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The name Paynita is proposed for a new dagmaritin genus from the upper Changhsingian (Permian) carbonates of the Southern Biofacies Belt in Turkey. Paynita permotaurica differs from its ancestor Paradagmarita monodi by a hook-shaped fold in the apertural flap terminating systematically against the inner surface of the septal wall to protect the opening from one chamber to the other. It is associated with several species of dagmaritins, belonging to Paradagmarita, Paradagmacrusta, Louisettita, Dagmarita, Danielita, and Bidagmarita. The overall analysis of dagmaritins reveals that the stratigraphic range of the group is from Wordian to Changhsingian. The revised chronostratigraphy in the type area of the genus Sengoerina indicates that this oldest dagmaritin was derived from Globivalvulina cyprica in the Wordian. The first occurrences of genera Dagmarita and Danielita postdate the first occurrence of Sengoerina in the Wordian. Paynita is the last evolutionary step of the Sengoerina-Dagmarita-Crescentia-Paradagmarita lineage characterized by a planar apertural flap whose structure practically remained unchanged during the process of evolution. Paynita is the first genus in this lineage displaying fold in the apertural flap similar to the evolution of Louisettita from Dagmarita.

Foraminifera are important components of tropical marine benthic ecosystems and their recovery pattern from the end-Permian mass extinction can yield insights into the Mesozoic history of this group. Here we report the calcareous and agglutinated foraminifera recovered from five measured stratigraphic sections on the Great Bank of Guizhou, an uppermost Permian to Upper Triassic isolated carbonate platform in the Nanpanjiang Basin, south China. The material contains >100 Triassic species, including three that are newly described (Arenovidalina weiin. sp.,Meandrospira?enosin. sp., andSpinoendotebanella lehrmannin. gen., n. sp.), ranging from Griesbachian (Induan) to Cordevolian (Carnian) age. The species belong to the classes Miliolata, Textulariata, Fusulinata, Nodosariata, and to an unknown class housing all aragonitic forms of the orders Involutinida and Robertinida. Based on previously established conodont zones and carbon isotope chemostratigraphy, the Griesbachian (early Induan) through Illyrian (late Anisian) interval has been subdivided into 12 foraminiferal zones and two unnamed intervals devoid of foraminifera. Following the extinction at the Permian-Triassic boundary, habitable ecological niches of Griesbachian age were invaded by disaster taxa that subsequently became extinct during the Dienerian (late Induan) and left no younger descendants. The disaster taxa were replaced by Lazarus taxa with Permian origins, which were then decimated by the Smithian-Spathian (mid-Olenekian) boundary crisis. The tempo of recovery appears to have been modulated by environmental changes during the Griesbachian through Smithian that involved both climate change and expansion of anoxic ocean bottom waters. Uninterrupted and lasting recovery of benthic foraminifera did not begin until the Spathian.UUID:http://zoobank.org/2a6e9061-b163-402a-9098-8765a80576b3

The sedimentology, geochemistry and paleontology of the pelagic upper Campanian Maastrichtian Bozova Formation in the "Mazidag" (Mazıdağı) - Mardin area, SE Turkey, reveal paleoceanographic and paleoecological changes for the first time. A 119.25 m-thick composite stratigraphic section is characterized by alternating marls, clayey limestones, shales, and black shales; no coarse siliciclastic admixture or turbidite intercalations were recorded in the section. Biostratigraphic data indicate the presence of the Radotruncana calcarata Zone, and the UC15de/UC16 nannofossil zones. Stable isotope and elemental geochemical analyses have been carried out in the studied section. The isotope curves display similar patterns compared to reference curves from European and Chinese basins in the same interval. The prominent negative carbon isotope excursion determined in the upper interval can be correlated with the Late Campanian Event. Proxy elements display generally two relative rising trends in productivity from the lower part and the middle part of the succession. The lower part of the section records relatively more dysoxic/anoxic conditions and coincides with common black shale beds. The presence of both diverse planktonic foraminifera and calcareous nannofossils in the studied interval indicates a fully marine, warm-water, low-latitude Tethysian oceanic environment. In addition, the plant fossils derived from the nearby land mass indicate that a tropical humid climate was similar to that in northeast Australia. Therefore, warm water, tropical humid atmospheric conditions developed in the studied area causing the rise in productivity, precipitation and transportation of plant debris into offshore environments.

The end-Cretaceous mass extinction is a unique event such that it potentially coincides with both the Chicxulub bolide impact and the Deccan volcanism. Among these two drivers, the role of the Deccan volcanism is crucial to decipher if there is a causal relationship between volcanism and environmental stress, and if so, how stressed the environment was during the latest Maastrichtian. To assess the cause-and-effect relationship between Deccan volcanism and climate change and mass extinctions, high-resolution biostratigraphy, quantitative species analysis coupled with geochemical measurements have been performed on complete sections of Mudurnu-Göynük and Haymana basins (Turkey).Detailed quantitative study on planktonic foraminifera of the Haymana Basin revealed that planktonic foraminiferal community in the latest Maastrichtian is dominated by ecological generalists with small, simple morphologies (e.g., Heterohelix, Globigerinelloides, Guembelitria). Among them low oxygen tolerant Heterohelix globulosa is the most dominant taxa and their abundance changing with the presence of stress marker Guembelitria cretacea. In all sections, the K/Pg boundary itself is characterized by 2-3 mm thick reddish oxidized layer which corresponds to sudden annihilation of large, ornamented ecological specialists (e.g., Globotruncana, Rugoglobigerina, Racemiguembelina). Right after the boundary, there is an acme of calcareous dinoflagellate cysts (Thoracosphaera) and a surge of Guembelitria cretacea indicate ecosystem collapse in post-K/Pg environment.On the other hand, detailed quantitative analysis shows a systematic reduction in the species richness throughout the Plummerita hantkeninoides Zone corresponding to the final 150 kyr of the Cretaceous. Proliferations of the Guembelitria cretacea through late Maastrichtian is known as an indicator of high terrigenous influx; therefore, enhanced food resources. The high sedimentation rates observed in all the studied sections might be linked to increased greenhouse conditions due to Deccan volcanism leading to enhanced weathering. Overall, our multiproxy approach including quantitative biostratigraphy and geochemical analyses highlights the influence of the Deccan volcanism by releasing high amounts of atmospheric CO2 and SO2, leading to the climatic changes and associated biotic stress, which predisposed faunas to eventual extinction at the K/Pg boundary.

Testing of Middle Permian – Lower Triassic stratigraphic data from the Antalya Nappes in a half-graben/tilt-block system has revealed the presence of episodic rifting events separated by periods of tectonic quiescence. Following a period of uplift during the Permian (Late Artinskian to Roadian), the basement rocks have been activated by displacement faults and several depocenters in half-graben-like asymmetrical basins began to be filled with Roadian to Wordian continental clastic deposits intercalated with coal and marine rocks. The Early Capitanian time was a period of tectonic quiescence. The second event occurred in Middle to Late Capitanian times and produced basaltic volcanic rocks intercalated in the shallow marine fossiliferous carbonate successions. Following the Lopingian (Wuchiapingian and Changhsingian) and Permian–Triassic boundary interval representing a long tectonic quiescence, the last rifting episode started with an abrupt facies change in the late Griesbachian. Variegated shales, limestones, volcanics, talus breccia, and debris flow deposits were laid down in a half-graben/tilt-block system. As normal faulting has become active, the deposition continued on the subsiding hanging wall side. The stratigraphic gap increased in magnitude as the erosional truncation has incised deeply the footwall side. This initial rifting phase in the Antalya Nappes is prior to the onset of a stronger and more continuous rifting event that occurred in the Anisian–Carnian interval including a variety of deepwater clastic and carbonate deposits, radiolarites containing sometimes blocks and clasts derived from the basin margins, and volcanic rocks carrying intraoceanic setting character.

The Mardin Group strata, as a product of the Cretaceous carbonate platform developed in the northern margin of the Arabian Platform, consists of a thick sedimentary sequence composed mostly of carbonates with subordinate clastic sediments. In this study, three stratigraphic sections Turkoglu, Derik and Inisdere addressing this sequence have been investigated in terms of lithostratigraphy and biostratigraphy combined with microfacies analysis and sequence stratigraphic interpretation. A comprehensive examination of both benthic and planktonic foraminifers in thin sections has revealed that the age of the Mardin Group ranges from early Aptian to Santonian. The lower Aptian and Cenomanian deposits are characterized by benthic foraminifers, whereas the planktonic foraminifers predominate in the upper Albian, Turonian, Coniacian and Santonian. Following a detailed microfacies analysis, a wide depositional environment ranging from inner to outer ramp have been recognized in the Mardin Group carbonates. A sequence stratigraphic analysis has been carried out in order to trace the signals of global sea—level changes during the deposition of Areban, Sabunsuyu and Derdere formations of the Mardin Group. Twenty one depositional sequences are recognized in the interval from lower Aptian to upper Turonian and, under the control of paleontological data, sequence boundaries are correlated with the cycle boundaries of global charts. Eustatic signals enable to recognize several time lines within the Aptian, Albian, Cenomanian and Turonian stages and some important eustatic events like mid—Aptian sea—level fall and the onset of a more accentuated sea—level rise starting from the early Albian.

Recent multi-disciplinary efforts demonstrate a correlation between continental flood basalt (CFB) volcanism and major environmental catastrophes associated with four out of the five largest Phanerozoic mass extinctions. Unique among these is the end-Cretaceous mass extinction, which is potentially coincident with both the Chicxulub bolide impact and the Deccan volcanism. Among these two drivers, the role of the Deccan volcanism is crucial in order to decipher if there is a causal relationship between volcanism and environmental stress, and if so, how stressed the environment was during the latest Maastrichtian. To assess the cause-and-effect relationship between Deccan volcanism and climate change and mass extinctions, high-resolution biostratigraphy, quantitative species analysis coupled with geochemical measurements have been performed on complete sections of Mudurnu-Göynük and Haymana basins (Turkey).In both basins Maastrichtian sedimentation is characterized by monotonous mudstones, which sharply in turn to marl-calcareous mudstone alternations in the earliest Danian. Detailed quantitative study on planktonic foraminifera of the Haymana Basin revealed that planktonic foraminiferal community in the latest Maastrichtian is dominated by ecological generalists with small, simple morphologies (e.g., Heterohelix, Globigerinelloides, Guembelitria). Among them low oxygen tolerant Heterohelix globulosa is the most dominant taxa and their abundance changing with the presence of stress marker Guembelitria cretacea. In all sections, the K/Pg boundary itself is characterized by 2-3 mm thick reddish oxidized layer which corresponds to sudden annihilation of large, ornamented ecological specialists (e.g., Globotruncana, Rugoglobigerina, Racemiguembelina). Right after the boundary, there is an acme of calcareous dinoflagellate cysts (Thoracosphaera) and a surge of Guembelitria cretacea indicate ecosystem collapse in post-K/Pg environment.On the other hand, detailed quantitative analysis shows a systematic reduction in the species richness throughout the Plummerita hantkeninoides Zone corresponding to the final 150 kyr of the Cretaceous. Proliferations of the Guembelitria cretacea through late Maastrichtian is known as an indicator of high terrigenous influx; therefore, enhanced food resources. The high sedimentation rates observed in all the studied sections might be linked to increased greenhouse conditions due to Deccan volcanism leading to enhanced weathering. Overall, our multiproxy approach including quantitative biostratigraphy and geochemical analyses highlights the influence of the Deccan volcanism by releasing high amounts of atmospheric CO2 and SO2, leading to the climatic changes and associated biotic stress, which predisposed faunas to eventual extinction at the K/Pg boundary.

During Late Jurassic-Early Cretaceous the Pontides were the site of a wide carbonate platform facing the Tethys ocean in the south. In the western Pontides the Upper Jurassic-Lower Cretaceous shallow marine carbonates abut the Tethyan Izmir-Ankara suture with no evidence for platform margin deposits. The Sivrihisar klippe 50 km south of the Izmir-Ankara suture preserves a record of the missing platform margin. In the Upper Jurassic-Lower Cretaceous carbonates exposed in this Sivrihisar klippe, two coeval but dissimilar rock packages, separated by a thrust fault, have been detected. The lower succession is composed of Kimmeridgian-Valanginian slope to basin deposits. Within these carbonates the following biozones are defined: Globuligerina oxfordiana - Mohlerina basiliensis Zone (Kimmeridgian), Saccocoma Zone (lower Tithonian), Protopeneroplis ultragranulata Zone (upper Tithonian), Crassicollaria Zone (massutiana Subzone - uppermost Tithonian), Calpionella Zone (alpina, Remaniella, elliptica Subzones - lower Berriasian), Calpionellopsis Zone (simplex, oblonga Subzones - upper Berriasian) and Calpionellites Zone (darderi Subzone - lower Valanginian). These slope to basin deposits are overthrust from north to south by Kimmeridgian shallow marine carbonates. Within this unit Labyrinthina mirabilis - Protopeneroplis striata Zone (Kimmeridgian) is recognized. Based on the distribution of microfacies types and fossil assemblages, a Kimmeridgian-Valanginian depositional model is proposed for the western Sakarya Zone Carbonate Platform (SCP). The position of the studied sections with respect to the SCP, biofacies and microfacies associations suggest that the studied basin and slope deposits represent the remnants of the southern margin and slope of this carbonate platform largely truncated by erosion. The slope and basinal carbonates overthrusted by the coeval shallow marine deposits in a region situated to the south of the main Izmir-Ankara suture indicates an important imbrication and shortening related to the closure of the Tethys ocean. (C) 2018 Elsevier Ltd. All rights reserved.

During the Cretaceous, vast amounts of marine sediments were deposited along the south-facing active margin of the Eurasia. A stratigraphic section of 91 m was analyzed for planktonic foraminifera (75 samples), with the aim of establishing a refined biostratigraphy of Cenomanian–Campanian deposits in Central Anatolia. A biostratigraphic framework comprising nine biozones was established. In ascending order, the Rotalipora cushmani, Whiteinella archaeocretacea and Helvetoglobotruncana helvetica zones were defined in the uppermost Cenomanian–Turonian interval. The lack of Coniacian index markers suggests the existence of a hiatus for this interval. In the upper part of the section, the Dicarinella asymetrica, Globotruncanita elevata, Contusotruncana plummerae, Globotruncanella havanensis and Globotruncana aegyptiaca zones were identified for the Santonian and Campanian deposits. The presence of Gansserina gansseri, Globotruncanita angulata, G. conica and G. pettersi in the uppermost part of the section shows that the section ends at the base of the Gansserina gansseri Zone, indicating uppermost Campanian. The planktonic foraminifera biozonation framework provides strong evidence for the timing of the depositional history of the active continental margin that developed south of the Pontides. These phases are mainly the formation of olistostromes of pre-Santonian age, following condensed carbonate deposition during the Santonian and finally the switch from forearc deposition to the formation of a thick sequence of siliciclastic succession starting in the Campanian.

In this study, we describe as the earliest representatives of involutinids a new population comprising one new genus (Praetriadodiscus) and two new species (P. zaninettiae and P. tappanae) from the Great Bank of Guizhou in the Nanpanjiang Basin of south China. This new population appears to have diverged from an undetermined pseudoammodiscid ancestor in the late Smithian, during the second phase of foraminiferal recovery from the end-Permian mass extinction. The new genus exhibits a two-layered wall, inner microgranular and outer hyaline, fibrous and aragonitic, and a planispirally coiled, lenticular test with one lamella for one complete whorl of the deuteroloculus. The genus Triadodiscus, which may represent the last common ancestor of the Order Involutinida, is potentially the direct descendant of this new population characterized by a two-layered wall.

Angelina Altiner, 1988 has been considered to be a junior synonym of Xingshandiscus Zheng, 1986. This synonymy is irrelevant, because Angelina is unilayered pseudofibrous, whereas Xingshandiscus exhibits a bilayered wall consisting of an inner dark microgranular layer and an outer clear pseudofibrous layer. Furthermore, as Angelina is a pre-occupied name, it was mechanically replaced without any taxonomic discussion by Altineria Ozdikmen, 2009. Altineria is re-discussed and emended in this study; it reveals the most advanced evolutionary stage of pseudovidalinid foraminifers. The parallel evolution of lasiodiscoids and archaediscoids is again verified, since the evolved lasiodiscoid Altineria is a homeomorph of the evolved archaediscid Browneidiscus . This remarkable homeomorphy of both groups (with the same stages, involutus, concavus, angulatus and tenuis) explains the earlier mistakes made in the recognition of some so-called Late Carboniferous–Early Permian archaediscids, which belong in reality to pseudovidalinids.

The newly recognized Upper Cretaceous (similar to 87Ma) olistostrome belt in central Turkey west of Ankara extends for more than 112 km subparallel to the Izmir-Ankara suture with a width of 10 km. The Alacaatl Olistostromes are stratigraphically underlain by a Triassic basement, and are up to 2 km thick. Over 80% of the blocks in the olistostromes consist of pelagic limestones, which reach up to 300 m in size; other blocks include basalt, chert, serpentinite, tuff, and sandstone. The limestone blocks are Jurassic and Cretaceous in age with micropaleontology documenting the presence of Callovian-Oxfordian, Tithonian, Berriasian, Aptian, Albian, Cenomanian, and Turonian stages. The flows are separated by intrabasinal sediments of shale, siltstone, and volcaniclastic sandstone with Albian (108-101 Ma) detrital zircons. The olistostromes show minor tectonic deformation, and are unconformably overlain by Santonian pelagic limestones. The deposition of the Alacaatl Olistostromes was followed by arc magmatism, which started in the Campanian (similar to 78Ma) after a period of shortening and uplift, and the region became a fore-arc basin with deposition of shale and volcaniclastic sandstone with Campanian (78-72 Ma) detrital zircons. A number of peculiar features of these olistostromes including rapid uplift and erosion before the creation of a deep, short-lived (89-86 Ma) ephemeral basin, dominance of deep marine limestone blocks, and inception of arc magmatism approximately 9 Myr after their deposition indicate a major tectonic event involving the disruption of the continental margin prior to the onset of arc magmatism. This event is interpreted as a change from transform margin to subduction.

The Cretaceous–Paleogene (K/Pg) boundary in the Haymana Basin, Central Anatolia, Turkey, was delineated using planktonic foraminiferal biostratigraphy, microfacies analysis, and sequence stratigraphy. An ∼ 29 m outcrop consisting of limestone and marl was measured, and four planktonic foraminiferal biozones were identified spanning the boundary. Planktonic foraminiferal extinction across the K/Pg boundary was catastrophic and abrupt. The extinction level is overlain by a unit (Zone P0) showing an increase in echinoid fecal pellets and authigenic clay minerals such as glauconite, suggesting low sedimentation rates in the early Danian. Ten microfacies types were identified indicating inner-ramp to basinal paleoenvironments based on the sedimentological characteristics and microfossil and macrofossil assemblages. Maastrichtian carbonates contain large benthic foraminifera, calcareous red algae, bryozoans, fragments of echinoderms and mollusks, and planktonic foraminifera. Overlying Maastrichtian–Danian silty marls and silty limestones have common planktonic and benthic foraminifera. Progradation of carbonates into the basin took place during the highstand systems tract, and deposition of a silty marl succession occurred during the transgressive systems tract. The K/Pg boundary is in the upper part of the transgressive systems tract, below a maximum flooding surface. Sequence stratigraphic analysis of a second section, Campo Pit, New Jersey, USA, showed that the K/Pg boundary occurs within a transgressive systems tract in New Jersey as well, suggesting a global sea-level rise across the K/Pg boundary.

Three Late Jurassic–Early Cretaceous carbonate platform stratigraphic sections have been studied in central western Turkey (Bilecik carbonate platform at Bilecik and Saricakaya) and in the Taurides in southern Turkey (Tauride carbonate platform at Beysehir) by using sedimentological and cyclostratigraphical methods. One section was analyzed by detailed magnetic susceptibility measurements. Peritidal carbonates on both platforms display cyclic patterns throughout the sections and do not contain any siliciclastic material. This cyclicity is generally expressed as shallowing upward cycles and interpreted as records of short-term sea-level changes. Magnetic susceptibility (MS) analysis revealed that small scale changes in the MS values can be followed by cyclic alternation of facies and may indicate that varying detrital input during wet and dry climate alternation can be one of the controlling factors for short term sea level changes. The large-scale MS evolution records an increase just around the Jurassic–Cretaceous boundary interval, and a decrease above the boundary. This curve pattern can be correlated with some European MS sections and seems to indicate a consistent MS pattern around this critical interval. Consequently, this study implies that sea-level variations on studied shallow carbonate platforms were on the order of few meters. Pelagic equivalents of these sea-level records can be traced along the margins. Short term climatic control can be seen as one of the controlling factors for small-scale sea-level changes. The large-scale changes can be associated with oceanographic/climatic, third-order sea-level changes and the influence of regional tectonics.

Delayed Earth system recovery following the end-Permian mass extinction is often attributed to severe ocean anoxia. However, the extent and duration of Early Triassic anoxia remains poorly constrained. Here we use paired records of uranium concentrations ([U]) and (238)U/(235)U isotopic compositions (δ(238)U) of Upper Permian-Upper Triassic marine limestones from China and Turkey to quantify variations in global seafloor redox conditions. We observe abrupt decreases in [U] and δ(238)U across the end-Permian extinction horizon, from ∼3 ppm and -0.15‰ to ∼0.3 ppm and -0.77‰, followed by a gradual return to preextinction values over the subsequent 5 million years. These trends imply a factor of 100 increase in the extent of seafloor anoxia and suggest the presence of a shallow oxygen minimum zone (OMZ) that inhibited the recovery of benthic animal diversity and marine ecosystem function. We hypothesize that in the Early Triassic oceans-characterized by prolonged shallow anoxia that may have impinged onto continental shelves-global biogeochemical cycles and marine ecosystem structure became more sensitive to variation in the position of the OMZ. Under this hypothesis, the Middle Triassic decline in bottom water anoxia, stabilization of biogeochemical cycles, and diversification of marine animals together reflect the development of a deeper and less extensive OMZ, which regulated Earth system recovery following the end-Permian catastrophe.

The Haymana Basin, Turkey, hosts complete record of sedimentation across the Cretaceous-Paleogene (K-Pg) boundary. To examine the K-Pg boundary transition and delineate the bioevents, two consecutive sections (UH and UKHB) were measured and sampled at high resolution. Three biozones were established: Plummerita hantkeninoides, P0 and Pα. A detailed quantitative study on planktonic foraminifera was carried out for the P. hantkeninoides and the P0 zones for 63–150 μm and >150 μm size fractions. Results show dominance of ecological generalists with small, simple tests over ecological specialists with large, robust, ornamented morphologies. Heterohelicids are the most dominant group on both size fractions throughout the late Maastrichtian, however right after the K-Pg boundary Guembelitria cretacea blooms and dominates the planktonic foraminiferal assemblage in early Danian P0 Zone. The K-Pg boundary characterizes itself as 2–3 mm thick reddish oxidized layer and its transition reveals a series of events: A rapid change in sedimentation from Maastrichtian mudstones to Danian marls. A sudden annihilation of large, ornamented ecological specialists (e.g., Globotruncana, Rugoglobigerina, Planoglobulina) right at the reddish layer (even though quantitative study revealed that there is a systematic reduction in the foraminiferal species richness throughout the P. hantkeninoides Zone). Spikes of calcareous dinoflagellate Thoracosphaera and fecal pellets right after the K-Pg boundary in the Danian P0 Zone. Anomalous increase in CaO rich spherules and amorphous grains coupled with barite crystals right at the K-Pg boundary layer. Paleobathymetric calculations also revealed approximately 400 m paleodepth for the study area corresponding the upper bathyal zone.

The chronostratigraphy of Guandao section has served as the foundation for numerous studies of the end-Permian extinction and biotic recovery in south China. Guandao section is continuous from the Permian–Triassic boundary to the Upper Triassic. Conodonts enable broad delineation of stage and substage boundaries and calibration of foraminifer biostratigraphy as follows. Changhsingian–Griesbachian: first Hindeodus parvus, and first appearance of foraminifers Postcladella kalhori and Earlandia sp. Griesbachian–Dienerian: first Neospathodus dieneri, and last appearance of foraminifer P. grandis. Dienerian–Smithian: first Novispathodus waageni and late Dienerian first appearance of foraminifer Hoyenella ex gr. sinensis. Smithian–Spathian: first Nv? crassatus and last appearance of foraminifers Arenovidalina n. sp. and Glomospirella cf. vulgaris. Spathian–Aegean: first Chiosella timorensis and first appearance of foraminifer Meandrospira dinarica. Aegean–Bithynian: first Nicoraella germanica and first appearance of foraminifer Pilammina densa. Bithynian–Pelsonian: after last Neogondolella regalis, prior to first Paragondolella bulgarica and first appearance of foraminifer Aulotortus eotriasicus. Pelsonian–Illyrian: first Pg. excelsa and last appearance of foraminifers Meandrospira? deformata and Pilamminella grandis. Illyrian–Fassanian: first Budurovignathus truempyi, and first appearance of foraminifers Abriolina mediterranea and Paleolituonella meridionalis. Fassanian–Longobardian: first Bv. mungoensis and last appearance of foraminifer A. mediterranea. Longobardian–Cordevolian: first Quadralella polygnathiformis and last appearance of foraminifers Turriglomina mesotriasica and Endotriadella wirzi. The section contains primary magnetic signature with frequent reversals occurring around the Permian–Triassic, Olenekian–Anisian, and Anisian–Ladinian boundaries. Predominantly normal polarity occurs in the lower Smithian, Bithynian, and Longobardian–Cordevolian. Predominantly reversed polarity occurs in the upper Griesbachian, Induan–Olenekian, Pelsonian and lower Illyrian. Reversals match well with the GPTS. Large amplitude carbon isotope excursions, attaining values as low as −2.9‰ δ13C and high as +5.7‰ δ13C, characterize the Lower Triassic and basal Anisian. Values stabilize around +2‰ δ13C through the Anisian to Carnian. Similar signatures have been reported globally. Magnetic susceptibility and synthetic gamma ray logs show large fluctuations in the Lower Triassic and an overall decline in magnitude of fluctuation through the Middle and Upper Triassic. The largest spikes in magnetic susceptibility and gamma ray, indicating greater terrestrial lithogenic flux, correspond to positive δ13C excursions. High precision U–Pb analysis of zircons from volcanic ash beds provide a robust age of 247.28 ± 0.12 Ma for the Olenekian–Anisian boundary at Guandao and an age of 251.985 ± 0.097 Ma for the Permian–Triassic boundary at Taiping. Together, the new U–Pb geochronology from the Guandao and Taiping sections suggest an estimated duration of 4.71 ± 0.15 Ma for the Early Triassic Epoch.

The Adana Basin is one of the major Neogene basins situated in SW Turkey with sedimentary successions providing good records of the paleoenvironmental changes that affected the Mediterranean area. Since a detailed biochronostratigraphic framework has not been properly established in the Adana Basin yet, this study will be the first multidisciplinary approach carried out in this region. In addition, a detailed biozonation based on marine palynomorphs was the first ever documented from the K€opekli Formation deposited during the Miocene (from late Burdigalian to Langhian) and the established biozones were correlated with those of planktonic foraminifera and calcareous nannofossils. According to the first occurrences (FOs) and the last occurrences (LOs) of selected taxa, five biozones (P-1, P-2, P-3, P-4 and P-5) based on dinoflagellate cysts; five biozones (M4a, M4b, M5a, M5b and M6) based on planktonic foraminifera; and two biozones (NN4 and NN5) based on calcareous nannofossils were established in the Miocene K€opekli Formation. In order to achieve a worldwide biostratigraphic perspective based on dinoflagellate cysts, the present biozones were compared with those described from NW Europe (Denmark, Germany, the Netherlands), the East Coast of the US and Egypt. After calibration to the established Turkish foraminifera and nannofossils standard, the palynological analysis shows that the recorded dinoflagellate cysts events (e.g. FO of Labyrinthodinium truncatum, Cerebrocysta poulsenii and Unipontidinium aquaeductus and LO of Palaeocystodinium ventricosum) occurred chronostratigraphically earlier in SE Turkey than in NW Europe and on the East Coast of the US.

Necdetina (type species N. taurica n. sp.) is described here as a new fusulinoidean genus with a replaced or recrystallized wall from the Middle Permian (Capitanian) of Turkey. In addition to its distinctive wall structure, which was probably originally keriothecal and composed of aragonite or high-Mg calcite, the genus is characterized by an ovate shell with rounded to acute poles and axially elongated, biserially enrolled chambers. Chomata are absent, but inconsistently developed parachomata-like structures are present in the test where biserially enrolled chambers overlap. Circular foramina alternate in two rows at the bases of the apertural face and septa. Phylogenetic analysis indicates that Necdetina belongs in the clade of staffellid fusulinoideans, a group whose walls are invariably altered. Among the staffellids, Necdetina is allied with other genera in which the coiling axis is elongated to produce a spherical, oval or fusiform test. In this subclade, Necdetina is further united with Thailandina and Neothailandina in possessing parachomata and having well-organized foramina along the antetheca and septa. Necdetina is the only known staffellid, indeed the only known fusulinoidean, with biserial chambers.

The agglutinating annelid Terebella lapilloides Münster, 1833 is commonly encountered in reefal deposits from the Late Jurassic. This annelid is described and documented for the first time from the Upper Jurassic-Lower Cretaceous carbonates of the İnaltı Formation in the Central Pontides, Turkey. The whole İnaltı formation, 395 m in thickness, was studied near Bürnük village and 105 samples were collected along the section. The investigated thin sections reveal the shallow water and the reefal/fore-reefal character of the carbonates with coral-sponge frame-builders. The bioconstituents are accompanied by various microencrusters and microproblematica (such as Lithocodium aggregatum, Bacinella-type structures, Koskinobullina socialis, Radiomura cautica, Perturbatacrusta leini, Thaumatoporella parvovesiculifera, and encrusting sponges and bryozoans), boring bivalves, annelids (serpulids and terebellids), echinoids, rare benthic foraminifera, and abundant Crescentiella morronensis. Rare occurrences of calpionellids - particularly in the upper levels of the section - are also observed. The morphological analysis clearly indicates that the Terebella lapilloides population belongs to the agglutinated annelids, which are classified under the phylum Annelida, class Polychaete, and order Terebellida. Terebella lapilloides is a typical marker of fore-reef to upper slope or toe of slope breccia facies and is generally found in low-energy settings with dysoxic conditions. In some levels of the studied section, Terebella and Crescentiella form an in situ association; however, Terebella never cooccurs with other microencrusters.

Facies architecture of submarine fans and channel–levee complexes in the Eastern Black Sea Basin and their evolution from the Late Miocene until the present day are studied using a three-dimensional seismic data set covering an area of approximately 1161 km 2 . The interpretation of the observations reveals the outcome of the changing interplay between rate of sedimentation and compressional tectonism in the area through time. The Upper Tertiary sedimentary succession in the Eastern Black Sea Basin is characterized by various depositional elements of northeasterly sourced turbidite systems that were deposited in a progressively deforming basin at settings ranging from lower to upper slope. Depositional elements interpreted from seismic character and geometry include canyons, canyon-confined channels, levees, mass transport complexes, sediment waves, sheets and hemipelagic drapes. Two anticlines formed in a compressional tectonic regime subdividing the study area into three mini-basins acted as sediment barriers and controlled the geometry of the basin, and thus, the accommodation space, throughout the Plio-Quaternary period. Sheets that were deposited due to abrupt reduction in structural slope gradients and knickpoints that mark the boundary between site of incision and site of deposition within canyons both have displayed southwestward migration through time, which clearly reflects the basinward advance of compressional deformation in the Eastern Black Sea Basin.

The name Charliella is proposed for a new biseriamminid genus characterized by a four-layered wall that thickens along the anterior side of the septa and partially occludes the chamber cavity. Charliella rossae was derived from the Globivalvulina graeca-Globivalvulina vonderschmitti lineage which also constituted the root stock of true Paraglobivalvulina ( P. mira ) in Late Permian time. The Globivalvulina decrouezae-Septoglobivalvulina gracilis-Paraglobivalvulinoides septulifer lineage is another trend in the evolution of biseriamminids. The recognition of such a lineage in the Late Permian necessitates taxonomic revision of the biseriamminids to attribute globular and involute forms with thin and undifferentiated walls to Septoglobivalvulina, a genus which was synonymized under Paraglobivalvulina in previous work.

The late Hauterivian platform drowning has been recorded in the Hauterivian/Barremian boundary beds in western Turkey. This drowning event recorded by presence of hardgrounds, glauconite- and phosphate-bearing facies over the platform carbonates is followed up by pelagic carbonates. “Ammonitico Rosso” like reddish colored, thick-bedded limestones include multiple hardgrounds, abundant ammonites, belemnites and bivalves just below the Hauterivian/Barremian boundary. The hardground surfaces contain macro and micro-scale manganese and iron encrustations, micro- and macro-boring structures, calcite mineralization and glauconite minerals. Geochemical analysis indicates that Mn encrustation in the hardground is related to hydrothermal and/or hydrogenetic-detrital and associated with continental margin occurrence. A red pelagic limestone succession with planktonic foraminifera overlies the last hardground surface at the Hauterivian–Barremian boundary and is followed up by the alternation of gray colored bioturbated sandy/silty limestones with radiolaria and black shales or sandy/silty mudstones. A black shale level including ammonite, manganese, iron, pyrite and glauconite minerals takes place around the early Barremian–late Barremian boundary. At the top of the sections, there is a succession composed of alternation of thicker sandy limestone and shale/marl covering the black shale interval. The record of “mid-Barremian” black shale interval over the platform carbonates and the overlying pelagic succession with radiolaria indicate that the “mid-Barremian” Oceanic Anoxic Event took place after the drowning of the platform. Stable δ 13 C and δ 18 O isotope excursions have been detected within black shale zone and display parallel pattern with European sections. This study presents the first record of the mid-Barremian anoxic oceanic event on the Sakarya Zone of Pontides in Turkey.

Detailed stratigraphic studies on the Middle-Upper Permian rocks of the Tahtalidag nappe (Antalya Nappes), largely exposed along the Guzelsu Corridor in central Taurides, have revealed the presence...

One of the best-recognized patterns in the evolution of organismal size is the tendency for mean and maximum size within a clade to decrease following a major extinction event and to increase during the subsequent recovery interval. Because larger organisms are typically thought to be at higher extinction risk than their smaller relatives, it has commonly been assumed that size reduction mostly reflects the selective extinction of larger species. However, to our knowledge the relative importance of within- and among-lineage processes in driving overall trends in body size has never been compared quantitatively. In this study, we use a global, specimen-level database of foraminifera to study size evolution from the Late Permian through Late Triassic. We explicitly decompose size evolution into within- and among-genus components. We find that size reduction following the end-Permian mass extinction was driven more by size reduction within surviving species and genera than by the selective extinction of larger taxa. Similarly, we find that increase in mean size across taxa during Early Triassic biotic recovery was a product primarily of size increase within survivors and the extinction of unusually small taxa, rather than the origination of new, larger taxa. During background intervals we find no strong or consistent tendency for extinction, origination, or within-lineage change to move the overall size distribution toward larger or smaller sizes. Thus, size stasis during background intervals appears to result from small and inconsistent effects of within- and among-lineage processes rather than from large but offsetting effects of within- and among-taxon components. These observations are compatible with existing data for other taxa and extinction events, implying that mass extinctions do not influence size evolution by simply selecting against larger organisms. Instead, they appear to create conditions favorable to smaller organisms.

Delayed biotic recovery from the end-Permian mass extinction has long been interpreted to result from environmental inhibition. Recently, evidence of more rapid recovery has begun to emerge, suggesting the role of environmental inhibition was previously overestimated. However, there have been few high-resolution taxonomic and ecological studies spanning the full Early and Middle Triassic recovery interval, leaving the precise pattern of recovery and underlying mechanisms poorly constrained. In this study, we document Early and Middle Triassic trends in taxonomic diversity, assemblage evenness, and size distribution of benthic foraminifers on an exceptionally exposed carbonate platform in south China. We observe gradual increases in all metrics through Early Triassic and earliest Middle Triassic time, with stable values reached early in the Anisian. There is little support in our data set for a substantial Early Triassic lag interval during the recovery of foraminifers or for a stepwise recovery pattern. The recovery pattern of foraminifers on the GBG corresponds well with available global data for this taxon and appears to parallel that of many benthic invertebrate clades. Early Triassic diversity increase in foraminifers was more gradual than in ammonoids and conodonts. However, foraminifers continued to increase in diversity, size, and evenness into Middle Triassic time, whereas diversity of ammonoids and conodonts declined. These contrasts suggest decoupling of recovery between benthic and pelagic environments; it is unclear whether these discrepancies reflect inherent contrasts in their evolutionary dynamics or the differential impact of Early Triassic ocean anoxia or associated environmental parameters on benthic ecosystems.

The Cenomanian/Turonian oceanic anoxic event as recorded in many parts of the world is characterized by presence of black shales and global carbon isotope peaks. Cyclic variations within the anoxic event and association with pelagic red beds are indicated by many studies. Global tectonic/volcanic controls on the origin and the chronostratigraphic position of the anoxic event within the global sea-level changes are important for understanding the paleoceanographic and paleoclimatic conditions during the deposition of Cenomanian/Turonian sediments. Three measured stratigraphic sections in the Central Pontides and the Central Sakarya region of Turkey on the Sakarya Zone of the Pontides have been studied in detail. Cyclic facies alternations have been analysed and Ficher plot curves have been established for the measured sections. According to the cyclostratigraphic analysis, position of the C/T boundary with black shales/mudstones coincides with the global sea-level rise. This indicates that global sea-level change is one of the controlling parameters of black shale generation at the boundary and the long distance correlation between pelagic/hemipelagic successions of different parts of the Sakarya Zone and with global counterparts displays the effect of a large-scale event rather than local. A positive shift in the δ 13 C curve has been obtained just below the C/T boundary similar to many curves obtained around the world. The depletion of Mn indicates oxygen-depleted bottom conditions. Parallel increase of Cd, P, Ba, and Fe indicates increased productivity. Increase in Zn, Cu, Pb and the presence of volcanoclastic sands just below the boundary indicate the fact that volcanism was present during the deposition of anoxic sediments and affected the productivity. TOC values of black shales reach up to 1, 95% at the boundary but drop suddenly after the boundary in parallel with other proxies. The Milankovitch-scale frequent rise and fall of the sea-level superimposed on larger cycles also triggered the nutrient enrichment and the ventilation of the basin resulting in the repetitive alternation of black shales and red marls or cherts. Therefore, this study indicates that the OAE2 including cyclic black shale and red marl/chert alternations on the Sakarya Zone was developed by the cooperation of volcanism, productivity and small and large-scale sea level changes.

The Lapta Group, Late Cretaceous-Middle Eocene in age, mainly consists of basal breccias, micritic limestones and clayey limestoneswith volcanic, calciturbidite and breccia interbeds. It unconformably overlies the Triassic-Lower Cretaceous platform carbonates in the Besparmak (Kyrenia) Range. The detailed study of planktonic foraminiferal assemblages obtained from three stratigraphic sections through the Lapta Group revealed six biozones: Racemiguembelina fructicosa Zone and Abathomphalus mayaroensis Zone of Maastrichtian age; and Acarinina uncinata Zone (P2), Morozovella angulata Zone (P3), Globanomalina pseudomenardii Zone (P4) and Morozovella velascoensis Zone (P5) of Paleocene age. The Cretaceous-Tertiary boundary and the lower part of the Danian including Guembelitria cretacea (P0), Parvularugoglobigerina eugubina (Pa) and Parvularugoglobigerina eugubina-Praemurcia uncinata (P1) zones have not been recorded. Absence of this interval has been attributed to the volcanic level between micritic limestones and clayey limestones in the lower part of the sequence. The clayey limestones of the Lapta Group are overlain by radiolarian calcareous mudstones which pass into alternating siltstone and sandstone of the Ardahan Formation. In contrast to the Lapta Group, the Ardahan Formation lacks zonal marker species and is characterized generally by poorly preserved, less diverse and less abundant planktonic foraminiferal assemblageswhich hamper biozonation. However, the occurrences of typical Middle Eocene planktonic foraminiferal taxa such as Acarinina bullbrooki (Bolli), Globigerinatheka kugleri (Bolli, Loeblich and Tappan), Globigerinatheka subconglobata (Shutskaya), Morozovella spinulosa (Cushman), Morozovella lehneri (Cushman and Jarvis), Truncorotaloides topilensis (Cushman) and Truncorotaloides rohri Bronnimann and Bermudez together with Turborotalia cerroazulensis cerroazulensis (Cole) and Globorotaloides suteri Bolli suggest a Bartonian age for the Ardahan Formation.

We have measured 36Cl in three rock surfaces of the Yenicekale building complex in Hattusha (Bogazkoy, Turkey). Hattusha was the capital of Hittite Empire which lasted from about 1650/1600 to 1200 BC. At Yenicekale, Hittite masons flattened the summit of an outcropping limestone knoll to form an artificial platform as the foundation for a building. Next they built a circuit wall along the lateral precipices of the flattened bedrock platform. We took one sample from the limestone bedrock platform and two samples from limestone building blocks of the circuit wall for cosmogenic 36Cl analysis. Calculated exposure ages are 20 ± 1 ka for the sample from the bedrock platform and 24 ± 1 ka and 52 ± 2 ka for the circuit wall blocks. These exposure ages are significantly older than the age expected based on the estimated time of construction between 3.2 ka and 3.7 ka. We conclude that the sampled surfaces contain significant inherited cosmogenic 36Cl. We cannot directly determine exposure ages for the building complex based on these three samples. On the other hand we may use the measured concentrations to determine how much of the rock was removed from the platform during flattening. To this end we modeled the variation of 36Cl production with depth at Yenicekale using the results from the bedrock sample. We conclude that the Hittite masons removed only around 3 m from top of the limestone block. This means that the volume of rock removed from the bedrock platform is significantly less than the volume in the circuit wall atop the platform. They did not gain enough rock from this flattening to make the building. In agreement with this, the first results of our detailed microfacies analysis indicate that many of the building blocks are not of the same facies as the underlying limestone and must have been quarried elsewhere. Although we were not able to exposure date the Yenicekale complex due to the presence of inherited 36Cl, our data suggest that Hittite masons excavated (most of) the building stones not at Yenicekale, but in quarries outside of Hattusha and then transported them to the construction site. These quarries have not yet been identified.

The stratigraphic distribution of benthic foraminiferal and dasycladacean algal taxa in the Jurassic platform carbonate succession of the Bolkar Mountains permitted to recognise five zones and two subzones in the Jurassic (Bajocian to Tithonian). These are in ascending order: J1-Bosniella croatica/Riyadhella regularis zone (Bajocian); J2-Redmondoides lugeoni/R. cf. rotundatus zone (lower Bathonian) comprising J2a-Paravalvulina complicata subzone in its middle part; J3-Paleopfenderina trochoidea/P. salernitana zone (upper Bathonian-Callovian) comprising J3a-Satorina apuliensis/Kilianina blancheti subzone in its lower part; J4-Kurnubia ex.gr. palastiniensis zone (Oxfordian-lower Kimmeridgian); J5-Clypeina jurassica zone (upper Kimmeridgian-Tithonian). This biostratigraphic scheme corresponds to those for the peri-Mediterranean Jurassic platforms, except for J2 zone and J2a subzone which are first time introduced from the Bolkar Mountains Jurassic succession. Some benthic foraminiferal taxa which are less known from the peri-Mediterranean Jurassic platforms are discussed in their taxonomic positions and local stratigraphic ranges. Riyadhella regularis which is associated with Bosniella croatica is restricted to the Bajocian, whereas in the other peri-Mediterranean platforms it ranges up to the end of the Callovian as long as Bosniella croatica. Paravalvulina complicata and Redmondoides cf. rotundatus are recorded from the lower Bathonian, below the Satorina apuliensis/Kilianina blancheti subzone (upper Bathonian). Pseudomarssonella gr. maxima is considered as a pfenderinid taxon herein, and ranges from the upper part of the lower Bathonian to the lower Tithonian. "Tokayella" taurica may be related to the genus Bosniella, and is restricted to the Kurnubia ex.gr. palastiniensis zone (Oxfordian-lower Kimmeridgian). The re-establishment of the Bolkar Daon in shallow and restricted marine environments varying from lagoon to peritidal flat of an inner platform.

The Haymana region in Central Anatolia is located in the southern part of the Pontides close to the A degrees zmir-Ankara suture. During the Cretaceous, the region formed part of the south-facing active margin of the Eurasia. The area preserves a nearly complete record of the Cretaceous system. Shallow marine carbonates of earliest Cretaceous age are overlain by a 700-m-thick Cretaceous sequence, dominated by deep marine limestones. Three unconformity-bounded pelagic carbonate sequences of Berriasian, Albian-Cenomanian and Turonian-Santonian ages are recognized: Each depositional sequence is preceded by a period of tilting and submarine erosion during the Berriasian, early Albian and late Cenomanian, which corresponds to phases of local extension in the active continental margin. Carbonate breccias mark the base of the sequences and each carbonate sequence steps down on older units. The deep marine carbonate deposition ended in the late Santonian followed by tilting, erosion and folding during the Campanian. Deposition of thick siliciclastic turbidites started in the late Campanian and continued into the Tertiary. Unlike most forearc basins, the Haymana region was a site of deep marine carbonate deposition until the Campanian. This was because the Pontide arc was extensional and the volcanic detritus was trapped in the intra-arc basins and did not reach the forearc or the trench. The extensional nature of the arc is also shown by the opening of the Black Sea as a backarc basin in the Turonian-Santonian. The carbonate sedimentation in an active margin is characterized by synsedimentary vertical displacements, which results in submarine erosion, carbonate breccias and in the lateral discontinuity of the sequences, and differs from blanket like carbonate deposition in the passive margins.

On shallow-marine carbonate buildups in south China, Turkey, and Japan, uppermost Permian skeletal limestones are truncated by an erosional surface that exhibits as much as 10 cm of topography, including overhanging relief. Sedimentary facies, microfabrics, carbon isotopes, and cements together suggest that erosion occurred in a submarine setting. Moreover, biostratigraphic data from south China demonstrate that the surface postdates the uppermost Permian sequence boundary at the global stratotype section and truncates strata within the youngest known Permian conodont zone. The occurrences of similar truncation surfaces at the mass-extinction horizon on carbonate platforms across the global tropics, each overlain by microbial buildups, and their association with a large negative excursion in δ 13 C further suggest a causal link between erosion of shallow-marine carbonates and mass extinction. Previously proposed to account for marine extinctions, the hypothesis of rapid carbon release from sedimentary reservoirs or the deep ocean can also explain the petrographic observations. Rapid, unbuffered carbon release would cause submarine carbonate dissolution, accounting for erosion of uppermost Permian skeletal carbonates, and would be followed by a pulse of high carbonate saturation, explaining the precipitation of microbial limestones containing upwardgrowing carbonate crystal fans. Models for other carbon-release events suggest that at least 5 × 10 18 g of carbon, released in

The Permian–Triassic boundary, examined at two sections in the Southern Alps, occurs ∼1.0 to 1.5 m above the base of the Tesero Oolite Member of the Werfen Formation in a depositionally continuous sequence of inner neritic carbonates. Lagenide foraminifers from the boundary interval comprise 27 species in 15 genera plus additional unidentified taxa, most of which became extinct during the end-Permian crisis. The only survivors were “Nodosaria” elabugae and unidentified species in Geinitzina and Nodosinelloides, with representatives of the latter two genera being short-term holdovers. The end-Permian lagenide extinction level occurs a few decimeters below the biostratigraphically defined erathem boundary, just above the contact between the Bulla Member of the Bellerophon Formation and the overlying Tesero Oolite Member. Confidence intervals (>96%) for the lagenide extinction at the two sections are 0.03 and 0.04 m thick. Plots of species' stratigraphic abundance versus their last observed occurren...

Barremian–Aptian shallow marine mixed carbonate–siliciclastic successions of the Zonguldak area (NW Turkey) have been studied in detail along three measured stratigraphic sections. Field and laboratory analysis of microfacies and sedimentary structures have demonstrated that sections are composed of meter-scale shallowing-upward cycles. Cyclicity of shallow water mixed carbonate–siliciclastic successions are generally observed in the form of alternating sandstone/siltstone or sandy limestone and limestone. A prominent level of charophyte packstone within the successions of Zonguldak and Kozlu is interpreted as a sequence boundary. In the Cengellidere section, cyclicity is generally represented by an alternation of sandstone/conglomerate and bioclastic limestone. The first level of conglomerate within the section is interpreted as a sequence boundary. Smaller-scale cyclic arrangements are also recorded within meter-scale cycles. 4th-, 5th- and 6th-order cycles are superimposed and create a hierarchical stacking. However, 6th-order cycles present a relatively random distribution and termed as episodic. Thickness variation of cycles along the section and frequency of sand and/or silt rich cycle types are used to interpret systems tracts within the sequences.

The Aladag Unit, one of the tectonostratigraphic units in the Tauride Belt (Turkey), comprises a nearly uninterrupted Upper Paleozoic succession including the Visean–Serpukhovian boundary beds. These boundary beds in the Eastern Taurides are made up of mainly carbonates with some intercalations of sandstone and shale. A detailed micropaleontological study has revealed three biozones based on foraminifera. These biozones are, in ascending order, Eostaffella ikensis-Vissarionovella tujmasensis Zone (Mikhailovsky; Late Visean), Endothyranopsis (Reitlingeropsis) cf. sphaerica-Biseriella parva Zone (Venevsky; Late Visean) and Eostaffella pseudostruvei Zone (Tarussky; Early Serpukhovian). Traditional Visean–Serpukhovian boundary lies between the Endothyranopsis (Reitlingeropsis) cf. sphaerica-Biseriella parva Zone and the Eostaffella pseudostruvei Zone. The presence of ‘Millerella’ sp. aff. ‘M.’ tortula specimens in the last levels of the Venevsky horizon also suggests that the measured section, has the potential for the redefinition of the Visean–Serpukhovian boundary, which would coincide with the datum marked by the evolutionary appearance of the conodont Lochriea ziegleri. Boundary beds were deposited in open-marine, shoal, or bank and tidal flat environments, which were interpreted based on the analysis of 12 microfacies and 11 sub-microfacies types. The main microfacies types are (1) bioclastic packstone; (2) bioclastic packstone to grainstone; (3) bioclastic grainstone; (4) bioclastic-intraclastic grainstone; (5) intraclastic grainstone; (6) sandy bioclastic grainstone; (7) peloidal packstone to wackestone (8) wackestone-mudstone; (9) shale; (10) peloidal grainstone or peloidal packstone to grainstone with dark micritic intraclasts; (11) peloidal packstone to grainstone with fenestral fabric; (12) quartz arenitic sandstone. Based on the stacking patterns and vertical evolution of microfacies, several meter-scale shallowing-upward cycles, three sequences, and two intervening sequence boundaries were recognized in the studied section. Sequence boundaries, lying within the Mikhailovsky and Venevsky horizons, are the records of global sea-level changes during the first episodes of the Late Paleozoic Ice Age. The Visean–Serpukhovian boundary falls within the transgressive systems tract of the third sequence and is correlatable with the boundary delineated in Russia. The duration of cycles is calculated as 117 ky and interpreted as orbitally induced (Milankovitch eccentricity) glacioeustatic cycles.

A detailed taxonomical study was carried out for the identification of encrusting micro-organisms. Among these microencrusters, Perturbatacrusta leini, Iberopora bodeuri, Calcistella jachenhausenensis, and Pseudorothpletzella schmidi have been taxonomically revealed for the first time in Turkey. Within the biostratigraphic frame of the Inalti Formation consisting of Mesoendothyra izjumiana zone (Kimmeridgian), Calcistella jachenhausenensis zone (Lower Tithonian–Upper Tithonian) and Protopeneroplis ultragranulata zone (Upper Tithonian–Berriasian), carbonate sedimentation occurred in five depositional environments comprising slope, fore-reef, reef, back-reef and lagoonal environments. The majority of the reefal deposits of the Inalti carbonates can be classified as coral-microbial-microencruster boundstones, which frequently occur in association with back-reef and fore-reef deposits within the Kimmeridgian–Berriasian interval. A shallowing and a subsequent deepening of water depth in the Berriasian have been revealed by the examination of stacking patterns and vertical evolution of the microfacies. Based on the observed microfacies and general features of micro-encrusting organisms, it is concluded that Inalti carbonates share many similarities with the reefal carbonate deposits of Intra-Tethyan domain in terms of microfacies types and microencruster content.

The sedimentology and cyclic stratigraphy of palaeokarst structures in Aptian peritidal carbonate successions are interpreted using field and laboratory microfacies analyses of closely spaced samples from measured outcrop stratigraphic sections in southwest Turkey. Cycles displaying shallowing-upward metre-scale cyclicity are generally composed of lime mudstones/wackestones/packestones at the bottom and stromatolites or lime mudstones with charophytes and ostracods at the top. Subaerial exposure structures such as in situ karst breccias, dissolution vugs/pipes, mud cracks and sheet cracks are encountered at the top of the cycles. The presence of limestone layers between the successive karst breccia levels indicates that they are in situ palaeokarst structures, not recent karstifications or deep penetration from the upper palaeokarst surface down to the older strata. Palaeokarst breccia deposits are interpreted as mantling breccia formed as a result of epikarstification. Three main palaeokarst levels are recorded in nearly all sections. The sedimentology of the palaeokarst breccias, their position in cyclic peritidal carbonates and the biostratigraphic framework are used to trace the record of the global mid-Aptian sea-level fall in the southwest Taurides. The successive occurrences of three karst breccia levels close to the mid-Aptian sea-level fall correspond to falling periods of high-amplitude sea-level fluctuation within a late high-stand or early fall condition of a third-order sea level.

Ninety-one percent of calcareous foraminiferal genera became extinct during the end-Permian mass extinction. The Early Triassic Epoch was a survival phase characterized by a short-lived proliferation of disaster forms and then a prolonged interval of low diversity. The orders Miliolida and Lagenida experienced limited taxonomic re-diversification in Early and Late Anisian time, respectively. All fusulinoidean fusulinides became extinct in Late Permian time, and only two non-fusulinoidean genera persisted into the Early Triassic. Triassic fusulinides diversified to just five genera before the order became entirely extinct in Late Triassic time. Involutinides originated in Olenekian time from an unknown ancestor. They did not significantly diversify until Late Triassic time. To cite this article: J.R. Groves, D. Altiner, C. R. Palevol 4 (2005) .

The Bornova Flysch Zone (BFZ) in western Turkey is a regional olistostrome-melange belt located between the Izmir-Ankara Tethyan suture in northwest and the Menderes Massif in the southeast. The BFZ consists mostly of tectonized gravity mass flows. The blocks are Mesozoic limestone and ophiolite, which are enclosed in Cretaceous-Paleocene sheared sandstone and shale. The limestone blocks are of two types. The first type consists of Late Triassic to Cretaceous shallow marine carbonates. The second type has an Upper Triassic shallow marine section overlain by Jurassic to Cretaceous pelagic limestones. A semi-intact part of the platform occurs in the Karaburun peninsula and on the island of Chios. The ophiolitic blocks in the BFZ include ultramafic rock, gabbro, basalt and radiolarian chert of Middle Triassic to Cretaceous in age. The formation of the BFZ overlaps with the Cretaceous subduction and HP/LT metamorphism of the northern passive continental margin of the Anatolide-Tauride Block. This subduction zone was bounded in the west by a strike-slip tear fault. The BFZ formed in a narrow basin between this tear fault and the Tethyan ocean. The mass flows came from the southeast from the overriding ophiolite and accretionary complex, and from the northwest from the uplifted segments of the platform margin. This model provides an explanation as why the BFZ is unmetamorphosed, whereas the equivalent strata in the Menderes Massif were metamorphosed at depths of over 20 km. It also explains the prominence of gravity flows and the southward younging in the BFZ, and for the apparently anomalous observation that, although the Tethyan ocean lay to the northwest, the ophiolitic blocks are more common on the southeastern part of the BFZ. Regions away from the tear fault, such as the Karaburun peninsula, were least affected by subsidence and deformation during the Cretaceous and Paleocene. (C) 2012 Elsevier B.V. All rights reserved.

The most widespread blocks within the Cretaceous ophiolitic melange (North Anatolian ophiolitic melange) in Central Anatolia (Turkey) are pillow basalts, radiolarites, other ophiolitic fragments and Jurassic-Cretaceous carbonate blocks. The pillow basalts crop out as discrete blocks in close relation to radiolarites and ophiolitic units in Cretaceous ophiolitic melange. The geochemical results suggest that analyzed pillow basalts are within-plate ocean island alkali basalts. The enrichment of incompatible elements (Nb, Ta, Light REE, Th, U, Cs, Rb, Ba, K) demonstrates the ocean island environment (both tholeiites and alkali basalts) and enriched MORB. Dated calcareous intrafills and biodetrital carbonates reveal an age span of Callovian—Early Aptian. The thin-shelled protoglobigerinids, belonging to the genus Globuligerina, in the calcareous intrafills between pillow basalt lobes indicates a Callovian—Barremian age interval, most probably, Valanginian to Late Barremian. The volcanic and radiolarite detrit...

Paleozoic lagenide foraminifera are strikingly similar morphologically to Mesozoic and Cenozoic Lagenida, but because benthic foraminifers suffered a catastrophic reduction in diversity during the end-Permian mass extinction, it is unclear whether the similarities of Paleozoic lagenides and younger unquestioned Lagenida link them evolutionarily or are the product of convergence. Seven species representing five families of Paleozoic lagenide foraminifers were examined and found to possess mostly monolamellar hyaline-radial walls, as in extant nodosariid Lagenida. Exceptions are Protonodosaria rauserae Gerke, 1959, whose wall is not optically radial, and Syzrania amazonica Altiner and Savini, 1997, whose hyaline-radial wall may or may not be accompanied by a secreted inner microgranular layer. The inner microgranular layer is an element that is thought to have been inherited from the ancestral Fusulinida. Its absence in all but the earliest and morphologically simplest Paleozoic lagenides indicates...

The Order Lagenida is a monophyletic group of calcareous foraminifers that originated in Middle Pennsylvanian time via acquisition of hyaline-radial wall structure and loss of microgranular wall structure, the latter being characteristic of the close sister group and likely ancestor, the Fusulinida. Early lagenides are delineated into subgroups on the basis of presence or absence of partitioning within their tests, and among partitioned forms, on continuous versus discontinuous growth styles. Partitioned, discontinuously growing forms may be further delineated on the basis of test symmetry and on modifications to chamber shape and apertural complexity. Early lagenides underwent rapid taxonomic differentiation during late Moscovian and early Kasimovian time. Taxonomic differentiation was accompanied by rapid dispersal from the presumed center of origin in the midcontinent-Andean area to tropical and subtropical shelves worldwide. By Early Permian time certain lagenides were adapted to cool water paleoenvironments, as evidenced by their occurrences in high paleolatitudes and even in glaciomarine basins. Early Permian lagenides do not exhibit marked provincialism, but there is evidence for paleolatitudinal control on assemblages. The midcontinent-Andean and present Arctic areas contain similar, diverse faunas from low- to mid paleolatitudes along the western margin of Pangaea. These faunas share many elements in common with faunas from the tropical and subtropical eastern margin of Pangaea (Paleotethys). In contrast, the Europe-Urals, Siberian and Australian areas are characterized by a slightly different faunal association from mid- to high paleolatitudes in both hemispheres. Panthalssan faunas are less well known, but seemingly contain only cosmopolitan taxa.

Kılıç, Ali Murat (Balikesir Author), The basement of the Central Pontides, and by implication that of Crimea, consists of pre-Permian low-grade metaclastic rocks intruded by latest Permian-Early Carboniferous (305290 Ma) granitoids. Further up in the stratigraphic sequence are Triassic limestones, which are now preserved as olistoliths in the deformed Upper Triassic turbidites. New conodont and foraminifera data indicate an Anisian to Carnian (Middle to Late Triassic) age for these hemi-pelagic Hallstatt-type limestones. The siliciclastic turbidites surrounding the Triassic limestone contain the Norian (Late Triassic) bivalve Monotis salinaria; the same species is also found in the Tauric series in Crimea. The Upper Triassic flysch in the Central Pontides is locally underlain by basaltic pillow lavas and includes kilometre-size tectonic slices of serpentinite. Both the flysch and the serpentinite are cut by an undeformed acidic intrusion with an Ar-Ar biotite age of 162 +/- 4 Ma (Callovian-Oxfordian). This indicates that the serpentinite was emplaced into the turbidites before Middle Jurassic time, most probably during latest Triassic or Early Jurassic time, and that the deformation of the Triassic sequence pre-dates the Middle Jurassic. Regional geological data from the circum-Black Sea region, including widespread Upper Triassic flysch, Upper Triassic eclogites and blueschists of oceanic crustal affinity, and apparent absence of a 'Cimmerian continent' between the Cretaceous and Triassic accretionary complexes indicate that the latest Triassic Cimmeride orogeny was accretionary rather than collisional and is probably related to the collision and accretion of an oceanic plateau to the southern active margin of Laurasia., TUBA

Continuous shallow marine carbonates spanning the Triassic-Jurassic boundary are exposed in the Karaburun Peninsula, Western Turkey. The studied section (Tahtaiskele section) consists of Upper Triassic cyclic shallow marine carbonates intercalated with clastics overlain by Lower Liassic carbonates. Based on the microfacies stacking patterns, three main types of shallowing-upward cycles have been recognized. Cycles are mostly composed of subtidal facies at the bottom, intertidal/supratidal facies and/or subaerial exposure structures at the top. The duration of the cycles suggests that cycles were driven by the precessional Milankovitch rhytmicity. In the sequence stratigraphic frame of the Tahtaiskele section 4 sequence boundaries were detected and globally correlated. The first sequence boundary is located at the Alaunian-Sevatian boundary nearly coinciding with the first appearance of Triasina hantkeni. The second falls in the Rhaetian corresponding to a major sea level fall which led to the invasion of forced regressive siliciclastic deposits over the peritidal carbonates. The third occurs close to the T/J boundary and the fourth lies slightly above the base of the Jurassic. In the studied section, extinction, survival and recovery intervals have been recognized based on the stratigraphic occurrence patterns of benthic foraminifera and algae. Foraminifers became nearly totally extinct in the inner carbonate shelves at the Triassic-Jurassic boundary and an interval of approximately 0.5 my passed before the begining of the recovery of Jurassic foraminifera. (C) 2014 Elsevier Ltd. All rights reserved.

Subtidal, intertidal, and supratidal carbonate facies are recognized in the Upper Jurassic (Kimmeridgian)-Upper Cretaceous (Cenomanian) peritidal carbonates of the Fele area (Western Taurides, Turkey). Vertical stacking patterns of these facies are of a cyclical character; shallowing upward is the trend of the cyclicity in these carbonate facies. In-situ karstic breccias, collapse breccias, caliche (laminar calcrete), “Microcodium” accretion, and root casts are structures commonly indicative of third-order sequence boundaries. However, mud cracks, solution pores or vugs, sheet cracks, loferites, and birds-eye structures are commonly delineated by parasequence boundaries. In-situ or collapse breccias can be genetically derived from sheet cracks, mud cracks, solution pores or vugs, and birds-eye structures with increasing exposure time. The use of such sedimentary structures in the recognition of sequence boundaries is highly practical in the ancient carbonate platforms of the world, inasmuch as the sequenc...