Journal articles: 'Coniacian-Santonian'

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Hildebrand-Habel, Tania, and Helmut Willems. "New calcareous dinoflagellates (Calciodinelloideae) from the Middle Coniacian to Upper Santonian chalks of Lägerdorf (northern Germany)." Journal of Micropalaeontology 23, no. 2 (November 1, 2004): 181–90. http://dx.doi.org/10.1144/jm.23.2.181.

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Abstract. Three new calcareous dinoflagellate species from the Middle Coniacian to Upper Santonian chalks of Lägerdorf (northern Germany) are formally described: Calcicarpinum macrogranulum n. sp., Pirumella fragilis n. sp. and Ruegenia quinqueangulata n. sp. The species show differing vertical distribution patterns which might result from local sea-level changes: P. fragilis and R. quinqueangulata are restricted to the possibly transgressive upper Mid-Coniacian to Lower Santonian interval and C. macrogranulum occurs consistently only in the probably regressive lower Mid-Coniacian and Middle to Upper Santonian intervals.

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Jimenez, Monica, Simon P. Holford, Rosalind C. King, and Mark A. Bunch. "Controls on gravity-driven normal fault geometry and growth in stacked deltaic settings: a case study from the Ceduna Sub-basin." APPEA Journal 61, no. 2 (2021): 632. http://dx.doi.org/10.1071/aj20073.

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Kinematics of gravity-driven normal faults exerts a critical control on petroleum systems in deltaic settings but to date has not been extensively examined. The Ceduna Sub-basin (CSB) is a passive margin basin containing the White Pointer (Albian-Cenomanian) and Hammerhead (Campanian-Maastrichtian) delta systems that detach on shale layers of Albian-Cenomanian and Turonian-Coniacian ages, respectively. Here we present evidence for spatially variable fault growth styles based on interpretation of the Ceduna 3D seismic survey and fault kinematic analyses using displacement–distance, displacement–depth and expansion index methods. We identified faults that continuously grew either between the Cenomanian–Santonian or Santonian and the Maastrichtian located throughout the study area and faults that exhibit growth between the Cenomanian–Maastrichtian that are geographically separated into three areas according to their evolution histories: (i) Northern CSB faults exhibit constant growth between the Cenomanian and Maastrichtian. (ii) Central CSB faults show two dip-linkage intervals between (a) Cenomanian and Coniacian–Late Santonian, (b) Coniacian–Late Santonian and Late Santonian–Maastrichtian segments, respectively. (iii) Central and southern CSB faults exhibit dip-linkage intervals between Cenomanian–early Santonian and Late Santonian–Maastrichtian segments. Our study demonstrates a relationship between the location of the Cenomanian–Maastrichtian faults and their evolution history suggesting constant growth evolution at north and dip linkage at the central and south areas.

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Kennedy, W. J., and W. K. Christensen. "Coniacian and Santonian ammonites from Bornholm, Denmark." Bulletin of the Geological Society of Denmark 38 (February 19, 1991): 203–26. http://dx.doi.org/10.37570/bgsd-1990-38-19.

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The ammonite faunas from the Amager Limestone and Bavnodde Greensand Formations of the island of Bornholm, Denmark are described. The Amager Limestone at its type locality has yielded five species, including the age diagnostic Scaphites (Scaphites) kieslingswaldensis kieslingswaldensis · Langenhan & Grundey, 1891 and Peroniceras tridorsatum (Schliiter, 1867). The Bavnodde Greensand has yielded seven species, including Scaphites (Scaphites) kieslingswaldensis fischer Riede!, 1931, which firs! appears in the Lower Santonian elsewhere in Europe. The age of the two formations is discussed. The Amager Limestone Formation is in part at least Middle Coniacian on ammonite evidence, Lower Coniacian on inoceramid bivalve evidence, while foraminifera suggest thai the formation spans most of the Coniacian. Tue Bavnodde Greensand Formation is referable to the upper Coniacian-Lower Santonian on the basis of ammonites, belemnites, and inoceramid bivalves.

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Dhondt, Annie V., Marcos A. Lamolda, and Jose Maria Pons. "Stratigraphy of the Coniacian–Santonian transition." Cretaceous Research 28, no. 1 (February 2007): 1–4. http://dx.doi.org/10.1016/j.cretres.2006.05.015.

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Tröger, Karl-Armin, and Walter Kegel Christensen. "Upper Cretaceous (Cenomanian-Santonian) inoceramid bivalve faunas from the island of Bornholm, Denmark. With a review of the Cenomanian-Santonian lithostratigraphic formations and locality details." Danmarks Geologiske Undersøgelse Serie A 28 (June 30, 1991): 1–47. http://dx.doi.org/10.34194/seriea.v28.7048.

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The inoceramid bivalve faunas from the Arnager Greensand, Arnager Limestone, and Bavnodde Greensand Formations of the island of Bornholm, Denmark are described. The fauna from the basal part of the Arnager Greensand s. str. is from the Lower Middle Cenomanian and includes Inoceramus crippsi Mantell, /. crippsi hoppenstedtensis Trager, and I. schoendorfi Heinz. The Arnager Limestone at its type locality immediately west of Arnager yielded a diverse fauna, including /. waltersdorfensis cf. hannovrensis Heinz, /. lusatiae Andert, I. cf. rotundatus Fiege, /. striatoconcentricus Gumbel, I. (Heroceramus) cf. hercules Heinz, I. cf. wandereri Andert, I. cf. annulatus Goldfuss, I. cf. renngarteni Bodilevski & Schulgina, and/. (Mytiloides) incertus Jimbo. This fauna is Lower Coniacian. I. cf. lusatiae and /. cf. guerichi Heinz are recorded from the top part of the formation east of Horsemyre Odde, which is Lower Coniacian. /. (Cremnoceramus) schloenbachi Bohm from the upper Lower Coniacian is reported from the Arnager Limestone Formation at Muleby. /. (Volviceramus) koeneni Muller and /. (V.) alievimussensis lvannikov occur in 4 the top part of the Arnager Limestone Formation at Stampe A; this fauna is probably Lower Middle Coniacian. The fauna of the Bavnodde Greensand Formation at the type locality consists of /. (Sphenoceramus) pachti cf. pachti Arkhangelsky and /. (S.) cardissoides Goldfuss which are Lower, but not lowest, Santonian. At Risenholm, the formation yielded I. (S.) subcardissoides Schluter, I. (S.) cardissoides, I. (S. ?) bornholmensis n. sp., /. (S.) sp. ex gr. pachtilcardissoides, and incomplete, poorly preserved inoceramids possibly belonging to the I. (Magadiceramus) subquadratus group; this fauna is basal Santonian. The fauna of the formation at Jydegard comprises I. (S. ?) bornholmensis n. sp. and /. (S.) sp. ex gr. pachti/cardissoides, and the formation here is lowest Santonian and possibly highest Coniacian. The Cenomanian-Santonian lithostratigraphic formations of Bornholm are reviewed and their ages are discussed with regard to various fossil groups, including inoceramid bivalves, ammonites, belemnites, and foraminifera. Locality details are given.

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Nachev, Ivan, and Ekaterina Dimitrova. "Upper Cretaceous stratigraphy of the Eastern Sredna Gora Zone." Geologica Balcanica 25, no. 3-4 (August 30, 1995): 3–26. http://dx.doi.org/10.52321/geolbalc.25.3-4.3.

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The litostratigraphic subdivision includes the Kardif (Cenomanian?), Cerovska (Cenomanian, Turonian), Gradište (Coniacian, Santonian), Kubadin (Coniacian-Campanian), Sinemorec (Coniacian-Campanian), Izgrev (Coniacian-Campanian), Glušnik (Campanian), Konjovo (Campanian) and Dryankovec (Maastrichtian) Formations. The chronostratigraphy is based on microfaunistic (foraminifers) associations. The Cenomanian consists of limnic and coal-bearing undated rocks (Kardif Formation) or of shallow-marine dated clastic rocks and limestones (Cerovska Formation). The Turonian includes the upper part of the shallowwater rocks (Cerovska Formation). The Coniacian is represented by deep-marine graywacke-silstone flysch (Gradište Formation), limestones and arillaceous limestones (Kubadin Formation), tephroturbidite flysch (Sinemorec Formation) and volcanic tuffs (Izgrev Formation). The Santonian includes deepmarine rocks, which are similar to these of the Coniacian. The Campanian is represented by deepmarine limestones and argillaceous limestones (the upper part of Kubadin Formation), tephroturbidite flysch (Sinemorec Formation), limestones and argillaceous limestones (Glušnik Formation), volcanic tuffs (Izgrev Formation) and clastic-limestone flysch (Konjovo Formation). The Maastrichtian is characterized by shallow-marine limestones, sandstones and siltstones (Dryankovec Formation). The sedimentary environments had changed temporally: limnic (Cenomanian?); shallow epicontinental sea (Cenomanian, Turonian); deep-marine Sredna Gora intra-arc trough (Coniacian-Campanian); superimposed shallow epicontinental sea (Maastrichtian). The Early Subhercynian orogenic movements had occured between the Turonian and the Coniacian. The Late Subhercynian orogeny have caused a folding after the Campanian, but before the Maastrichtian.

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Nachev, Ivan, and Ekaterina Dimitrova. "Upper Cretaceous stratigraphy of the Eastern Balkan Mountains." Geologica Balcanica 25, no. 5-6 (December 30, 1995): 43–74. http://dx.doi.org/10.52321/geolbalc.25.5-6.43.

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The lithostratigraphic subdivision of the Upper Cretaceous in the Eastern Balkan Mountains includes the Balkanbas (Cenomanian?), Dobromir (Cenomanian, partly Turonian), Radova (partly Turonian – Santonian), Trânak (partly Turonian – Coniacian), Karaveljovo (Coniacian, Santonian) and Emine (partly Turonian – Maastrichtian) Formations. The chronostratigraphy is based on foraminiferal microfauna. The Cenomanian is represented by limnic conglomerates, sandstones, siltstones and shales with coals, as well as of shallow-marine clastic, argillaceous and calcareous rocks. The Turonian includes the upper part of the shallow-marine rocks and the lower part of the deep-marine Emine flysch. The Coniacian is represented by flysch consisting of alternation of graywackes, siltstones and shales or marls, clastic limestones, micritic limestones and argillaceous limestone ("marls") or of tephraturbidites, volcanic tuffs and effusive rocks. The Santonian is represented by flysch, analogical in composition to this of the Coniacian. The Campanian includes mainly clastic-limestone flysch, and locally, in the lower part a mixed flysch. The Maastrichtian consists mainly of clastic limestone flysch, locally (Emine Mountain) of mixed flysch. The boundary between the Maastrichtian an,d the Paleocene (Danian) is under discussion. Most probably it coincides with the boundary between the Emine and the lrakli flysch, where some shales occur. In the Emine back-arc marginal Sea (partly Turonian – Maastrichtian) through processes of normal sedimentation and resedimentation a flysch has been deposited. The Maastrichtian limestones are replaced by Paleocene clays.

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Akinin, V. V., L. B. Golovneva, and S. V. Shchepetov. "Isotopic age of flora-bearing beds from the Amka Formation stratotype, Okhotsk-Chukotka volcanic belt." Palaeobotany 7 (2016): 38–46. http://dx.doi.org/10.31111/palaeobotany/2016.7.38.

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U-Pb SHRIMP-dating of zircons from flora-bearing volcanic rocks of the Amka Formation stratotype (Ul'ya depression, Okhotsk-Chukotka volcanic belt) yield weighted mean 206Pb/238U age of 85.5 ±2 Ma (Santonian to Coniacian stage). This isotope dating is consistent with inferred Coniacian age of Ul’ya flora from the Amka Formation.

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Remin, Zbyszek, Michał Gruszczyński, and Jim D. Marshall. "Changes in paleo-circulation and the distribution of ammonite faunas at the Coniacian–Santonian transition in central Poland and western Ukraine." Acta Geologica Polonica 66, no. 1 (March 1, 2016): 107–24. http://dx.doi.org/10.1515/agp-2016-0006.

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Abstract Ammonite distribution patterns and carbon and oxygen stable isotopes from the Lipnik-Kije (Poland) and Dubovcy (Ukraine) sections allow us to propose a model of sea water paleo-circulation in central Europe for the Coniacian- Santonian interval. The tectonic evolution of the south-eastern part of Poland, and expansion of the Krukienic Island areas, appears to have been one of the most important factors affecting paleotemperatures and the distribution of ammonite faunas in the shallow, epicontinental sea in this part of Europe. In the Lipnik-Kije section, low-latitude Tethyan ammonites, especially of the genera Nowakites, Parapuzosia and Saghalinites, are mixed with the cold water loving ammonite genus Kitchinites in the Lower Santonian. In the Dubovcy section (western Ukraine), Tethyan ammonites disappear abruptly in the earliest Santonian, giving place to temperate ammonites of the Kitchinites group in the early Early Santonian and to Boreal belemnites of the genus Gonioteuthis in the Middle and Late Santonian. Despite evidence for the effects of diagenesis in both sections, bulk-rock δ18O records from the limestones support higher seawater paleotemperatures in the Polish sea and cooler conditions in the western Ukraine. The proposed paleo-circulation model and paleotemperature distribution across Europe is supported independently by changes in faunal and nannoflora evidence (ammonites, foraminifera and nannoplankton), and rather unexpectedly with the bulk δ18O data. These data allow the recognition of the end-Coniacian-Early Santonian cooling event, resulting from cold currents flowing from the north, which is traceable, with different magnitude, in several European sections. Facies changes in both sections are related to the input of terrigenous material, and linked to Subhercynian tectonic movements which affected the eastern (Ukrainian) and central (Holy Cross) segment of the Mid Polish Trough at different times. Uplift and sediment input moved westwards through time. Clastic input is detectable at the Coniacian-Santonian boundary in the Ukrainian segment. Similar facies changes reached the Holy Cross segment in Poland distinctly later, somewhen in the Middle Santonian. It is likely that tectonics together with paleo-circulation changes markedly restricted or even cut-off the western Ukraine area from Tethyan ocean influences in the Early Santonian.

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Toshimitsu, Seiichi, Takashi Hasegawa, and Ken Tsuchiya. "Coniacian–Santonian stratigraphy in Japan: a review." Cretaceous Research 28, no. 1 (February 2007): 128–31. http://dx.doi.org/10.1016/j.cretres.2006.05.023.

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Farouk, Sherif, Mahmoud Faris, and Zaineb Elamri. "Coniacian-Santonian Planktic Stratigraphy in central Tunisia." Cretaceous Research 78 (October 2017): 13–26. http://dx.doi.org/10.1016/j.cretres.2017.05.017.

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Guzhikova, Anastasia A., Vladimir A. Grishchenko, Vladimir A. Fomin, Evgeniy Yu Baraboshkin, and Dmitry A. Shelepov. "Magnetostratigraphy of Turonian – Santonian strata on the Samara Right Bank." Izvestiya of Saratov University. Earth Sciences 21, no. 4 (November 22, 2021): 248–63. http://dx.doi.org/10.18500/1819-7663-2021-21-4-248-263.

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The paper presents the results of petro- and paleomagnetic studies of two sections of Turonian – Santonian on the Samara Right Bank – near Novodevichye, Podval’e villages and detailed geological description of the Novodevichye section. The magnetostratigraphic subdivision and detailed correlation of the sections were carried out. Unknown unconformity in the Podval’e section was recognized. Reverse polarity corresponds to a significant part of the Coniacian – Santonian deposits, the presence of which contradicts the existing ideas about the regime of the Turonian – Santonian geomagnetic field, but partly agrees with the data on deposits of the same age found in other sections in the Volga region.

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Yudova, D. A., L. B. Golovneva, and P. I. Alekseev. "The distribution of the genus Dalembia E. Lebedev et Herman (Magnoliophyta) in Late Cretaceous floras of Northern Pacifica." Palaeobotany 7 (2016): 66–79. http://dx.doi.org/10.31111/palaeobotany/2016.7.66.

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New findings of the genus Dalembia from Late Cretaceous sediments are described: Dalembia sp. from lower part of the Sym Formation (Coniacian – Santonian) of Eastern Siberia; Dalembia sp. from upper part of the Timmerdyakch Formation (Turonian – Coniacian) of Western Siberia; D. vachrameevii E. Lebedev et Herman and the new species D. argentea Yudova et Golovneva from the Chingandzha Formation (Turonian – Coniacian) of Okchotsk-Chukotka volcanogenic belt (Northeastern Russia). The stratigraphic range of the genus Dalembia stretch from the late Albian to Campanian. The geographical area includes the territories of Alaska, northern China, Northeastern Russia, Western and Eastern Siberia. The highest quantity of occurrences associated with Nothern Pacific region.

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Grabovskiy, A. A. "Genus Arctopteris (Pteridaceae) in the Cretaceous floras of the Northeast of Russia." Palaeobotany 12 (2021): 34–55. http://dx.doi.org/10.31111/palaeobotany/2021.12.34.

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The ferns of the genus Arctopteris from the Cretaceous deposits of the North-East of Russia (the Aigur, Galimov, Krivorechenskaya, Arman, Amka, Gidra, Kananyga, Tylpegyrgynai, Poperechnaya, Emuneret, Barykov and Rarytkin formations) were re-examined. In the result eight species were included in this genus: A. lenaensis Vassilevskaja (Aptian), A. heteropinnula Kiritchkova (lower–middle Albian), A. kolymensis Samylina (lower–middle Albian), A. obtusipinnata Samylina (lower–middle Albian), A. rarinervis Samylina (lower Albian-Coniacian), A. penzhinensis E. Lebedev (Turonian-Coniacian), A. ilirnensis Golovneva (Turonian-upper Santonian) и A. rarytkinensis Vassilevskaja (Coniacian-Danian). Species A. microphylla Philippova and A. rarinervis are united under the name A. rarinervis.

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Ljubović-Obradović, Darivojka, Ivana Carević, Monika Mirković, and Nenad Protić. "Upper Cretaceous volcanoclastic-sedimentary formations in the Timok Eruptive Area (eastern Serbia): new biostratigraphic data from planktonic foraminifera." Geologica Carpathica 62, no. 5 (October 1, 2011): 435–46. http://dx.doi.org/10.2478/v10096-011-0031-x.

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Upper Cretaceous volcanoclastic-sedimentary formations in the Timok Eruptive Area (eastern Serbia): new biostratigraphic data from planktonic foraminifera The biostratigraphy of the Upper Cretaceous volcanoclastic-sedimentary formations cropping out in the Timok Eruptive Area of the eastern Serbian Carpatho-Balkanides is presented. Four lithostratigraphic units of formation rank are recognized in the Timok area: Stublica Clastics (Upper Albian/Cenomanian), Oštrelj (Lower Turonian/Santonian), Bor Clastics (Campanian/Maastrichtian) and Bukovo (Campanian/?Maastrichtian). Forty two species of planktonic foraminifera have been determined in the studied area. Eight planktonic foraminiferal zones of Middle Cenomanian through Middle Campanian age have been recognized. These are: Thalmanninella reicheli Interval Zone (Middle Cenomanian), Rotalipora cushmani Taxon Range Zone (Upper Cenomanian), Helvetoglobotruncana helvetica Taxon Range Zone (Lower Turonian), Marginotruncana sigali-Dicarinella primitiva Interval Zone (Upper Turonian to lowermost Coniacian), Dicarinella concavata Interval Zone (Lower Coniacian to lowermost Santonian), Dicarinella asymetrica Taxon Range Zone (Santonian), Globotruncanita elevata Interval Zone (Lower Campanian) and the Globotruncana ventricosa Interval Zone (Middle Campanian). The scarcity or lack of zonal species in the Lower Cenomanian and Upper Campanian/Maastrichtian strata prevents recognition of the nominal zones. The Upper Cretaceous planktonic foraminiferal zones from the Timok Eruptive Area are correlated with coeval zones from adjacent regions of Bulgaria and Romania and from other Tethyan regions.

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Candeiro, Carlos Roberto, Rodrigo Pinto De Azevedo, and Priscila Maria Da Silva. "PRELIMINARY APPROACH ON DEPOSITIONAL ENVIRONMENTAL OF THE UBERABA FORMATION (UPPER CRETACEOUS), PEIRÓPOLIS SITE, MINAS GERAIS STATE, BRAZIL: AN INTRODUCTION." Caminhos de Geografia 8, no. 22 (September 22, 2007): 81–85. http://dx.doi.org/10.14393/rcg82215625.

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The Coniacian-Santonian Uberaba Formation of Triângulo Mineiro region hás yielded a important paleofauna from fluvial and associated paleoenvironments. Although poor, fossil content are represented by invertebrates and vertebrates. The paleontological and geological data suggested that Uberaba Formation is characterized by a fluvial of a braided type.

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Akinin, Vyacheslav V., Lina B. Golovneva, Ekaterina B. Salnikova, Irina V. Anisimova, Sergey V. Shczepetov, and Natalya V. Nosova. "The composition and age of the Ul’ya flora (Okhotsk-Chukotka volcanic belt, North-East of Russia): paleobotanical and geochronological constraints." Acta Palaeobotanica 59, no. 2 (December 1, 2019): 251–76. http://dx.doi.org/10.2478/acpa-2019-0014.

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Abstract The Ul’ya flora comes from the Amka Formation of the Ul’ya Depression, located in the Okhotsk–Chukotka volcanic belt (North-East Russia). This flora includes ~50 species, among which conifers predominate. Ferns and angiosperms are also diverse. The Ul’ya flora is characterized by high endemism and by the presence of numerous Early Cretaceous relicts (Hausmannia, Podozamites, Phoenicopsis, Baiera, Sphenobaiera). Four new endemic species of conifers from the Ul’ya flora are described: Elatocladus amkensis Golovneva, sp. nov., Araucarites sheikashoviae Golovneva, sp. nov., Elatocladus gyrbykensis Golovneva, sp. nov. and Pagiophyllum umitbaevii Golovneva, sp. nov. Two-lobed leaves of Sphenobaiera are assigned to S. biloba Prynada based on their epidermal structure. Because of its systematic composition the Ul’ya flora is correlated with the Coniacian Chaun flora of Central Chukotka, with the Coniacian Aliki flora from the Viliga–Tumany interfluve area, and with the Coniacian Kholchan flora of the Magadan Region. The U-Pb age of zircon (ID-TIMS method) from plant-bearing tuffites within the Amka Formation at the Uenma River is 86.1 ± 0.3 Ma. Thus, Coniacian age (most likely the end of the Coniacian, near the Coniacian/Santonian boundary) is assigned to the Ul’ya flora and plant-bearing pyroclastic deposits of the Amka Formation on the basis of paleobotanical and isotopic data.

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Andrieu, Simon, Nicolas Saspiturry, Marine Lartigau, Benoit Issautier, Paul Angrand, and Eric Lasseur. "Large-scale vertical movements in Cenomanian to Santonian carbonate platform in Iberia: indicators of a Coniacian pre-orogenic compressive stress." BSGF - Earth Sciences Bulletin 192 (2021): 19. http://dx.doi.org/10.1051/bsgf/2021011.

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The Cenomanian to early Santonian interval is usually considered a time of postrifting tectonic quiescence around the northern margins of Iberia that preceded the onset of the Pyrenean convergence by crustal thrusting in the latest Santonian. However, plate kinematic models of the Mesozoic evolution of Iberia poorly constrain the Turonian-Santonian position of Iberia relative to Eurasia. This study reconstructs changes in the sedimentary facies and architecture of the Iberian carbonate platform throughout the Late Cretaceous and sheds new light on the geodynamic evolution of the Iberia-Eurasia relationship at that time. Sixteen outcrop sections were described and 24 sedimentary facies identified that define 5 depositional environments ranging from the deep marine basin to the continental setting. From these and previously published field data we reconstruct the evolution of the Pyrenean carbonate platform, on an east-west transect nearly 400 km long, on the basis of 11 short-term depositional sequences and 5 long-term hemicycles. In our interpretation, the Cenomanian and Turonian correspond to a postrift stage during which the European and Iberian margins, together with the deep basin between them, subside gently, as shown by accommodation rates varying from ∼15 to 30 m/My in the margins and ∼100 to 150 m/My in the basin. The Coniacian and early Santonian are characterized by a large-scale flexural response consisting of (1) uplift of the southern Iberian margin, with negative accommodation rates, karstified surfaces and paleosols, and (2) increasing subsidence rates in the basin and its edges (the northern Iberian margin and eastern Aquitaine platform), with accommodation rates several times greater than during the Turonian. We propose that far-field stress possibly related to the northeastward motion of Africa, and/or onset of shortening at the Iberia-Europe boundary in the central and eastern Pyrenees led to the incipient large-scale flexural deformation in the Pyrenean domain. The late Santonian and Campanian are an early orogenic stage marked by rapid subsidence throughout the Pyrenean domain, except at its western end. We evidence for the first time a pre-orogenic flexure at the Iberia-Europe plate boundary induced by regional plate reorganisation between Africa and Europe during the Coniacian and the early Santonian.

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Squires, Richard L. "Northeast Pacific Cretaceous record ofPyropsis(Neogastropoda: Pyropsidae) and paleobiogeography of the genus." Journal of Paleontology 85, no. 6 (November 2011): 1199–215. http://dx.doi.org/10.1666/11-063.1.

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The neogastropod genusPyropsisConrad, 1860 (family Pyropsidae Stephenson, 1941) is recognized for the first time from Upper Cretaceous shallow-marine siliciclastic rocks in the region extending from Vancouver Island, British Columbia southward to southern California. Four new species were detected:Pyropsis aldersoni(earliest Coniacian, southern California),Pyropsis californica(early Coniacian, northern California),Pyropsis louellae(late Coniacian or early Santonian, northern California), andPyropsis grahami(late early Campanian, Vancouver Island).A critical review of the global reports ofPyropsis, a genus that has been commonly confused with other genera (especiallyTudiclaRöding, 1798), establishes thatPyropsishad an amphitropical distribution and lived in warm-temperate waters adjacent to a broad tropical realm. It is rare to uncommon wherever found, and its geologic range is middle Cenomanian to an age near the Cretaceous/Paleogene boundary (probably earliest Paleocene). It was moderately widespread before the Maastrichtian but was predominantly restricted to the New World during the Maastrichtian.

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Gaspard, Danièle, and Sylvain Charbonnier. "The debated question of asymmetrical rhynchonellids (Brachiopoda, Rhynchonellida): examples from the Late Cretaceous of Western Europe." BSGF - Earth Sciences Bulletin 191 (2020): 1. http://dx.doi.org/10.1051/bsgf/2019016.

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Many Cretaceous asymmetrical rhynchonellid brachiopods (Brachiopoda, Rhynchonellida) have long been considered as Rhynchonella difformis (Valenciennes in Lamarck, 1819). After a revision, Owen (1962) included the Cenomanian specimens from Europe in Cyclothyris M’Coy, 1844. Later, Manceñido et al. (2002) confirmed this decision and critically mentioned the name of another asymmetrical rhynchonellid genus from Spain, Owenirhynchia Calzada in Calzada and Pocovi, 1980. Specimens with an asymmetrical anterior margin (non particularly ecophenotypical), from the Late Coniacian and the Santonian of Les Corbières (Aude, France) and Basse-Provence (SE France) are here compared to specimens of the original Cenomanian species C. difformis. They are also compared to new material from the Northern Castilian Platform (Coniacian-Santonian, N Spain) and to Rhynchonella globata Arnaud, 1877 (Campanian, Les Charentes, Dordogne, SW France) and Rh. vesicularis Coquand, 1860 (Campanian, Charente, SW France). These observations document the great morphological diversity among all these species and lead us to erect a new species: Cyclothyris grimargina nov. sp. from the type material of Arnaud, and two new genera: Contortithyris nov. gen. including Contortithyris thermae nov. sp., Beaussetithyris nov. gen. including Beaussetithyris asymmetrica nov. sp. All of these brachiopods fundamentally present an asymmetrical state which origin is discussed.

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Herkat, Missoum. "Eustatic and palaeogeographic control of the western Aurès Upper Cretaceous sedimentation (Algeria)." Bulletin de la Société Géologique de France 175, no. 3 (May 1, 2004): 273–88. http://dx.doi.org/10.2113/175.3.273.

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Abstract The Upper Cretaceous sedimentation in the Aurès Mountains occurred in a subsident basin delimited to the south by the Saharan platform and by the Preatlasic high zone to the north. In these series 4 transgressive-regressive megasequences are distinguished, the first one (I) in the late Albian-Cenomanian, the second one (II) in the Turonian, the third one (III) in the Coniacian - Santonian and the fourth one (IV) in the Campanian - Maastrichtian. Each megasequence is made up of three or four sequences, which correspond to third order cycles identified in the eustatic chart of Haq et al. [1987]. In late Albian and lower Turonian periods, during the deposition of basal sequences of the megasequences I and II, the reactivation of basement faults in the Aurès basin occurs consecutively to distension phases, resulting in the formation of rotated blocks. At the same time high eustatic levels are reached according to the global eustatic curve. These processes control the drowning of the carbonate platforms pre-existing to these sequences, and deep ramps progressively form on the tilted block tops. This sedimentary setting generates in the late Albian and lower Turonian series anoxic sequences made up of calcareous and shaly transgressive pelagic intervals. The succeeding sequences lack pelagic facies and are composed of alternate marls / carbonate beds deposited on a homoclinal ramp, indicating a gradual development of shallow open marine conditions, which became progressively restricted upwards. Toward the top of these megasequences, lagunal muds and isolated rudists mounds, surrounded by bioclastic and ooid / pellet banks occur. The Coniacian-Santonian and Campanian-Maastrichtian megasequences are characterized by a shallow ramp sedimentation, essentially marly during the Coniacian, Santonian and Campanian periods, interlayered with some bioclastic / ooid carbonate banks and upwards by sequences mostly homogeneous. The Maastrichtian platform carbonates are composed of bioclastic / ooid sands and were deposited in a ramp-barrier-bank system. Some sequences in the Campanian-Maastrichtian megasequence are condensed or absent due to the accommodation reduction related to a weak subsidence rate period.

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22

Bell, Gorden L., Kenneth R. Barnes, and Michael J. Polcyn. "Late Cretaceous mosasauroids (Reptilia, Squamata) of the Big Bend region in Texas, USA." Earth and Environmental Science Transactions of the Royal Society of Edinburgh 103, no. 3-4 (September 2012): 571–81. http://dx.doi.org/10.1017/s1755691013000406.

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ABSTRACTUpper Cretaceous marine rocks of the Big Bend Region of trans-Pecos Texas preserve a number of marine-adapted mosasauroids. At least three unnamed taxa of basal mosasauroids are represented by remains from shaly limestones in the middle Turonian portion of the Boquillas Formation. These occur along with remains of larger derived mosasaurs referable to Russellosaurina and an undescribed tylosaurine. Derived mosasaurs from the middle to late Coniacian include the first report of Tylosaurus kansasensis outside of Kansas, T. nepaeolicus, Platecarpus planifrons, and Platecarpus aff. P. planifrons. Clidastes liodontus is found in the latest Coniacian or early Santonian part of the Pen Formation. An undescribed species of Ectenosaurus, Clidastes sp. and an indeterminate plioplatecarpine occurs in the middle Santonian to early Campanian interval of the Pen Formation. The mosasaur fauna from the Big Bend region is quite similar to that from the Smoky Hill Chalk of Kansas, a thousand kilometres to the north. We refine the position of the Cenomanian–Turonian boundary within the Ernst Member of the Boquillas Formation, based on ammonite faunas. We also corroborate previous interpretations describing the time-transgressive nature of the onset of deposition of the Pen Formation based on a west-to-east descending level of the Inoceramus (Cremnoceramus) undulatoplicatus FAD.

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23

Cooper, Dee Ann, Roger W. Cooper, James B. Stevens, M. S. Stevens, William A. Cobban, and Ireneusz Walaszczyk. "The Boquillas Formation of the Big Bend National Park, Texas, USA, a reference Cenomanian through Santonian (Upper Cretaceous) carbonate succession at the southern end of the Western Interior Seaway." Acta Geologica Polonica 67, no. 4 (December 1, 2017): 547–65. http://dx.doi.org/10.1515/agp-2017-0033.

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Abstract The upper lower Cenomanian through middle Santonian (Upper Cretaceous) of the Boquillas Formation in the Big Bend Region of Trans-Pecos Texas consists of a marine carbonate succession deposited at the southern end of the Western Interior Seaway. The Boquillas Formation, subdivided into the lower, c. 78 m thick limestone-shale Ernst Member, and the upper, c. 132 m thick limestone/chalk/marl San Vicente Member, was deposited in a shallow shelf open marine environment at the junction between the Western Interior Seaway and the western margins of the Tethys Basin. Biogeographically, the area was closely tied with the southern Western Interior Seaway. The richly fossiliferous upper Turonian, Coniacian and lower Santonian parts of the Boquillas Formation are particularly promising for multistratigraphic studies.

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24

Radoicic, Rajka, Vladan Radulovic, Dragoman Rabrenovic, and Barbara Radulovic. "The age of the brachiopod limestones from Guca, western Serbia." Annales g?ologiques de la Peninsule balkanique, no. 71 (2010): 73–93. http://dx.doi.org/10.2298/gabp1071073r.

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The asymmetric rhynchonellide brachiopod Cyclothyris? globata (ARNAUD, 1877) has a large distribution in the Coniacian, Santonian and Campanian outcrops of the western Tethys. The species has also been identified in Guca, (Vardar Zone, western Serbia), where it occurs together with the capillate terebratuloid ?Terebratula? sp. (gen. et sp. nov.). In addition to Serbia, this brachiopod association is found in many localities of northeastern Bulgaria (Shumen Formation). In older literature, in Romania and Bulgaria, ?Terebratula? sp. (gen. et sp. nov.) was confused with the Late Maastrichtian Terebratulina striata (WAHLENBERG, 1821). The present microfaunal study based on planktonic foraminifera showed that the age of the beds with Cyclothyris? globata and ?Terebratula? sp. (gen. et sp. nov.) in Guca may be dated as Lowermost Campanian, i.e., the Santonian/Campanian boundary.

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25

Wagreich, M. ""OAE 3" – regional Atlantic organic carbon burial during the Coniacian–Santonian." Climate of the Past 8, no. 5 (September 20, 2012): 1447–55. http://dx.doi.org/10.5194/cp-8-1447-2012.

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Abstract. The Coniacian–Santonian time interval is the inferred time of oceanic anoxic event 3 (OAE 3), the last of the Cretaceous OAEs. A detailed look on the temporal and spatial distribution of organic-rich deposits attributed to OAE 3 suggests that black shale occurrences are restricted to the equatorial to mid-latitudinal Atlantic and adjacent basins, shelves and epicontinental seas like parts of the Caribbean, the Maracaibo Basin and the Western Interior Basin, and are largely absent in the Tethys, the North Atlantic, the southern South Atlantic, and the Pacific. Here, oxic bottom waters prevailed as indicated by the widespread occurrence of red deep-marine CORBs (Cretaceous Oceanic Red Beds). Widespread CORB sedimentation started during the Turonian after Oceanic Anoxic Event 2 (OAE 2) except in the Atlantic realm where organic-rich strata continue up to the Santonian. The temporal distribution of black shales attributed to OAE 3 indicates that organic-rich strata do not define a single and distinct short-time event, but are distributed over a longer time span and occur in different basins during different times. This suggests intermittent and regional anoxic conditions from the Coniacian to the Santonian. A comparison of time-correlated high-resolution δ13C curves for this interval indicates several minor positive excursions of up to 0.5‰, probably as a result of massive organic carbon burial cycles in the Atlantic. Regional wind-induced upwelling and restricted deep basins may have contributed to the development of anoxia during a time interval of widespread oxic conditions, thus highlighting the regional character of inferred OAE 3 as regional Atlantic event(s).

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26

Van Melle, Jeremie, Washinton Vilema, Bastien Faure-Brac, Martha Ordoñez, Henriette Lapierre, Nelson Jimenez, Etienne Jaillard, and Milton Garcia. "Pre-collision evolution of the Piñón oceanic terrane of SW Ecuador: stratigraphy and geochemistry of the “Calentura Formation”." Bulletin de la Société Géologique de France 179, no. 5 (September 1, 2008): 433–43. http://dx.doi.org/10.2113/gssgfbull.179.5.433.

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Abstract The stratigraphic revision of the southern coastal Ecuadorian series makes possible the reconstruction of the pre-collision history of the Caribbean plateau accreted to the Ecuadorian margin. The Coniacian age of the oceanic basement (Piñón Fm) indicates that the latter is part of the Caribbean oceanic plateau. It is overlain by the Calentura Fm, which comprises from base to top: (i) 20 to 200 m of lavas and volcanic breccias of arc affinity (Las Orquídeas Mb), (ii) siliceous, organic rich black limestones of (middle?) Coniacian age, (iii) red, radiolarian rich, calcareous cherts ascribed to the Santonian-early Campanian, and (iv) marls, greywackes and island arc tuffs of Mid Campanian age. The latter are overlain by volcaniclastic turbidites of Mid to Late Campanian age (Cayo Fm), coeval to the Campanian-Maastrichtian island arc series locate farther west (San Lorenzo Fm). The Las Orquídeas magmatic unit is interpreted as resulting from the melting of the Caribbean plateau, rather than from an ephemeral subduction process. The transition from coniacian limestones to santonian red cherts would be related to the thermal subsidence of the Caribbean plateau. The uplift of the latter and the development of the San Lorenzo island arc in the Middle Campanian would be due to the collision of the Caribbean plateau with the Mexican margin. Early in the Late Maastrichtian, the collision of the Caribbean plateau with the Ecuadorian margin would have triggered the cessation of the San Lorenzo arc activity. In the Late Paleocene, the Caribbean plateau was split into two terranes: the western Piñón terrane, which collided with the eastern Guaranda terrane.

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27

Wagreich, M. ""OAE 3" – a low- to mid-latitude Atlantic oceanic event during the Coniacian-Santonian." Climate of the Past Discussions 8, no. 2 (April 16, 2012): 1209–27. http://dx.doi.org/10.5194/cpd-8-1209-2012.

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Abstract. The Coniacian-Santonian time interval is the inferred time of oceanic anoxic event 3 (OAE 3), the last of the Cretaceous OAEs. A detailed look on the temporal and spatial distribution of organic-rich deposits attributed to OAE 3 suggests that black shale occurrences are restricted to the equatorial to mid-latitudinal Atlantic and adjacent basins, shelves and epicontinental seas like parts of the Caribbean, the Maracaibo Basin and the Western Interior Basin, and are largely absent in the Tethys, the North Atlantic, the southern South Atlantic, and the Pacific. Here, oxic bottom waters prevailed as indicated by the widespread occurrence of red deep-marine CORBs (Cretaceous Oceanic Red Beds). Widespread CORB sedimentation started during the Turonian after Oceanic Anoxic Event 2 (OAE 2) except in the Atlantic realm where organic-rich strata continue up to the Santonian. The temporal distribution of black shales attributed to OAE 3 indicates that organic-rich strata do not define a single and distinct short-time event, but are distributed over a longer time span and occur in different basins during different times. This suggests intermittent and regional anoxic conditions from the Coniacian to the Santonian. A comparison of time-correlated high-resolution δ13C curves for this interval indicates several minor positive excursions of about 0.5 permil, probably as a result of massive organic carbon burial cycles in the Atlantic. Regional wind-induced upwelling and silled deep basins may have contributed to the development of anoxia during a global oxic time interval, thus highlighting the regional character of inferred OAE 3 as an Atlantic anoxic event (AAE).

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28

Cooper, Michael R. "On the status of Kaiparaites Matsumoto, 1955 (Cretaceous; Ammonoidea: Kossmaticeratidae)." Neues Jahrbuch für Geologie und Paläontologie - Abhandlungen 294, no. 3 (December 1, 2019): 307–10. http://dx.doi.org/10.1127/njgpa/2019/0861.

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The kossmaticeratid ammonite Kaiparaites was on its inception synonymized by its author (Matsumoto 1955) with Natalites (Collignon 1954). However, close comparison of the type species of these two genera shows them to be morphologically and stratigraphically distinct. Whereas Santonian Natalites shares the flexed constrictions of late Turonian–Coniacian Kossmaticeras, the straight constrictions of late Campanian – Maastrichtian Kaiparaites are shared with Caledonites, Gunnarites, Grossouvrites and Jacobites. Consequently, Kaiparaites is resurrected from the synonymy of Natalites and demonstrates that, under phylogenetic consideration, characters first thought to be of prime taxonomic significance actually turn out to be secondary. Since treatment of Natalites as a subgenus of Kossmaticeras emphasizes primitive characters, it is returned to generic rank, as is Santonian Karapadites although, for those who find use for subgenera, the latter can be treated as a subgenus of Natalites.

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29

Golovneva, L. B. "The Late Cretaceous flora of the Khatanga depression." Palaeobotany 3 (2012): 32–61. http://dx.doi.org/10.31111/palaeobotany/2012.3.32.

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Fossil plants from the Late Cretaceous deposits of the Khatanga depression are joined in three floristic assemblages: the Ledyanaya assemblage (the Turonian-Coniacian), the Kheta assemblage (the late Coniacian-early Santonian) and Mutino assemblage (the late Santonian-early Campanian). The Ledyanaya floristic assemblage contains ferns (Anemia rarinervis Abramova), cycadophytes (Nilssonia sp.), ginkgoales (Ginkgo ex gr. sibirica Heer), conifers (Taxodium sp., Sequoia tenuifolia (Schmalh.) Sveshn. et Budants.) and angiosperms (Pseudoprotophyllum hatangaense Abramova, Liriodendropsis simplex (Newb.) Newb., Trochodendroides sp., ะกissites sp., Dicotylophyllum sp.). The characteristic features of this assemblage are depauperated composition of angiosperms and survival of the Early Cretaceous relic elements. The Kheta floristic assemblage contains only Taxodium sp. and Trochodendroides sp. The Mutino floristic assemblage contains Sequoia tenuifolia, Pseudoprotophyllum hatangaense, Quereuxia angulata (Newb.) Krysht. ex Baik. and Cobbania corrugata (Lesq.) Stockey, Rothwell et Johnson. The Ledyanaya floristic assemblage is very similar with the Newsiberian flora from the Derevyannye Gory Formation of New Siberia Island. The Mutino floristic assemblage have common elements with Kundur flora (the Campanian) from the Kundur Formation of Amur region. The abundance of large leaves of Pseudoprotophyllum in the Mutino flora is evidence of the preservation of humid warm-temperate climate in the northern part of Siberia up to the Campanian. The presence of water plants Quereuxia angulata and Cobbania corrugada indicates the westward migration of some characteristic elements of the Pacific ocean lowlands.

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30

Lindgren, Johan, and Mikael Siverson. "Tylosaurus ivoensis: a giant mosasaur from the early Campanian of Sweden." Transactions of the Royal Society of Edinburgh: Earth Sciences 93, no. 1 (March 2002): 73–93. http://dx.doi.org/10.1017/s026359330000033x.

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ABSTRACTThe nominal species Mosasaurus ivoensis from the latest early Campanian of the Kristianstad Basin in southern Sweden, is redescribed and assigned to the tylosaurine genus Tylosaurus on the basis of its dental and vertebral morphology. A partial skeleton (KUVP 1024) from the late Coniacian to earliest Campanian Smoky Hill Chalk Member of the Niobrara Formation in western Kansas, USA, was previously referred to “M”. ivoensis. Nevertheless, its marginal teeth are markedly different, both in size and morphology, from those of topotypic T. ivoensis.Examination of type specimens and topotypic material of the nominal tylosaurines Hainosaurus pembinensis from the late early Campanian of Manitoba, Canada, H. gaudryi from the late Santonian or early Campanian of northwestern France, and H. lonzeensis from the Coniacian or Santonian of Belgium, indicates that all three may be Tylosaurus.The utility of isolated tooth-crowns in mosasaur taxonomy has been hampered by the often poor quality of the published illustrations of these fossils in combination with poor stratigraphic control. All Swedish remains of T. ivoensis, including 172 marginal teeth, 6 pterygoid teeth, several jawbone fragments and 12 vertebrae, were collected from a narrow stratigraphic interval corresponding to the highest biozone in the German eight-fold division of the early Campanian, providing the first good insight into the intraspecific dental variation in a tylosaurine mosasaur.

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31

Jenkyns, H. C., A. S. Gale, and R. M. Corfield. "Carbon- and oxygen-isotope stratigraphy of the English Chalk and Italian Scaglia and its palaeoclimatic significance." Geological Magazine 131, no. 1 (January 1994): 1–34. http://dx.doi.org/10.1017/s0016756800010451.

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AbstractA detailed carbon- and oxygen-isotope stratigraphy has been generated from Upper Cretaceous coastal Chalk sections in southern England (East Kent; Culver Cliff, Isle of Wight; Eastbourne and Seaford Head, Sussex; Norfolk Coast) and the British Geological Survey (BGS) Trunch borehole, Norfolk. Data are also presented from a section through the Scaglia facies exposed near Gubbio, Italian Apennines. Wherever possible the sampling interval has been one metre or less. Both the Chalk and Scaglia carbon-isotopic curves show minor positive excursions in the mid-Cenomanian, mid- and high Turonian, basal Coniacian and highest Santonian–lowest Campanian; there is a negative excursion high in the Campanian in Chalk sections that span that interval. The well-documented Cenomanian–Turonian boundary ‘spike’ is also well displayed, as is a broad positive excursion centred on the upper Coniacian. A number of these positive excursions correlate with records of organic-carbon-rich deposition in the Atlantic Ocean and elsewhere. The remarkable similarity in the carbon-isotope curves from England and Italy enables cross-referencing of macrofossil and microfossil zones and pinpoints considerable discrepancy in the relative positions of the Turonian, Coniacian and Santonian stages.The oxygen-isotope values of the various Chalk sections, although showing different absolute values that are presumably diagenesis-dependent, show nonetheless a consistent trend. The East Kent section, which is very poorly lithified, indicates a warming up to the Cenomanian–Turonian boundary interval, then cooling thereafter. Regional organic-carbon burial, documented for this period, is credited with causing drawdown of CO2 and initiating climatic deterioration (inverse greenhouse effect). Data from other parts of the world are consistent with the hypothesis that the Cenomanian–Turonian temperature optimum was a global phenomenon and that this interval represents a major turning point in the climatic history of the earth.

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32

Shczepetov, S. V., and A. B. Herman. "On the non-marine stratigraphy and floras of north-eastern Russia." Стратиграфия 27, no. 3 (April 22, 2019): 40–52. http://dx.doi.org/10.31857/s0869-592x27340-52.

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Some decisions of the Third Inter-departmental Regional Stratigraphic Meeting on Precambrian, Paleozoic and Mesozoic of North-eastern Russia (St. Petersburg, 2002) are analysed in the light of latest data obtained. It is shown that regional stratigraphic units (‘Horizons’) of non-marine Cretaceous recognised in this Meeting are in fact not the basic subdivisions, but rather specialised biostratigraphic units, namely ‘Beds with flora’. Ages of some of these units are specified, notably Beds with Arman Flora is Turonian–Coniacian, Beds with Amka Flora is Coniacian and Beds with Arkagala Flora is Santonian–Campanian. We recommend to keep the previous names for the Penzhina, Barykov and Koryak phases of floral development and for the corresponding stratigraphic units. An updated version of the non-marine Cretaceous stratigraphic chart of the Okhotsk-Chukotka structural-facial Region is proposed to discuss.

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33

Dimitrova, Ekaterina, and Boris Valchev. "Attempt for Upper Cretaceous planktic foraminiferal zonation of the Srednogorie and Eastern Balkan Zones (Bulgaria)." Geologica Balcanica 36, no. 1-2 (June 30, 2007): 55–63. http://dx.doi.org/10.52321/geolbalc.36.1-2.55.

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Thirteen biostratigraphical zones were defined as a result of summarizing of the available data on the taxonomy, stratigraphical range and occurrence of the Upper Cretaceous planktic foraminifera from the Srednogoriå and East Balkan. The zones are: Rotalipora cushmani Taxon Range Zone (Late Cenomanian), Dicarinella imbricata Interval Zone (Early Turonian), Marginotruncana renzi – Marginotruncana sigali Interval Zone (Middle Turonian), Marginotruncana schneegansi Interval Zone (Late Turonian), Dicarinella primitiva Interval Zone (Early Coniacian), Dicarinella concavata Interval Zone (Late Coniacian to Early Santonian), Globotruncanita elevata Interval Zone (Early Campanian), Globotruncanita stuartiformis Interval Zone (Early Late Campanian), Radotruncana calcarata Taxon Range Zone (Late Late Campanian), Globotruncana falsostuarti Interval Zone (Early Maastrichtian), Contusotruncana contusa Interval Zone (Early to Late Maastrichtian), Abathomphalus mayaroensis Taxon Range Zone (Late Late Maastrichtian). The zones were successfully correlated to the biostratigraphical schemes in the Carpathians, Mediterranean Basin, Caribbean Basin, and some generalized zonations.

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34

Gonzalez, Wilma B. Aleman, Jean M. Self-Trail, W. Burleigh Harris, Jessica Pierson Moore, and Kathleen M. Farrell. "Depositional sequence stratigraphy of Turonian to Santonian sediments, Cape Fear arch, North Carolina Coastal Plain, USA." Stratigraphy 16, no. 1 (December 11, 2020): 293–314. http://dx.doi.org/10.29041/strat.17.4.293-314.

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ABSTRACT: A new sequence stratigraphic framework for Turonian to Santonian (94-84 Ma) sediments is established using data from the USGS Kure Beach and Elizabethtown cores collected from the Atlantic Coastal Plain of North Carolina (NC). These sediments represent some of the oldest marine units deposited on the southeastern Atlantic Coastal Plain and record the early development of a clastic wedge atop crystalline basement. Sediments were deposited as transitional marginal-marine to marine units in a complex interplay of fluvial, estuarine, and shelf environments. Repetitive lithologies and minimal biostratigraphic control requires an integrated analysis of grain-size data, geophysical logs, biostratigraphy, and 87Sr/86Sr isotopic data to identify systems tracts and establish a sequence stratigraphic framework. From this integrated approach, three Turonian to Santonian sequences in the Elizabethtown core and six in the Kure Beach core are identified. The new sequences from oldest to youngest are Clubhouse II, Fort Fisher I, Fort Fisher II, Collins Creek I, Collins Creek II, Pleasant Creek I, and Pleasant Creek II. Sequences from North Carolina document significant shifts of global and regional sea-level during greenhouse conditions in the early Late Cretaceous. Maximum sea-level rise occurred globally during the early Turonian and is documented from the marine sediments of the Clubhouse II sequence. This sequence is unconformably overlain by terrestrial sediments deposited during a major fall in sea level and maximum progradation of the shoreline, as evidenced by the Fort Fisher I sequence. Global sea-level rise in the Coniacian resulted in the deposition of the Fort Fisher II sequence, which is present only in the Kure Beach core. Local marine circulation and erosion on the shelf is suggested by the absence of the Collins Creek I sequence at Kure Beach; this sequence is present only in the up-dip Elizabethtown core. Activation of a possible buried fault structure along the Cape Fear arch resulted in the formation of a regional depocenter during the late Coniacian to early Santonian and is reflected in the unusual thickness of the Collins Creek II and Pleasant Creek I sequences. The return to a more global sea-level influence occurred in the late Santonian with the deposition of the Pleasant Creek II sequence. A comparison of temporal distribution of sequences in the Elizabethtown and Kure Beach cores to corresponding sequences in New Jersey indicates significant differences in erosional and tectonic processes in the Cape Fear region during the Turonian and Santonian.

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35

Pervushov, Evgeniy M. "Genus Tremabolites Zittel, 1878 (Porifera, Hexactinellida)." Izvestiya of Saratov University. New Series. Series: Earth Sciences 21, no. 2 (June 24, 2021): 103–17. http://dx.doi.org/10.18500/1819-7663-2021-21-2-103-117.

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Tremabolites sponges known among the Middle-Late Cretaceous beds in Europe are reliably identifiable due to the numerous openings against the background of the skeleton smooth upper surface. The ideas of the level of organization in these sponges and of the species characteristics are far from being univocal. The paper deals with the species diversity of Tremabolites common in the Coniacian – Santonian rocks from the Volga Region. Examples of regeneration and budding in the representatives of the group are presented.

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36

Al-Rifaiy, I. A., O. H. Cherif, and B. A. El-Bakri. "Late Coniacian - Early Santonian Foraminifera from the Wadi Ghudran Formation in Jordan." Géologie Méditerranéenne 18, no. 4 (1991): 207–19. http://dx.doi.org/10.3406/geolm.1991.1464.

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37

März, C., B. Beckmann, C. Franke, Christoph Vogt, T. Wagner, and S. Kasten. "Geochemical environment of the Coniacian–Santonian western tropical Atlantic at Demerara Rise." Palaeogeography, Palaeoclimatology, Palaeoecology 273, no. 3-4 (March 2009): 286–301. http://dx.doi.org/10.1016/j.palaeo.2008.05.004.

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38

López, Gregorio, Ricard Martínez, and Marcos A. Lamolda. "Biogeographic relationships of the Coniacian and Santonian inoceramid bivalves of northern Spain." Palaeogeography, Palaeoclimatology, Palaeoecology 92, no. 3-4 (April 1992): 249–61. http://dx.doi.org/10.1016/0031-0182(92)90085-j.

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39

Kopaevich, Ludmila F., Vladimir N. Beniamovski, and Aleksey Yu Sadekov. "Middle Coniacian–Santonian foraminiferal bioevents around the Mangyshlak Peninsula and Russian Platform." Cretaceous Research 28, no. 1 (February 2007): 108–18. http://dx.doi.org/10.1016/j.cretres.2006.05.018.

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40

Golovneva, L. B., T. M. Kodrul, and E. V. Bugdaeva. "The Late Cretaceous floras of the Zeya-Bureya Basin." Palaeobotany 11 (2020): 5–47. http://dx.doi.org/10.31111/palaeobotany/2020.11.5.

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A general characterization of the Late Cretaceous floras of the Zeya-Bureya Basin is provided based on floristic assemblages from Russia (Amur Region) and China (Heilongjiang Province). Four phases of floral evolution were revealed: the Turonian-Coniacian (the Sutara flora), the Santonian (the Yong’ancun and Middle Kundur floras), the Campanian (the Taipinglinchang and Late Kundur floras) and the late Maastrichtian (Bureya flora). This long paleofloral succession provides possibility for investigation of different trends in the evolution of the Late Cretaceous taxa, flora, and climate.

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41

PAUL, C. R. C., and M. A. LAMOLDA. "Testing the precision of bioevents." Geological Magazine 146, no. 5 (May 15, 2009): 625–37. http://dx.doi.org/10.1017/s0016756809006463.

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AbstractDeciding which of two bioevents is the less diachronous is a common problem in biostratigraphy. The most accurate correlation uses the finest timescale available. Chemostratigraphy or cyclostratigraphy offer a potential precision of about 10 ka. Graphic correlation can then be used to test the precision of bioevents and to quantify any mismatch. It can also be used to determine in which section any event occurs earlier. Application of these ideas to correlation of the Cenomanian–Turonian and Coniacian–Santonian boundaries demonstrates that some bioevents are as precise as chemo- and cyclostratigraphy, but that most are not. Two problems occur with bioevents. First they may not be recognizable in all sections. Second, where they are recognizable, they may be diachronous. In the former case, calculating confidence intervals on known ranges in sections where the relevant fossil has been recorded is an alternative test. Large confidence intervals suggest that both first and last occurrences of a fossil may be diachronous bioevents. At the Cenomanian–Turonian boundary the following bioevents (in stratigraphic order) appear to be reliable time planes for international correlation. The last occurrences of (1) Corolithion kennedyi, (2) Rotalipora greenhornensis, (3) Axopodorhabdus albianus, (4) Rotalipora cushmani, (5) Lithraphidites acutus, (6) Microstaurus chiastius and (7) the first occurrence of Quadrum gartneri. At the Coniacian–Santonian boundary only the first and last occurrences of Platyceramus undulatoplicatus, and the first occurrences of Platyceramus cycloides and Lucianorhabdus cayeuxii have been identified as potentially reliable bioevents.

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42

Banjesevic, Miodrag. "Upper cretaceous magmatic suites of the Timok magmatic complex." Annales g?ologiques de la Peninsule balkanique, no. 71 (2010): 13–22. http://dx.doi.org/10.2298/gabp1071013b.

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The Upper Cretaceous Timok Magmatic Complex (TMC) developed on a continental crust composed of different types of Proterozoic to Lower Cretaceous rocks. The TMC consists of the magmatic suites: Timok andesite (AT) - Turonian-Santonian, Metovnica epiclastite (EM) - Coniacian-Campanian, Osnic basaltic andesite (AO) and Jezevica andesite (AJ) - Santonian-Campanian, Valja Strz plutonite (PVS) - Campanian and Boljevac latite (LB). The sedimentary processes and volcanic activity of the TMC lasted nearly continuously throughout nearly the whole Late Cretaceous. The sedimentation lasted from the Albian to the Maastrichtian and the magmatism lasted for 10 million years, from the Upper Turonian to the Upper Campanian. The volcanic front migrated from East to West. The volcanic processes were characterized by the domination of extrusive volcanic facies, a great amount of volcanic material, a change in the depositional environment during the volcanic cycle, sharp facial transitions and a huge deposition of syn- and post-eruptive resedimented volcaniclastics.

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Packer, Stephen R., and Malcolm B. Hart. "Coniacian–Santonian Radiolaria from the Upper Cretaceous of Bornholm, Denmark: A preliminary investigation." Bulletin of the Geological Society of Denmark 52 (December 31, 2005): 141–58. http://dx.doi.org/10.37570/bgsd-2005-52-11.

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A moderately diverse fauna of Late Cretaceous Radiolaria are described for the first time from the Arnager Limestone and Bavnodde Greensand formations exposed on the island of Bornholm (Denmark). Our preliminary investigation suggests that the fauna from the Arnager Limestone Formation is relatively abundant and is assigned to the Orbiculiforma vacaensis Subzone (Alievium praegallowayi Zone) of Coniacian age. Relatively poor recovery from the Bavnodde Greensand Formation precludes assignment to the zonation scheme of Pessagno, although, the radiolarian taxa present indicate that the formation can be no younger than Santonian. The ages given for both formations by the radiolarian faunas compare favourably with published macrofossil and microfossil data. The radiolarian faunas described are of moderate abundance and diversity when compared to contemporaneous faunas described elsewhere, particularly the Tethyan area. Maximum radiolarian abundance and diversity is reached in the middle of the Arnager Limestone Formation equating to a level of maximum water depth from the foraminiferal data. A decline in radiolarian recovery is recognised into the Bavnodde Greensand Formation and is associated with a reduction in relative water depth to inner and (?)middle shelf conditions, as indicated by foraminiferal data.

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Landman, Neil H., A. Guy Plint, and Irek Walaszczyk. "Allostratigraphy and Biostratigraphy of the Upper Cretaceous (Coniacian-Santonian) Western Canada Foreland Basin." Bulletin of the American Museum of Natural History 414 (June 2017): 1–172. http://dx.doi.org/10.1206/0003-0090-414.1.2.

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El-Hedeny, M. M., A. A. Abdel Aal, M. Maree, and J. Seeling. "Plicatulid bivalves from the Coniacian–Santonian Matulla Formation, Wadi Sudr, western Sinai, Egypt." Cretaceous Research 22, no. 3 (June 2001): 295–308. http://dx.doi.org/10.1006/cres.2001.0257.

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Gallemí, Jaume, Gregorio López, Ricardo Martínez, and Jose Maria Pons. "Macrofauna of the Villamartín Section: Coniacian/Santonian boundary, North Castilian Platform, Burgos, Spain." Cretaceous Research 28, no. 1 (February 2007): 93–107. http://dx.doi.org/10.1016/j.cretres.2006.05.016.

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SCHLAGINTWEIT, FELIX, FRANCISCO SÁNCHEZ-BERISTAIN, HYAM SALEH DAOUD, and KOOROSH RASHIDI. "ACANTHOCHAETETES FISCHERI N. SP. (CORALLINE DEMOSPONGE) FROM THE UPPER PALEOCENE (THANETIAN) OF IRAQ (KURDISTAN REGION) AND IRAN (SISTAN SUTURE ZONE)." Acta Palaeontologica Romaniae, no. 18 (2) (January 21, 2022): 53–62. http://dx.doi.org/10.35463/j.apr.2022.02.02.

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The new coralline demosponge Acanthochaetetes fischeri n. sp. is described from the upper Paleocene (Thanetian) of Iraq (Kurdistan Region, Khurmala Formation) and Iran (Sistan Suture Zone). The genus Acanthochaetetes Fischer is a long-ranging genus known from the Upper Jurassic (A. foroiuliensis), through Upper Cretaceous (e.g., Coniacian A.? krumbachensis) and Eocene (A. eocenica) to Recent. A. fischeri n. sp. is the first record from the Paleocene following the K-Pg mass-extinction, thereby closing the gap within the Santonian-Eocene interval. It occurs in platform-margin/upper slope depositional settings associated with coralline algae, corals, and echinoids.

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Sahakyan, Lilit. "The age of Vedi alkaline lamprophyre diatreme." Proceedings of NAS RA. Earth Sciences 75, no. 2 (October 6, 2022): 16–28. http://dx.doi.org/10.54503/0515-961x-2022.75.2-16.

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The alkaline lamprophyres of Vedi diatreme are composed mostly of green globular volcanic glass and have typical mineral composition for these rocks. Vedi diatreme is located in the Mankouk anticline (Khosrov reserve), where Middle Jurassic ophiolite complex where the obduction took place during the Late Coniacian to Santonian. U-Pb age of pyroclastic rocks of the diatreme is determined 182±3 Ma (n=17) by LA-ICP MS ablation on zircon grains. Broken rims of zircon grains indicate that they are affected by explosion. Alkaline lamprophyres are formed in an extensional environment of a subduction setting.

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Ardestani, Meysam Shafiee, Mohammad Vahidinia, Abbas Sadeghi, José Antonio Arz, and Docho Dochev. "Integrated biostratigraphy of the Upper Cretaceous Abderaz Formation of the East Kopet Dagh Basin (NE Iran)." Geologica Balcanica 41, no. 1-3 (December 2012): 21–37. http://dx.doi.org/10.52321/geolbalc.41.1-3.21.

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Based on planktonic foraminifera, inoceramids and echinoids, we present a detailed biostratigraphic analysis of the Abderaz Formation at the 606 m thick Padeha section, NE Iran. This sequence consists mainly of gray shales and marls with four levels of chalky limestones intercalated. The lower boundary of the Abderaz Formation with the Aitamir Formation is a paraconformity, while the upper boundary with the Abtalkh Formation represents a gradual transition. Fifty four species of planktonic foraminifera from 15 genera were identified, and five zones were recognized, namely: Whiteinella archaeocretacea (Bolli) Partial-Range-Zone; Helvetoglobotruncana helvetica (Sigal) Total-Range-Zone; Marginotruncana schneegansi (Dalbiez) Interval-Range-Zone; Dicarinella concavata (Brotzen) Interval-Range-Zone; and Dicarinella asymetrica (Sigal) Total-Range-Zone. Based on these data, the age of the Abderaz Formation is determined as earliest Turonian to earliest Campanian. Inoceramid bivalves Cremnoceramus walterdorfensis walterdorfensis (Andert) and Cremnoceramus deformis deformis (Meek) were identified in the uppermost Turonian and in the middle part of the early Coniacian, respectively. Echinocorys ex. gr. scutata and Cordiceramus sp. were recorded near the Coniacian/Santonian boundary.

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Vishnevskaya, Valentina S., and Ludmila F. Kopaevich. "Microfossil assemblages as key to reconstruct sea-level fluctuations, cooling episodes and palaeogeography: The Albian to Maastrichtian of Boreal and Peri-Tethyan Russia." Geological Society, London, Special Publications 498, no. 1 (November 18, 2019): 165–87. http://dx.doi.org/10.1144/sp498-2018-138.

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AbstractThe main palaeogeographic features of the Late Cretaceous Eastern European Platform and its southern framework are reconstructed mainly based on micropalaeontological data. An integrated foraminiferal–radiolarian zonation for the Upper Albian–Maastrichtian serves as a basis for palaeogeographic reconstructions and as a framework for the interpretation of palaeoclimate and sea-level trends. The study focuses on time slices of late Albian–Cenomanian, Turonian–Coniacian and Santonian–Campanian intervals. The late Albian was characterized by the gradual disappearance of a meridional seaway and the opening of connections into the Tethys Ocean and parts of the Peri-Tethys seas during the Cenomanian. As a result, mainly carbonate sedimentation prevailed during middle Turonian–Santonian times, characterized by high global sea-level. A cold Boreal water influence can be discerned not only along the northern margin of the Eastern European Platform, but as far south as the Northern Caucasus during certain time intervals, particularly during the Campanian. The Western Siberia Boreal Basin also influenced the study area, giving evidence of cooler-water episodes through the Palaeo-Ural territory and the Turgai Seaway.

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Journal articles on the topic 'Coniacian-Santonian'

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