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a-b, Kasimophyllum demuesensis n. gen., n. sp.; a, U. of M. 827/9-11, BM-277, Demués section, x62, longitudinal section, enlargment of part of the holotype, with different nicol orientation; b, Same as a, x 26, holotype. c-e, Archaeolithophyllum johnsoni Rácz 1966; c, U. of M. 825/3, BM-257, Inguanzo, x26, longitudinal section; d, U. of M. 725/19-20, BM-72, Las Llacerias section, x26, longitudinal section with a fragment of Hikorocodium?; e, U. of M. 815/ 23, BM-11, Las Llacerias section, x26. f-i, Archaeolithophyllum delicatum Johnson 1956; f, U. of M. 814/6, as d, but x30, longitudinal section; g, U. of M. 825/14, as c, but x30, showing branches; h, U. of M. 818/20-21, BM-128, Berodia-II section, x26, longitudinal section; i, U. of M. 827/18, BM-281, Demués section, x26, with the perithallic cells.
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A taxonomic revision of shallow-water Carboniferous (Pennsylvanian) red and green algae observed in Ponga, Picos de Europa and Pisuerga-Carrión Units in NW Spain is presented. Some microproblematics are included. Thirty-two genera are described; three genera and four species are new: Anatolipora cantabriensis n. sp., Pelayella multiporosa n. gen.,...
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Citations
... A problematic algae/foraminifera Elles-Cengiz Okuyucu, U. Kagan Tekin, Cagri Guzgun and Kaan Sayit merella subparallela Flügel and Flügel-Kahler recovered from this sample were originally described from the upper part of the Late Artinskian -Early Kungurian Trogkofel Limestone of Valcanale (Italy) (Davydov et al., 2013). It was also recorded from the Kasimovian succession of Spain (Mamet and Villa, 2021), the Late Carboniferous succession of Croatia (Sremac and Aljinovic, 1997) and recently in the Sakmarian-Early Artinskian succession of Turkey (Mersin Mélange; Okuyucu et al., 2020). The occurrence of these taxa in sample 18-T-73 implies that the age of this sample should be younger than the Late Artinskian-Early Kungurian (late Early Permian). ...
The Beyşehir-Hoyran Nappes, one of the tectonostratigraphic units of the Taurides, are thought to be originated from the Izmir-Ankara Ocean (northern branch of Neotethys). In this study, Late Paleozoic rock units from the blocks of Beyşehir-Hoyran Nappes were studied in detail using foraminiferal assemblages in two different locations from the southwest of Karaman City (southern Turkey).
In both places, blocks/slices and pebbles of various origins are embedded within a highly sheared matrix of Late Cretaceous age, and the whole unit can be regarded as a sedimentary mélange. The ages of the blocks from the southwest of Karaman City range from the Late Serpukhovian (Late Mississippian) to Late Capitanian (Middle Permian) with some depositional breaks (e.g., Bashkirian, Kasimovian).
Combined with the previous data from the Mersin Mélange, which also include the remnants of the Beyşehir-Hoyran Nappes, our new findings suggest that a shallowing-upward sequence, characterized by a shallow water environment with foraminifera-bearing limestones, was deposited over the Tournaisian pelagic sequence in the Beyşehir-Hoyran Nappes till the Early Moscovian (Early Middle Pennsylvanian). This shallowing-upward sequence in the Beyşehir-Hoyran Nappes could be related to the Late Paleozoic Glaciation on the Gondwana supercontinent (Glacial II), which resulted in a sea-level drop and deposition of platform carbonates during the Viséan–Early Moscovian (Middle Mississippian to Early Middle Pennsylvanian) time interval. The absence of the main part of the Middle–Upper Pennsylvanian deposits (continental phase during the Middle Moscovian – Middle Gzhelian) in the Beyşehir-Hoyran Nappes can be mainly attributed to the occurrence of a mantle plume and partially to the effect of Late Paleozoic Gondwanan Glaciation (Glacial III). Progressive uplifting by the buoyant mantle plume material
has resulted in rifting at the center of the basin where the Beyşehir-Hoyran Nappes have deposited. The rifting process led to tectonic destabilization of the platform in the basin, causing accumulation of the upper Gzhelian (uppermost Pennsylvanian) detrital limestone with broken and abraded foraminiferal shells. Following this, deep basinal conditions prevailed during the Late Asselian–Kungurian (Early Permian), as revealed in the Mersin Mélange, where radiolarian cherts are associated with continental within-plate lavas of extreme incompatible trace element enrichment. Similar processes were responsible for the continual deposition of detrital limestones in the same basin until the end of Late Capitanian (Middle Permian). Based on all these, the uplifting process followed by rift-related volcanic rocks and
detrital limestones can be interpreted as the opening of the Izmir-Ankara Ocean (northern Neotethys).
... e-f). Both species are characteristic of the Bashkirian and are distributed up to the Asselian Stage of the Lower Permian in Arctic Canada (Mamet et al., 1987), northern Spain (Mamet & Villa, 2004), northwestern Serbia (Pajić & Fillipović, 1995) and in Urals, Donets Basin and Tajikistan (Ivanova, 2013 Fig. h) and Anthracoporellopsis cf. machaevii Maslov (Pl. ...
The Olistostrome member of the Sana-Una Paleozoic complex of the Ljubija ore mine in Bosnia and Herzegovina contains limestone fragments of pebble to block size that have been examined paleontologically. The recovered conodont fauna of the first sample is characterized by the species Declinognathodus lateralis, Idiognathoides sulcatus sulcatus and Idiognathodus sp. confirming its mid-Bashkirian age. This report is the first on the occurrence of these taxa in the area. The second sample with chaetetid demosponges yields an abundant diversified microbiota consisting of cyanobacteria, algae and foraminifera. Chlorophyts are marked by the common siphonoclad occurrence of Donezella lutugini and D. lunaensis, whereas rhodophyts include rare representatives of Stacheia, Stacheoides, Pseudoungdarella and Masloviporidium. The presence of Asphaltinella horowitzi and Aphralysia carbonaria of unclear taxonomic position is also documented. Pseudostaffellids, eostaffellids and other foraminifera, mostly endothyrids are present. The examined associations of fossils point to the Bashkirian age of the primary rock that originated in a very shallow habitat most probably linked to a high-energy reef environment.
... The large dasycladacean alga Anthracoporella Pia is fairly abundant (thin section KD-12-01-14 g) (Fig. 7). The genus is well known from the Bashkirian-Moscovian of the Urals (4 species; see Ivanova, 2013), the Lower Carboniferous of Kazakhstan (Maslov, 1956), the Tyumen-Kustanay depression (Ivanova, 2008) and Japan, the Gzhelian-Asselian of the Carnic Alps, Karavanke Mountains and Texas (Bebout and Coogan, 1964), and the uppermost Moscovian-Gzhelian in the Cantabrian Mountains of Spain (Mamet and Villa, 2004). It was found in the Nansen Formation (Canadian Arctic) in the Pennsylvanian-Lower Permian (Ivanova, 2013). ...
The chapter presents results of studying the seabed rocks from scarps of steep mountainsides of the Mendeleev Rise collected during the Arctic-2012 expedition. The seabed collection consists of five thousand samples dominated by sedimentary rocks of shallow shelf facies. Carbonates are dominated by massive dolomites and limestones, which contain Devonian to Permian fauna. Terrigenous rocks are mainly represented by quartz sandstone and siltstone. Judging by the composition and age, the sedimentary rocks of the Mendeleev Rise belonged to the platform cover of the Early Precambrian cratonic block, which forms the crystalline basement of the uplifts in the Central Arctic. Basalt and gabbro-dolerite occupy no more than 10–20% of the raised seabed rocks. The basalt of the Mendeleev Rise belongs to the intraplate moderately alkaline Permian-Triassic basalt of the trap formation of Siberia and the Jurassic-Cretaceous basalt of the High Arctic Province (HALIP).
... The upper part of the succession, represented by clayey limestone and quartz sandstone alternation, corresponds to the interval from Cingey-10 to Cingey-13. Within this interval, the lowest sample Cingey-10 includes Ellesmerella subparallela Flü gel et Flü gel-Kahler that was first described from the upper part of the late Artinskian-early Kungurian Trogkofel Limestone (Davydov et al., 2013) of Valcanale (Italy), and also recorded from the Kasimovian succession of Spain (Mamet and Villa, 2004) and Late Carboniferous succession of Croatia (Sremac and Aljinovic, 1997). Globivalvulina cf. ...
The Mersin Mélange (MM) as a part of the Mersin Ophiolitic Complex in southern Turkey is a sedimentary complex including blocks and tectonic slices within a Late Cretaceous matrix. Two blocks (Keven and Cingeypinari) within the MM originated from the northern branch of Neotethys (Izmir-Ankara-Erzincan Ocean) and have been studied in detail using foraminiferal assemblages to correlate them with coeval successions in the Taurides and to approach the Early Permian evolution of the northern branch of the Neotethys. The Keven Block includes mainly slope deposits (poorly-sorted carbonate breccia and fossiliferous calcarenite) and dated as late Asselian-Sakmarian, whereas Cingeypinari Block consists of platform deposits (fossiliferous platform carbonate and quartz sandstone alternation) assigned to the Sakmarian-early Artinskian. These Early Permian Cingeypinari and Keven blocks from the Beysehir-Hoyran Nappes are biostratigraphically well correlated to the northerly originated Hadim nappe and its equivalents in the Tauride belt. Considering recent studies on the Mersin Mélange, a possible mantle plume existed during the Late Carboniferous-Early Permian time interval along the northern Gondwanan margin. This event led to the opening of the northern Neotethys and deposition of the pelagic “Karincali” sequence with volcanic material in the basinal conditions. The data presented suggest that the Keven block relates to the slope and the Cingeypinari block to platform conditions deposited as a lateral equivalent of the Karincali sequences during the Early Permian.
... The large dasycladacean alga Anthracoporella Pia is fairly abundant (thin section KD-12-01-14g) (Fig. 7). The genus is well known from the Bashkirian-Moscovian of the Urals (4 species; see Ivanova, 2013), the Lower Carboniferous of Kazakhstan (Maslov, 1956), the Tyumen-Kustanay depression (Ivanova, 2008) and Japan, the Gzhelian-Asselian of the Carnic Alps, Karavanke Mountains and Texas (Bebout, Coogan, 1964), and the uppermost Moscovian-Gzhelian in the Cantabrian Mountains of Spain (Mamet, Villa, 2004). It was found in the Nansen Formation (Canadian Arctic) in the Pennsylvanian-Lower ...
... Maslov (1929) originally assigned Donezella to the red algae (Johnson 1963), however, in successive subsequent studies Donezella has been considered to be: green (Codiaceae) alga (Rácz 1964), alga incertae sedis (Rich 1967), Foraminifera (Riding 1979), calcareous sponges (Termier et al. 1977), microproblematica (Riding 1979;Chuvashov and Riding 1984), green (Paleosiphonocladales) algae (Shuysky 1985;Ivanova 1999), green algae of incertae familiae (Groves, 1986), green (Dasycladales) algae (Deloffre, 1988) and pseudo-algae (Vachard et al. 1989). Recent work regarding Donezella refers to the genus as green (Chlorophycophyta) algae (Mamet and Villa 2004), algae incertae sedis (Mamet and Zhu 2005), algospongia (Vachard and Cózar 2010) or more commonly, microproblematica (Samankassou 2001;Della Porta et al. 2002;Choh and Kirkland 2006;Corrochano et al. 2012). Donezella accumulations are often interpreted to have grown within a warm, shallow (low to moderate energy, below fair-weather wave base) environment but have been shown to thrive over a range of water depths up to 200 m (Della Porta et al. 2002;Choh and Kirkland 2006;Corrochano et al. 2012). ...
... Specimens of Claracrusta (Fig. 3a) are observed as laminar rows of irregular, often bean and ovoid to subquadratic shaped cells which have a honey or yellow coloured calcite wall. The cells have been referred to as tubular (Cózar 2005, and elsewhere), but here, appear to be ovoid or subquadratic, agreeing with Mamet and Villa (2004). Individual cells have been observed to range from 10 to 110 μm but the average cell size is around 50 μm. ...
Purpose: Mounds from the Pennsylvanian aged San Emiliano Formation (Cantabrian Mountains, Spain) are commonly well exposed. These mounds range from 2 to 50 m in height and are observed to be primary geological features. The mounds are described and classified and the factors and controls of mound nucleation, growth and demise have been established. Methods: Microfacies analysis of 177 thin sections has revealed the composition of the mounds and surrounding carbonates. Results: Composite mounds, exhibiting characteristic components of both Cluster mounds and Agglutinated Microbial mounds are described. The mounds are skeletal-microbial/pack-wackestones. Peloidal, homogenous and clotted micrites are the main sedimentological constituents of the mounds. Microfossils are dominant with Donezella, Claracrusta, Rothpletzella and Girvanella being common. Small foraminifera, bryozoans, corals and algae are all present within the mounds, but are more common within off-mound carbonates. Conclusions: The formation of the mounds was controlled by a dynamic relationship between Donezellacean algae, and microscopic encrusters, a bio-mechanism not observed in mud mounds elsewhere. Fluctuating environmental conditions lead to the alternate dominance between the two groups, resulting in accretion and stabilisation of carbonate muds. These mounds are compositionally different to their Pennsylvanian counterparts.
... According to several authors (Groves, 1986;Mamet and Villa, 2004;Mamet and Pré at, 2010;Vachard and Có zar, 2010), Efluegelia Vachard in Massa and Vachard, 1979, is synonymous with Fourstonella. However, some important differences have been noted between both taxa (Vachard et al., 1989: text- fig. ...
The microfloral and microfaunal assemblages of the MFZ11 foraminiferal biozone (late early Viséan; formerly V2a) are well developed in the Kiyasar section of the Sari area (central Alborz; northern Iran). Regionally, this biozone MFZ11 may be subdivided into three subzones. The lower subzone, MFZ11A, is characterized by the appearances of the algae Koninckopora tenuiramosa, coeloporellacean indet., Fourstonella fusiformis, and Nanopora anglica and, among the foraminifers, by the occurrence of Ammarchaediscus bozorgniai and the disappearance of Eoparastaffella simplex; the absence of Uralodiscus rotundus, U. spp., and primitive Glomodiscus spp. in this subzone is noticeable. The next subzone, MFZ11B1, is well characterized by the appearance of Glomodiscus spp. (G. oblongus and G. cf. miloni) and the local range zone of Pararchaediscus, a genus emended herein and interpreted as a junior synonym of Archaediscus at the involutus stage and Propermodiscus; only a few characteristic issinellacean and palaeoberesellacean algae are present in this subzone. Then, the last subzone, MFZ11B2, is characterized by Hemiarchaediscus (emended herein) and Glomodiscus miloni; the upper part of this latter subzone is only marked by the apparent absence of the archaediscids and the presence of two incertae sedis algae: Crassikamaena scabrosa and Epistacheoides bozorgniai nov. sp. These assemblages indicate that at that time, Alborz remained located on the Perigondwanan southern border of the Palaeotethys, and was probably connected with the Urals as well as the northwestern branch the Palaeotethys, from Belgium to the Donets Basin.
... 76). What is more, both genera are known from the late Palaeozoic shelf carbonates (they contributed to reef formation [31]), and therefore their presence in the Late Palaeozoic fresh or brackish water (see discussion on ecology) may be unlikely. Our material also resembles the non-calcifying alga Perissothallus, described from the late Carboniferous and Permian of USA and Germany. ...
The Lower Carboniferous (Visean) Granton Lagerstätte (Edinburgh, Scotland) is principally known for the discovery of the conodont animal, but has also yielded numerous crustaceans and other faunas. Here we report on small branching colonies, reaching 10 mm in length. They are small, erect, arborescent, and irregularly branched with predominant monopodial and dichotomous growth. They bud in a single plane. In one specimen the wall microstructure is well preserved and it is composed of evenly spaced, linear fibers, running parallel to the axis of the stems, and connected by transverse bars. We discuss possible biological affinities of these organisms; we consider algal, poriferan, hydrozoan and bryozoan affinities. The general pattern of branching, presence of fan-like structures (interpreted here as possible gonophores) and microstructure suggests affinity to Hydrozoa, affinity to non-calcifying algae is less likely. Assuming hydrozoan nature; the microstructure might suggest affinities with the extant family Solanderiidae Marshall, 1892 that possess an internal chitinous skeleton. The EDS analysis shows that fossils discussed here are preserved as phosphates. The skeletons were probably not mineralized, the presence of phosphorus suggests that the colonies were originally composed of chitin. We describe these organisms as Caledonicratis caridum gen. et sp. nov. (Solanderiidae?, Capitata?). Colonies of C. caridum gen et. sp. nov. sometimes encrust the exuviae of crustaceans, which very probably lived in fresh to brackish water thus indicating a likely habitat of Caledonicratis.
... Various terms have been employed to describe the cortical siphons in late Paleozoic anchicodiacean algae. The most extended term is ''utricle'' (e.g., Konishi and Wray, 1961; Baars and Torres, 1991; Baars, 1992; Torres and Baars, 1992a; Torres et al., 1992 Torres, 1995 Torres, , 1997 Mamet and Villa, 2004), although other expressions, such as ''cylindrical cells'' (Khvorova, 1946), ''utricular casts'' (Torres and Baars, 1992b), or ''secondary threads'' (Daryan and Rashidi, 2010) have been employed. In the present paper, the different cortical siphon orders or series will be termed ''primary cortical siphons,'' ''secondary cortical siphons,'' ''tertiary cortical siphons,'' and ''quaternary cortical siphons'' (Fig. 3). ...
The cortical structure of the green anchicodiacean alga Anchicodium in the Pennsylvanian Dueñas Formation of the Cantabrian Zone (northwestern Spain) is described and illustrated. Anchicodium is characterized by a broad phylloid or leaflike calcified thallus, consisting of a bilateral cortex and a poorly calcified central medulla. The organization and morphology of the cortical system have been revealed with great detail using cathodoluminescence microscopy. Anchicodium cortex is composed of up to three (four?) orders of dichotomized branched cortical siphons that are usually swollen at the center; primary siphons are bulbous and are followed by elongate cylindrical siphons. Cortical siphons are preserved as dull-bright luminescent molds filled with micrite or microsparite, and contrast sharply with the surrounding non-luminescent calcite infilling the intersiphonal spaces, originally occupied by aragonite. Anchicodium in the Dueñas Formation exhibits a variety of preservational stages. Through a compilation of the taxonomic nomenclature and morphologic re-interpretations, it is concluded that some late Paleozoic anchicodiacean algae might represent diagenetic stages of Anchicodium or Eugonophyllum without any taxonomic significance. This conclusion is suggested particularly for the taphotaxon Ivanovia.
... In those packages numerous decimetre-to metre-thick buildups of chaetetids (facies Md1, only present in sequence 1), syringoporids (facies Md2), dasycladaceans (mainly Anthracoporella) and phylloid algae (facies Md3 and Md4, respectively) occur. B1 lithofacies are black nodular marly wackestones and packstones punctuated by interbeds of marls (Fig. 9A) and contain abundant algae, conspicuous swarms of Penella (Mamet and Villa, 2004), polyaxon sponge spicules and very rich heterozoan fauna including abundant foraminifers (Fig. 9B, C, D). Laminar chaetetids are characteristic (Fig. 9A), along with sphinctozoan and less abundant inozoan and lithistid sponges, tabulate syringoporids, solitary rugose geoyerophyllid corals and echinoderms. ...
High-diversity marine biotic communities characterize the lower Kasimovian (Upper Pennsylvanian) carbonates of the Las Llacerias Formation in the Ándara Massif (Picos de Europa Province, Cantabrian Mountains, Spain). The carbonates accumulated on a small thrust-top ramp system. Within the shallow, low energy and euphotic realms, biotic communities were characterized by abundant photozoans (calcareous algae and cyanobacteria) and heterozoans including filter and suspension feeders (calcareous and siliceous sponges, bryozoans, brachiopods, crinoids), diverse other metazoans (rugose solitary and colonial corals,
tabulate corals, bivalves, gastropods and echinoids), benthic foraminifers including very abundant small
incrusting “tubiforms” and conspicuous swarms of cement-filled spheres (calcispheres or Penella). Smallsized buildups of chaetetid sponges, syringoporids, branching rugose corals, Anthracoporella and phylloid algae commonly developed in these shallow-water environments. Meanwhile, mud mounds formed at greater water depths, mostly below the lower limit of the phothic zone. The occurrence of such diverse biotic communities and the grain composition of the shallow-water deposits, not recorded in the platform-top
successions of the antecedent Bashkirian–Moscovian carbonate shelf (Valdeteja and Picos de Europa formations) are interpreted as linked to increased nutrient levels mesotrophic to mildly eutrophic conditions) in the actual sea-surface water. The nutrients are inferred to have resulted from land-derived fluxes from the rivers draining the adjacent growing Variscan Orogenic chain. Nutrients were subsequently transported into the narrowed marine shallowing foreland basin located in the eastern side of Pangea, within
the palaeoequatorial humid belt. Comparison to the Pennsylvanian Auernig Group in the Carnic Alps allows the discrimination between the influence of land-derived versus upwelling-derived nutrients, providing a useful tool in the interpretation of biotic assemblages in the fossil rock record.
