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764 results for “foraminifera”
Data from: Lower Jurassic foraminifera from the Llanbedr (Mochras Farm) Borehole, North Wales, UK
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Data from: Blooms of aberrant planktic foraminifera across the K/Pg boundary in the Western Tethys: causes and evolutionary implications
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Data from: Heterochronic origin of spherical fusulinid foraminifera in the Late Paleozoic
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Data from: Ecological incumbency impedes stochastic community assembly in Holocene foraminifera from the Huon Peninsula, Papua New Guinea
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Data from: Nomenclature for the nameless: a proposal for an integrative molecular taxonomy of cryptic diversity exemplified by planktonic foraminifera
Investigations of biodiversity, biogeography and ecological processes rely on the identification of "species" as biologically significant, natural units of evolution. In this context, morpho-taxonomy only provides an adequate level of resolution if reproductive isolation matches morphological divergence. In many groups of organisms, morphologically defined species often disguise considerable genetic diversity, which may be indicative of the existence of cryptic species. The diversity hidden by morphological species can be disentangled through genetic surveys, which also provide access to data on the ecological distribution of genetically circumscribed units. These units can be identified by unique DNA sequence motifs and allow studies of evolutionary and ecological processes at different levels of divergence. However, the nomenclature of genetically circumscribed units within morphological species is not regulated and lacks stability. This represents a major obstacle to efforts to synthesize and communicate data on genetic diversity for multiple stakeholders. We have been confronted with such an obstacle in our work on planktonic foraminifera, where the stakeholder community is particularly diverse, involving geochemists, paleoceanographers, paleontologists and biologists, and the lack of stable nomenclature beyond the level of formal morphospecies prevents effective transfer of knowledge. To circumvent this problem, we have designed a stable, reproducible and flexible nomenclature system for genetically circumscribed units, analogous to the principles of a formal nomenclature system. Our system is based on the definition of unique DNA sequence motifs collocated within an individual, their typification (in analogy with holotypes), utilization of their hierarchical phylogenetic structure to define levels of divergence below that of the morphospecies, and a set of nomenclature rules assuring stability. The resulting molecular operational taxonomic units (MOTUs) remain outside the domain of current nomenclature codes, but are linked to formal morphospecies as regulated by the codes. Subsequently we show how this system can be applied to classify genetically defined units using the SSU rDNA marker in planktonic foraminifera and we highlight its potential use for other groups of organisms where similarly high levels of connectivity between molecular and formal taxonomies can be achieved.
Data from: Evolutionary ecology of Early Paleocene planktonic foraminifera: size, depth habitat and symbiosis
The carbon stable isotope (δ13C) composition of the calcitic tests of planktonic foraminifera has an important role as a geochemical tracer of ocean carbon system changes associated with the Cretaceous/Paleogene (K/Pg) mass extinction event and its aftermath. Questions remain, however, about the extent of δ13C isotopic disequilibrium effects and the impact of depth habitat evolution on test calcite δ13C among rapidly evolving Paleocene species, and the influence this has on reconstructed surface-to-deep ocean dissolved inorganic carbon (DIC) gradients. A synthesis of new and existing multispecies data, on the relationship between δ13C and δ18O and test size, sheds light on these issues. Results suggest that early Paleocene species quickly radiated into a range of depths habitats in a thermally stratified water column. Negative δ18O gradients with increasing test size in some species of Praemurica suggest either ontogenetic or ecotypic dependence on calcification temperature that may reflect depth/light controlled variability in symbiont photosynthetic activity. The pattern of positive δ13C test-size correlations allows us to (1) identify metabolic disequilibrium δ13C effects in small foraminifera tests, as occur in the immediate aftermath of the K/Pg event, (2) constrain the timing of evolution of foraminiferal photosymbiosis to 63.5 Ma, ∼0.9 Myr earlier than previously suggested, and (3) identify the apparent loss of symbiosis in a late-ranging morphotype of Praemurica. These findings have implications for interpreting δ13C DIC gradients at a resolution appropriate for incoming highly resolved K/Pg core records.
Simultaneous determination of I/Ca and other elemental ratios in foraminifera: comparing results from acidic and basic solutions
<p>This is the supplementary data for paper "Simultaneous determination of I/Ca and other elemental ratios in foraminifera: comparing results from acidic and basic solutions" published in AGU journal Geochemistry, Geophysics, Geosystems. </p>
Fig. 5 in Seasonal response of benthic foraminifera to anthropogenic pressure in two stations of the Gulf of Trieste (northern Adriatic Sea, Italy): the marine protected area of Miramare versus the Servola water sewage outfall
Fig. 5: Distribution of the foraminiferal density of those species and genera comprising at least 4% of the assemblage in at least one sample from the studied stations. Red histogram: Ser station; blue histogram: Res station. Note that y-axis scale is variable depending on species foraminiferal density.
Fig. 3 in Annular Chambers In Cretaceous Orbitolinidae (Larger Benthic Foraminifera): An Overview
Fig. 3 Annular chambers in Coskinolinella daguini Delmas & Deloffre (upper Aptian Reocín Formation of Spain; a–-c, d?, f), Coskinolinella santanderensis Ramírez del Pozo (early Albian of Spain; g-h), Pseudorbitolina schroederi Luger (upper Maastrichtian Tarbur Formation of Iran; e, i–j, k, m-n: reconstruction of Henson, 1948), and some comparisons with Gusicella minima (Henson) (upper Maastrichtian Tarbur Formation of Iran; l, o). a subaxial section. Note the presence of foramina (left side) of unknown distribution pattern throughout the test. b–c oblique sections. d Drawing of the dorsal side of an isolated specimen with two annular chambers highlighted in colours (modified from Hofker, 1965, fig. 1, without scale, illustrated as C. daguini it might in fact belong to C. santanderensis). e subaxial section. Note the concentric arrangement of foramina (radial tubular apertures sensu Henson, 1948) in line between subsequent chambers in the middle part of the annular chambers (solid red left in the test, dotted red in the reconstructed part). f tangential section; approximate position shown in b (1------2). g-h tangential section showing intercalary beams. i axial section of a megalospheric specimen (em = embryo). j Detail from Fig. 3e (axial section) showing aligned tubular apertures (= tubular foramina, t.f.) sensu Henson (1948). k Schematic drawing modified from Henson (1948, fig. 16a) showing aligned tubular foramina (t.f., arrows towards test base) and primary chambers (p.ch.) in axial section (arrows); t.a. aperture at test base. l Part of the test in axial section showing aligned tubular foramina at the transition marginal to central zone. m–n Tangential sections showing aligned main partitions (m: thin-section, n: reconstruction from Henson, 1948, fig. 16e). o Part of the test in tangential section showing from left to right the cellular subepidermal network, and aligned vertical main partitions and tubular foramina.
Fig. 2 in Siphopfenderina Gen. Nov. (Type-Species Arenobulimina Geyikensis Solak, 2022), A Primitive Pfenderinid Foraminifera From The Cretaceous Of Neotethys
Fig. 2 Siphopfenderina geyikensis (Solak, 2022) gen. et comb. nov. from the Aptian of Turkey (1-6; Solak, 2022: Pl. 1, fig. a, pl. 2, fig. 1, pl. 1, fig. e, pl. 2, fig. b, pl. 1, fig. c, pl. 1, fig. h). Siphopfenderina sp. aff. geyikensis (Solak) from the Aptian of central Iran (7, 10, 12-13, 15-21), and Cantabria, northern Spain (8-9, 11, 14). Siphopfenderina ssp. from the Coniacian- Santonian? of Serbia (22-26), Cenomanian of SW Iran (27-28), Campanian of Croatia (29-30). Abbreviations: co. = (hollow) central columella, fo. = foramen, p.k. = pseudo-keriotheca, pr. = proloculus, se. = septum.
FIGURE 11. Field photos showing the depositional sequences, A in Eocene planktonic foraminifera from the north Eastern Desert, Egypt: Biostratigraphic, paleoenvironmental and sequence stratigraphy implications
FIGURE 11. Field photos showing the depositional sequences, A shows the boundary between Qurn (sequence 2) and Tarbul members (sequence 3); B shows the depositional sequence 3 representing Tarbul Member and the overlying sequence 4 of Maadi Formation; C shows shale and marly facies that represented the transgressive systems tracts of sequence 3; D shows the reefal facies with bivalvia (black arrows) that represented the highstand systems tracts (HST) of sequence 4.
FIGURE 10 in Eocene planktonic foraminifera from the north Eastern Desert, Egypt: Biostratigraphic, paleoenvironmental and sequence stratigraphy implications
FIGURE 10. Correlation chart shows correlation of the planktonic zones, planktonic foraminiferal ratio (P%), paleodepth of the studied succession with the tethyan sea level, and depositional sequences as well as the international planktonic zones.
FIGURE 9 in Eocene planktonic foraminifera from the north Eastern Desert, Egypt: Biostratigraphic, paleoenvironmental and sequence stratigraphy implications
FIGURE 9. Correlation of the recorded planktonic biozones in the study area with the international zonal schemes and those in and outside Egypt.
FIGURE 14 in Quaternary foraminifera and mollusc assemblages on the southwestern African shelf
FIGURE 14. Distribution maps of benthic foraminifera occurring in Namibian and western South African outer shelf (blue shading = Lowry, 1987; black dots = Compton et al., 2002, 2004 and this study), lower to middle upper Quaternary sediments (green-yellow dots = McMillan, 1987) and inner shelf surface grab sediments (red-yellow dots = Schmidt-Sinns, 2008). Samples from McMillan (1987), Compton et al. (2002, 2004) and this study represent Pleistocene-aged foraminifera and samples from Lowry (1987) and Schmidt-Sinns (2008) are from surface grab sediments.
FIGURE 15 in Quaternary foraminifera and mollusc assemblages on the southwestern African shelf
FIGURE 15. Mid to late Pleistocene/Holocene environmental interpretation of the southwestern margin of Africa based on foraminifera and mollusc species found in outer shelf sediments. Slope data and occurrences are based on reports from ODP Leg 175 (Wefer et al., 1998) and results from cores GeoB 20601-4, 8342-6 and 8336-6 (Meteor Cruises M123 and M57/1) in Chapter 7 of Bergh (2019).
FIGURE 10 in Quaternary foraminifera and mollusc assemblages on the southwestern African shelf
FIGURE 10. Whole and fragmented shells (top) (core 2658, 10-15 cm sampling interval), Nuculana bicuspidata (bottom left) shells including articulated valves (core 2634, 78-85 cm) and Pecten spp. fragments (bottom right) (core 2658, 88-90 cm) from the northern Namibian cores.
FIGURE 11. Planktic foraminifera from the Namibian outer shelf with primary apertural views visible. 1 in Quaternary foraminifera and mollusc assemblages on the southwestern African shelf
FIGURE 11. Planktic foraminifera from the Namibian outer shelf with primary apertural views visible. 1. Globorotalia (Globoconella) inflata (d'Orbigny, 1839b) (core 2670, 98 cm); 2. Globorotalia menardii (Parker, Jones and Brady, 1865) (core 2670, 23 cm); 3. Globorotalia truncatulinoides (d'Orbigny, 1839b) (core 2670, 23 cm); 4. Neogloboquadrina dutertrei (d'Orbigny, 1839a) (core 2670, 43 cm); 5. Neogloboquadrina incompta (Cifelli, 1961) (core 2670, 85 cm); 6 Globigerina bulloides d'Orbigny, 1826 (core 2670, 85 cm); 7. Globigerinella siphonifera (d'Orbigny, 1839b) (core 2670, 33 cm); 8. Globigerinoides ruber white (d'Orbigny, 1839a) (core 2670, 13 cm); 9. Trilobatus sacculifer (Brady, 1877) (core 2670, 63 cm); 10. Orbulina bilobata (d'Orbigny, 1846) (core 2670, 3 cm); 11. Orbulina universa d'Orbigny, 1839a (core 2670, 33 cm).
FIGURE 8 in Quaternary foraminifera and mollusc assemblages on the southwestern African shelf
FIGURE 8. Mollusc shells from the gravel fraction of the uppermost 2 units of the Walvis Bay-Lüderitz cores. 1. Dosinia lupinus (Linnaeus, 1758) (core 1407, 0-4 cm sampling interval); 2. Lucinoma capensis (Jaeckel and Thiele, 1931) (core 1397, 0-4 cm); 3. Tellina (Moerella) analogica Sowerby III, 1904 (core 1478, 8-12 cm); 4. Ostrea sp. (core 1657, 0-4 cm); 5. Nassarius vinctus (Marrat, 1877) (core 1407, 0-4 cm); 6. Turritella declivis Adams and Reeve, 1850 (core 1657, 20-24 cm); 7. Comitas saldanhae (Barnard, 1958) (core 1307, 0-4 cm).
FIGURE 12 in Quaternary foraminifera and mollusc assemblages on the southwestern African shelf
FIGURE 12. Distribution maps of benthic foraminifera occurring in Namibian and western South African outer shelf (blue shading = Lowry, 1987; black dots = Compton et al., 2002, 2004 and this study), lower to middle upper Quaternary sediments (green-yellow dots = McMillan, 1987) and inner shelf surface grab sediments (red-yellow dots = Schmidt-Sinns, 2008). Samples from McMillan (1987), Compton et al. (2002, 2004) and this study represent Pleistocene-aged foraminifera and samples from Lowry (1987) and Schmidt-Sinns (2008) are from surface grab sediments.
FIGURE 13 in Quaternary foraminifera and mollusc assemblages on the southwestern African shelf
FIGURE 13. Distribution maps of benthic foraminifera occurring in Namibian and western South African outer shelf (blue shading = Lowry, 1987; black dots = Compton et al., 2002, 2004 and this study), lower to middle upper Quaternary sediments (green-yellow dots = McMillan, 1987) and inner shelf surface grab sediments (red-yellow dots = Schmidt-Sinns, 2008). Samples from McMillan (1987), Compton et al. (2002, 2004) and this study represent Pleistocene-aged foraminifera and samples from Lowry (1987) and Schmidt-Sinns (2008) are from surface grab sediments.
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