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84 results for “Upper Ordovician”
Fig. 1 in Pyritized tube feet in a protasterid ophiuroid from the Upper Ordovician of Kentucky, U.S.A.
Fig. 1. Protasterina flexuosa (Miller and Dyer, 1878), Edenian (Upper Ordovician) near Covington, Kentucky. Specimen with pyritized tube feet, CMC 25001. A. Fragmented specimen originally figured by Ulrich (1878), ventral, photographed on sand for support. B. Disk, and proximal portions of arms, small disk spines are visible along edges. C. Mouth frame, note depressions on mouth angle plates, and preserved buccal tentacles (arrows); possible remains of small spines visible on abradial edge of one of the mouth angle plates (circle). D. Madreporite. E. Two podial basins with remnants of pyritized tube feet. F. Ventral surface of ambulacrals and podial basins without pyritized tube feet; proximal ends of groove spines preserved, laterals attach to ambulacrals via an elongated process. G. Dorsal surface of ambulacrals with large interambulacral muscle gaps. H. Section of arm bearing numerous remnants of tube feet; note groove spines on laterals.
Fig. 2 in The earliest known Kinnella, an orthide brachiopod from the Upper Ordovician of Manitoulin Island, Ontario, Canada
Fig. 2. Stratigraphic position of Kinnella laurentiana sp. nov. British graptolite zonation follows Webby, Cooper et al. (2004). North American graptolite and Atlantic faunal region conodont zonations and correlations are based on Bergström and Mitchell (1986), McCracken and Nowlan (1988), Melchin et al. (1991) and Goldman and Bergström (1997). Chitinozoan zonation from Achab (1989) and Asselin et al. (2004). Manitoulin Island graptolite species ranges from Goldman and Bergström (1997). Correlation of Pusgillian–Cautleyan and equivalent graptolite zones is based on the assumption that the Amorphognathus superbus–A. ordovicicus zonal boundary is not significantly diachronous globally. NA St., North American Stage; Se., Series; St., Stage. Graptolite genera: A., Amplexograptus; C., Climacograptus; G., Geniculograptus; O., Orthograptus; R., Rectograptus.
Fig. 3 in The earliest known Kinnella, an orthide brachiopod from the Upper Ordovician of Manitoulin Island, Ontario, Canada
Fig. 3. Orthide brachiopod Kinnella laurentiana sp. nov.; Kagawong Submember, upper Georgian Bay Formation, Richmondian (mid−Ashgill), Manitoulin Island. A. GSC 117898, paratype, dorsal (A1), ventral (A2), lateral (A3), posterior (A4), anterior (A5), and enlarged (A6) costae. B. GSC 117899, holotype, dorsal (B1), ventral (B2), lateral (B3), posterior (B4), anterior (B5), and enlarged (B6) delthyrium. C. GSC 117900, paratype, dorsal (C1), ventral (C2), lateral (C3), posterior (C4), and anterior (C5) views. D. GSC 117901, paratype, dorsal (D1), lateral (D2), and posterior (D3) views of immature shell. E. GSC 117902, paratype, dorsal (E1) and lateral (E2) views of immature shell, showing nearly catacline ventral interea.
Fig. 1 in The earliest known Kinnella, an orthide brachiopod from the Upper Ordovician of Manitoulin Island, Ontario, Canada
Fig. 1. Map of Manitoulin Island showing the localities of Kinnella laurentiana sp. nov. in the lower Kagawong Submember, upper Georgian Bay Formation. Dark shaded region corresponds to the outcrop belt of the Kagawong Submember.
Fig. 6 in The earliest known Kinnella, an orthide brachiopod from the Upper Ordovician of Manitoulin Island, Ontario, Canada
Fig. 6. Cluster analysis of Kinnella−bearing brachiopod faunas worldwide. Software: PAST (Hammer et al. 2001; Hammer and Harper 2005); algorithm: unweighted pair−group; Raup−Crick similarity coefficient. Refer to Appendix 1 for identification of assemblage localities, published sources and taxa employed in the analysis.
Fig. 4 in The earliest known Kinnella, an orthide brachiopod from the Upper Ordovician of Manitoulin Island, Ontario, Canada
Fig. 4. Plot of measurements of 50 conjoined shells of Kinnella laurentiana sp. nov.; Kagawong Submember, upper Georgian Bay Formation, Richmondian (mid−Ashgill), Manitoulin Island. Note the largely isometric shell outline (consistent length/width ratio) and convexity (thickness/width ratio) with ontogeny.
Fig. 5 in The earliest known Kinnella, an orthide brachiopod from the Upper Ordovician of Manitoulin Island, Ontario, Canada
Fig. 5. Orthide brachiopod Kinnella laurentiana sp. nov.; Kagawong Submember, upper Georgian Bay Formation, Richmondian (mid−Ashgill), Manitoulin Island. A. GSC 117903, paratype, various views of interior of ventral valve (A1) showing dental plates (A2) and large interarea (A3). B. GSC 117904, paratype, interior of ventral valve. C. GSC 117905, paratype, interior of ventral valve (C1) showing dental plates and muscle field (C2). D. GSC 117906, paratype, interior of dorsal valve (D1), with details of cardinalia and adductor muscle scars (D2 and D3). E. GSC 117907, paratype, interior of dorsal valve, with relatively strong median ridge. F. GSC 117908, paratype, interior of dorsal valve (F1), with crenulated, anteriorly swollen cardinal process (F2).
FIG. 8 in New Monticuliporidae (Bryozoa, Trepostomata) from the Cystoid Limestone Formation (Upper Ordovician) of the Iberian Chains (NE Spain)
FIG. 8. — Monticuliporidae sp. indet., MPZ 2006/110: A, longitudinal thin section showing the large acanthostyles (ac), the peculiar cystiphragms (cy), and the narrow mesozooecia (mz); B, tangential thin section showing the regular hexagonal autozooecia (az) with wall sections having gently beaded (bd) outline, the mesozooecia (mz) in an area where hexagonal autozooecia are not so regular, and large acanthostyles (ac); C, a high-magnification detail of the longitudinal section of an acanthostyle (ac) showing the central lumen on the lower part of the figure and lamination around the lumen; D, a high-magnification detail of the cross section of an acanthostyle (ac) showing the light coloured central lumen (lu) and surrounding dark lamina. Scale bars: A, B, 1 mm; C, D, 0.1 mm.
FIG. 1 in New Monticuliporidae (Bryozoa, Trepostomata) from the Cystoid Limestone Formation (Upper Ordovician) of the Iberian Chains (NE Spain)
FIG. 1. — Outcrops of Ordovician rocks in the Eastern Iberian Chain and their location in the Iberian Peninsula. The lower rectangle marks the location of the study area and measured sections. 1, Valdelaparra; 2, La Peña del Tormo.
FIG. 4. — Monticulipora cystiphragmata n in New Monticuliporidae (Bryozoa, Trepostomata) from the Cystoid Limestone Formation (Upper Ordovician) of the Iberian Chains (NE Spain)
FIG. 4. — Monticulipora cystiphragmata n. sp., schematic tangential section of the holotype (MPZ 2006/134). It shows the disposition of the square- and triangular-shaped mesozooecia (mz), the location of acanthostyles (ac), and the autozooecial aperture shape (az). Scale bar: 0.1 mm.
FIG. 3. — A-D, Monticulipora cystiphragmata n in New Monticuliporidae (Bryozoa, Trepostomata) from the Cystoid Limestone Formation (Upper Ordovician) of the Iberian Chains (NE Spain)
FIG. 3. — A-D, Monticulipora cystiphragmata n. sp.; A, C, longitudinal thin sections of the holotype (MPZ 2006/134) and paratype (MPZ 2006/132),respectively,showing the autozooecia (az), the large cystiphragms (cy) joined in some cases to the opposite wall by diaphragms (dp), and the narrow mesozooecia (mz); B, D, tangential thin sections of the holotype and the same paratype as in C showing square and triangular mesozooecia (mz) in B, and the cystiphragms (cy) cross sections inside autozooecial (az) sections in D; E, F, Monticulipora kolaluensis Jaroshinskaja,1962, MPZ 2006/109; E, longitudinal thin section showing the stylolitic contact with another monticuliporid bryozoan; F, tangential thin section showing the macular autozooecia (maz), the mesozooecia (mz), the acanthostyles (ac) in the common vertex of three autozooecia, and a cross section of a cystiphragm (cy) inside an autozooecial (az) section. Scale bars: 1 mm.
FIG. 2 in New Monticuliporidae (Bryozoa, Trepostomata) from the Cystoid Limestone Formation (Upper Ordovician) of the Iberian Chains (NE Spain)
FIG. 2. — Stratigraphic columns of the Cystoid Limestone Formation: A, Valdelaparra section; B, La Peña del Tormo section. The horizons where bryozoans were collected are marked with a double head arrow in A and with an asterisk in B. Scale bars: A, 10 m; B, 1 m.
FIG. 7. — Prasopora spjeldnaesi n in New Monticuliporidae (Bryozoa, Trepostomata) from the Cystoid Limestone Formation (Upper Ordovician) of the Iberian Chains (NE Spain)
FIG. 7. — Prasopora spjeldnaesi n. sp., schematic longitudinal section showing the shape and distribution of autozooecial (az) cystiphragms (cy) and diaphragms (dp) and a group of densely tabulate mesozooecia (mz) with diaphragms at the same level. In 1 a large mesozooecium divides to form two smaller mesozooecia. Scale bar: 1 mm.
FIG. 5. — A, B in New Monticuliporidae (Bryozoa, Trepostomata) from the Cystoid Limestone Formation (Upper Ordovician) of the Iberian Chains (NE Spain)
FIG. 5. — A, B, Monticulipora kolaluensis Jaroshinskaja, 1962, MPZ 2006/109, longitudinal thin sections; A, area of the zoarium with large cystiphragms (cy) attached to one side of the autozooecial (az) wall that are joined to the opposite wall by diaphragms (dp); B, an area with smaller cystiphragms (cy) located in both sides of the wall as single rows or isolated; C-E, Prasopora carnica Vinassa de Regny, 1915, MPZ 2006/113; C, longitudinal thin section showing the autozooecia (az), the cystiphragms (cy), and the mesozooecia (mz); D, E, two tangential thin sections separated by less than 3 mm and in the same depth of the colony; D, the autozooecia (az) are completely surrounded by mesozooecia (mz); E, the autozooecia (az) are in contact with other autozooecia in most part of their outline, having two cystiphragms (cy) inside, and scarce mesozooecia (mz); F, Prasopora spjeldnaesi n. sp., MPZ 2006/99, basal surface showing the concentrically wrinkled base and the initial point of growth of the zoarium (ipg). Scale bars: 1 mm.
FIG. 10 in New Monticuliporidae (Bryozoa, Trepostomata) from the Cystoid Limestone Formation (Upper Ordovician) of the Iberian Chains (NE Spain)
FIG. 10.— Monticuliporidae sp. indet.,schematic longitudinal section showing a prominent acanthostyle (ac), the shape of diaphragms (dp), cystiphragms (cy) and autozooecial tubes (az), as well as the narrow mesozooecia (mz). Scale bar: 0.1 mm.
FIG. 6. — Prasopora spjeldnaesi n in New Monticuliporidae (Bryozoa, Trepostomata) from the Cystoid Limestone Formation (Upper Ordovician) of the Iberian Chains (NE Spain)
FIG. 6. — Prasopora spjeldnaesi n. sp., holotype (MPZ 2006/99): A, general view of the colony; B, surface of the colony showing autozooecia (az) completely surrounded by mesozooecia (mz), and a cross section of a cystiphragm (cy) inside an autozooecial aperture; C, tangential thin section with abundant mesozooecia (mz) completely isolating autozooecia (az); D, longitudinal thin section showing the autozooecia (az) and mesozooecia (mz) as well as the peculiar cystiphragms (cy); E, a group of mesozooecia (mz) with their diaphragms (dp) at the same level forming a square network. Scale bars: 1 mm.
Text-fig. 2. (A) Orientation of Schizocrania filosa (HALL, 1847) on articulated shells of benthic brachiopod Rafinesquina sp. (A1–A3 – on dorsal valve of articulated shells, A4 – on ventral valve of articulated shell; forward growth direction is unclear in three specimens) from Upper Ordovician, Corryville Formation, Lawrenceburg, Indiana (after www.drydredgers.org/scizo.htm). (B) Orientation of Schizocrania multistriata (REED, 1905) shells on outer face of conulariid Metaconularia imperialis test (Dobrotivá Formation, Kařízek mine, Barrandian area; after Havlíček and Vaněk 1996); preserved conulariid shell in white, suggested outline of incomplete conulariid test in grey. Arrows indicate direction of forward growth of Schizocrania specimens. in Schizocrania (Brachiopoda, Discinoidea): Taxonomy, Occurrence, Ecology And History Of The Earliest Epizoan Lingulate Brachiopod
Text-fig. 2. (A) Orientation of Schizocrania filosa (HALL, 1847) on articulated shells of benthic brachiopod Rafinesquina sp. (A1–A3 – on dorsal valve of articulated shells, A4 – on ventral valve of articulated shell; forward growth direction is unclear in three specimens) from Upper Ordovician, Corryville Formation, Lawrenceburg, Indiana (after www.drydredgers.org/scizo.htm). (B) Orientation of Schizocrania multistriata (REED, 1905) shells on outer face of conulariid Metaconularia imperialis test (Dobrotivá Formation, Kařízek mine, Barrandian area; after Havlíček and Vaněk 1996); preserved conulariid shell in white, suggested outline of incomplete conulariid test in grey. Arrows indicate direction of forward growth of Schizocrania specimens.
Text-fig. 5. Ichnofabric and tiering models for the Loděnice – vinice locality. in Early Complex Tiering Pattern: Upper Ordovician, Barrandian Area, The Czech Republic
Text-fig. 5. Ichnofabric and tiering models for the Loděnice – vinice locality.
Text-fig. 2. Schematic map of the Prague Basin with position of the Loděnice – vinice locality. in Early Complex Tiering Pattern: Upper Ordovician, Barrandian Area, The Czech Republic
Text-fig. 2. Schematic map of the Prague Basin with position of the Loděnice – vinice locality.
Data from: Evenness and diversity in Upper Cambrian – Lower Ordovician trilobite communities from the Central Andean Basin (Cordillera Oriental, Argentina)
Community evenness has recently received much attention, either because it is related to ecosystem functioning or because it may affect estimation of diversity. Temporal and environmental trends in diversity and evenness of trilobite communities during the Late Cambrian – Early Ordovician of the Cordillera Oriental (north-western Argentina) are here analysed. Richness and evenness increase through time in both deep subtidal (between fair-weather and storm wave base) and offshore (below storm wave base) communities. Two significant patterns are superimposed on this general trend: (1) the magnitude of the increase in evenness is much more pronounced in deep than in shallower settings, and (2) richness and evenness trajectories are decoupled (while a significant rise in evenness is recorded in the middle Tremadocian (Tr2), an increase in richness is delayed until the late Tremadocian (Tr3)). In contrast to expectations, a single family (Olenidae) is dominant in samples associated with this earlier rise in evenness relative to richness. Hence, this trend is explained neither by the number of families present in the communities nor by the familial identity of the most abundant taxon. Large-scale comparisons of the timing and geographical components of these trends are restricted to the patterns recognized in Laurentian North American studies. Results from the Cordillera Oriental mirror those of Laurentia regarding the rise in both metrics in deep marine settings. Nevertheless, the timing of this increase in richness and evenness is delayed in the Cordillera Oriental, supporting the idea that palaeogeographical regions differed in the nature and timing of ecological changes. Finally, the rise in trilobite alpha-diversity through the Late Cambrian – Early Ordovician of the Cordillera Oriental supports the idea that trilobite alpha-diversity did not decline worldwide, suggesting that the relative decline in trilobite alpha-diversity is most probably caused by the dilution effect.
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