Abstract:The benthic foraminiferal biostratigraphy of Oligo-Miocene aged Muratlı and Petekkaya formations which crop out over wide regions around Akçadağ town, west of Malatya province in Eastern Taurids were revealed in this study. Systematical sampling was carried out in measured stratigraphical sections in four locations in order to perform stratigraphical and paleontological investigations. Benthic foraminifera taken from 182 hard rock samples were defined and three biozones were determined as; SBZ 21-22, belonging… Show more
“…15) interpreted A. asmariensis as a Miocene descendant of Oligocene-Miocene A. striata. Their interpretation of the biostratigraphic range of A. asmariensis as early Miocene (Aquitanian?-Burdigalian) is not in agreement with the range given by Adams (1968), Rupelian-Aquitanian, and it is contradicted by its occurrence in the Rupelian and early Chattian sediments in Oman (Gallardo et al 2001) and Turkey (Gedik 2015), and in upper Chattian deposits from northern Italy (Bassi et al 2007 and references therein), western Greece (Accordi et al 1998), and southern Spain (this paper). A comprehensive revision of the distribution of this species can be found in Bassi et al (2007).…”
Section: Rebaldí Sectionmentioning
confidence: 85%
“…A few specimens with large piles (Fig. 6G, 6H) resemble N. partita Douvillé 1925, a species reported from diverse Oligocene sites, from France, Spain and Tunisia (Douvillé 1925, Gómez Llueca 1929 to Turkey (e.g., Sirel 2013;Gedik 2015) and Iran (e.g., Amirshahkarami 2013). According to Gómez Llueca (1929, p. 348), there is a continuous gradation from pustulated N. partita to N. praemarginata without pustules, as well as pustulated N. morgani indistinguishable from N. partita in external appearance.…”
Section: Rebaldí Sectionmentioning
confidence: 93%
“…There is no consensus in the literature on the stratigraphic range of N. vascus. According to several authors, the stratigraphic range of Nummulites vascus is limited to the Rupelian (Laursen et al 2009;Amirshahkaram 2013;Maghfouri-Moghadam et al 2014), or to the Rupelian-lower Chattian, SBZ 21-22B Poignant 1997, 1998;Báldi et al 1999;Gedik 2008Gedik , 2014Gedik , 2015Özcan et al 2010;Braga and Bassi 2011;Zoeram et al 2013;Sirel 2013Sirel , 2015. The presence of N. cf.…”
The Rebaldí section, a succession of late Oligocene limestones 3 km north of the Benitatxell section, shows a similar association with Peneroplis thomasi, A. asmariensis, M. complanatus, Neorotalia viennoti, N. lithothamnica, Heterostegina aff. assilinoides, Spiroclypeus blanckenhorni, Cycloclypeus mediterraneus, A. bohdanowiczi, and Risananeiza pustulosa; it is interpreted as the early part of SBZ 23. This section also contains Praebullalveolina aff. oligocenica, described from the early Rupelian of Turkey, and Schlumbergerina alveoliniformis, previously interpreted as Burdigalian-Recent. Prior to this work, Cycloclypeus mediterraneus was considered to go extinct and be replaced by C. eidae at the SBZ 22B-23 boundary. However, its presence in the Benitatxell and Rebaldí sections extends its range to the late Chattian in the Eastern Betics and indicates an asynchronous extinction in the Tethys. The presence of Amphistegina mammilla Fichtel and Moll 1798 in late Chattian deposits from the western Tethys contradicts the currently accepted hypothesis that places its origin in the Indo-Pacific province in the early Miocene, from where it would have migrated into the Parathethys during the middle Miocene. In addition, the biogeographic range of P. thomasi, A. asmariensisi, and P. oligocenica is extended to the westernmost part of the Tethys.
“…15) interpreted A. asmariensis as a Miocene descendant of Oligocene-Miocene A. striata. Their interpretation of the biostratigraphic range of A. asmariensis as early Miocene (Aquitanian?-Burdigalian) is not in agreement with the range given by Adams (1968), Rupelian-Aquitanian, and it is contradicted by its occurrence in the Rupelian and early Chattian sediments in Oman (Gallardo et al 2001) and Turkey (Gedik 2015), and in upper Chattian deposits from northern Italy (Bassi et al 2007 and references therein), western Greece (Accordi et al 1998), and southern Spain (this paper). A comprehensive revision of the distribution of this species can be found in Bassi et al (2007).…”
Section: Rebaldí Sectionmentioning
confidence: 85%
“…A few specimens with large piles (Fig. 6G, 6H) resemble N. partita Douvillé 1925, a species reported from diverse Oligocene sites, from France, Spain and Tunisia (Douvillé 1925, Gómez Llueca 1929 to Turkey (e.g., Sirel 2013;Gedik 2015) and Iran (e.g., Amirshahkarami 2013). According to Gómez Llueca (1929, p. 348), there is a continuous gradation from pustulated N. partita to N. praemarginata without pustules, as well as pustulated N. morgani indistinguishable from N. partita in external appearance.…”
Section: Rebaldí Sectionmentioning
confidence: 93%
“…There is no consensus in the literature on the stratigraphic range of N. vascus. According to several authors, the stratigraphic range of Nummulites vascus is limited to the Rupelian (Laursen et al 2009;Amirshahkaram 2013;Maghfouri-Moghadam et al 2014), or to the Rupelian-lower Chattian, SBZ 21-22B Poignant 1997, 1998;Báldi et al 1999;Gedik 2008Gedik , 2014Gedik , 2015Özcan et al 2010;Braga and Bassi 2011;Zoeram et al 2013;Sirel 2013Sirel , 2015. The presence of N. cf.…”
The Rebaldí section, a succession of late Oligocene limestones 3 km north of the Benitatxell section, shows a similar association with Peneroplis thomasi, A. asmariensis, M. complanatus, Neorotalia viennoti, N. lithothamnica, Heterostegina aff. assilinoides, Spiroclypeus blanckenhorni, Cycloclypeus mediterraneus, A. bohdanowiczi, and Risananeiza pustulosa; it is interpreted as the early part of SBZ 23. This section also contains Praebullalveolina aff. oligocenica, described from the early Rupelian of Turkey, and Schlumbergerina alveoliniformis, previously interpreted as Burdigalian-Recent. Prior to this work, Cycloclypeus mediterraneus was considered to go extinct and be replaced by C. eidae at the SBZ 22B-23 boundary. However, its presence in the Benitatxell and Rebaldí sections extends its range to the late Chattian in the Eastern Betics and indicates an asynchronous extinction in the Tethys. The presence of Amphistegina mammilla Fichtel and Moll 1798 in late Chattian deposits from the western Tethys contradicts the currently accepted hypothesis that places its origin in the Indo-Pacific province in the early Miocene, from where it would have migrated into the Parathethys during the middle Miocene. In addition, the biogeographic range of P. thomasi, A. asmariensisi, and P. oligocenica is extended to the westernmost part of the Tethys.
“…5). Figure 8. Generalized columnar sections of the Çakraz Formation in Çamdağ, Zonguldak (Ereğli, Alaplı) and Çakraz areas of the ZT, highlighting the lithological differences (Alişan & Derman, 1995; Altun & Aksay, 2002; Gedik & Aksay, 2002; Timur & Aksay, 2002; Tüysüz, Aksay & Yiğitbaş, 2004; Stolle, 2012, 2014). …”
Section: Discussionmentioning
confidence: 99%
“…Biostratigraphic and fossil data to help determine the age of the Çakraz Formation are rare. It was informally declared as Permo-Triassic in age by Altun & Aksay (2002), Gedik & Aksay (2002), Timur & Aksay (2002) and Tüysüz, Aksay & Yiğitbaş (2004). The age of the Çakraz Formation has also been proposed as early Permian (Grancy, 1938; Wedding, 1970), Permian (Tokay, 1962), Triassic (Jongmans, 1939) and Permian-Triassic (Akyol et al 1974; Kaya, Wiedmann & Kozur, 1986; Yergök et al 1987) in previous studies.…”
Late Permian fluvio-lacustrine successions of the Çakraz Formation in the Zonguldak Terrane between the regions of Akçakoca and Ereğli were investigated in order to describe the litho- and biostratigraphic properties and explain the depositional environment. The studied succession with black, dark-grey to greenish-grey shales, siltstones and limestones is named the Alaplı Member to distinguish it from the classical red clastic successions, which are tentatively named the Ereğli Member of the Çakraz Formation. The organic-rich black shales, mudstones and limestones of the Alaplı Member yielded palynological assemblages suggesting a Lopingian (Tatarian) age. The lack of any marine macro- or microfossils, the fine-grained character of the lithofacies with abundant plant material and the association of poorly sorted conglomerates in the middle part of the succession indicate possible deposition in a broad range of fluvial and lacustrine environments. Successions of similar age and depositional environment are known from the East European Variscan Belt in Bulgaria and Romania. Common successions were also developed in actively extending shallow-marine platforms on the NW Palaeotethyan margin at the end of the Permian Period.
The lower Miocene marine units of NW Iran (Hamedan-Miandoab area) were studied to establish a high-resolution biostratigraphy framework in the context of European standard biozonation (SBZ zonal scheme). The units are dominated by larger and small benthic foraminifera together with coralline algae and corals. Due to its position in the Tethyan Seaway between the Mediterranean and Indo-Pacific, the investigated area has high significance in palaeobiogeography. Seven species of benthic foraminifera were described, including Miogypsina globulina, Amphistegina bohdanowiczi, Elphidium crispum, Elphidium sp. 1, Borelis curdica, Austrotrillina asmariensis, and Peneroplis thomasi. The occurrence of Miogypsina globulina in the shallow-marine carbonates of the studied sections documents the Burdigalian SBZ 25 Zone. Austrotrillina asmariensis and Peneroplis thomasi occur with M. globulina. Simultaneously, their stratigraphical range is extended to the Burdigalian in the Middle East. Based on the discovery of lower Miocene deposits in the Hamedan-Miandoab area (previously mapped as Oligocene-Miocene units), the stratigraphy of northwest Central Iran is revised. The biostratigraphic results also present a more precise chronology for the marine transgression in the study area, initiating in the late early Miocene. The coralline algal assemblages and the abundance and diversity of larger benthic foraminifera indicate that shallow-marine Qom Formation got deposited in tropical to subtropical warm waters.
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