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Fig. 6 in A new Y-shaped trace fossil attributed to upogebiid crustaceans from Early Pleistocene of Italy

Fig. 6. Trace fossils associated with Parmaichnus stironensis. They penetrate from the discontinuity surface in the Quaternary sediments of the Stirone section. A–C. Thalassinoides cf. paradoxicus (Woodward, 1830). D. Pyritised tube indicated by arrow.

Fig. 5. Different Y in A new Y-shaped trace fossil attributed to upogebiid crustaceans from Early Pleistocene of Italy

Fig. 5. Different Y−shaped trace fossils (B, D, G, U) and Recent burrows compared to Parmaichnus stironensis (P–S). Redrawn from photographs. A. After Seike and Nara (2007: fig. 3c). B. Holotype of Psilonichnus upsilon, Hanna Bay, San Salvador, Bahamas, from AU photograph. C. After Bruce (1987: fig. 6). D. After Fürsich (1981: pl. 3: 2). E. After Curran and Frey (1977: pl. 1e). F. After Frey (1968: text−fig. 1). G. After Seilacher (1990: fig. 5D). H. After Dworschak (2004: fig. 2B); arrows point the turning chambers. I. After Swinbanks and Luternauer (1987: fig. 2.1). J. After Ott et al. (1976: pl. 1: 2). K. After Ott et al. (1976: pl. 1: 3). L. After Dworschak et al. (2006: fig. 1A). M. After Nash et al. (1984: pl. 2a); see also Bromley (1996: fig. 4.32). N. After Curran and Martin (2003: fig. 6). O. After Asgaard et al. (1997: fig. 6). P–S. Parmaichnus stironensis igen. nov. et isp. nov. P. Holotype, ING UJ 200P11, see also Fig. 3. Q. P1070193, see also Fig. 4B. R. P1070182, see also Fig. 4A. S. P1070196, see also Fig. 4D. T. After Atkinson and Taylor (1991: fig. 1f). U. Psilonichnus tubiformis, after Fürsich (1981: pl. 1: 1).

Fig. 2 in A new Y-shaped trace fossil attributed to upogebiid crustaceans from Early Pleistocene of Italy

Fig. 2. View of the Early Pleistocene part of the Stirone section (about 90 m), with the distinct unconformity in the middle (pointed by arrow) separating silts covered by sands.

Fig. 1. Location map and the geological section. A in A new Y-shaped trace fossil attributed to upogebiid crustaceans from Early Pleistocene of Italy

Fig. 1. Location map and the geological section. A. The study region on the map of Italy. B. Location of the study area. C. Location of the studied section. D. The studied section with indication of Parmaichnus stironensis igen. nov. et isp. nov.

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Fig. 4. Bioerosion trace Caulostrepsis. A. Specimen DZP−18422 in Biotic interaction between spionid polychaetes and bouchardiid brachiopods: Paleoecological, taphonomic and evolutionary implications

Fig. 4. Bioerosion trace Caulostrepsis. A. Specimen DZP−18422, ventral valve of Bouchardia rosea showing the typical morphology of Caulostrepsis. Note the well−developed central ridge, and the straight morphology of the trace. B, C. Specimens DZP−18423 and 18424, respectively. Note that the galleries are roughly straight, and not enlarged at their distal extremities. The apertural groove (arrow) is well marked. D. Specimen DZP−18425, dorsal valve, showing multiple (arrows), straight traces. E, F. X−ray images of the specimens DZP−18426 and 18427, respectively. Note the straight morphology of unabraded tubes and the apertural groove (arrow) in the specimen DZP−18427. Scale bars 5 mm.

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Fig. 2. Sketches illustrating anomiid and trace morphology. A in Centrichnus eccentricus revisited: A new view on anomiid bivalve bioerosion

Fig. 2. Sketches illustrating anomiid and trace morphology. A. Shell exterior of left valve. B. Shell interior of right valve. C. Morphological features and measured dimensions of Centrichnus eccentricus. D. Schematic cross section of a living anomiid attached to the substrate illustrating the position of etching traces (modified after Yamaguchi 1998).

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.

Fig. 4 in Paleobiology of the crustacean trace fossil Spongeliomorpha iberica in the Miocene of southeastern Spain

Fig. 4. Interpretative reconstruction of a Spongeliomorpha iberica burrow system. The morphology of the apertures is not known, here they are shown as a simple vertical shaft. Inset shows the bioglyph pattern with "Y"−shaped and transverse scratch marks.

Fig. 2. Crustacean trace fossil Spongeliomorpha iberica Saporta, 1887 in Paleobiology of the crustacean trace fossil Spongeliomorpha iberica in the Miocene of southeastern Spain

Fig. 2. Crustacean trace fossil Spongeliomorpha iberica Saporta, 1887 from the Miocene of La Muela de Maraón, Spain. A, B. Field sketches of burrow systems as seen in the sole of the limestone units. C. Sole of a limestone unit displaying a high density of burrows. D. Burrows penetrating into the underlying marls.

Fig. 3. Crustacean trace fossil Spongeliomorpha iberica Saporta, 1887 in Paleobiology of the crustacean trace fossil Spongeliomorpha iberica in the Miocene of southeastern Spain

Fig. 3. Crustacean trace fossil Spongeliomorpha iberica Saporta, 1887 from the Miocene of La Muela de Maraón, Spain. A. Field photograph showing a typical burrow termination with multiple acuminate blind tunnels. B. Tunnel displaying the characteristic rhomboidal bioglyph and an enlargement or alcove (UB−IC522). C. Specimen with a "Y"−branching point (UB−IC533). D. Burrow with strongly marked rhomboidal bioglyphs and less impressed transverse scratch marks in the lower part (UB−IC530). E. Specimen with thick Y−shaped and thin transverse bioglyphs (UUIC−2089)). F. Plasticine cast of a burrow displaying how the rhomboidal bioglyph is constituted by "Y"−shaped individual marks (UB−IC194. G. Detail of a burrow termination with two blind tunnels and exhibiting both types of scratch marks (UB−IC520).

Fig. 1 in Paleobiology of the crustacean trace fossil Spongeliomorpha iberica in the Miocene of southeastern Spain

Fig. 1. Geological setting of the study area. A. Geological map of the Betic Cordillera, modified from Sanz de Galdeano and Vera (1992). B. Geological map of the Muela de Maraón sector, modified from Jerez Mir et al. (1974) and Loiseau et al. (1990).

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Fig. 7. Trace element environmental proxies for the F–F in The Frasnian-Famennian events in a deep-shelf succession, Subpolar Urals: biotic, depositional, and geochemical records

Fig. 7. Trace element environmental proxies for the F–F transition in the Syv'yu River section. Bio−productivity tracers* are normalized according to Schmitzetal.(1997).DownwardarrowedtrendsarebasedonthesinglesampleCB99−222,located2.15mbelow;recognizedMo/Alenrichment,indicative of anoxic−sulfidic deposition, is shown as well. For explanations see Fig. 4.

FIGURE 5 in Hidden subsurface garden on own faeces - the trace fossil Tubulichnium rectum (Fischer-Ooster, 1858) from the Cretaceous-Palaeogene deep-sea sediments

FIGURE 5. Macroscopic and microscopic and SEM observations of Tubulichnium rectum (Fischer-Ooster, 1858) occurring in turbiditic sandstones of the Inoceramian Beds (Upper Cretaceous–Paleocene), Słopnice, Poland (1, 4-8) and turbiditic marls of the Pagliaro Formation (Paleocene), Italy (2, 3): 1, specimen with elevated edges and bent down roof as seen on upper bedding surface (INGUJ144P195); 2, 3, depressions of pellets in the burrow margin after pellets have been partly or completely removed (INGUJ196P36 and 38); 4, photomicrograph of transverse cross-section; note deformed laminae above the collapsed burrow; 5, 6, burrow margin showing depressions of pellets that have been removed by weathering; 7, part of split pellets in place consisting of clay minerals and siliciclastic silt grains; 8, outer part of a split pellet showing platy minerals oriented ±parallel to surface.

FIGURE 4 in Hidden subsurface garden on own faeces - the trace fossil Tubulichnium rectum (Fischer-Ooster, 1858) from the Cretaceous-Palaeogene deep-sea sediments

FIGURE 4. Tubulichnium rectum (Fischer-Ooster, 1858) on the lower bedding surfaces (1-3) of and in longitudinal (4) and transverse (5-10) cross-sections of turbiditic sandstones from the Inoceramian Beds (Upper-Cretaceous-Paleocene) at Słopnice: 1, note external and internal parts INGUJ144P176; 2, note sandy mantle covering the pelleted part, INGUJ144P193a, 3, note wrinkles on the mantle, INGUJ144P187a; 4, longitudinal cross section (Tr), INGUJ144P193; 5-10, transverse sections, E – INGUJ144P182d, F – INGUJ144P180, G – INGUJ144P192b, H – INGUJ144P170a, I – INGUJ144P190, J – INGUJ144P192c, K – INGUJ144P192.

FIGURE 3 in Hidden subsurface garden on own faeces - the trace fossil Tubulichnium rectum (Fischer-Ooster, 1858) from the Cretaceous-Palaeogene deep-sea sediments

FIGURE 3. Tubulichnium rectum (Fischer-Ooster, 1858) on upper bedding surfaces from different formations: 1, on the upper surface of turbiditic marl with Chondrites intricatus (Chi), Pagliaro Formation (Paleocene), Cabella Ligure, Northern Apennines, Italy, field photograph; 2, curved example of T. rectum (Tr), Scolicia isp. (Sc) and Phycosiphon incertum (Ph), Ropianka Formation (Upper Cretaceous), Wara, Skole Nappe, Carpathians, Poland, UJTF 1426, Książkiewicz collection; 3, several specimens of T. rectum (Tr), some cross cut by Chondrites intricatus (Chi), Pagliaro Formation (Paleocene), Cabella Ligure, Northern Apennines, Italy, field photograph; 4, specimen with two (1, 2) superimposed pellet pavements. Inoceramian Beds (Upper Cretaceous-Paleocene), Słopnice, INGUJ144P190a; 5; specimens with elevated edges and collapsed roof, Inoceramian Beds (Upper Cretaceous-Paleocene), Słopnice, INGUJ144P140; 6, example of spindle-shaped burrow enlargement, Pagliaro Formation (Paleocene), Cabella Ligure, Northern Apennines, Italy, field photograph; 7, T. rectum cut by Ophiomorpha annulata (Oa), Inoceramian Beds (Upper Cretaceous-Paleocene), Słopnice, INGUJ143P66.

FIGURE 6 in Hidden subsurface garden on own faeces - the trace fossil Tubulichnium rectum (Fischer-Ooster, 1858) from the Cretaceous-Palaeogene deep-sea sediments

FIGURE 6. Short sections showing position of Tubulichnium rectum and associated traces fossils in strata of the Ropianka Formation (Inoceramian Beds) at Słopnice, Magura Nappe, Carpathians, Poland. GPS coordinates: section A: 49°42.982'N, 020°20.448'E; section B: 49°42.974'N, 20°20.453'E, section C: 49°42.610'N, 20°20.687'E.

FIGURE 7 in Hidden subsurface garden on own faeces - the trace fossil Tubulichnium rectum (Fischer-Ooster, 1858) from the Cretaceous-Palaeogene deep-sea sediments

FIGURE 7. Stratigraphic range of Tubulichnium rectum (Fischer-Ooster, 1858) and number of formations per stage in which it occurs.