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Fig. 8. Caulostrepsis, a in In vivo and post-mortem bioerosion traces in solitary corals from the upper Pliocene deposits of Tunisia

Fig. 8. Caulostrepsis, a domichnion produced by polychates, in the skeleton of caryophylliid coral Ceratotrochus (Edwardsotrochus) duodecimcostatus Goldfuss, 1826), from the El Melah stream section, the upper part of the Argiles de Sidi Barka Formation (upper Pliocene) of Tunisia. A. Caulostrepsis cretacea (Voigt, 1971), INGUJ265P156. B. Caulostrepsis taeniola Clarke, 1908 and Pinaceocladichnus onubensis Mayoral, 1988 (Pn), INGUJ265P154. C. Caulostrepsis avipes Bromley and D'Alessandro, 1983, INGUJ265P176. D. A cluster of Caulostrepsis taeniola Clarke, 1908, INGUJ265P162. E–G. Caulostrepsis penicillus isp. nov. E. INGUJ265P158 holotype (a), and paratype (b). F. INGUJ265P174 paratype. G. INGUJ265P172, partial views (G1, G2).

Fig. 7 in In vivo and post-mortem bioerosion traces in solitary corals from the upper Pliocene deposits of Tunisia

Fig. 7. Benthic foraminifera from upper Pliocene deposits in a tributary valley of the El Melah stream, north-east of Hammamet town, Tunisia. A. Uvigerina peregrina Cushman, 1923, (FSTDG22H2, sample H2). B. Melonis affinis (Reuss, 1851) (FSTDG22H11, sample H1), side (B1) and apertural (B2) views. C. Nonion commune (d'Orbigny, 1846) (FSTDG22H10, sample H10). D. Textularia conica d'Orbigny, 1839b, (FSTDG22H12, sample H1). E. Elphidium crispum (Linnaeus, 1758) (FSTDG22H25, sample H25). F. Ammonia beccarii (Linnaeus, 1758) (FSTDG22H201, sample H20). G. Neoconorbina terquemi (Rzehak, 1888) (FSTDG22H21, sample H21). H. Uvigerina mediterranean Hofker, 1932, (FSTDG22H17, sample H17). I. Bolivina dilatata Reuss, 1850, (FSTDG22H22, sample H2). J. Amphycoryna scalaris (Batsch, 1791) (FSTDG22H1, sample H17). K. Planulina ariminensis d'Orbigny, 1826, (FSTDG22H24, sample H2). L. Bulimina costata d'Orbigny, 1852, (FSTDG22H9, sample H9). M. Spiroloculina sp. (FSTDG22H72, sample H7). N. Bolivina punctata d'Orbigny, 1839c, (FSTDG22H241, sample H24).

Fig. 6 in In vivo and post-mortem bioerosion traces in solitary corals from the upper Pliocene deposits of Tunisia

Fig. 6. Planktonic foraminifera foraminifera from upper Pliocene deposits in a tributary valley of the El Melah stream, north-east of Hammamet town, Tunisia. A. Globigerina bulloides d'Orbigny, 1826, (FSTDG22H31, sample H3). B. Globigerinoides ruber (d'Orbigny, 1839b) (FSTDG22H21, sample H2). C. Globigerinoides extremus Bolli and Bermudez, 1965, FSTDG22H71, sample H7). D. Orbulina universa (d'Orbigny, 1839a) FSTDG22H181, sample H18). E. Globorotalia crassaformis (Galloway and Wissler, 1927) (FSTDG22H30, sample H30). F. Globorotalia puncticulata (Deshayes, 1832) (FSTDG22H17, sample H17).

Fig. 5 in In vivo and post-mortem bioerosion traces in solitary corals from the upper Pliocene deposits of Tunisia

Fig. 5. Structural features of the caryophylliid coral Ceratotrochus (Edwardsotrochus) duodecimcostatus (Goldfuss, 1826) coralla from upper Pliocene deposits in a tributary valley of the El Melah stream, north-east of Hammamet town, Tunisia. A. Virtual sections of INGUJ265P153 in lower (A1) and in more distal part (A2) of corallum. B. Thin-section 3/76 of INGUJ265P139 that shows nearly completely developed 5 cycles of septa. Positions of 10 S1 septa marked with black dots. C. Thin section 2/118 of INGUJ265P138, enlarged region of transversely sectioned corallum to show diverse pat- terns of mid-septal zone development (from zig-zag in S1, S2 septa to straight in S4 septa). D. Thin sections of INGUJ265P137, transverse (D1, thin section T1/8) and longitudinal (D2, thin section T1/9) sections to show some variability of septal cycle development (D1), and development of tabular dissepiments (D2). E. INGUJ265P188, distal (E1) and lateral (E2) views of specimen with major structural features indicated. F. Longitudinal thin section 5/29 of INGUJ265P136 with the boring Maeandropolydora sulcans Voigt, 1965. G. Virtual longitudinal section of INGUJ265P188 with the boring Maeandropolydora elegans Bromley and D'Alessandro, 1983.

Fig. 3 in In vivo and post-mortem bioerosion traces in solitary corals from the upper Pliocene deposits of Tunisia

Fig. 3. Lithological column of the Oued El Melah section with lithostratigraphic divisions, indications of samples, and field photographs of some fossiliferous levels.

Fig. 4 in In vivo and post-mortem bioerosion traces in solitary corals from the upper Pliocene deposits of Tunisia

Fig. 4. Exposures of the El Melah stream the section, upper part of the Argiles de Sidi Barka Formation (upper Pliocene) of Tunisia. A. Coral level III. General view (A1), close view of the sampling area (A2). B. The coral level II/coral level III boundary. C. Coral level II. General view (C1), close view of the sampling area (C2). D. General view of coral level I. Quadrangles indicate sampling areas.

Fig. 2 in In vivo and post-mortem bioerosion traces in solitary corals from the upper Pliocene deposits of Tunisia

Fig. 2. Lithostratigraphy and subdivision of the Neogene and Quaternary series of northern (A) and north-eastern Tunisia (B) (Burollet 1951; Colleuil 1976).

Fig. 1. A in In vivo and post-mortem bioerosion traces in solitary corals from the upper Pliocene deposits of Tunisia

Fig. 1. A. Location of the studied area in the north-eastern Tunisia and north Africa (inset). (Ben Ali and Gaaloul 2021). B. Detailed geological map of northern and north-eastern Tunisia (1:50000; National Mining Office of Tunisia) showing Pliocene marine deposits of the Hammamet area. S, study section.

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Fig. 3. Trace fossil Gyrochorte comosa Heer, 1865 in Gyrochorte "highways" and their environmental significance in shallow-marine sediments

Fig. 3. Trace fossil Gyrochorte comosa Heer, 1865 on bed surfaces structured by wave ripples; Mulichinco Formation, Lower Cretaceous, Puerto Curaco, Neuquén Province, Argentina (field photographs). A. Gyrochorte comosa on bed surface exhibiting parallel-crested, symmetric ripples. B. Parallelcrested, slightly asymmetric ripples traversed by G. comosa being more frequent at the stoss-side and the crest of the ripples. C. Bed surface structured by interfering symmetric ripples documenting sequorichnial behaviour of G. comosa producers (black arrows, "converging" traces; white arrows, "diverging" traces); note acute angle between diverging or converging traces. D. Bed surface exhibiting parallel-crested, slightly asymmetric ripples; G. comosa is overtopped by sand at the lee side of the ripples (white arrows). All specimens left in the field.

Fig. A4 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. A4: Cr (total, nlh and %nlh) per transect [transects are presented from west to east, (•) the outlier value symbol and numbers refer to the isobaths].

Fig. A3 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. A3: Mn (total, nlh and %nlh) per transect [transects are presented from west to east, (•) the outlier value symbol and numbers refer to the isobaths].

Fig. A5 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. A5: Total Cu, Pb and Zn and nlhZn per transect [transects are presented from west to east, (•) the outlier value symbol and numbers refer to the isobaths].

Fig. A2 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. A2: Al and Fe (total, nlh and %nlh) per transect [transects are presented from west to east, (•)the outlier value symbol and numbers refer to the isobaths].

Fig. 8 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. 8: Map showing the sampling stations in 1989 (referred by Poulos et al., 2009) (·) and those of the present investigation (x) over the bathymetry.

Fig. 7 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. 7: Spatial distribution of non-lattice held (nlh) metals in surficial seabed sediments (a: Fe; b: Zn; c: Mn; d: Cr).

Fig. 6 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. 6: Spatial distribution of total metal content in sediments (Al distribution is not presented, as it is similar to Fe) [a: Fe; b: Zn; c: Pb; d: Mn; e: Cu; f: Cr].

Fig. 5 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. 5: (a): Carbonate content box plots grouped by percent silt+clay, b) Carbonate content box plots per transect (west to east) [(•) outlier value symbol, (*) extreme value symbol, numbers refer to the isobaths].

Fig. 4 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. 4(a): Particulate Organic Carbon (POC) values box-plot grouped by percent silt+clay; (b): Particulate Organic Carbon (POC) values box-plot per transect (from west to east) [(•) outlier value symbol, numbers refer to the isobaths].

Fig. 3 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. 3: Texture map based on grain size analysis according to Folk 1974. [gmS: gravelly muddy Sand; S: Sand; zS: silty Sand; sZ: sandy Silt; Z:Silt; C: Clay; M: Mud (=silt+clay) and hc: closure depth in red].

Fig. 2 in Trace metal concentrations in the offshore surficial sediments of Heraklion Gulf (Crete Island, East Mediterranean Sea) Abstract

Fig. 2: Determination of the offshore zone (blue zone) by means of L/4 (according to Komar, 1976) for approaching waves of different wave lengths (L). Closure depth limit (hc) is also presented (12 m isobath).