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Fig. 1 in Conodont faunas with Lenodus variabilis in the upper Arenigian to lower Llanvirnian of Sweden
Fig. 1. Location of areas (provinces) and sections in Sweden where samples have been taken.
FIGURE 7 in Graphic correlation of the upper Eifelian to lower Frasnian (Middle-Upper Devonian) conodont sequences in the Spanish Central Pyrenees and comparison with composite standards from other areas
FIGURE 7. Correlation of the three sections based on the results of the graphic correlation method.
Fig. 6 in Conodont-based event stratigraphy of the Early-Middle Frasnian transition on the South Polish carbonate shelf
Fig. 6. Location sketch of Wietrznia quarry sections at Kielce (see Figs. 2, 7, 8).
Dataset and script to: Morphometric variance, evolutionary constraints and their change through time in Late Devonian Palmatolepis conodonts
<p>Phenotypic variation is the raw material of evolution. Standing variation can facilitate response to selection along "lines of least evolutionary resistance", but selection itself might alter the structure of the variance. Shape was quantified using 2D geometric morphometrics in <i>Palmatolepis </i>conodonts through the Late Devonian period. Patterns of variance were characterized along the record by the variance-covariance matrix (P-matrix) and its first axis (Pmax). The Late Frasnian was marked by environmental oscillations culminating with the Frasnian/Famennian mass extinction. A shape response was associated with these fluctuations, together with a deflection of the Pmax and the P-matrix. Thereafter, along the Famennian, <i>Palmatolepis </i>mean shape shifted from broad elements with a large platform to slender elements devoid of platform. This shift in shape was associated with a reorientation of Pmax and the P-matrix, due to profound changes in the functioning of the elements selecting for new types of variants. Both cases provide empirical evidences that moving adaptive optimum can reorient phenotypic variation, boosting response to environmental changes. On such time scales, the question seems thus not to be whether the P-matrix is stable, but how it is varying in response to changes in selection regimes and shifts in adaptive optimum.</p>
Data from: An expanded Smithian-Spathian (Early Triassic) boundary from a reefal build-up record in Oman: Implications for conodont taxonomy, high-resolution biochronology and the carbon isotope record
<p><span>Some 2.7 Ma after the Permian-Triassic boundary mass extinction (PTME), a stepwise extinction of the nekton (ammonoids and conodonts) ended at the Smithian-Spathian boundary (SSB) during an episode of climate cooling. SSB records from continental shelves are usually affected by an unconformity, suggesting a forced regression of glacio-eustatic origin. Here, we document a new 30 m-thick SSB section from Jebel Aweri (Batain Plain, Oman) that provides an exceptionally complete and expanded record preserved in an exotic block. Most of this SSB section consists of metazoan reefal build-ups that formed in shallow water on an offshore sea mount. In Wadi Musjah (Hawasina nappes, Oman), another exotic block records the SSB in a deeper water setting represented by Hallstatt-type facies. These two sections provide a unique perspective on the early Spathian rapid re-diversification of conodonts. They led to a thorough revision of conodont taxonomy around the SSB and to the construction of the highest resolution biochronological scheme for this time interval in the Tethys. A total of five SSB sections from Oman representing both offshore sea mounts and lower slope deposits were included in a high-resolution, quantitative Unitary Associations analysis. The resulting 8 conodont biozones are intercalibrated with ammonoid zones and with the carbonate carbon isotope record ultimately placing the SSB in the interval of separation between UAZ<sub>3</sub> and UAZ<sub>4</sub>. Only the association of <em>Nv. pingdingshanensis</em> with <em>Ic. crassatus</em> can be used to unambiguously characterize the base of the Spathian.</span></p>
Data from: Conodont size, trophic level and the evolution of platform elements.
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Data from: An expanded Smithian-Spathian (Early Triassic) boundary from a reefal build-up record in Oman: Implications for conodont taxonomy, high-resolution biochronology and the carbon isotope record
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Data from: Evolution of the conodont Diplognathodus ellesmerensis from D. benderi sp. nov. at the Bashkirian-Moscovian (Lower-Middle Pennsylvanian) boundary in South China
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Data from: Spatiotemporal dynamics of Nektonic biodiversity and vegetation shifts during the Smithian–Spathian Transition: Conodont and Palynomorph insights from Svalbard
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Patterns of bilateral asymmetry and allometry in Late Devonian Polygnathus conodonts
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Dataset and script to: Morphometric variance, evolutionary constraints and their change through time in Late Devonian Palmatolepis conodonts
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Data from: Morphometric analysis of the conodont Chiosella timorensis (Nogami) from the early Anisian of Romania and China, and its significance for the definition of the Olenekian-Anisian Boundary
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Data from: Ontogenetic variability in crystallography and mosaicity of conodont apatite: Implications for microstructure, paleothermometry and geochemistry
<p>X-ray diffraction data from Silurian conodonts belonging to various developmental stages of the species <i>Dapsilodus obliquicostatus </i>demonstrate changes in crystallography and degree of nanocrystallite ordering (mosaicity) in both hyaline and albid crown tissue. The exclusive use of a single species in this study, combined with systematic testing of each element type at multiple locations, provided insight into microstructural and crystallographic differentiation between element position (S<sub>a</sub>, S<sub>b-c</sub>, M) as well as between juveniles and adults. A relative increase in the unit cell dimensions of the <i>a</i>-axis/<i>c</i>-axis ratio of nanocrystallites during growth was apparent in areas demonstrating single-crystal behavior but no such relationship was seen in dominantly polycrystalline areas. Systematic variations in mosaicity were identified, with mosaicity (as a proxy for disorder) increasing during growth, as well as along elements from tip to base. These results provide potential insight into the integrity of conodont apatite as a recorder of paleoseawater chemistry, as well as demonstrate the need to consider the influence of ontogeny and element position on the use of conodonts in paleothermometry and geochemical investigations. </p>
Data from: A review of the evolution, biostratigraphy, provincialism and diversity of Middle and early Late Triassic conodonts
The taxonomy, diversity, evolutionary lineages, and stratigraphical distributions of Middle and early Late Triassic conodonts are reviewed and re-evaluated. Twenty-five genera are recognized in the Middle and early Late Triassic, including a new genus cited in open nomenclature. Of these, 24 genera are assigned to two families and seven subfamilies. The family Gondolellidae consists of the subfamilies Cornudininae, Epigondolellinae, Neogondolellinae, Novispathodinae, Paragondolellinae and Pseudofurnishiinae. The family Gladigondolellidae is monotypic, consisting of the subfamily Gladigondolellinae. The genus Neostrachanognathus is not assigned to any family or subfamily as its origin is unclear. Conodont provincialism was low in the early Anisian, but from the late Anisian faunistic differences started to increase and became stronger during the early Ladinian, reaching a peak around the mid-Ladinian. Provincialism remained strong until the earliest Carnian and changed to an all-Triassic low in the early Tuvalian. The provincialism between North America and Tethys rebounded on the specific level during the late Tuvalian. Diversities on generic and specific levels have been established, and two major conodont diversity cycles are recognized: the first ranges from the Bithynian (early Anisian) to the Julian (late early Carnian), and the second is restricted to the Tuvalian (late Carnian).
Data from: Wear, tear and systematic repair: testing models of growth dynamics in conodonts with high-resolution imaging
Conodont elements are the earliest mineralised vertebrate dental tools and the only ones capable of extensive repair. Two models of conodont growth, as well as the presence of a larval stage, have been hypothesised. We analysed normally and pathologically developed elements to test these hypotheses and identified three ontogenetic stages characterised by different anisometric growth and morphology. The distinction of these stages is independently corroborated by differences in tissue strontium content. The onset of the last stage is marked by the appearance of wear resulting from mechanical food digestion. At least five episodes of damage and repair could be identified in the normally developed specimen. In the pathological element, function was compromised by development of abnormal denticles. This development can be reconstructed as addition of new growth centres out of the main growth axis during an episode of renewed growth. Our findings support the model of periodic retraction of elements and addition of new growth centres. Changes in strontium content coincident with distinct morphology and lack of wear in the early life stage indicate that conodonts might have assumed their mature feeding habit of predators or scavengers after an initial larval stage characterised by a different feeding mode.
Data from: Late Triassic (Julian) conodont biostratigraphy of a transition from reefal limestones to deep-water environments on the Cimmerian terranes (Taurus mountains, southern Turkey)
Sections at Aşağiyaylabel and Yukariyaylabel, Taurus Mountains, southern Turkey, provide a rare opportunity to investigate conodont faunas in detail across a reef to slope transition. Intensive sampling of limestone beds (wackestones to packstones) through approximately 3 m at these locations has led to the recognition of a new lower Carnian (Julian 1/2) conodont fauna within the Kartoz and Kasimlar formations. Members of the subfamilies Paragondolellinae and Pseudofurnishiinae are recognized. The genus Kraussodontus is reported for the first time from the Taurus Mountains. Mosherella postkockeli and Mosherella praebudaensis sp. nov. occur within the lower Carnian Carbonate Member of the Kasimlar Formation from the Taurus Platform Units. The discovery of the new conodont assemblages from Aşağiyaylabel and Yukariyaylabel facilitates a correlation with faunal assemblages worldwide.
Data from: Allometry in Anisian (Middle Triassic) segminiplanate conodonts and its implications for conodont taxonomy
Conodonts are a clade of chordates and are valuable indicator fossils for biostratigraphy. The segminiplanate (neogondolelliform) conodonts represent a major morphological group ranging from upper Carboniferous to Upper Triassic marine sediments. However, the morphological similarity of segminiplanate P1 elements generates problems for taxonomy, especially in the Permian and Triassic clades. This paper represents the first study of morphological variation in Triassic segminiplanate conodonts using a geometric morphometric approach. The laminar microstructures observed in conodont cross-sections indicate that, within our analysed specimens, smaller conodonts with fewer laminae are generally from an earlier ontogenetic stage while larger conodonts with more laminae are from a later stage of ontogeny. Using linear regressions between relative warp scores from both upper and lateral views and conodont length, we demonstrate strongly allometric growth patterns for the species Paragondolella bifurcata Budurov & Stefanov. Our results indicate that the species-group taxon Pg. praeszaboi bystrickyi (Kovacs et al.) is an early growth stage of Pg. bifurcata and thus synonymous. We suggest that the allometry of conodonts should be considered seriously, especially when there are numerous transitional morphologies between large- and small-sized conodonts. Reconstructing the ontogenetic series and using larger-sized conodonts within the numerous transitional morphologies in the population of a rock sample for the definition of new species are suggested for future studies.
Data from: Katian (Upper Ordovician) conodonts from Wales
Middle and Upper Katian conodonts are previously known in the British Isles from relatively small collections obtained from a few localities. The present study is mainly based on 17 samples containing more than 17,000 conodont elements from an approximately 14 m thick succession of the Sholeshook Limestone in a road cut near Whitland, South Wales that yielded a diverse fauna of more than 40 taxa. It is dominated by representatives of Amorphognathus, Aphelognathus/Plectodina, and Eocarniodus along with several coniform taxa. Representatives of Decoriconus, Istorinus and Sagittodontina are reported from the Ordovician of UK for the first time. The fauna is a typical representative of the British Province of the Atlantic Realm and includes a mixture of taxa of North American, Baltoscandic, and Mediterranean affinities along with pandemic species. Based on the presence of many elements of Amorphognathus ordovicicus and some morphologically advanced specimens of A. superbus, the Sholeshook Limestone is referred to the lower A. ordovicicus Zone. Most of the unit is also coeval with Zone 2 of the Cautleyan Stage in the British regional stage classification, and Stage Slice Ka3 of the middle Katian Stage in the global stratigraphical classification, an age assignment consistent with data from trilobites, graptolites, and chitinozoans. The unusually large collection of M elements of Amorphognathus provides insight into the complex morphological variation of this element of some Katian species of this genus. The Sholeshook conodont fauna is similar to those of the Crûg and Birdshill limestones but differs in several respects from the slightly older ones from the Caradocian type area in the Welsh Borderland. Although having some species in common, the Sholeshook conodont fauna clearly differs from coeval Baltoscandic faunas, and is even more different in composition compared with equivalent North American Midcontinent faunas.
Data from: Taxonomic and evolutionary pattern revisions resulting from geometric morphometric analysis of Pennsylvanian Neognathodus conodonts, Illinois Basin
Conodont fossils are highly valuable for Paleozoic biostratigraphy and for interpreting evolutionary change, but identifying and describing conodont morphologies, and characterizing gradual shape variation remain challenging. We used geometric morphometrics (GM) to conduct the first landmark-based morphometric analysis of the biostratigraphically useful conodont genus Neognathodus. Our objective is to assess whether previously defined morphotype groups are reliably distinct from one another. As such, we reevaluate patterns of morphologic change in Neognathodus P1elements, perform maximum likelihood tests of evolutionary modes, and construct novel, GM-based biozonations through a Desmoinesian (Middle Pennsylvanian) section in the Illinois Basin. Our GM results record the entire spectrum of shape variability among Neognathodus morphotypes thus alleviating the problem of documenting and classifying gradual morphologic transitions between morphotypes. Statistically distinct GM groups support previously established classifications of N. bassleri, N. bothrops, and N. roundyi. Statistically indistinct pairs of GM groups do not support literature designations of N. medadultimus and N. medexultimus, and N. dilatus and N. metanodosus, and we synonymize each pair. Maximum likelihood tests of evolutionary modes provide the first statistical assessment of Neognathodus evolutionary models in the Desmoinesian. The most likely evolutionary models are an unbiased random walk or a general random walk. We name four distinct biozones through the Desmoinesian using GM results and these align with previous biozonation structure based on the Neognathodus Index (NI) illustrating that Neognathodus-based biostratigraphic correlations would not change between GM or NI methods. The structural similarity between both biozonations showcases that determining GM-based biozones is not redundant, as this comparison validates using landmark-based GM work to construct viable biozonations for subsequent stratigraphic correlations. Although this study is limited to the Illinois Basin, our quantitative methodology can be broadly applied to additional genera to test taxonomic designations, interpret statistically-robust evolutionary patterns, and construct valid biozones for this significant chordate group.
PLATE 16 in Taxonomy and stratigraphic distribution of Lotagnostus (Agnostida: Agnostidae) and associated trilobites and conodonts in the Upper Cambrian (Furongian) of Laurentia
PLATE 16. Taxa from Hedinaspis-Charchaqia Fauna in the Hales Formation, Hot Creek section. Each white scale bar represents 2mm. 1. Lotagnostus nolani n. sp. Carapace (latex peel of external mold), USMN 775754, with Mendoparabolina nyensis, cephalon (counterpart of holotype), USMN 218571 (= Taylor, 1976, pl. 3, fig. 16), from D7130-CO, dorsal view, x7.8. 2, 3. Lotagnostus nolani n. sp. Cephalon, USMN 775755, from D7133-CO, dorsal and anterior views, x11.0. 4-5. Lotagnostus nolani n. sp. Cephalon, USMN 775756, from D7130-CO, dorsal and lateral views, x9.7. 6. Lotagnostus nolani n. sp. Pygidium, USMN 775757, from D7130-CO, dorsal view, x12.2. 7. Lotagnostus nolani n. sp., pygidium, USMN 775758, from D7130-CO, dorsal view, x10.3. 8. Pseudagnostus? sp., carapace, USMN 775759, from D7130-CO, dorsal view, x8.0. 9. Pseudagnostus? sp., carapace, USMN 775760, from D7133-CO, dorsal view, x8.3. 10. Mendoparabolina nyensis (Taylor, 1976), small cranidium, USMN 775761, from D7133- CO, dorsal, x14.3. 11. Mendoparabolina nyensis (Taylor, 1976), pygidium, USMN 775762, from D7130-CO, dorsal view, x7.5. 12. Lotagnostus sp., cephalon, USMN 775763, from D7130-CO, dorsal view, x16.8. 13. Ceratopygid undet., cranidium, USMN 775764, from D7129-CO, dorsal view, x3.9. 14. Lotagnostus sp., cephalon, USMN 775765, from D7130-CO, dorsal view, x8.6. 15. Lotagnostus sp., pygidium, USMN 775766, from D7131-CO, dorsal view, x4.4. 16. Lotagnostus sp., pygidium, USMN 775767, from D7130-CO, dorsal view, x6.5. 17. Ceratopygid undet., pygidium, USMN 775768, from D7129-CO, dorsal view, x2.6.
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