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Fig. 4 in Taxonomic, biogeographic, and taphonomic reassessment of a large extinct species of paca from the Quaternary of Brazil

Fig. 4. Fossils of the extinct paca Cuniculus rugiceps (Lund, 1837) from Cuvieri Cave (minimum age of ~30 ky) (A, B) and modern specimen of Cuniculus paca Linnaeus, 1766 from Rio Grande do Sul (C). A. Fossil 7 (CVL3 P13160), cranial roof in dorsal (A1) and lateral (A3) views, detail (A2). B. Fossil 8 (CVL3 P13168), right zygomatic arch in dorsal (B1) and lateral (B2) views, detail (B3). C. MCN.D 207, skull in dorsal (C1) and lateral (C3) views, details (C2, C4).

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Fig. 5 in Taxonomic, biogeographic, and taphonomic reassessment of a large extinct species of paca from the Quaternary of Brazil

Fig. 5. Lower cheek teeth of the extinct paca Cuniculus rugiceps (Lund, 1837) from Cuvieri Cave (minimum age of ~30 ky). A1, B–F, ontogenetic sequence of cheek teeth. A. Fossil 6 (CVL3 P13344) (image inverted). A1, dp4–m2, the m3 is lacking due to fragmentation. A2, dentary in medial view showing p4 replacing the dp4 (arrow). B. Fossil 4 (CVL3 P13342) (image inverted), showing dp4–m3. C. Fossil 1 (CVL3 4052), showing the p4 erupting and the m3 completely functional. D. Fossil 5 (CVL3 P13145), showing p4–m3. E. Fossil 3 (CVL3 P13149), showing p4–m3. F. Fossil 2 (CVL3 P11221), showing p4–m3. G, H. Isolated molars from Toca de Cima dos Pilão deposits; in occlusal (G1, H1) and lingual (G2, H2) views. G. FUMDHAM 188-19036, possible right m3. H. FUMDHAM 188-19521, possible right m2.

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Fig. 2 in Youngest record of the extinct walrus Ontocetus emmonsi from the Early Pleistocene of South Carolina and a review of North Atlantic walrus biochronology

Fig. 2. Right canine tusk of odobenid walrus Ontocetus emmonsi (CCNHM 1144) from the Lower Pleistocene?Waccamaw Formation, Austin Sand Pit, South Carolina, in lingual (A), proximal (B), anterior (C), and labial (D) views.

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Fig. 1. A in Youngest record of the extinct walrus Ontocetus emmonsi from the Early Pleistocene of South Carolina and a review of North Atlantic walrus biochronology

Fig. 1. A. Map showing the location of South Carolina and Austin Sand Pit near Ridgeville in Dorchester County (asterisked). B. Generalized stratigraphic column of the Austin Sand Pit with biostratigraphically significant vertebrate fossils from the?Waccamaw Formation (C, D). Colors approximate sediments exposed in the Austin Sand Pit.

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Fig. 3 in Youngest record of the extinct walrus Ontocetus emmonsi from the Early Pleistocene of South Carolina and a review of North Atlantic walrus biochronology

Fig. 3. Scatterplot of ratio of proximal transverse width/anteroposterior length versus radius of the arc of curvature for tusks of Odobenus and Ontocetus, including CCNHM 1144. Original plot modified from Kohno and Ray (2008: fig. 27).

Fig. 5 in The Alvarez impact theory of mass extinction; limits to its applicability and the "great expectations syndrome"

Fig. 5. Evolving timing of the multi−ring Woodleigh impact structure, manifested in purported causal connection with the P–T and F–F mass extinctions, as a reflection of variously dated processes. Age constraints still range from post−Middle Devonian to pre−Early Jurassic, but the connection with the D–C global event seems to be most likely (Glikson et al. 2005).

Fig. 4 in The Alvarez impact theory of mass extinction; limits to its applicability and the "great expectations syndrome"

Fig. 4. Evolving timing of the Siljan Ring (53 km diameter; see Fig. 2), depending on different timescales and improved radiometric dates.

Fig. 3 in The Alvarez impact theory of mass extinction; limits to its applicability and the "great expectations syndrome"

Fig. 3. Extraterrestrial elemental proxy Ir, and supplementary Ni, against other geochemical markers in the F–F boundary beds at Kowala, Holy Cross Mountains (after Racki et al. 2002: fig. 8; used with permission from Elsevier); Ir values from an unpublished report (dated 2004) by Yuichi Hatsukawa and Mohammad Mahmudy Gharaie; Ni contents from Racka (1999: table 2); for other data see references in Racki et al. (2011).

Fig. 2 in The Alvarez impact theory of mass extinction; limits to its applicability and the "great expectations syndrome"

Fig. 2. Crater temporal distribution, with possible record at the F–F boundary (A), plotted against Devonian biodiversity losses in terms of substages (B), data from Bambach 2006: fig. 1 (used with permission from the Annual Review of Earth and Planetary Sciences, Volume 34 © 2006 by Annual Reviews, http://www.annualreviews.org.), re−arranged according to the timescale of Kaufman (2006; see the updated tiiming in Becker et al. 2012; Fig. 4); the reconstructed middle Frasnian Alamo crater is also shown to reveal low biodiversity loss in that time (arrowed), as well as the controversial Woodleigh impact structure (see Fig. 5) and the biostratigraphically dated Flynn Creek submarine crater (Schieber and Over 2005). Vertical lines correspond to possible temporal ranges. Abbreviations: Carb., Carboniferous; Givet., Givetian; Lochk., Lochkovian; Prag., Pragian; Silur, Silurian.

Fig. 1 in The Alvarez impact theory of mass extinction; limits to its applicability and the "great expectations syndrome"

Fig. 1. Scheme of the three successive levels in the testing process, encompassing application of the Alvarez impact theory of mass extinction, and possible errors resulting from the "great expectations syndrome" (sensu Tsujita 2001).

Fig. 6 in The Alvarez impact theory of mass extinction; limits to its applicability and the "great expectations syndrome"

Fig. 6. The Late Triassic cratering record plotted against extinction events (based on Lucas and Tanner 2008: fig. 8; crater dates modified after Schmieder and Buchner 2008 and Martin Schmieder personal communication, 2011) and two alternative time scales. Note that the 100 km−sized and precisely dated Manicouagan crater (214.56±0.05 Ma; see ottawa−rasc.ca/wiki/index.php?title=Odale−Articles− Manicouagan) is within the age range of the end−Carnian extinction only in the ICS 2009 geochronologic scheme (see also Lucas et al. 2012). Carbon isotope events compiled from Tanner (2010) and Ruhl and Kürschner (2011: fig.1). Vertical lines correspond to possible temporal ranges. J., Jurassic.

Fig. 3 in Mandible morphometrics, dental microwear pattern, and palaeobiology of the extinct Balearic Dormouse Hypnomys morpheus

Fig. 3. Shape differentiation of the mandible on the first two axes of the Principal Components Analysis (PCA) performed on Fourier coefficients of the mandibles. Outlines are reconstructed on the first two canonical axes, the light grey outline represents the maximum values of the axes, and the dark grey outline corresponds to extreme reconstruction.

Fig. 4 in Mandible morphometrics, dental microwear pattern, and palaeobiology of the extinct Balearic Dormouse Hypnomys morpheus

Fig. 4. Plot of the discriminant analysis of the shape coordinates (the first twelve PCS, i.e., 98% of the interspecific shape variance) versus geographic range.

Fig. 1 in Mandible morphometrics, dental microwear pattern, and palaeobiology of the extinct Balearic Dormouse Hypnomys morpheus

Fig. 1. Zygomasseteric construction in Balearic dormice. A. Skull of extant Eliomys quercinus ophiusae (MNHN1983−832) in lateral (A1) and anterior (A2) views. B. Skull of Hypnomys morpheus in lateral (B1) and anterior (B2) views. Arrows show the origin and the insertion of the lateral portions of the masseter. The skull of Hypnomys morpheus (B) corresponds to a reconstruction. Eliomys and Hypnomys are represented at the same scale. The map summarizes the evolutionary history of Balearic glirids—Hypnomys is a lineage derived from an Eliomys species isolated by the sea level rise that followed the Messinian salinity crisis, then Eliomys quercinus ophiusae followed the first human colonization (dashed arrow represents a hypothetical pathway of colonization).

Fig. 5 in Mandible morphometrics, dental microwear pattern, and palaeobiology of the extinct Balearic Dormouse Hypnomys morpheus

Fig. 5. Allometric relationship between the size (estimated from the square root of outline area) and the main shape signal (scores on the first principal components). The dashed line represents the linear regression between both variables for all extant glirids.

Fig. 6 in Mandible morphometrics, dental microwear pattern, and palaeobiology of the extinct Balearic Dormouse Hypnomys morpheus

Fig. 6. Digitized photographs of the protoconid of the second molars. A. Eliomys quercinus ophiusae (IMEDEA 7357), Formentera, Balearic Islands; extant specimen. B. Hypnomys morpheus (IMEDEA 63839), Cova Estreta, Pollença, Mallorca, Holocene. Note the higher number of fine scratches in Hypnomys.

Fig. 4 in A new Early Triassic gastropod genus and the recovery of gastropods from the Permian/Triassic extinction

Fig. 4. Werfenella rectecostata redrawn from Neri and Posenato (1985: pl. 3: 7, 8). This relatively large and undeformed steinkern (composite mould from Val Sorda, western Dolomites, Italy) shows the purpurinid shape of Werfenella and its obliquely elongated, subrectangular aperture. The axial ornament is visible while the nodular ornament at the carinations is obscured.

Fig. 2 in A new Early Triassic gastropod genus and the recovery of gastropods from the Permian/Triassic extinction

Fig. 2. Limestone slab with several specimens of Werfenella rectecostata; Werfen Formation, Cencenighe Member, Bad Radein/Redgano, Italian Dolomites, Weisshorn (MHI 1819). The specimens show unusually wellpreserved shells with a pronounced nodular ornament at the carinations which cannot be seen in the steinkern−preservation which is usual for gastropods from the Werfen Formation.

Fig. 1. A–F in A new Early Triassic gastropod genus and the recovery of gastropods from the Permian/Triassic extinction

Fig. 1. A–F. Werfenella rectecostata from the Early Triassic (Olenekian) Werfen Formation. A. Reproduction of Frech's (1912: pl. 7: 7a–c) illustrations of exceptionally well−preserved specimens of Werfenella rectecostata from the Tirolites−Marls near Csopak (Iszkahegy, Hungary). B. Reproduction of Hauer's (1851: pl. 20: 10) original illustrations of "Turbo" rectecostatus. C–F. Werfenella rectecostata in typical preservation as more or less deformed steinkerns. Despite poor preservation species identity is strongly suggested by the characteristic shape and traces of the axial ornament. C. NHMW 1865 IX 22, Heilig Kreuz near St. Cassian, Südtirol. D. NHMW 1858 IX 3A, Heilig Kreuz near St. Cassian, Südtirol. E. NHMW 1884 D 475, Pitzberg, Südtirol. F. BMNH G 9059314A, Fachiade Monzoni. G. Chartronella? pagina Batten and Stokes, 1986, from Batten and Stokes (1986: fig. 10); this species from the Olenekian of Utah resembles Werfenella rectecostata. H. Chartronella unicostata Batten and Stokes, 1986, from Batten and Stokes (1986: fig. 8). I. Chartronella diagonata Cossmann, 1902, topotype material of the type species of Chartronella from the lowermost Jurassic (Hettangian) of France (from Gründel 1997: pl. 2: 1, 2).

Fig. 3 in A new Early Triassic gastropod genus and the recovery of gastropods from the Permian/Triassic extinction

Fig. 3. Limestone slab with specimens of Werfenella rectecostata and Natiria costata forming a characteristic gastropod assemblage in the Werfen Formation; Werfen Formation, Cencenighe Member, Bad Radein/Redgano, Italian Dolomite, Weisshorn (MHI 1820).