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Fig. 4. 50 in A new Eliomys from the Late Miocene of Spain and its implications for the phylogeny of the genus

Fig. 4. 50% majority rule consensus of the seven most parsimonious trees (L = 21, retention index = 0.619, consistency index = 0.619) resulting from the phylogenetic analysis. Numbers next to clades indicate the percentage of most parsimonious trees in which the clade was recovered. The extant glirid Dryomys nitedula, a form closely related to Eliomys, was chosen as outgroup.

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Fig. 3 in A new Eliomys from the Late Miocene of Spain and its implications for the phylogeny of the genus

Fig. 3. Comparison of length and width measurements (in mm) of p4 (A), P4 (B), m1, m2 (C), M1, M2 (D), m3 (E), and M3 (F) of Eliomys truci from Aljezar B, Hautimagne, Los Mansuetos, Orrios, Sarrión, Sete, Villalba Alta (Adrover 1986), Concud 2 and 3, Concud Barranco de los Calaveros, Los Mansuetos, Masada del Valle 2, 5 and 7, Tortojada A and C (Weerd 1976), DHS-1 and 16, PUR-23, 24, and 25A, OTU-1, TCH-1B and 13 (García-Alix et al. 2008a), Negratín-1 (Minwer-Barakat et al. 2009); Moreda 1A, 1B, Rambla Seca 1 (Castillo 1990) and Puente Minero (Alcalá et al. 1991); Eliomys yevesi sp. nov. from VVm-A, B, BC, C, and D, ABS-3A, AF-1'06, AF-1'07, CLC-3B, and PUR-4; Eliomys intermedius from Arquillo 3, Sete, Orrios 3, Villalba Alta (Adrover 1986), Escorihuela, Orrios (Weerd 1976), PUR-13, TCH-1 and 1B, TCH3, TCH-13 (García-Alix et al. 2008), Moreda 1A, 1B, Bélmez 1 and Rambla Seca A1 and A2 (Castillo 1990) and Alozaina (Aguilar et al. 1993); Eliomys quercinus from Vallparadís and Cal Guardiola (Minwer-Barakat et al. 2011, Baños de Mula (Agustí et al. 1990), Peña de Estebanvela (Sesé 2006b), Valdocarros (Sesé et al. 2011), Sima de los Huesos (Cuenca-Bescós et al. 1997), Bois Roche (Sesé and Villa 2008), Santenay (Chaline 1972); and Eliomys aff. quercinus from Huétor Tájar 1 and 8.

opencc-by-4.0Nov 2014View details →

Fig. 2 in A new brittle star from the early Carboniferous of Poland and its implications on Paleozoic modern-type ophiuroid systematics

Fig. 2. Ophiurin brittle star Aganaster jagiellonicus sp. nov. from the upper Tournaisian to lower Visean (lower Carboniferous) Mazurowe Doły Formation, Rudawa Group of Czatkowice quarry, Dębnik Massif, southern Poland; MZUJ T/0282, holotype. A. General view of the specimen, exposing the ventral side (also illustrated by O'Hara et al. 2014). B. Oral skeleton. C. Detail of the oral skeleton; photograph (C1), interpretative drawing (C2). D. Detail of basal arm segments; photograph (D1), interpretative drawing (D2).

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Fig. 1 in A new brittle star from the early Carboniferous of Poland and its implications on Paleozoic modern-type ophiuroid systematics

Fig. 1. Geographical position of the investigated specimen (map after Salata 2013, with modifications).

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Fig. 3 in A new brittle star from the early Carboniferous of Poland and its implications on Paleozoic modern-type ophiuroid systematics

Fig. 3. Ophiurin brittle star Aganaster jagiellonicus sp. nov. from the upper Tournaisian to lower Visean (lower Carboniferous) Mazurowe Doły Formation, Rudawa Group of Czatkowice quarry, Dębnik Massif, southern Poland; MZUJ T/0282, holotype. Detail of ventral side (A); median arm segments, showing the transition from between-plate tentacle pores to within-plate tentacle pores (B); median arm segments in ventro-lateral view (C); proximal arm segments in dorso-lateral view (D).

Fig. 3 in Composite Phymatoderma from Neogene deep-marine deposits in Japan: Implications for Phanerozoic benthic interactions between burrows and the trace-makers of Chondrites and Phycosiphon

Fig. 3. Composite Phymatoderma burrows from the Shiramazu Formation, Hiraiso section, Chiba Prefecture, central Japan. A, B. Phymatoderma reworked by Chondrites. Phymatoderma tunnels with dark gray-colored scoriaceous infill reworked by white-colored Chondrites (arrows). C, D. Phymatoderma reworked by Phycosiphon. Even within the pelletal infill of Phymatoderma, cores (white arrows) and surrounding mantles (black arrows) of Phycosiphon are sometimes clearly recognized (C). Field photos; A, B, parallel to the bedding plane; C, obliquely cut vertical cross-sectional view; D, vertical cross-sectional view. Scale bars 10 mm.

Fig. 4 in Composite Phymatoderma from Neogene deep-marine deposits in Japan: Implications for Phanerozoic benthic interactions between burrows and the trace-makers of Chondrites and Phycosiphon

Fig. 4. Schematic diagram showing the measured parameters. DCh, burrow diameter of Chondrites; DPc, burrow (i.e., central core) diameter of Phycosiphon; DPm, burrow diameter of Phymatoderma; PWmax, maximum pellet width; X and Y are the numbers of measured specimens, X ranges from 4–10, Y from 2–37.

Fig. 6 in Composite Phymatoderma from Neogene deep-marine deposits in Japan: Implications for Phanerozoic benthic interactions between burrows and the trace-makers of Chondrites and Phycosiphon

Fig. 6. Scatter plots showing the relationships between Phymatoderma burrow diameter and its maximum pellet width (black plot) and reworking trace-fossil diameter. A. Chondrites. B. Phycosiphon. Note that diameters of both ichnogenera that reworked Phymatoderma tunnels are within the size-range of them occurring in the host siltstone (shade), although pellet width increases with increasing Phymatoderma burrow diameter. D Ch, burrow diameter of Chondrites; D Pc, burrow (i.e., central core) diameter of Phycosiphon; D Pm, burrow diameter of Phymatoderma; PW max, maximum pellet width; n, number of measured burrows.

Fig. 5 in Composite Phymatoderma from Neogene deep-marine deposits in Japan: Implications for Phanerozoic benthic interactions between burrows and the trace-makers of Chondrites and Phycosiphon

Fig. 5. Size distributions of Phymatoderma from the Shiramazu Formation. A. Non-reworked Phymatoderma. B. Phymatoderma reworked by Chondrites. C. Phymatoderma reworked by Phycosiphon. D. Comparison of burrow diameter between non-reworked Phymatoderma, and tunnels reworked by Chondrites and Phycosiphon. Note that Phymatoderma reworked by Phycosiphon has significantly larger size. n, number of measured burrows.

opencc-by-4.0Dec 2009View details →

Fig. 1. A in Crustacean microcoprolites from the Upper Jurassic- Lower Cretaceous of the Neuquén Basin, Argentina: Systematics and biostratigraphic implications

Fig. 1. A. Location map of the Neuquén Basin with study localities and a stratigraphic chart of the Mendoza Group. 1, Tres Esquinas; 2, Loncoche creek; 3–4, Bardas Blancas; 5, Rahue creek; 6, Yeso creek; 7, Cara Cura range. B. Microcoprolites distribution in the Vaca Muerta Formation. Ammonite Zonation according to Aguirre−Urreta et al. (2008) and Riccardi (2008).

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Fig. 2 in Crustacean microcoprolites from the Upper Jurassic- Lower Cretaceous of the Neuquén Basin, Argentina: Systematics and biostratigraphic implications

Fig. 2. Transversal section of crustacean microcoprolites from the Vaca Muerta Formation. A. Palaxius azulensis Kietzmann isp. nov. (CPBA−N° 20675, early Valanginian, Rahue creek). B. Palaxius caracuraensis Kietzmann isp. nov. (CPBA−N° 20689, late Tithonian, Cara Cura range). C. Helicerina? isp. A aff. Helicerina siciliana Senowbari−Daryan, Schäfer, and Catalano, 1979 (CPBA−N° 20675, early Valanginian, Rahue creek). D. Helicerina isp. B (CPBA−N° 20675, early Valanginian, Rahue creek).

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Fig. 3 in Crustacean microcoprolites from the Upper Jurassic- Lower Cretaceous of the Neuquén Basin, Argentina: Systematics and biostratigraphic implications

Fig. 3. Schematic diagrams of the different ichnospecies of Palaxius and Helicerina mentioned in this work (Modified from Blau and Grün (2000), not to scale). A. Palaxius ichnospecies with 4 canals: Palaxius caucaensis (A1), P. kumaensis (A2), P. salataensis (A3), P. tetraochetarius (A4), P. osaensis (A5), and P. azulensis Kietzmann isp. nov (A6). B. Palaxius ichnospecies with 10 canals: Palaxius colombiensis (B1), P. decaochetarius (B2), P. habanensis (B3), P. decemlunulatus (B4), P. decemporatus (B5), and P. caracuraensis Kietzmann isp. nov. (B6). C. Helicerina ichnospecies with simple canals: Helicerina siciliana (C1), H. alata (C2), H. spinosa (C3), H. keuperiana (C4), and Helicerina isp. A aff. H. siciliana (C5). D. Helicerina isp. with multiple canals: Helicerina ruttei (D1), H. kainachensis (D2), H. kalakyra (D3), and Helicerina isp. B (D4).

opencc-by-4.0Jun 2010View details →

Fig. 1 in The platacanthomyine rodent Neocometes from the Miocene of South Korea and its paleobiogeographical implications

Fig. 1. Location of Tertiary basins in South Korea (A) and geologic map of the Bukpyeong area (B), indicating the Jiga−dong site (arrow): (1) Yangnam Basin, (2) Pohang Basin, (3) Yeonghae Basin, (4) Bukpyeong Basin.

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Fig. 2 in The platacanthomyine rodent Neocometes from the Miocene of South Korea and its paleobiogeographical implications

Fig. 2. Platacanthomyine rodent Neocometes aff. similis from the Miocene Bukpyeong Formation, South Korea. KIGAM VP 200315, left first lower molar in lingual (A), labial (B), occlusal (C) views; D, dental terminology used in the text. Abbreviations: Ald, anterolophid; Atr (= Vqs), anterior transversal extra ridge (= "Vorderer Quersporn"); End, entoconid; Hyd, hypoconid; Mald, metalophid; Med, metaconid; Meld, mesolophid; Msd, mesoconid; Pad, paraconid; Pld, posterolophid; Prd, protoconid; Ptr, posterior transverse extra ridge; Ia, I, II, III, and IV, synclines (= anterofossette, parafossette, mesofossette, metafossette, and posterofossette, respectively).

Fig. 5 in The castorid Steneofiber from NW Germany and its implications for the taxonomy of Miocene beavers

Fig. 5. Cheek teeth of the castorid Steneofiber depereti from the middle Miocene of Hambach 6C, northwestern Germany. DP4 in occlusal view: IPB−HaH 5166 (A); P4 in occlusal view: IPB−HaH 5088 (B), IPB−HaH 6374 (C), IPB−HaH 6376 (D), IPB−HaH 6380 (E); M1/2 in occlusal view: IPB−HaH 5102 (F), IPB−HaH 6377 (G), IPB−HaH 6383 (H), IPB−HaH 6384 (I), IPB−HaH 6385 (J), IPB−HaH 6401 (K); M3 in occlusal view: IPB−HaH 5101 (L), IPB−HaH 6390 (M), IPB−HaH 5165 (N); dp4 in occlusal view: IPB−HaH 6392 (O), IPB−HaH 6393 (P), IPB−HaH 6394 (Q); p4 in occlusal view: IPB−HaH 6396 (R), IPB−HaH 6397 (S), IPB−HaH 6440 (T); m1/2 in occlusal view: IPB−HaH 5043 (U); P4 in lingual view: IPB−HaH 6375 (V); M3 in labial view: IPB−HaH 5165 (W); dp4 in lingual view: IPB−HaH 6394 (X); p4 in labial view: IPB−HaH 6396 (Y), IPB−HaH 6440 (Z), IPB−HaH 6397 (AA); m1/2 in lingual view: IPB−HaH 5043 (AB).

Fig. 2 in The castorid Steneofiber from NW Germany and its implications for the taxonomy of Miocene beavers

Fig. 2. Mandibles of the castorid Steneofiber depereti from the middle Miocene of Hambach 6C, northwestern Germany. A. IPB−HaH 6409 in lingual (A1) and labial (A2) views. B. IPB−HaH 5149 in labial (B1), lingual (B2), ventral (B3), and posterior (B4) views; B5, tooth row in occlusal view. C. IPB−HaH 5167, tooth row in occlusal view.

Fig. 6 in The castorid Steneofiber from NW Germany and its implications for the taxonomy of Miocene beavers

Fig. 6. Occlusal pattern of upper cheek teeth of the castorid Steneofiber depereti from the middle Miocene of Hambach 6C, northwestern Germany. Deciduous tooth (A), premolars (B–G), molars (H–S); left DP4, IPB−HaH 5166 (A); right P4, IPB−HaH 6376 (B); left P4, IPB−HaH 6375 (C); left P4, IPB−HaH 6374 (D); left P4, IPB−HaH 6378 (E); left P4, IPB−HaH 5088 (F); left P4, IPB−HaH 6380 (G); left M1/2, IPB−HaH 6388 (H); left M1/2, IPB−HaH 6387 (I); right M1/2, IPB−HaH 6377 (J); left M1/2, IPB−HaH 6382 (K); right M1/2, IPB−HaH 5109 (L); right M1/2, IPB−HaH 5107 (M); right M1/2, IPB−HaH 6386 (N); left M1/2, IPB−HaH 6401 (O); right M3, IPB−HaH 6391 (P); left M3, IPB−HaH 6389 (Q); right M3, IPB−HaH 5101 (R); left M3, IPB−HaH 6390 (S).

Fig. 4 in The castorid Steneofiber from NW Germany and its implications for the taxonomy of Miocene beavers

Fig. 4. Occlusal pattern of lower cheek teeth of the castorid Steneofiber depereti from the middle Miocene of Hambach 6C, northwestern Germany. Mandibular tooth rows (A–E), deciduous teeth (F, G), premolars (H–J), molars (K–R); left p4–m3, IPB−HaH 6408 (A); right p4–m3, IPB−HaH 6409 (B); left p4–m3, IPB−HaH 5149 (C); right m1–m3, IPB−HaH 5150 (D); left p4–m2, IPB−HaH 5167 (E); left dp4, IPB−HaH 6392 (F); right dp4, IPB−HaH 6393 (G); right p4, IPB−HaH 6396 (H); right p4, IPB−HaH 6395 (I); left p4, IPB−HaH 6397 (J); left m1/2, IPB−HaH 6399 (K); right m1/2, IPB−HaH 5100 (L); right m1/2, slightly worn with a lingually open metaflexid, IPB−HaH 5043 (M); right m1/2, IPB−HaH 5106 (N); right m1/2, IPB−HaH 6400 (O); right m3, IPB−HaH 5110 (P); left m3, IPB−HaH 6404 (Q); right m3, IPB−HaH 6402 (R).

Fig. 3 in The castorid Steneofiber from NW Germany and its implications for the taxonomy of Miocene beavers

Fig. 3. Incisors of the castorid Steneofiber depereti from the middle Miocene of Hambach 6C, northwestern Germany. A. Tip of right I (IPB−HaH 6418) in oblique−lateral (A1) and lingual (A2) views. B. Tip of left I (IPB−HaH 6419) in lateral view.

Fig. 8 in The castorid Steneofiber from NW Germany and its implications for the taxonomy of Miocene beavers

Fig. 8. Lengths of mandibular tooth rows of Steneofiber depereti from the middle Miocene of Hambach 6C, in comparison to other representatives of the genus from early and middle Miocene localities in France, and in comparison to representatives of Chalicomys. For St. Gérand and Hambach are both given the lengths of occlusal surfaces and the alveole lengths. Data for Steneofiber castorinus and S. depereti from Artenay (marked with *) from Stefen (2005), for subspecies of S. depereti in the Loire Basin from Hugueney (1999), for "Chalicomys" batalleri from Casanovas−Vilar et al. (2008), and for Chalicomys jaegeri from Kaup (1833) and Ünay (1976).