submarină. Muzeul Național, II, 257-272","Sturt F., Flemming N.C., Carabias D., Jons H, Adams J. (2018). The next frontiers in research on submerged prehistoric sites and landscapes on the continental shelf. Proceedings of the Geologists' Association, 129, 654-683"]}

International audience; The Zambezi Delta draining the Southern African Plateau and the southern part of the East African Rift is one of a the largest delta of Africa with a long-lasting history starting during Early Cretaceous with more than 12 km of sediments deposited. The Zambezi Delta is therefore a unique archive of the past topographic evolution of southern and eastern Africa and their related deformations, but also of the climate changes, global and regional (consequences of local topographic growths). Understanding this archive supposes to get a high-resolution dating of the sediments. Our two objectives are here (1) to construct an age model of the Zambezi Cenozoic delta using a combination of biostratigraphy, orbital stratigraphy and sequence stratigraphy and (2) to determine the palaeoprecipitation variations of the Zambezi catchment from the Oligocene to present day in a known tectonic framework. The Neogene sequences were dated at high-resolution assuming that the third order sequences are of eustatic origin and record long-term eccentricity cycles. The sequences were correlated in ages on the calculated Earth orbital solutions of Laskar for the time intervals provided by the biostratigraphy (nannofossils, planktonic foraminifers). The palaeoprecipitation record was based on the definition of a humidity index based on pollen analysis and associated botanical associations. The late Oligocene was a quite wet period getting dryer in the uppermost Chattian. The base Tortonian (11 Ma) was a humid period. The Messinian was a dry period with a slight increase of the humidity during the Zanclean and a sharp increase around the Zanclean-Piacenzian boundary. The Zambezi Delta has recorded the uplifts of the Southern African Plateau (around 85 Ma and around 25 Ma) and those of the southward migration of the East African Rift (since 5.5 Ma).