An Albian–Turonian shallow-marine carbonate succession of the Bey Dağları (Western Taurides, Turkey): biostratigraphy and a new benthic foraminifera Fleuryana gediki sp. nov.
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Cenomanian
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In the Cenomanian shallow-water carbonates of Northwestern Istria five biostratigraphic zones have been established: CEN-1 Ovalveolina maccagnoae and Sellialveolina viallii biozone in the early Lower Cenomanian; CEN-2 O. maccagnoae to Chrysalidina gradata interval zone in the late Lower Cenomanian; CEN-3 C. gradata biozone in the early Middle Cenomanian, locally subdivided into two subzones: CEN-3a C. gradata and orbitolinids (lower part) CEN-3b C. gradata without orbitolinids (upper part); CEN-4 C. gradata and Broeckina (P.) balcanica biozone in the late Middle Cenomanian, and CEN-5 C. gradata, B. (P.) balcanica and Vidalina radoicicae biozone in the Upper Cenomanian.
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Cenomanian succession (Sarvak Formation) is well distributed along Zagros area particularly in the south portion of the Zagros (Fars area). This study attempts to determine the precise biostratigraphic biozones of four stratigraphic sections selected from the Cenomanian strata south Zagros basin, including the sections of Nour Abad, Samghan, Doroodzan, and Arsanjan. The vertical distribution of the index foraminifers confirms a faunal assemblage of benthic and planktic foraminifers in the mentioned stratigraphic sections. The received Biostratigraphic data of this work reveals well developed benthic foraminifers and well distributed Cenomanian planktons in the uppermost lithostratigraphic part of the studied Sarvak exposures. However, the established biozones of the Sarvak Formation represent the Cenomanian age, which is similar to many recognized Cenomanian biozones in the Tethyan realm, whereas the foraminiferal biostratigraphy of the Arsenjan stratigraphic column is assigned to the Late Albian to Early Cenomanian age. Since benthic foraminifers are well expanded in studied section of Sarvak Formation, the presence of pelagic biofacies is a proof of transgression in some studied sections. However, the established biozones support that geologic setting is the most factor which controls vertical distribution of foraminifers and other microfossils during the deposition of Sarvak Formation. The received biostratigraphic data of the Sarvak Formation determines subdivision of Cenomanian age in the South Zagros basin clearly.
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Larger foraminifera were collected from various Paleocene and Eocene localities in western Cuba. Included was a mea- sured section at San Francisco de Paula in Ciudad de la Habana Province in the Apolo and Capdevila Formations. This section spans the Paleocene/Eocene boundary and has been the focus of intensive biostratigraphic work. In this study, the stratigraphic occurrences of the larger foraminifera were correlated to biozonations based on planktonic foraminifera, calcareous nannofossils, radiolaria, and smaller benthic foraminifera already identified at San Francisco de Paula. Most of the above localities consist of synorogenic sedimentary rocks and the larger foraminifera collected from these sites have in fact been transported to deep water. In order to obtain some in situ larger foraminfera, additional upper Paleocene and lower Eocene samples were obtained from 10 wells in episutural basins from throughout Cuba. In all, eleven species of larger foraminifera were identified from the upper Paleocene and lower Eocene of Cuba. These are: Ranikothalia catenula (Cushman and Jarvis) (=Operculina catenula 1932), Discocyclina barkeri Vaughan and Cole, Discocyclina anconensis Barker, Discocyclina weaveri Vaughan, Eoconuloides lopeztrigoi (Palmer) (=Amphistegina lopeztrigoi 1934), Eoconu- loides wellsi Cole and Bermudez, Eofabiania cushmani (Vaughan) (=Discocyclina cushmani 1929), Athecocyclina stephensoni (Vaughan) (=Discocyclina stephensoni 1929), Pseudophargmina cedarkeysensis, Cole, Hexagonocyclina cristensis (Vaughan) (=Orbitoclypeus? cristensis 1924), and Cushmania americana (Cushman) (=Conulites americana 1919). The larger foraminifera from Paleocene age samples contain an assemblage recognized throughout the Caribbean and Gulf Coastal Plain as the Ranikothalia catenula fauna. Eocene samples contain an assemblage of larger foraminifera refered to here as the Eoconuloides wellsi fauna. Based onI data collected at the San Francisco de Paula section, the change from the Ranikothalia catenula fauna to the Eoconuloides wellsi fauna appears to post-date the benthic faunal turnover associated with the bathyal realm.
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Ten benthic larger foraminifera species Cisalveolina cf. lehneri� (rEichEl, 1941),�C.�frassi (Gűmbel, 1872), Sellialveolinaviallii cOlalOnGO, 1963, Reticulinellareicheli�(cuvilliEr etal., 1969), Orbitolina (Mesorbitolina)�texana�(rOEmEr, 1849), Spiroloculina� cenomanachiOcchini, 2008, Spirosigmoilina sp., CuneolinacylindricahEnSOn, PalaeosigmoilopsisapenninicachiOcchini, 2008, and PraechrysalidinainfracretacealuPErtO Sinni, 1979 have been recorded from the Cenomanian sediments of west-central Sinai for the first time. Due to the scarcity of index fossils such as ammonites and planktonic foraminifera and the high-diversity of the larger foraminifera species, three biozones have been recorded during Cenomanian based on larger foraminifera. In addition, two step patterns extinctions of larger foraminifera have been observed in the Late Cenomanian shallow-water carbonates of the studied area. The first step (E1) occurs at the middle part of the larger foraminifera Praealveolinacretacea Zone and the second one (E2) occurs near the top of the same latter zone with low-diversity of miliolids and textularids. The latter two extinction events (E1 & E2) are correlated with the record of sea-level change of eustatic curve of haQ etal. (1988).
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The last decade saw a revival of the debate on the exact stratigraphical position of the Upper Ordovician P. linearis graptolite biozone. Chitinozoan biostratigraphy can be useful to help address this question. Here, we provide a high-resolution chitinozoan biostratigraphy through the Dicellograptus Shale Formation at Vasagård on the Island of Bornholm (Denmark), which recently also was subject to a thorough revision of its graptolite fauna, representing the Dicellograptus folicaceus, Dicranograptus clingani and Pleurograptus linearis biozones. We have identified close to 9000 individual chitinozoan vesicles from 26 samples through the upper c. 9m of the Dicellograptus Shale Formation. The Spinachitina cervicornis, Fungochitina spinifera and Tanuchitina bergstroemi chitinozoan biozones are identified, and their boundaries carefully calibrated against the revised graptolite biostratigraphy. A correlation with the chitinozoan biozonation in the British Cautley district, which has a predominantly Baltoscandian, mid-latitude signature and is well-correlated with the graptolite and shelly fauna biozones described from the historical type region, is established.
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Within the Turonian deposits of the area beteen Dambovitza Valley and the upper part of the Buzau Valley the foraminiferal fauna is represented by two very distinct assemblages. One of them mainly consists of planctonic foraminifera - up to 90 % (Whiteinella, Helvetoglobotruncana, Dicarinella, Marginotruncana, Hedbergella, Praeglobotruncana, Schackoina). The remaining 10 % belong to benthic (agglutinated and calcareous ) foraminifera. The other association consists totally of small and primitive agglutinated taxa with siliceous wall cement and a long stratigraphic range. The corresponding biozones show also a relatively large range (Bulbobaculites problematicus, Uvigerinammina jankoi ): from the Upper Cenomanian to the Lower Senonian. The comparative study of these two micropaleontological assemblages allows a correlation between the standard (areal) biozone established on planktonic foraminifera and the local agglutinated deep water assemblages.
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Eocene larger benthic foraminifera including orthophragmines, nummulitids and alveolinids from the Jahrum and Pabdeh formations in the Zagros region are presented. The studied 20-m-thick stratigraphic interval contains, Asterocyclina Gumbel 1870, Nemkovella Less 1987, Orbitoclypeus Silvestri 1907, Discocyclina Gumbel 1870, Nummulites Lamarck 1801, Assilina d'Orbigny 1826 and Alveolina d'Orbigny 1826. This larger benthic foraminiferal assemblage testifies for the shallow benthic zones (SBZs) 15 to 17, which ranges from the middle Lutetian up to the early Bartonian. Further micropaleontological analysis made on intercalated planktonic-rich levels helps calibrate the larger foraminifera biostratigraphy, demonstrating a correlation with the E11 biozone. This confirms that the chronostratigraphic calibration of the SBZs made by previous authors for the peri-Mediterranean area can, through the middle Lutetian to the early Bartonian, be applicable in the Middle East as well.
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