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Fig. 2 in The cephalopods of the Boda Limestone, Late Ordovician, of Dalarna, Sweden
Fig. 2. Polished median section of a fragment of a phragmocone of Geisonoceras wegelini (Angelin in Angelin & Lindström, 1880) comb. nov., PMU 26747, Unskarsheden. The chamber is filled with epiand hypsoseptal deposits (a), a layered wackestone with bird's eye structures (b), a concentration of ostracods (c) and a sparitic space (d). Picture on the right is detail of picture on the left. Left scale = 10 mm, right scale = 1 mm.
Fig. 16 in The cephalopods of the Boda Limestone, Late Ordovician, of Dalarna, Sweden
Fig. 16. Dawsonoceratidae and Proteoceratidae of the Boda Limestone. A-B. Dawsonoceras fenestratum (Eichwald, 1860), Kallholn. A. PMU 26702, nearly mature specimen with adorally decreasing angle of expansion. B. PMU 26712, juvenile specimen. C. Gorbyoceras sp. A, PMU 26772, Osmundsberget. D. Goryboceras sp. B, PMU 26773, Kallholn. E. Dawsonoceras stumburi sp. nov., PMU 26717, holotype, Kallholn. F. Gorbyoceras alternestriatum (Strand, 1934) comb. nov., PMU 26771, Unskarsheden. Scale bars: A-C, E = 10 mm; D = 10 mm; F = 10 mm.
Fig. 3 in The cephalopods of the Boda Limestone, Late Ordovician, of Dalarna, Sweden
Fig. 3. Variation in relative siphuncle size, position and angle of expansion in Cameroceras hasta (Eichwald, 1860) (grey points) and Cameroceras turrisoides sp. nov. SPR = the minimum distance of the connecting ring from the conch margin, divided by the corresponding conch height.
Fig. 7 in The cephalopods of the Boda Limestone, Late Ordovician, of Dalarna, Sweden
Fig. 7. Breviconic cephalopods of the Boda Limestone and details of an endocerid. A. Dalecarlioceras constrictum Frye, 1987, PMU 24777, holotype, Kallholn. B. Dalecarlioceras dalecarlicum (Frye, 1987) comb. nov., PMU 24774, holotype, Kallholn. C. Cyrtorizoceras thorslundi sp. nov., PMU 26658, Kallholn; note the morphological transition between D. constrictum and C. thorslundi sp. nov.; the adult size increases in Dalecarlioceras and the mature body chamber is gibbous. D. Cameroceras turrisoides sp. nov., PMU 26623, Osmundberget, lateral view of apical fragment with abrupt transition between embryonic and juvenile conch. E. Strandoceras sphinx (Schmidt, 1858), PMU 26629, Kallholn. Scale bars: A-C, E = 10 mm; D = 10 mm.
Fig. 18 in The cephalopods of the Boda Limestone, Late Ordovician, of Dalarna, Sweden
Fig. 18. Shell ornamentation of selected Cephalopoda of the Boda Formation. A. Order, gen. et sp. indet., PMU 26950, Kallholn, lateral view. B. Palaeodawsonocerina? nicolletoides sp. nov., PMU 26727, holotype, Kallholn. C. Palaeodawsonocerina senckenbergi (Teichert, 1930), PMU 26718, Kallholn. D. Geisonoceras wegelini (Angelin in Angelin & Lindström, 1880) comb. nov., PMU 26745, Unskarsheden. E. Pleurorthoceras osmundsbergense sp. nov., NRM-PZ Mo 150126, holotype, Osmundsberget. F. Warburgoceras longitudinale (Angelin in Angelin & Lindström, 1880) comb. nov., NRM-PZ Mo 154065, Unskarsheden. G. Redpathoceras depressum sp. nov., PMU 26931, Kallholn. Scale bar = 5 mm for all figures.
Fig. 21 in The cephalopods of the Boda Limestone, Late Ordovician, of Dalarna, Sweden
Fig. 21. Reconstruction of the details of the septal necks and connecting ring of Nathorstoceras sp. nov., Kallholn, Boda Limestone. A. Nathorstoceras kallholnense sp. nov., PMU 26729, holotype. B. Nathorstoceras adnatum sp. nov., PMU 26733, holotype.
FIGURE 1 in Diverse endobiotic symbiont fauna from the late Katian (Late Ordovician) of Estonia
FIGURE 1. Map illustrating the exposure of the Ordovician in Estonia and location of studied localities. 1- Saxby North, 2- Saxby, 3- Hosholm, 4- Paluküla, 5- Vohilaid, 6- Sutlema.
Fig. 11. Heliolitine tabulate coral Acdalopora sokolovi Bondarenko, 1958 in Early Katian, Late Ordovician, heliolitine corals from southern Kuruktag in northeastern Tarim Basin of China
Fig. 11. Heliolitine tabulate coral Acdalopora sokolovi Bondarenko, 1958, from the Yuanbaoshan Formation (lower Katian) of southern Kuruktag, Tarim Basin, Northwest China. A. NIGP 201009. A1, A2, transverse sections. A3, longitudinal section. B. NIGP 201008. B1, B2, transverse sections. B3, longitudinal section.
FIGURE 2 in Revision of the Early Ordovician (late Tremadocian; Stairsian) cheirurid trilobite Tesselacauda Ross, with species from the Great Basin, western USA
FIGURE 2.
Text-fig. 4. Palaeogeographical reconstruction of the Katian (after Popov et al. 2011, modified) showing geographical distribution of the Middle and Late Ordovician craniides and craniopsides. White arrow = Boda Event expansion of craniiates and craniopsides to Perunica; black arrow = Hirnantian low-latitude expansion of the Hirnantia Fauna. in Lingulate And Craniate Brachiopods From The Top Of The Králův Dvůr Formation (Latest Katian) And Their Contribution To Palaeogeography
Text-fig. 4. Palaeogeographical reconstruction of the Katian (after Popov et al. 2011, modified) showing geographical distribution of the Middle and Late Ordovician craniides and craniopsides. White arrow = Boda Event expansion of craniiates and craniopsides to Perunica; black arrow = Hirnantian low-latitude expansion of the Hirnantia Fauna.
Data from: Evolutionary and biogeographical shifts in response to the Late Ordovician mass extinction
The Late Ordovician mass extinction was an interval of high extinction with inferred low ecological selectivity, resulting in little change in community structure after the event. In contrast, the mass extinction may have fundamentally changed evolutionary dynamics in the surviving groups. We investigated the phylogenetic relationships among strophomenoid brachiopods, a diverse brachiopod superfamily that was a primary component of Ordovician ecosystems. Four Ordovician families/subfamilies sampled in the analysis (Rafinesquinidae, Strophomeninae, Glyptomenidae and Furcitellinae) were reconstructed as monophyletic groups, and the base of the strophomenoid clade that dominated the Silurian recovery was reconstructed as diversifying alongside these families during the Middle Ordovician. We time‐calibrated the phylogeny and used geographical occurrences to investigate biogeographical changes in the strophomenoids through time with the R package BiogeoBEARS. Our results indicate that extinction was higher in taxa whose ranges were constrained to tropical or subtropical regions. Furthermore, our results suggest important shifts in the diversification patterns of these brachiopods after the mass extinction. While most of the strophomenoid families survived the Late Ordovician event, ecologically abundant taxonomic groups during the Ordovician were either driven to extinction, reduced in diversity, or slowly died off during the Silurian. The new abundant strophomenoid taxa derived from one clade (consisting of Silurian–Devonian groups such as Douvillinidae, Strophodontidae and Amphistrophiidae) that diversified during the post‐extinction radiation. Our results suggest the selective diversification during the Silurian radiation, rather than selective extinction in the Late Ordovician, had a greater impact on the evolutionary history of strophomenoid brachiopods.
Figure 20. A–E in Middle to Late Ordovician (Darriwilian-Sandbian) Conodonts from the Dawangou Section, Kalpin Area of the Tarim Basin, Northwestern China
Figure 20. A–E, Protopanderodus cooperi (Sweet & Bergström, 1962), from the Pratt Ferry Formation of Alabama. A–C, M element, OSU 52802, from the topotype locality, A–B, posterior views (IY170-024, IY170-025), C, anterior view (IY171-011). D–E, Sb element, OSU 52803, from the topotype locality, D, outer lateral view (IY171-012), E, inner lateral view (IY170-023). F–L, Protopanderodus varicostatus (Sweet & Bergström, 1962); from the Pratt Ferry Formation of Alabama. F–H, M2 element, OSU 52804, topotype, sample 64B2-12 from the top bed of the formation, F–G, posterior views (IY170-002, Iy170-001), F, anterior view (IY171-015); I–J, M2 element, OSU 52805 from the topotype locality, I, posterior view (IY170-007), J, anterior view (IY171-018). K–L, M1 element, OSU 52806, topotype, sample 64B2-12 from the top bed of the formation, K, posterior view (170-026), L, anterior view (IY171-013). Scale bars 100 µm.
FIG. 1 in Statistical comparisons of late Caradoc (Ordovician) brachiopod faunas around the Iapetus Ocean, and terranes located around Australia, Kazakhstan and China
FIG. 1. — Reconstructions for Mid-Ordovician (460 Ma) times. Redrawn from: A, Scotese (2002); B, Golonka (2002); C, Cocks & Fortey (2002) amended by Fortey & Cocks (2003); D, Rong et al. (1999).
FIGURE 4 in Morphological features of Late Ordovician (Sandbian) bryozoans from the basin of Khrevitsa River (north-western Russia) and description of a new species of the genus Prophyllodictya Gorjunova, 1987
FIGURE 4. Phylogenetic relationships of the genus Prophyllodictya Gorjunova, 1987
Data from: Identifying the most surprising victims of mass extinction events: an example using Late Ordovician brachiopods
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Data from: Evolutionary and biogeographical shifts in response to the Late Ordovician mass extinction
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Data from: Phylogenetic clustering of origination and extinction across the Late Ordovician mass extinction
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Data from: Effects of mass extinction and recovery dynamics on long-term evolutionary trends: a morphological study of Strophomenida (Brachiopoda) across the Late Ordovician mass extinction
Mass extinctions affect the history of life by decimating existing diversity and ecological structure and creating new evolutionary and ecological pathways. Both the loss of diversity during these events and the rebound in diversity following extinction had a profound effect on Phanerozoic evolutionary trends. Phylogenetic trees can be used to robustly assess the evolutionary implications of extinction and origination. We examine both extinction and origination during the Late Ordovician mass extinction. This mass extinction was the second largest in terms of taxonomic loss but did not appear to radically alter Paleozoic marine assemblages. We focus on the brachiopod order Strophomenida, whose evolutionary relationships have been recently revised, to explore the disconnect between the processes that drive taxonomic loss and those that restructure ecological communities. A possible explanation for this disconnect is if extinction and origination were random with respect to morphology. We define morphospace using principal coordinate analysis (PCO) of character data from 61 Ordovician-Devonian taxa and their 45 ancestral nodes, defined by a most parsimonius reconstruction in Mesquite. A bootstrap of the centroid of PCO values indicates that genera were randomly removed from morphospace by the Late Ordovician mass extinction, and new Silurian genera were clustered within a smaller previously unoccupied region of morphospace. Diversification remained morphologically constrained throughout the Silurian and into the Devonian. This suggests that the recovery from the Late Ordovician mass extinction resulted in a long-term shift in strophomenide evolution. More broadly, recovery intervals may hold clues to understanding the evolutionary impact of mass extinctions.
Data from: Effects of mass extinction and recovery dynamics on long-term evolutionary trends: a morphological study of Strophomenida (Brachiopoda) across the Late Ordovician mass extinction
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PLATE 10. Tesselacauda morrisoni n in Revision of the Early Ordovician (late Tremadocian; Stairsian) cheirurid trilobite Tesselacauda Ross, with species from the Great Basin, western USA
PLATE 10. Tesselacauda morrisoni n. sp., from Section MME 49.8 m, Fillmore Formation (upper Tremadocian; Stairsian; Rossaspis leboni Zone), Middle Mountain, Ibex area, Millard County, western Utah, USA. 1, 2, 4. Cranidium, SUI 147569, dorsal, right lateral, and anterior views, x10. 3, 5, 6. Cranidium, SUI 147570, dorsal, left lateral, and anterior views, x15. 7, 8, 11. Cranidium, SUI 147571, dorsal, right lateral, and anterior views, x15. 9, 13, 16. Cranidium, SUI 147572, dorsal, anterior, and left lateral views, x17. 10, 12, 14. Cranidium, SUI 147573, dorsal, left lateral, and anterior views, x15. 15. Left librigena, SUI 147574, external view, x12. 17, 20. Left librigena, SUI 147575, external and internal views, x12. 18, 21. Right librigena, SUI 147576, external and ventrolateral views, x12. 19, 22. Left librigena, SUI 147577, external and internal views, x12. 23. Left librigena, SUI 147578, external view, x12.
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