Han et al. (2018) publican un estudio sobre la morfología de la especie de conulárido Carinachites spinatus basado en un nuevo espécimen recolectado de la Formación Kuanchuanpu del Cámbrico inferior (China). [12]
Zhang et al. (2018) publicaron estudios sobre el desarrollo ontogenético de los primeros braquiópodos acrotretoides basados en especímenes bien conservados de las primeras especies cámbricas Eohadrotreta zhenbaensis y Eohadrotreta? zhujiahensis de la Formación Shuijingtuo ( China ). [37] [38]
García Joral, Baeza-Carratalá y Goy (2018) publican un estudio sobre el tamaño corporal de varias asociaciones de braquiópodos registradas en el intervalo de extinción anterior al recambio Toarciense , recolectadas en localidades representativas alrededor del Macizo Ibérico ( España y Portugal ). [40]
Nuevos taxones
Moluscos
Equinodermos
Conodontos
Investigación
Shirley et al. (2018) publicaron un estudio que prueba los modelos propuestos de crecimiento de elementos conodontes . [75]
Wheeley et al. (2018) publican un estudio que evalúa la variación de δ 18 O dentro de un conjunto de conodontes rico en especies del miembro Factory Cove del Ordovícico ( Floiano ) de la Formación Shallow Bay , Grupo Cow Head (oeste de Terranova, Canadá ), así como también evalúa las implicaciones de estos datos para determinar la paleotermometría de los océanos antiguos y los modelos ecológicos de conodontes. [ 77] [78] [79]
Zhang et al. (2018) publicaron un estudio sobre el tamaño corporal y la diversidad de conodontos del Carniano del sur de China y sus implicaciones para inferir los cambios bióticos y ambientales durante el evento pluvial del Carniano. [80]
Golding (2018) publicó un estudio que evalúa la similitud de las faunas de conodontes del Paleozoico tardío y el Triásico conocidas en Cache Creek Terrane ( Canadá ). [81]
Golding (2018) presenta la reconstrucción del aparato multielemental del conodonto del Triásico Medio de Columbia Británica (Canadá) perteneciente al grupo Neogondolella regalis dentro del género Neogondolella . [82]
La reconstrucción del número y disposición de elementos en el aparato de Hindeodus parvus publicada por Zhang et al. (2017) [83] es criticada por Agematsu, Golding y Orchard (2018); [84] Purnell et al. (2018) defienden sus conclusiones originales. [85]
Suttner, Kido y Briguglio (2018) describen un grupo de conodontos icriodóntidos pertenecientes a la especie Caudicriodus woschmidti , que aporta nueva información sobre la estructura del aparato de los conodontos icriodóntidos, a partir de sedimentos del Devónico inferior en el sur de Burgenland ( Austria ). [86]
Zimmerman, Johnson y Polly (2018) publican un estudio sobre las especies pertenecientes al género Neognathodus , en el que se evalúa si los grupos de morfotipos previamente definidos son fiables y distintos entre sí. [87]
Nuevos taxones
Pez
Anfibios
Reptiles
Sinápsidos
Sinápsidos no mamíferos
Investigación
Romano, Brocklehurst y Fröbisch (2018) publican una descripción del material postcraneal correspondiente a la especie de caseido Ennatosaurus tecton . [109]
Brocklehurst y Fröbisch (2018) publican un estudio sobre la anatomía y las relaciones filogenéticas de Milosaurus mccordi . [110]
Rey et al. (2018) publican un estudio sobre las composiciones de isótopos estables de oxígeno y carbono de la apatita dentinaria en los dientes de veintiocho especímenes de Diictodon feliceps y sobre sus implicaciones para inferir el papel potencial del clima en la extinción masiva de tetrápodos terrestres a finales del Capitaniano . [113 ]
Araújo et al. (2018) publican un estudio sobre la anatomía del laberinto óseo de los especímenes del género dicinodonte Endothiodon recolectados de la Formación Pérmica K5 ( Mozambique ), comparándolo con el género estrechamente relacionado Niassodon . [115]
Un estudio sobre la historia tafonómica de un yacimiento óseo monotípico compuesto por varios individuos atribuible al dicinodonte Dinodontosaurus recolectado en una localidad clásica del Triásico Medio en Brasil , y sobre sus implicaciones para inferir un posible comportamiento gregario en Dinodontosaurus , es publicado en línea por Ugalde et al. (2018). [116]
Angielczyk, Hancox y Nabavizadeh (2018) publican una redescripción del género de dicinodontes Sangusaurus y un estudio sobre su sistema de alimentación y relaciones filogenéticas. [117]
Kammerer, Angielczyk y Nesbitt (2018) describen una extremidad posterior parcial de un dicinodonte cercano al tamaño de Stahleckeria potens del Miembro Lifua Triásico de los Lechos Manda ( Tanzania ) , lo que representa el elemento postcraneal de dicinodonte más grande de los Lechos Manda informado hasta el momento. [118]
La descripción de restos vegetales y palinomorfos preservados en los coprolitos producidos por grandes dicinodontes de la Formación Chañares del Triásico ( Argentina ), y un estudio sobre sus implicancias para inferir la dieta de los dicinodontes, es publicado por Pérez Loinaze et al. (2018). [119]
Citton et al. (2018) describen huellas de tetrápodos, probablemente producidas por dicinodontes, de la Formación Vera del Triásico Superior del Grupo Los Menucos (Argentina). [120]
Racki y Lucas (2018) publican en línea un estudio sobre la edad del supuesto dicinodonte rético de Lipie Śląskie ( Polonia ) , quienes consideran más probable que este dicinodonte fuera de la edad noriana . [121]
Bendel et al. (2018) publicaron un estudio sobre la anatomía del cráneo de Cynariops robustus . [122]
La descripción de la morfología del cráneo de Cynosaurus suppostus y un estudio sobre las relaciones filogenéticas de la especie fueron publicados por van den Brandt y Abdala (2018). [124]
Wynd et al. (2018) describen por primera vez fósiles de Cynognathus crateronotus de la Formación Ntawere ( Zambia ) y los yacimientos Manda ( Tanzania ) del Triásico. [125]
Sidor y Hopson (2018) describen un cráneo parcial y un esqueleto postcraneal de un miembro de la especie Cricodon metabolus de la Formación Ntawere del Triásico ( Zambia ), y también estudian las relaciones filogenéticas de los miembros de la familia Trirachodontidae . [127]
Lai, Biewener y Pierce (2018) publicaron un estudio sobre la musculatura, la postura y el rango de movimiento de la extremidad anterior de Massetognathus pascuali . [128]
Un nuevo ejemplar de Trucidocynodon riograndensis , casi un 20% más grande que el ejemplar holotipo , fue descrito en la secuencia Carniana de Candelária (sur de Brasil ) por Stefanello et al. (2018). [129]
Pacheco et al. (2018) describen el dentario derecho con dientes de Prozostrodon brasiliensis del Triásico Tardío de Brasil , lo que representa el segundo espécimen conocido de esta especie. [130]
La descripción de la anatomía del esqueleto postcraneal de Prozostrodon brasiliensis fue publicada por Guignard, Martinelli y Soares (2018). [131]
Botha-Brink, Bento Soares y Martinelli (2018) publican un estudio sobre la histología de los huesos de las extremidades y las historias de vida de Prozostrodon brasiliensis , Irajatherium hernandezi , Brasilodon quadrangularis y Brasilitherium riograndensis . [132]
Marsola et al. (2018) describen dientes de cinodonte (que representan un brasilodonto y una forma similar a Riograndia ) encontrados en la localidad Triásica de Brasil, que también produjo los fósiles de Sacisaurus agudoensis . [136]
Lautenschlager et al. (2018) publicaron un estudio sobre la evolución de la mandíbula de los mamíferos y no encontraron evidencia de una reducción simultánea del estrés en la articulación de la mandíbula y un aumento de la fuerza de mordida en taxones clave no mamíferos en la transición cinodonte-mamífero. [137]
Jones et al. (2018) publicaron un estudio sobre la diversidad morfológica de las regiones vertebrales en sinápsidos no mamíferos y sobre su implicación para dilucidar la evolución de regiones anatómicamente distintas de las espinas de los mamíferos. [139]
LeBlanc et al. (2018) publicaron un estudio sobre la ontogenia de los dientes en una amplia gama de linajes de sinápsidos extintos , e interpretaron sus hallazgos como una indicación de que el sistema de unión de los dientes ligamentosos no es exclusivo de los mamíferos de la corona dentro de los sinápsidos. [140]
Nuevos taxones
Mamíferos
Otros animales
Investigación
Sperling y Stockey (2018) publican una revisión y síntesis de estudios sobre el contexto temporal y ambiental de eventos importantes en la evolución animal temprana. [151]
Un estudio sobre las relaciones filogenéticas de los rangeomorfos , dickinsoniomorfos y erniettomorfos según lo indicado por lo que se conoce de la ontogenia del rangeomorfo Charnia masoni , el dickinsoniomorfo Dickinsonia costata y el erniettomorfo Pteridinium simplex es publicado por Dunn, Liu & Donoghue (2018), quienes consideran al menos a los rangeomorfos y dickinsoniomorfos como metazoos . [152]
Dececchi et al. (2018) publican un estudio sobre las relaciones filogenéticas de los rangeomorfos . [153]
Reid, García-Bellido y Gehling (2018) publican un estudio sobre la distribución del tamaño y las características morfológicas de una población de ejemplares juveniles de Dickinsonia costata de la localidad fósil de Crisp Gorge en Flinders Ranges ( Australia ). [154]
Bobrovskiy et al. (2018) publican un estudio sobre las relaciones filogenéticas de Dickinsonia basado en datos de biomarcadores lipídicos extraídos de macrofósiles ediacáricos preservados orgánicamente , quienes interpretan sus hallazgos como una indicación de que Dickinsonia era un animal. [155]
Hoyal Cuthill y Han (2018) publican un estudio sobre la anatomía y las relaciones filogenéticas de Stromatoveris , basado en datos de nuevos especímenes del Chengjiang Konservat-Lagerstätte ( China ), quienes interpretan a Stromatoveris como un miembro del grupo animal temprano Petalonamae que también incluía a Arborea , Pambikalbae , rangeomorfos, dickinsoniomorfos y erniettomorfos. [156]
Chen et al. (2018) describen nuevos fósiles traza del Miembro Shibantan de Ediacara de la Formación Dengying superior ( China ), que incluyen madrigueras y posibles huellas que probablemente fueron hechas por animales de tamaño milimétrico con apéndices bilaterales . [159]
Laflamme, Gehling y Droser (2018) describen nuevos especímenes tridimensionales de Charniodiscus arboreus ( Arborea arborea ), que permiten una reinterpretación detallada de su morfología funcional y taxonomía, a partir del Miembro Ediacara, Cuarcita Rawnsley de Australia del Sur . [161]
Mehra y Maloof (2018) presentan reconstrucciones 3D de agregados de Cloudina . [162]
Wood y Penny (2018) publicaron un estudio sobre la dinámica de crecimiento del sustrato, el modo de biomineralización y las posibles afinidades de Namapoikia rietoogensis . [164]
Gold (2018) publica una revisión de la evidencia de la existencia de animales nadadores durante el Neoproterozoico . [165]
Yin et al. (2018) publican un estudio sobre la naturaleza y la afinidad biológica del taxón cámbrico Archaeooides , quienes interpretan los fósiles de Archaeooides como restos embrionarios de animales. [168]
Zumberge et al. (2018) informan sobre un nuevo biomarcador de esterano fósil , que posee un esqueleto de hidrocarburo raro que se encuentra únicamente en taxones de demosponjas existentes , de rocas sedimentarias y aceites del Neoproterozoico tardío - Cámbrico , e interpretan este hallazgo como una indicación de que las demosponjas, y por lo tanto los animales multicelulares, fueron prominentes en algunos entornos marinos del Neoproterozoico tardío al menos hasta el período Criogénico . [169]
Botting et al. (2018) informan de fósiles de esponjas diversos y abundantes del intervalo límite Ordovícico-Silúrico en siete localidades del sur de China, y elaboran un modelo para la distribución y preservación de la fauna de esponjas. [170]
Skovsted y Topper (2018) publican la descripción de nuevas características morfológicas de la mobergellana cámbrica Discinella micans . [173]
Zhao et al. publican un estudio sobre las interrelaciones entre el eldonioide Pararotadiscus guizhouensis y los taxones fósiles asociados de Kaili Biota . (2018). [174]
Chambers & Brandt (2018) publican un estudio sobre la placa con una densa agregación de miembros de la especie Banffia constricta recuperada de Burgess Shale ( Canadá ) del Cámbrico y sus implicaciones para los hábitos de vida del animal. [175]
Li et al. (2018) publicaron un estudio sobre la morfología y las afinidades filogenéticas de Yuyuanozoon magnificissimi , basado en nuevos especímenes. [176]
Crampton et al . (2018) publican un estudio sobre el impacto de los ciclos astronómicos de largo período (los "grandes ciclos" de Milankovitch) asociados con la excentricidad y oblicuidad orbital de la Tierra en la varianza de la probabilidad de recambio de especies ( probabilidad de extinción más probabilidad de especiación ) en graptoloideos del Paleozoico Temprano . [178]
Hu et al. (2018) publican una redescripción de la especie Malongitubus kuangshanensis del Cámbrico Chengjiang Lagerstätte ( China ) , quienes interpretan este taxón como un pterobranquio . [179]
Pan et al. (2018) informan de la primera aparición de la especie de tommotiid Paterimitra Pyramidalis de la Formación Xinji ( China ). [181]
Zhuravlev y Wood (2018) publican un estudio sobre la distribución temporal de las especies esqueléticas de lofotrocozoos desde el Ediacárico superior hasta el Miaolingiano basal de la Plataforma Siberiana , y sobre sus implicaciones para la comprensión de la dinámica evolutiva de la explosión cámbrica . [182]
Un estudio que reinterpreta al supuesto lobopodiano cámbrico Mureropodia apae como un apéndice aislado parcial de un miembro del género Caryosyntrips , publicado por Pates & Daley (2017) [184] es criticado por Gámez Vintaned & Zhuravlev (2018); [185] Pates, Daley & Ortega-Hernández (2018) defienden sus conclusiones originales. [186]
Liu et al. (2018) describen un ejemplar juvenil de Lyrarapax unguispinus , que aporta nueva información sobre los apéndices frontales y el modo de alimentación de este taxón, de la Formación Chiungchussu del Cámbrico ( China ). [189]
Sheppard, Rival y Caron (2018) publicaron un estudio que evalúa la probable eficiencia de natación y maniobrabilidad de Anomalocaris canadensis . [190]
El animal cámbrico Pahvantia hastata de Wheeler Shale ( Utah , Estados Unidos ), originalmente clasificado como un posible artrópodo, [191] es reinterpretado como un radiodonte que se alimenta por suspensión por Lerosey-Aubril y Pates (2018). [192]
La presencia de divertículos metaméricos del intestino medio es reportada por primera vez en el artrópodo del tallo Fuxianhuia protensa por Ortega-Hernández et al. (2018), quienes interpretan su hallazgo como indicativo de una ecología depredadora o carroñera de los fuxianhuiidos. [193]
Liu et al. (2018) reinterpretan los supuestos restos de los sistemas nervioso y cardiovascular en numerosos individuos articulados de Fuxianhuia protensa como más probablemente biopelículas microbianas que se desarrollaron después de la descomposición del intestino, los músculos y otros tejidos conectivos. [194]
Fu et al. (2018) publicaron un estudio sobre el desarrollo postembrionario de Fuxianhuia protensa [195] .
Chen et al. (2018) publican la redescripción del fuxianhuido Liangwangshania biloba [196] .
Cobain et al. (2018) informan de evidencia de macrofauna que vive a profundidades de hasta 8 metros bajo el lecho marino en la Formación Pérmica Fort Brown ( Cuenca Karoo , Sudáfrica ). [199]
Sun et al. (2018) publican un estudio sobre las estrategias de alimentación y locomoción de los hiolítidos cámbricos, basado en especímenes conservados en coprolitos de la biota de Chengjiang y asociados con un cadáver de Tuzoia de la fauna de Balang ( China ). [201]
Berg-Madsen, Valent y Ebbestad (2018) describen el tracto digestivo de un espécimen de la especie hiolítica Circotheca johnstrupi de la Formación Læså del Cámbrico ( Bornholm , Dinamarca ). [202]
Feng et al. (2018) publican un estudio sobre madrigueras de sucesiones del Triásico Inferior-Medio en el sur de China asignadas al icnotaxón Rhizocorallium y sobre sus implicaciones para inferir el curso de la recuperación biótica después del evento de extinción del Pérmico-Triásico . [207]
O'Dea et al. (2018) publicaron un estudio que evalúa cómo respondieron diferentes especies de briozoos cupuládridos fósiles y actuales de vida libre a los cambios ambientales en el suroeste del Caribe durante los últimos 6 millones de años. [208]
A wide variety of morphological abnormalities in planktic foraminiferal tests from the earliest Danian, mainly from Tunisian sections, is described by Arenillas, Arz & Gilabert (2018).[263]
A study on the impact of the climatic and environmental perturbation on the morphology of foraminifera living during the Paleocene–Eocene Thermal Maximum is published by Schmidt et al. (2018).[264]
Taxonomic compilation and partial revision of early Eocene deep-sea benthic Foraminifera is presented by Arreguín-Rodríguez et al. (2018).[265]
A study on the responses of two species of foraminifera (extant Truncorotalia crassaformis and extinct Globoconella puncticulata) to climate change during the late Pliocene to earliest Pleistocene intensification of Northern Hemisphere glaciation (3.6–2.4 million years ago) is published by Brombacher et al. (2018).[266]
New taxa
Other organisms
Research
A study on putative stromatolites described from the 3,700-Myr-old rocks from the Isua supracrustal belt (Greenland) by Nutman et al. (2016)[298] is published by Allwood et al. (2018), who interpret these putative stromatolites as more likely to be structures of non-biological origin.[299]
Carbon isotope analyses of 11 microbial fossils from the ~3,465-million-year-old Apex chert (Australia) are published by Schopf et al. (2018), who interpret two of the five studied species as primitive photosynthesizers, one as an Archaealmethane producer, and two as methane consumers.[300]
The oldest well-preserved microbial mats fabrics are described from the ≈3,472-million-year-old Middle Marker horizon, Barberton Greenstone Belt (South Africa) by Hickman-Lewis et al. (2018).[301]
Direct fossil evidence for life on land 3,220 million years ago in the form of terrestrial microbial mats is reported from the Moodies Group (South Africa) by Homann et al. (2018).[302]
Microfossils representing 18 morphotypes are reported from the c. 2.4 billion years old Turee Creek Group (Western Australia) by Barlow & Van Kranendonk (2018).[303]
Ten representative types of exceptionally well-preserved mat-related structures, interpreted as likely to be of biological origin and including putative microbial mats and discoidal microbial colonies, are reported from the 2.1-billion-year-old Francevillian series in Gabon by Aubineau et al. (2018).[304]
A study on the chemical, isotopic and molecular structural characteristics of the putative multicellulareukaryote fossils from carbonaceous compressions in the 1.63 billion years old Tuanshanzi Formation (China) is published by Qu et al. (2018).[305]
Intact porphyrins, the molecular fossils of chlorophylls, are described from 1,100-million-year-old marine black shales of the Taoudeni Basin (Mauritania) by Gueneli et al. (2018), who also study the nitrogen isotopic values of the fossil pigments, and interpret their findings as indicating that the oceans of that time were dominated by cyanobacteria, while larger planktonicalgae were scarce.[306]
A study on the evolutionary history of bacteria is published by Louca et al. (2018), who interpret their findings as indicating that most bacterial lineages ever to have inhabited Earth are extinct.[307]
Bobrovskiy et al. (2018) report molecular fossils from organically preserved specimens of Beltanelliformis, and interpret the fossils as representing large spherical colonies of cyanobacteria.[308]
Discoid imprints sampled from the Precambrian terranes of central Dobruja (Romania) are described and assigned to the species Beltanelliformis brunsae by Saint Martin & Saint Martin (2018).[309]
A study on the age of the fossil red algaBangiomorpha pubescens is published by Gibson et al. (2018).[310]
A reassessment of the anatomy and taxonomy of Orbisiana, based on a restudy of the rediscovered original type material of O. simplex, is published by Kolesnikov et al. (2018).[311]
A study on the positions of fossil specimens in the assemblages of Ediacaran fossils from Mistaken Point (Canada), as well as on their implications for inferring the interactions and associations between the Ediacaran organisms, is published by Mitchell & Butterfield (2018).[312]
A study on the height of Ediacaran organisms from Mistaken Point, evaluating the link between the increase of height and resource competition or greater offspring dispersal, is published by Mitchell & Kenchington (2018).[313]
Evidence of a radiation of the Ediacaran biota that witnessed the emergence and widespread implementation of novel, animal-style ecologies is presented by Tarhan et al. (2018), who argue that this transition was linked to the expansion of Ediacaran taxa into dynamic, shallow marine environments characterized by episodic disturbance and complex and diverse organically-bound substrates, and propose that younger, second-wave Ediacaran communities resulting from said radiation were part of an ecological and evolutionary continuum with Phanerozoic ecosystems.[314]
A study on the size range, ontogeny and palaeoenvironment of Rugoconites is published by Hall, Droser & Gehling (2018).[315]
Elliptical body fossils are described from the Ediacaran–Fortunian deposits of central Brittany (France) by Néraudeau et al. (2018), representing the first body fossils described from these deposits.[316]
A study on the sandstone- and limestone-hosted occurrences of Palaeopascichnus linearis (including material from a new locality in Arctic Siberia), indicative of a greater range of taxonomic and taphonomic variation, is published by Kolesnikov et al. (2018).[317]
A study on the organic-walled microfossils from the Cambrian strata in the stratotype section of the Precambrian–Cambrian boundary in the Burin Peninsula (Canada) is published by Palacios et al. (2018).[318]
Description of fossils of nonmarine diatoms belonging to the genus Actinocyclus from the Lower to Middle Miocene lacustrine deposits in Japan and a study on the possible causal links between the evolution of nonmarine planktonic diatoms and the climatic and environmental changes that occurred during the Miocene is published by Hayashi et al. (2018).[321]
A study on the cell-size frequency distributions across calcareous nanoplankton communities through the Paleocene–Eocene Thermal Maximum, on their population biomass and on the impact of climate change on their cellular characteristics is published by Gibbs et al. (2018).[322]
New taxa
History of life in general
Research related to paleontology that concerns multiple groups of the organisms listed above.
A study on the history of life on Earth is published by McMahon & Parnell (2018), who argue that the subsurface "deep biosphere" outweighed the surface biosphere by about one order of magnitude for at least half of the history of life.[344]
A timescale of life on Earth, based on a reappraisal of the fossil material and new molecular clock analyses, is presented by Betts et al. (2018).[345]
A study on functional shifts in modern phototrophicmicrobial mats across redox gradients, and on its implications for inferring the metabolic transitions experienced during the Great Oxygenation Event, is published by Gutiérrez-Preciado et al. (2018).[346]
A study on living cyanobacteria, testing the hypothesis that planktonicsingle-celled cyanobacteria could drive the export of organic carbon from the surface to deep ocean in the Paleoproterozoic, is published by Kamennaya et al. (2018).[347]
A study on the abundance of bio-essential trace elements during the period in Earth's history known as the "Boring Billion" is published by Mukherjee et al. (2018), who interpret their findings as indicating that key biological innovations in eukaryote evolution (the appearance of first eukaryotes, the acquisition of certain cell organelles, the origin of multicellularity and the origin of sexual reproduction) probably occurred during the period of a scarcity of trace elements, followed by a broad-scale diversification of eukaryotes during the period of a relative abundance of trace elements.[348]
A study on the eukaryotic species richness during Tonian and Cryogenian is published by Riedman & Sadler (2018).[349]
A study on the Ediacaran ecosystem complexity is published by Darroch, Laflamme & Wagner (2018), who report evidence of the Ediacara biota forming complex-type communities throughout much of their stratigraphic range, and thus likely comprising species that competed for different resources and/or created niche for others.[350]
A study evaluating how temperature can govern oxygen supply to animals at oceanographic scales, as well as how temperature dynamically affects the absolute tolerance of partial pressure of oxygen in marine ectotherms, and re-examining bathymetric patterns within the Ediacaran fossil record in an ecophysiological context, is published by Boag et al. (2018).[351]
A study investigating possible water columnredox controls on the distribution and growth of the oldest animal communities, based on data from the Ediacaran Nama Group (Namibia), is published by Wood et al. (2018).[352]
A study on the duration of the faunal transition from Ediacaran to Cambrian biota, as indicated by data from a composite section in Namibia, is published online by Linnemann et al. (2018).[353]
A study on the evolution of the diversity of animal body plans, based on data from extant and Cambrian animals, is published by Deline et al. (2018).[354]
A review of the evidence for shell crushing (durophagy), drilling and puncturing predation in the Cambrian (and possibly the Ediacaran) is published by Bicknell & Paterson (2018).[355]
A study on the timing and process of ocean oxygenation in the early Cambrian and its impact on the diversification of early Cambrian animals, based on data from the Cambrian Niutitang Formation (China), is published by Zhao et al. (2018).[356]
A study on the evolution of marine animal communities over the Phanerozoic, evaluating the ecological changes caused by major radiations and mass extinctions, is published by Muscente et al. (2018).[357]
A study evaluating whether rapid warming preferentially increased the extinction risk of tropical marine fossil taxa throughout the Phanerozoic is published online by Reddin, Kocsis & Kiessling (2018).[358]
A study on the impact of mass extinctions on the global biogeographical structure, as indicated by data on time-traceable bioregions for benthic marine species across the Phanerozoic, is published by Kocsis, Reddin & Kiessling (2018).[359]
A study on the nektic and eunektic diversity and occurrences throughout the Paleozoic is published by Whalen & Briggs (2018).[360]
A study analyzing the link between net latitudinal range shifts of marine invertebrates and seawater temperature over the (post-Cambrian) Phanerozoic Eon is published by Reddin, Kocsis & Kiessling (2018).[361]
A study on within-habitat, between-habitat, and overall diversity of benthic marine invertebrates (gastropods, bivalves, trilobites, brachiopods and echinoderms) from Phanerozoic geological formations is published online by Hofmann, Tietje & Aberhan (2018).[362]
A study evaluating the link between macroevolutionary success (evolving many species) and macroecological success (the occupation of an unusually high number of areas by a species or clade) in fossil echinoid, cephalopod, bivalve, gastropod, brachiopod and trilobite species is published by Wagner, Plotnick & Lyons (2018).[363]
A study comparing the extinction events which occurred at the end of the Ordovician and at the end of the Capitanian (middle Permian) is published by Isozaki & Servais (2018).[364]
Vertebrate fossil fauna from the Tournaisian-age Ballagan Formation exposed on the beach at Burnmouth (Scotland) is described by Otoo et al. (2018).[366]
A study on the patterns of dispersal and vicariance of tetrapods across Pangaea during the Carboniferous and Permian is published by Brocklehurst et al. (2018).[368]
O'Connor et al. (2018) reconstruct the most likely karyotype of the diapsidcommon ancestor based on data from extant reptiles and birds, and argue that most features of a typical 'avian-like' karyotype were in place before the divergence of birds and turtles ≈255 million years ago.[369]
A study evaluating whether the fossil record supports the reality of the Permian Olson's Extinction, based on an analysis of the tetrapod species richness in the tetrapod-bearing formations of Texas preserving fossils from the time of the extinction, is published by Brocklehurst (2018).[370]
A study on the patterns of species richness, origination rates and extinction rates of the mid-Permian tetrapods from South Africa is published by Day et al. (2018).[371]
A study on the changes of distribution of terrestrial tetrapods from the Permian (Guadalupian) to the Middle Triassic and on the impact of the Permian–Triassic extinction event on the palaeobiogeography of terrestrial tetrapods is published by Bernardi, Petti & Benton (2018).[372]
A study on the causes of biotic extinction during the Guadalupian-Lopingian transition is published online by Huang et al. (2018).[373]
A study on the composition and biotic interactions in terrestrial paleocommunities from the Karoo Basin (South Africa) spanning the Permian-Triassic mass extinction is published online by Roopnarine et al. (2018), who propose a new hypothesis to explain the persistence of biotic assemblages and their reorganization or destruction.[374]
A study on the biogeographic patterns and severity of extinction of marine taxa during the Permian–Triassic extinction event, evaluating whether global warming and ocean oxygen loss can mechanistically account for the marine mass extinction, is published by Penn et al. (2018).[375]
A study on changes in the structure of phytoplankton communities in South China during the Permian-Triassic transition is published online by Lei et al. (2018).[376]
A study on the recovery of benthic invertebrates following the Permian–Triassic extinction event, based on analysis of changes in the species richness, functional richness, evenness, composition, and ecological complexity of benthic marine communities from the Lower Triassic Servino Formation (Italy), is published by Foster et al. (2018).[377]
Description of an Early Triassic marine fauna from the Ad Daffah conglomerate in eastern Oman, and on its implications for inferring the ecology and diversity during the early aftermath of the Permian–Triassic extinction event, is published online by Brosse et al. (2018).[378]
A study on microbial mounds from the Lower Triassic Feixianguan Formation (China), and their implications for inferring the course of biotic recovery after the Permian–Triassic extinction event, is published by Duan et al. (2018).[379]
A study on the timing and pattern of ecosystem succession during and after the Permian–Triassic extinction event for the duration of the entire Triassic, as indicated by the changing diversity among non-motile, motile and nektonic animals, is published by Song, Wignall & Dunhill (2018).[380]
Marine faunas characterized by unusually high levels of both benthic and nektonic taxonomic richness are described from two Early Triassic sections from South China by Dai et al. (2018).[381]
A study on the historical shifts in geographical ranges and climatic niches of terrestrial vertebrates (both endotherms and ectotherms) based on data from extant and fossil vertebrates is published by Rolland et al. (2018).[382]
A study on the stratigraphic distribution of the marine vertebrate fossils of the Xingyi Fauna from the Middle Triassic Falang Formation (China) is published by Lu et al. (2018), who interpret their findings as indicating that the Xingyi Fauna comprises two distinct vertebrate assemblages, resulting from a major faunal change, which was probably caused by a turnover of their ecological setting from nearshore to offshore.[383]
A study on the patterns of diversity change and extinction selectivity in marine ecosystems during the Triassic–Jurassic interval, especially in relation to the Triassic–Jurassic extinction event, is published by Dunhill et al. (2018).[384]
A study on the extinction selectivity of marine organisms through the Late Triassic and Early Jurassic, evaluating whether there are any substantial differences between the hyperthermal events during the Triassic–Jurassic extinction event and Toarcian turnover and the periods of normal background extinction, is published by Dunhill et al. (2018).[385]
A study on the morphological, ecological and behavioural traits linked to the evolution of tail weaponization in extant and fossil amniotes is published by Arbour & Zanno (2018).[387]
A study on the factors which led to the colonization of marine environments in the evolution of amniotes is published by Vermeij & Motani (2018).[388]
A review of marine reptile (plesiosaur, ichthyosaur and thalattosuchian) fossils from the Oxfordian sedimentary rocks in Great Britain (United Kingdom), focusing on the Corallian Group, is published by Foffa, Young & Brusatte (2018), who report evidence of a severe reduction in observed marine reptile diversity during the Oxfordian.[389]
A study evaluating how the structure of marine reptile ecosystems and their ecologies changed over the roughly 18-million-year history of the Jurassic Sub-Boreal Seaway of the United Kingdom, as indicated by data from fossil teeth, is published by Foffa et al. (2018).[390]
A diverse and ecologically informative faunal assemblage is described from the Lower Cretaceous Arundel Clay facies (Maryland, United States) by Frederickson, Lipka & Cifelli (2018).[391]
Description of an assemblage of Early Cretaceous (Barremian) coprolites from the Las Hoyas Konservat-Lagerstätte (Spain) and a study on their biological and environmental affinities is published by Barrios-de Pedro et al. (2018).[392]
A study on the taphonomic properties of the inclusions contained in the Las Hoyas coprolites, and their implications for inferring the patterns of digestive processes of the producers of these coprolites, is published by Barrios-de Pedro & Buscalioni (2018).[393]
Description of isocrinidcrinoids belonging to the genus Isocrinus from the Cretaceous amber from Myanmar is published by Mao et al. (2018), who also report coral columnals and oysters from the amber from Myanmar, and evaluate the age of this amber.[394]
A study on the taxonomic composition of the early Late Cretaceous fauna from the Cliffs of Insanity microvertebrate locality (Mussentuchit Member, Cedar Mountain Formation; Utah, United States) is published by Avrahami et al. (2018).[395]
Fossil assemblage including plant and vertebrate remains is described from the Turonian Ferron Sandstone Member of the Mancos Shale Formation (Utah, United States) by Jud et al. (2018), who report turtle and crocodilian remains and an ornithopodsacrum, as well as a large silicified log assigned to the genus Paraphyllanthoxylon, representing the largest known pre-Campanianflowering plant reported so far and the earliest documented occurrence of an angiosperm tree more than 1.0 m in diameter.[396]
A study comparing the ecological similarity of Cretaceous cold seep assemblages preserved in the Pierre Shale surrounding the Black Hills and modern cold-seep assemblages is published online by Laird & Belanger (2018).[397]
A record of foraminifera, calcareous nannoplankton, trace fossils and elemental abundance data from within the Chicxulub crater, dated to approximately the first 200,000 years of the Paleocene, is presented by Lowery et al. (2018), who report evidence indicating that life reappeared in the basin just years after the Chicxulub impact and a high-productivity ecosystem was established within 30,000 years.[398]
Vertebrate pathogens found associated with fossil hematophagous arthropods in Dominican, Mexican, Baltic, Canadian and Burmese amber are reported by Poinar (2018).[399]
Grimaldiet al. (2018) report biological inclusions (fungi, plants, arachnids and insects) in amber from the PaleogeneChickaloon Formation of Alaska, representing the northernmost deposit of fossiliferous amber from the Cenozoic.[400]
A synthesis of studies on the evolution of the cold-water coastal North Pacific biota over the last 36 million years, its origins and its influences on other temperate regions, is presented by Vermeijet al. (2018).[401]
A review of Neogene–Quaternary terrestrial vertebrate sites from the Middle Kura Basin (eastern Georgia and western Azerbaijan) is published by Bukhsianidze & Koiava (2018).[402]
A study on the reptile and amphibian fossils from the early Pleistocene site of the Russel-Tiglia-Egypte pit near Tegelen (Netherlands) is published by Villa et al. (2018).[403]
A study on the structure of the animal community known from the Okote Member of the Koobi Fora Formation at East Turkana (Kenya) as indicated by tracks and skeletal assemblages, and on the interactions of Homo erectus with environment and associated faunas from this site, is published by Roach et al. (2018).[404]
A revision of Middle Pleistocene faunal record from archeological sites in Africa, and a study on its implications for inferring potential links between hominin subsistence behavior and the Early Stone Age/Middle Stone Age technological turnover, is published online by Smith et al. (2018).[405]
Evidence of bird and carnivore exploitation by Neanderthals (cut-marks in golden eagle, raven, wolf and lynx remains) is reported from the Axlor site (Spain) by Gómez-Olivencia et al. (2018).[406]
A study on the compositions of the faunal and stone artifact assemblages at Liang Bua (Flores, Indonesia), aiming to determine the last appearance dates of Stegodon, giant marabou stork, Old World vulture belonging to the genus Trigonoceps, and Komodo dragon at the Liang Bua site, and to determine what raw materials were preferred by hominins from this site ~50,000–13,000 years ago and whether these are preferences were similar to those seen in the stone artifact assemblages attributed to Homo floresiensis or to those attributed to modern humans, is published by Sutikna et al. (2018).[407]
A study on the fossil Sporormiella, pollen and microscopic particles of charcoal recovered from sediments of Lake Mares and Lake Olhos d'Agua (Brazil) which spanned the time of megafaunal extinction and human arrival in southeastern Brazil, and on their implications for inferring the timing of the decline of local megafauna and its ecological implications, is published by Raczka, Bush & De Oliveira (2018).[408]
A study evaluating whether the occurrence and decline of spores of Sporormiella in sediments is a good proxy for the occurrence and extinction of megaherbivores, as indicated by data from Cuddie Springs in south-eastern Australia, is published by Dodson & Field (2018).[409]
A study evaluating how mega-herbivore animal species controlled plant community composition and nutrient cycling, relative to other factors during and after the Late Quaternary extinction event in Great Britain and Ireland, is published by Jeffers et al. (2018).[410]
A study on the impact of the late Quaternary extinction of megafauna on the megafauna-deprived ecosystems is published by Galetti et al. (2018).[411]
A study on the possible impact of the end of the millennial-scale climate fluctuations characteristic of the ice age (and the beginning of the more stable climate regime of the Holocene approximately 11,700 years ago) on the Late Quaternary megafaunal extinctions is published online by Mann et al. (2018).[412]
A study on the past biodiversity, population dynamics, extinction processes, and the impact of subsistence practices on the vertebrate fauna of New Zealand, based on analysis of bone fragments from archaeological and paleontological sites covering the last 20,000 years of New Zealand's past, is published by Seersholm et al. (2018).[413]
A study on changes in plant pathogen communities (fungi and oomycetes) in response to changing climate during late Quaternary, as indicated by data from solidified deposits of rodent coprolites and nesting material from the central Atacama Desert spanning the last ca. 49,000 years, is published by Wood et al. (2018).[414]
A study on the parsimony and Bayesian-derived phylogenies of fossil tetrapods, evaluating which of them are in closer agreement with stratigraphic range data, is published by Sansom et al. (2018).[415]
A study aiming to infer the causes of differences between estimates of speciation and extinction rates based on molecular phylogenies and those based on fossil record is published by Silvestro et al. (2018), who provide simple mathematical formulae linking the diversification rates inferred from fossils and phylogenies.[416]
A review of extinction theory and the fossil record of terrestrial diversity crises, comparing past diversity crises of terrestrial vertebrate faunas with the ongoing Holocene extinction, is published by Padian (2018).[417]
A new metric, which can be used to quantify the term "living fossil" and determine which organisms can be reasonably referred to as such, is proposed by Bennett, Sutton & Turvey (2018).[418]
A novel non-invasive and label-free tomographic approach to reconstruct the three-dimensional architecture of microfossils based on stimulated Raman scattering is presented by Golreihan et al. (2018).[419]
A study on melanosomes preserved in the integument and internal organs of extant and fossil frog specimens, evaluating their implications for inferring colours of extinct animals on the basis of melanosomes preserved in fossil specimens, is published by McNamara et al. (2018).[421]
A study on fossil vertebrate tissues and experimentally matured modern samples, aiming to the mechanism of soft tissue preservation and the environments that favor it, is published by Wiemann et al. (2018).[422]
A mechanistic model that simulates the history of life on the South American continent, driven by modeled climates of the past 800,000 years, is presented by Rangel et al. (2018).[423]
A study on temporal trends in biogeography and body size evolution of Australian vertebrates is published by Brennan & Keogh (2018), who interpret their findings as indicating that gradual Miocene cooling and aridification of Australia correlated with the restricted phenotypic diversification of multiple ecologically diverse vertebrate groups.[424]
A study evaluating how faithfully stratigraphic ranges of extant Adriatic molluscs are recorded in a series of cores drilled through alluvial, coastal and shallow-marine strata of the Po Plain (Italy) is published by Nawrot et al. (2018), who also evaluate the implications of their study for interpretations of the timing, duration and ecological selectivity of mass extinction events in general.[425]
A study on the evolution of morphological disparity (i.e. diversity of anatomical types), as indicated by data from 257 published character matrices of fossil taxa, is published by Wagner (2018).[426]
A study on the evolution of functional and ecological innovations in temperate marine multicellular organisms inhabiting North Pacific during and after the Late Eocene is published by Vermeij (2018).[427]
A method for dividing a paleontological dataset into bioregions is proposed by Brocklehurst & Fröbisch (2018), who apply the proposed method to a study of beta diversity of Paleozoictetrapods.[428]
A study aiming to estimate the magnitude and potential significance of palaeontological data from specimens housed in museum collections but not described in published literature is published by Marshall et al. (2018).[429]
Sallan et al. (2018) traced the cradle of evolutionary origins and diversification of fish from the mid-Paleozoic era in nearshore environments.[430]
Smith et al. (2018) examined the teeth of Neanderthal children who lived 250,000 years ago in France, in order to comprehend their nursing duration, and the effect of lead exposure and severe winters on them.[432]
Wiemann et al. (2018) studied dinosaur's egg colour evolution, in order to unravel whether modern birds inherited egg colour from their non-avian dinosaur ancestors.[433]
Trace fossils
A study on the Devonian strata in the Zachełmie Quarry (Poland) preserving tracks of early tetrapods is published by Qvarnström et al. (2018), who reinterpret the tracks as produced in non-marine environment.[434]
First tetrapod tracks from the Upper Permian–Lower Triassic (Lopingian–Induan) eolian strata of the Paraná Basin, southern Brazil, assigned to the ichnotaxa Dicynodontipus isp. and Chelichnus bucklandi, are described by Francischini et al. (2018).[435]
A study testing the hypothesis that chemodenitrification, the rapid reduction of nitric oxide by ferrous iron, would have enhanced the flux of nitrous oxide from Proterozoic seas, leading to nitrous oxide becoming an important constituent of Earth's atmosphere during Proterozoic and possibly life's primary terminal electron acceptor during the transition from an anoxic to oxic surface Earth, is published by Stanton et al. (2018).[437]
A study on the iron mineralogy of the 1.1-billion-year-old Paleolake Nonesuch (Nonesuch Formation), and on its implications for inferring whether the waters of this lake were oxygenated, is published by Slotznick, Swanson-Hysell & Sperling (2018).[438]
A study on the Earth's atmosphere and the productivity of global biosphere 1.4 billion years ago, based on triple oxygen isotope measurements sedimentary sulfates from the Sibley basin (Ontario, Canada), is published by Crockford et al. (2018).[439]
A study on the isotopically enriched chromium in Mesoproterozoic-aged shales from the Shennongjia Group (China) dating back to 1.35 billion years ago is published by Canfieldet al. (2018), who interpret their findings as document elevated atmospheric oxygen levels through most of Mesoproterozoic Era, likely sufficient for early crown group animal respiration, but attained over 400 million years before they evolved.[440]
A study on the rate of biotic oxygen production and the attendant large-scale biogeochemistry of the mid-Proterozoic Earth system is published online by Ozaki, Reinhard & Tajika (2018).[441]
A study on the causes of formation and on global extent of the Great Unconformity is published online by Keller et al. (2018), who interpret their findings as indicating that this unconformity may record rapid erosion during Neoproterozoic "Snowball Earth" glaciations, and that environmental and geochemical changes which led to the diversification of multicellular animals may be a direct consequence of Neoproterozoic glaciation.[443]
A study on the environments and food sources that sustained the Ediacaran biota is published by Pehr et al. (2018), who present the lipid biomarker and nitrogen and carbon isotopic data obtained from late Ediacaran (<560 million years old) strata from seven drill cores and three outcrops spanning Baltica.[444]
Gougeon et al. (2018) report evidence from the Lower Cambrian Chapel Island Formation (Canada) indicating that a mixed layer of sediment, of similar structure to that of modern marine sediments (which results from bioturbation by epifaunal and shallow infaunal organisms), was well established in shallow marine settings by the early Cambrian.[445]
A study on the effects of the rise of bioturbation on global elemental cycles during the Cambrian is published by van de Velde et al. (2018).[446]
A review of the history of the definition of the Great Ordovician Biodiversification Event, aiming to clarify its concept and duration, is published by Servais & Harper (2018).[447]
Evidence of multiple mercury enrichments in the two-step late Frasnian crisis interval from paleogeographically distant successions in Morocco, Germany and northern Russia is presented by Racki et al. (2018), who interpret their findings as indicating that the Late Devonian extinction was caused by rapid climatic perturbations promoted in turn by volcanic cataclysm.[449]
A study on the sedimentary facies, oxygen isotopes and the generic conodont composition in two continuous Devonian (late Frasnian to the end-Famennian) outcrops in the Montagne Noire (Col des Tribes section, France, part of the Armorica microcontinent in the Devonian) and in the Buschteich section (Germany, part of the Saxo-Thuringian microplate in the Devonian), assessing the water depth, approximate position relative to the shore and paleotemperatures in the Late Devonian, and evaluating whether environmental changes affected both areas similarly and at the same pace in the Late Devonian, is published online by Girard et al. (2018).[450]
A study on the onset and paleoenvironmental transitions associated with the Hangenberg Crisis within the Cleveland Shale member of the Ohio Shale is published online by Martinez et al. (2018).[451]
A study on the age of a bentonite layer from Bed 36 in the Frasnian–Famennian succession at the abandoned Steinbruch Schmidt Quarry (Germany), aiming to determine the precise age of the Frasnian–Famennian boundary and the precise timing of the Late Devonian extinction, is published by Percival et al. (2018).[452]
A study on the environmental changes and faunal turnover in the Karoo Basin (South Africa) during the late Permian is published by Viglietti, Smith & Rubidge (2018).[453]
A study on carbonate microfacies and foraminifer abundances in three Upper Permian sections from isolated carbonate platforms of the Nanpanjiang Basin (China), indicative of a marine environmental instability up to 60,000 years preceding Permian–Triassic extinction event, is published online by Tian et al. (2018).[454]
A study on the halogen compositions of Siberian rocks emplaced before and after the eruption of the Siberian flood basalts during the Permian–Triassic extinction event, and on its implications for inferring the source and nature of volatiles in the Siberian large igneous province, is published by Broadley et al. (2018).[455]
Evidence of enhanced continental chemical weathering at the Permian–Triassic boundary is reported from bulk rock samples from the Meishan section in South China by Sun et al. (2018), who also evaluate the potential impact of this enhanced weathering on global climate changes when the end-Permian extinction occurred.[456]
A study on the U-Pb geochronology, biostratigraphy and chemostratigraphy of a highly expanded section at Penglaitan (Guangxi, China) is published online by Shen et al. (2018), who interpret their findings as indicative of a sudden end-Permian mass extinction that occurred at 251.939 ± 0.031 million years ago.[457]
Evidence of sill intrusions which were likely cause of the Triassic–Jurassic extinction event is reported from the Amazonas and Solimões Basins (Brazil) by Heimdal et al. (2018).[460]
A study on the palaeoenvironmental conditions that existed during the time the Upper CretaceousWinton Formation (Australia) was deposited is published by Fletcher, Moss & Salisbury (2018).[461]
A study on the geology, age and palaeoenvironment of the main fossil-bearing beds of the Cretaceous Griman Creek Formation (New South Wales, Australia) is published online by Bell et al. (2018).[463]
A study on the nature of the fluvial systems of Laramidia during the Late Cretaceous, as indicated by data from vertebrate and invertebrate fossils from the Kaiparowits Formation of southern Utah, and on the behavior of dinosaurs over these landscapes, is published online by Crystal et al. (2018).[464]
A study on the rainfall seasonality and freshwater discharge on the Indian subcontinent in the Late Cretaceous (Maastrichtian), based on data from specimens of the mollusc species Phygraea (Phygraea) vesicularis from the Kallankuruchchi Formation (India), is published by Ghosh et al. (2018).[465]
A study on the oxygen isotopic composition of fish debris from the Global Boundary Stratotype Section and Point for the Cretaceous/Paleogene boundary at El Kef (Tunisia), indicative of a greenhouse warming in the aftermath of the Chicxulub impact, is published by MacLeod et al. (2018).[467]
A study on the environmental changes during the global warming following the brief impact winter at the Cretaceous-Paleogene boundary, based on geochemical, micropaleontological and palynological data from Cretaceous-Paleogene boundary sections in Texas, Denmark and Spain, is published by Vellekoop et al. (2018).[468]
A study on the Paleocene intermediate- and deep-water neodymium-isotope records from the North and South Atlantic Ocean, and on their implications for inferring the impact of changes in overturning circulation caused by the opening of the Atlantic Ocean on climate changes culminating in the greenhouse conditions of the Eocene, is published by Batenburg et al. (2018).[469]
A study on the magnetofossil concentrations preserved within sediments corresponding to the Paleocene–Eocene Thermal Maximum, as well as on the implications of magnetofossil abundance and morphology signatures for tracing palaeo-environmental conditions during the Paleocene–Eocene Thermal Maximum, is published by Chang et al. (2018).[470]
A study on the impact of greenhouse gas forcing and orbital forcing on changes in the seasonal hydrological cycle during the Paleocene–Eocene Thermal Maximum (for regions where proxy data is available) is published by Kiehlet al. (2018).[471]
A continuous Eocene equatorial sea surface temperature record is presented by Cramwinckel et al. (2018), who also construct a 26-million-year multi-proxy, multi-site stack of Eocene tropical climate evolution.[472]
A study on the continental silicateweathering response to the inferred CO2 rise and warming during the Middle Eocene Climatic Optimum is published by van der Ploeg et al. (2018).[473]
Su et al. (2018) use radiometrically dated plant fossil assemblages to quantify when southeastern Tibet achieved its present elevation, and what kind of floras existed there at that time.[474]
Description of a plant megafossil assemblage from the Kailas Formation in western part of the southern Lhasa terrane, and a study on its implications for inferring the elevation history of the southern Tibetan Plateau, is published online by Ai et al. (2018).[475]
A study on the relationship between the Rovno and Baltic amber deposits, based on stable carbon and hydrogen isotope analyses, is published by Mänd et al. (2018), who interpret their findings as indicative of distinct origin of Rovno and Baltic amber deposits.[476]
A study aiming to establish an accurate and precise age model for the eruption of the Columbia River Basalt Group, and to use it to test the hypothesis that there is a temporal relationship between the eruption of the Columbia River Basalt Group and the mid-Miocene climate optimum, is published by Kasbohm & Schoene (2018).[477]
A study on the causes of changes of environmental conditions in the Paratethys Sea of Central Europe during the middle Miocene is published online by Simon et al. (2018).[479]
A study on plant fossils spanning 14–4 million years ago from sites in Europe, Asia and East Africa, aiming to test the hypothesis of a single cohesive biome in the Miocene that extended from Mongolia to East Africa and at its peak covered much of the Old World, is published by Denk et al. (2018), who interpret data from plant fossil record as disproving the existence of a cohesive savannah biome from eastern Asia to northeast Africa, formerly inferred from mammal fossil record.[480]
A study on changes in local climate and habitat conditions in central Spain in a period from 9.1 to 6.3 million years ago, and on the diet and ecology of large mammals from this area in this time period as indicated by tooth wear patterns, is published online by De Miguel, Azanza & Morales (2018).[481]
Faith (2018) evaluates the aridity index, a widely used technique for reconstructing local paleoclimate and water deficits from oxygen isotope composition of fossil mammal teeth, arguing that in some taxa altered drinking behavior (influencing oxygen isotope composition of teeth) might have been caused by dietary change rather than water deficits.[482][483][484]
A study evaluating when the island of Sulawesi (Indonesia) gained its modern shape and size, and determining the timings of diversification of the three largest endemic mammals on the island (the babirusa, the Celebes warty pig and the anoa) is published by Frantz et al. (2018).[485]
A study on the Pliocene fish fossils from the Kanapoi site (Kenya) and their implications for reconstructing lake and river environments in the Kanapoi Formation is published online by Stewart & Rufolo (2018).[486]
Evidence indicating that reduced nutrientupwelling in the Bering Sea and expansion of North Pacific Intermediate Water coincided with the Mid-Pleistocene Transition cooling is presented by Kender et al. (2018), who assess the potential links between cooling, sea ice expansion, closure of the Bering Strait, North Pacific Intermediate Water production, reduced high latitude CO2 and nutrient upwelling, and development of the Mid-Pleistocene Transition.[487]
Domínguez-Rodrigo & Baquedano (2018) evaluate the ability of successful machine learning methods to compare and distinguish various types of bone surface modifications (trampling marks, crocodile bite marks and cut marks made with stone tools) in archaeofaunal assemblages.[488]
Description of new mammal and fish remains from the Olduvai Gorge site (Tanzania), comparing the mammal assemblage from this site to the present mammal community of Serengeti, and a study on their implications for reconstructing the paleoecology of this site at ~1.7–1.4 million years ago, is published by Bibi et al. (2018).[489]
A study on the environment in the interior of the Arabian Peninsula in the Pleistocene, as indicated by data from stable carbon and oxygen isotope analysis of fossil mammal tooth enamel from the middle Pleistocene locality of Ti's al Ghadah (Saudi Arabia), is published by Roberts et al. (2018).[490]
A study on the environmental dynamics before and after the onset of the early Middle Stone Age in the Olorgesailie Basin (Kenya) is published by Potts et al. (2018).[491]
A study on the chronology of the Acheulean and early Middle Stone Age sedimentary deposits in the Olorgesailie Basin (Kenya) is published by Deino et al. (2018).[492]
A study on the proxy evidence for environmental changes during past 116,000 years in lake sediment cores from the Chew Bahir basin, south Ethiopia (close to the key hominin site of Omo Kibish), and on its implications for inferring the environmental context for dispersal of anatomically modern humans from northeastern Africa, is published by Viehberg et al. (2018).[493]
A study on the environmental conditions in the area of present-day Basque Country (Spain) across the Middle to Upper Paleolithic transition, based on stable isotope data from red deer and horse bones, is published by Jones et al. (2018).[495]
The first reconstructions of terrestrial temperature and hydrologic changes in the south-central margin of the Bering land bridge from the Last Glacial Maximum to the present are presented by Wooller et al. (2018).[496]
A study on the fossil-bound nitrogenisotope records from the Southern Ocean is published by Studer et al. (2018), who interpret their findings as indicative of an acceleration of nitrate supply to the Southern Ocean surface from underlying deep water during the Holocene, possibly contributing to the Holocene atmospheric CO2 rise.[497]
A study on the causes of replacement of mature rainforests by a forest–savannah mosaic in Western Central Africa between 3,000 y ago and 2,000 years ago, based on a continuous record of 10,500 years of vegetation and hydrological changes from Lake Barombi Mbo (Cameroon) inferred from changes in carbon and hydrogen isotope compositions of plant waxes, is published by Garcin et al. (2018), who interpret their findings as indicating that humans triggered the rainforest fragmentation 2,600 years ago.[498][499][500][501][502]
A study on the vegetational and climatic changes since the last glacial period, based on data from 594 sites worldwide, and aiming to estimate the extent of future ecosystem changes under alternative scenarios of global warming, is published by Nolan et al. (2018).[503]
A study on the changing ecology of woodland vegetation of southern mainland Greece during the late Pleistocene and the early-mid Holocene, and on the ecological context of the first introduction of crop domesticates in the southern Greek mainland, as indicated by data from carbonized fuel wood waste from the Franchthi Cave, is published by Asouti, Ntinou & Kabukcu (2018).[504]
A study on the nitrogen isotope ratios, selenium abundances, and selenium isotope ratios from the ~2.66 billion years old Jeerinah Formation (Australia), providing evidence of transient surface ocean oxygenation ~260 million years before the Great Oxygenation Event, is published by Koehler et al. (2018).[506]
A study on the ocean chemistry at the start of the Mesoproterozoic as indicated by rare earth element, iron-speciation and inorganic carbon isotope data from the 1,600–1,550 million years old Yanliao Basin, North China Craton is published by Zhang et al. (2018), who report evidence of a progressive oxygenation event starting at ≈1,570 million years ago, immediately prior to the occurrence of complex multicellular eukaryotes in shelf areas of the Yanliao Basin.[507]
Evidence of euxinia occurring in the photic zone of the ocean in the Mesoproterozoic, based on measurements of mercury isotope compositions in late Mesoproterozoic (~1.1 billion years old) shales from the Atar Group and the El Mreiti Group (Tauodeni Basin, Mauritania), is presented by Zheng et al. (2018).[508]
A study on abundant pyriteconcretions from the topmost Nantuo Formation (China), deposited during the terminal CryogenianMarinoan glaciation, is published by Lang et al. (2018), who interpret these concretions as evidence of a transient but widespread presence of marine euxinia in the aftermath of the Marinoan glaciation.[509]
A study on wave ripples and tidal laminae in the Elatina Formation (Australia), interpreted as evidence of rapid sea level rise in the aftermath of the Marinoan glaciation, is published by Myrow, Lamb & Ewing (2018).[510]
A study on the global ocean redox conditions at a time when the Ediacaran biota began to decline, based on analysis of uranium isotopes in carbonates from the Dengying Formation (China), is published by Zhang et al. (2018), who interpret their findings as indicative of an episode of extensive oceanic anoxia at the end of the Ediacaran.[511]
New uranium isotope data from upper Ediacaran to lower Cambrian marine carbonate successions, indicative of short-lived episodes of widespread marine anoxia near the Ediacaran-Cambrian transition and during Cambrian Stage 2, is presented by Wei et al. (2018), who argue that the Cambrian explosion might have been triggered by marine redox fluctuations rather than progressive oxygenation.[512]
New δ15N data from late Ediacaran to Cambrian strata from South China is presented by Wang et al. (2018), who interpret their findings as indicating that ocean redox dynamics were closely coupled with key evolutionary events during the Ediacaran–Cambrian transition.[513]
A study on the isotopic composition and surface temperatures of early Cambrian seas, based on stable oxygen isotope data from the small shelly fossils from the Comley limestones (United Kingdom), is published by Hearing et al. (2018).[514]
High-resolution geochemical, sedimentological and biodiversity data from the Cambrian Sirius PassetLagerstätte (Greenland is presented by Hammarlund et al. (2018), who aim to assess the chemical conditions in the shelf sea inhabited by the Sirius Passet fauna.[515]
A study on the impact of the disruption of sediments caused by Fortunian bioturbation on the ocean chemistry, as indicated by data from the Chapel Island Formation (Canada), is published by Hantsoo et al. (2018).[516]
A study on the timing of the Sauk transgression in the Grand Canyon region is published by Karlstrom et al. (2018).[517]
A study on the oxygen isotope composition of seawater throughout the Phanerozoic is published by Ryb & Eiler (2018).[518]
Jin, Zhan & Wu (2018) present paleontological, sedimentological, and geochemical data to test a hypothesis that a cold surface current became established by the late Middle Ordovician in the equatorial peri-Gondwana oceans, similar to the eastern equatorial Pacific cold tongue today.[519]
Evidence from uranium isotopes from Upper Ordovician–lower Silurian marine limestones of Anticosti Island (Canada), indicative of an abrupt global-ocean anoxic event coincident with the Late Ordovician mass extinction, is presented by Bartlett et al. (2018).[520]
A study on the ocean redox conditions and climate change across a Late Ordovician to Early Silurian on the Yangtze Shelf Sea (China) and their implications for inferring the causes of the Late Ordovician mass extinction is published by Zou et al. (2018).[521]
Evidence of multiple episodes of oceanic anoxia in the Early Triassic, based on U-isotope data from carbonates of the uppermost Permian to lowermost Middle Triassic Zal section (Iran), is presented by Zhang et al. (2018).[522]
A study on changes in global bottom water oxygen contents over the Toarcian Oceanic Anoxic Event, based on thallium isotope records from two ocean basins, is published by Them et al. (2018), who report evidence of global marine deoxygenation of ocean water some 600,000 years before the classically defined Toarcian Oceanic Anoxic Event.[523]
A study on the palaeoenvironmental conditions of the seas at high latitudes (60°) of southern South America during the Early Cretaceous is published online by Gómez Dacal et al. (2018).[524]
A study evaluating the utility of oxygen-isotope compositions of fossilised foraminifera tests as proxies for surface- and deep-ocean paleotemperatures, and its implications for inferring Late Cretaceous and Paleogene deep-ocean and high-latitude surface-ocean temperatures, published by Bernard et al. (2017)[525] is criticized by Evans et al. (2018).[526][527]
Nitrogen isotope data from deposits from the northeast margin of the Tethys Ocean, spanning the Paleocene–Eocene Thermal Maximum, is presented by Junium, Dickson & Uveges (2018), who interpret their findings as indicating that dramatic change in the nitrogen cycle occurred during the Paleocene–Eocene Thermal Maximum.[529]
A study aiming to evaluate the global extent of surface ocean acidification during the Paleocene–Eocene Thermal Maximum is published by Babila et al. (2018).[530]
A study on the tropical sea-surface temperatures in the Eocene is published by Evans et al. (2018).[531]
A 25-million-year-long alkenone-based record of surface temperature change in the Paleogene from the North Atlantic Ocean is presented by Liu et al. (2018).[532]
A study on the likely magnitude of the sea-level drawdown during the Messinian salinity crisis, based on the analysis of the late Neogene faunas of the Balearic Islands, is published by Mas et al. (2018).[533]
An extensive, buried sedimentary body deposited by the passage of a megaflood from the western to the eastern Mediterranean Sea in the Pliocene (Zanclean), at the end of the Messinian salinity crisis, is identified in the western Ionian Basin by Micallef et al. (2018).[534]
A study on the impact of major, abrupt environmental changes over the past 30,000 years on the Great Barrier Reef is published by Webster et al. (2018).[535]
Evidence of sea level drop relative to the modern level at the shelf edge of the Great Barrier Reef between 21,900 and 20,500 years ago, followed by period of sea level rise lasting around 4,000 years, is presented by Yokoyama et al. (2018).[536]
Paleoclimatology
A study on the geologic record of Milankovitch climate cycles, extending their analysis into the Proterozoic and aiming to reconstruct the history of solar system characteristics, is published by Meyers & Malinverno (2018).[537]
A study on the effect of different forms of primitive photosynthesis on Earth's early atmospheric chemistry and climate is published by Ozaki et al. (2018).[538]
A quantitative estimate of Paleoproterozoic atmospheric oxygen levels is presented by Bellefroid et al. (2018).[539]
A study on the timing of the onset of the Sturtian glaciation, based on new stratigraphic and geochronological data from the upper Tambien Group (Ethiopia), is published by Scott MacLennan et al. (2018).[540]
A study on changes in the atmospheric concentration of carbon dioxide throughout the Phanerozoic, as indicated by data from a product of chlorophyll – phytane from marine sediments and oils, is published by Witkowski et al. (2018).[541]
A revised model and a new high-resolution reconstruction of the oxygenation of the Paleozoic atmosphere is presented by Krause et al. (2018).[542]
A study on the Early Ordovician climate, as indicated by new high-resolution phosphate oxygen isotope record of conodont assemblages from the Lange Ranch section of central Texas, is published by Quinton et al. (2018), who interpret their findings as consistent with very warm temperatures during the Early Ordovician.[543]
A study on the climate changes during the period of the Late Devonian extinction (and possibly causing it), inferred from a high-resolution oxygen isotope record based on conodontapatite from the Frasnian–Famennian transition in South China, is published by Huang, Joachimski & Gong (2018).[544]
A study on the impact of sulfur and carbon outgassing from the Siberian Traps flood basalt magmatism on the climate changes at the end of the Permian is published by Black et al. (2018).[546]
A study on the atmospheric carbon dioxide concentration levels in the Early Cretaceous based on data from specimens of the fossil conifer species Pseudofrenelopsis papillosa is published by Jing & Bainian (2018).[547]
A study on the terrestrial climate in northern China at the Cretaceous-Paleogene boundary, indicating the occurrence of a warming caused by the onset of Deccan Traps volcanism and the occurrence of extinctions prior to the Chicxulub impact, is published by Zhang et al. (2018).[548]
A study on the sources of secondary CO2 inputs after the initial rapid onset of the Paleocene–Eocene Thermal Maximum, contributing to the prolongation of this event, is published online by Lyons et al. (2018).[549]
Estimates of mean annual terrestrial temperatures in the mid-latitudes during the early Paleogene are presented by Naafs et al. (2018).[550]
A study on the early stages of development of Asian inland aridity and its underlying mechanisms, based on data from red clay sequence from the Cenozoic Xorkol Basin (Altyn-Tagh, northeastern Tibetan Plateau), is published by Li et al. (2018), who interpret their findings as indicating that enhanced Eocene Asian inland aridity was mainly driven by global palaeoclimatic changes rather than being a direct response to the plateau uplift.[551]
New mid-latitude terrestrial climate proxy record for southeastern Australia from the middle Eocene to the middle Miocene, indicative of a widespread cooling in the Gippsland Basin beginning in the middle Eocene, is presented by Korasidis et al. (2018).[552]
A study on CO2 concentrations during the early Miocene, as indicated by stomatal characteristics of fossil leaves from a late early Miocene assemblage from Panama and a leaf gas-exchange model, is published by Londoño et al. (2018).[553]
A study on the climate in the areas of the Iberian Peninsula inhabited by hominins during the Early Pleistocene, as indicated by data from macroflora and pollen assemblages, is published online by Altolaguirre et al. (2018).[554]
A study on the hydrological changes in the Limpopo Rivercatchment and in sea surface temperature in the southwestern Indian Ocean for the past 2.14 million years, and on their implications for inferring the palaeoclimatic changes in southeastern Africa in this time period and their possible impact on the evolution of early hominins, is published by Caley et al. (2018).[555]
A study evaluating whether changes of vegetation and diet of East African herbivorous mammals were linked to climatic fluctuations 1.7 million years ago, based on data from mammal teeth from the Olduvai Gorge site, as well as evaluating whether crocodile teeth from this site may be used as paleoclimatic indicators, is published by Ascari et al. (2018).[556]
Evidence for progressive aridification in East Africa since about 575,000 years before present, based on data from sediments from Lake Magadi (Kenya), is presented by Owen et al. (2018), who also evaluate the influence of the increasing Middle- to Late-Pleistocene aridification and environmental variability on the physical and cultural evolution of Homo sapiens in East Africa.[557]
A study on the climatic changes in the Lake Tana area in the last 150,000 years and their implications for early modern human dispersal out of Africa is published by Lamb et al. (2018).[558]
A high-resolution palaeoclimate reconstruction for the Eemian from northern Finland, based on pollen and plant macrofossil record, is presented by Salonen et al. (2018).[559]
A study on the extent and nature of millennial/centennial-scale climate instability during the Last Interglacial (129–116 thousand years ago), as indicated by data from joint pollen and ocean proxy analyses in a deep-sea core on the Portuguese Margin (Atlantic Ocean) and speleothem record from Antro del Corchia cave system (Italy), is published by Tzedakis et al. (2018).[560]
A study on the timing and duration of periods of climate deterioration in the interior of the Iberian Peninsula in the late Pleistocene, evaluating the impact of climate on the abandonment of inner Iberian territories by Neanderthals 42,000 years ago, is published by Wolf et al. (2018).[561]
A study on the climate changes in Europe during the Middle–Upper Paleolithic transition (based on speleothem records from the Ascunsă Cave and from the Tăușoare Cave, Romania), and on their implications for the replacement of Neanderthals by modern humans in Europe, is published by Fernández et al. (2018).[562]
A study on the timing of the latest Pleistocene glaciation in southeastern Alaska and its implication for inferring the route and timing of early human migration to the Americas is published by Lesnek et al. (2018).[563]
Quantitative estimates of climate in western North America over the past 50,000 years, based on data from plant community composition of more than 600 individual paleomiddens, are presented by Harbert & Nixon (2018).[564]
A study assessing the similarity of future projected climate states to the climate during the Early Eocene, the Mid-Pliocene, the Last Interglacial (129–116 ka), the Mid-Holocene (6 ka), preindustrial (c. 1850 CE), and the 20th century is published by Burke et al. (2018).[565]
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^Tiequan Shao; Yunhuan Liu; Baichuan Duan; Huaqiao Zhang; Hu Zhang; Qi Wang; Yanan Zhang; Jiachen Qin (2018). "The Fortunian (lowermost Cambrian) Qinscyphus necopinus (Cnidaria, Scyphozoa, Coronatae) underwent direct development". Neues Jahrbuch für Geologie und Paläontologie - Abhandlungen. 289 (2): 149–159. doi:10.1127/njgpa/2018/0755. S2CID 134628513.
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^ a b cMohamed Gameil; Abdelbaset S. El-Sorogy; Khaled Al-Kahtany (2020). "Solitary corals of the Campanian Hajajah Limestone Member, Aruma Formation, Central Saudi Arabia". Historical Biology: An International Journal of Paleobiology. 32 (1): 1–17. Bibcode:2020HBio...32....1G. doi:10.1080/08912963.2018.1461217. S2CID 90300789.
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^ a b c d eRoss A. McLean (2018). "Fasciphyllid and spongophyllid rugose corals from the Middle Devonian of western Canada". Palaeontographica Canadiana. 37: 1–117. ISBN 978-1-897095-85-0.
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^Kun Liang; Wenkun Qie; Luozhong Pan; Baoan Yin (2018). "Morphometrics and palaeoecology of syringoporoid tabulate corals from the upper Famennian (Devonian) Etoucun Formation, Huilong, South China". Palaeobiodiversity and Palaeoenvironments. 99 (1): 101–115. doi:10.1007/s12549-018-0363-y. S2CID 133849052.
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^Guang-Xu Wang; Xin-Yi He; Lan Tang; Ian G. Percival (2018). "Silurian amplexoid rugose coral genera Pilophyllia Ge and Yu, 1974 and Neopilophyllia new genus from South China". Journal of Paleontology. 92 (6): 982–1004. Bibcode:2018JPal...92..982W. doi:10.1017/jpa.2018.29. S2CID 134817990.
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^Chang-Min Yu (2018). "Restudy of the Early Devonian rugose coral Xystriphylloides from South China". Palaeoworld. 27 (2): 159–169. doi:10.1016/j.palwor.2017.06.001. S2CID 134820856.
^ a b c d e f g h iEmanuela Di Martino; Paul D. Taylor (2018). "Early Pleistocene and Holocene bryozoans from Indonesia". Zootaxa. 4419 (1): 1–70. doi:10.11646/zootaxa.4419.1.1. PMID 30313550.
^Ernst, Andrej; Krainer, Karl; Lucas, Spencer (2018). "Bryozoan fauna of the Lake Valley Formation (Mississippian), New Mexico". Journal of Paleontology. 92 (4): 577–595. Bibcode:2018JPal...92..577E. doi:10.1017/jpa.2017.146. S2CID 135266996.
^Zhiliang Zhang; Leonid E. Popov; Lars E. Holmer; Zhifei Zhang (2018). "Earliest ontogeny of early Cambrian acrotretoid brachiopods — first evidence for metamorphosis and its implications". BMC Evolutionary Biology. 18 (1): 42. Bibcode:2018BMCEE..18...42Z. doi:10.1186/s12862-018-1165-6. PMC 5880059. PMID 29609541.
^Zhiliang Zhang; Zhifei Zhang; Lars E. Holmer; Feiyang Chen (2018). "Post-metamorphic allometry in the earliest acrotretoid brachiopods from the lower Cambrian (Series 2) of South China, and its implications". Palaeontology. 61 (2): 183–207. Bibcode:2018Palgy..61..183Z. doi:10.1111/pala.12333. S2CID 3199997.
^Judith A. Sclafani; Curtis R. Congreve; Andrew Z. Krug; Mark E. Patzkowsky (2018). "Effects of mass extinction and recovery dynamics on long-term evolutionary trends: a morphological study of Strophomenida (Brachiopoda) across the Late Ordovician mass extinction". Paleobiology. 44 (4): 603–619. Bibcode:2018Pbio...44..603S. doi:10.1017/pab.2018.24. S2CID 92364910.
^Fernando García Joral; José Francisco Baeza-Carratalá; Antonio Goy (2018). "Changes in brachiopod body size prior to the Early Toarcian (Jurassic) Mass Extinction". Palaeogeography, Palaeoclimatology, Palaeoecology. 506: 242–249. Bibcode:2018PPP...506..242G. doi:10.1016/j.palaeo.2018.06.045. hdl:10045/77781. S2CID 135368506.
^Fernando Julián Lavié (2018). "Linguliformean brachiopods from the Las Plantas Formation (Ordovician, Sandbian), Argentine Precordillera". Ameghiniana. 55 (5): 600–606. doi:10.5710/AMGH.22.06.2018.3187. hdl:11336/88327. S2CID 134007925.
^Maurizio Gaetani; Marco Balini; Alda Nicora; Martino Giorgioni; Giulio Pavia (2018). "The Himalayan connection of the Middle Triassic brachiopod fauna from Socotra (Yemen)". Bulletin of Geosciences. 93 (2): 247–268. doi:10.3140/bull.geosci.1665. S2CID 134157425.
^ a bJuan L. Benedetto (2018). "The strophomenide brachiopod Ahtiella Öpik in the Ordovician of Gondwana and the early history of the plectambonitoids". Journal of Paleontology. 92 (5): 768–793. Bibcode:2018JPal...92..768B. doi:10.1017/jpa.2018.9. hdl:11336/129659. S2CID 135270782.
^ a b c d e f g h i j k l m n o p q r s t u v w x y z aa ab ac ad ae af ag ah ai aj ak al am an ao ap aq ar as at au av aw ax ay az ba bbJohn Bruce Waterhouse (2018). Late Carboniferous and Early Permian Brachiopoda and Mollusca from the lower Jungle Creek and upper Ettrain Formations of the Yukon Territory, Canada (PDF). Earthwise. Vol. 15. pp. 1–514.
^José Francisco Baeza-Carratalá; Alfréd Dulai; José Sandoval (2018). "First evidence of brachiopod diversification after the end-Triassic extinction from the pre-Pliensbachian Internal Subbetic platform (South-Iberian Paleomargin)". Geobios. 51 (5): 367–384. Bibcode:2018Geobi..51..367B. doi:10.1016/j.geobios.2018.08.010. hdl:10045/81989. S2CID 134589701.
^ a b c dValeryi V. Baranov; Robert B. Blodgett (2018). "Stringocephalid brachiopods in the upper Givetian (late Middle Devonian) of southeastern Alaska (Coronados Islands) and their paleobiogeographical significance". New Mexico Museum of Natural History and Science Bulletin. 79: 17–30.
^Colin D. Sproat; Renbin Zhan (2018). "Altaethyrella (Brachiopoda) from the Late Ordovician of the Tarim Basin, Northwest China, and its significance". Journal of Paleontology. 92 (6): 1005–1017. Bibcode:2018JPal...92.1005S. doi:10.1017/jpa.2018.31. S2CID 133780466.
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^ a b c d e f g h i j k l m n o p q r sR. E. Alekseeva; G. A. Afanasjeva; I. A. Grechishnikova; N. V. Oleneva; A. V. Pakhnevich (2018). "Devonian and Carboniferous brachiopods and biostratigraphy of Transcaucasia". Paleontological Journal. 52 (8): 829–967. Bibcode:2018PalJ...52..829A. doi:10.1134/S0031030118080014. S2CID 195319311.
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