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1 January 2008 A Giant Boring in a Silurian Stromatoporoid Analysed by Computer Tomography
Author Affiliations +
Abstract

This study describes the largest known Palaeozoic boring trace, Osprioneides kampto igen, et isp. nov., found within a stromatoporoid Densastroma pexisum from the Upper Visby Formation (lower Wenlock, Silurian) on the island of Gotland, Sweden. Differences between the physical properties of the stromatoporoid and the dense micritic infilling of the borings allowed the application of the CT-scan technology for the 2D and 3D-visualisation of this rare trace. The additional application of a stereoscopic technique on these CT images and movies enhances its value for unravelling spatial orientations. This non-destructive method has a great potential for future macro- as well as microboring analyses. The trace maker, most likely a worm, infested the hosting colony post-mortem with up to 120 mm long borings measuring 5–17 mm in diameter. Smaller forms of Trypanites and Palaeosabella within the same stromatoporoid preferentially occur in the outer coenosteum and occasionally in abandoned borings of O. kampto. The stratigraphic position of O. kampto follows the “Great Ordovician Biodiversification Event” in time, and reflects the increase in diversity of boring species. Borings with penetration depths of 120 mm are, however, unique findings for the Palaeozoic and were not exceeded until some 260 million years later (Bajocian, Middle Jurassic) when the “Mesozoic Marine Revolution” led to convergent reinventions as a result of enhanced predation, grazing pressure, and ecospace competition.

Introduction

During the Early Palaeozoic, major evolutionary adaptive radiations—referred to as the “Cambrian Explosion” (Gould 1989) and the “Great Ordovician Biodiversification Event” (Webby et al. 2004; Harper 2006)—produced a burst in marine invertebrate biodiversity. This general increase is also reflected in the ichnodiversity of trace fossils as indicated by the first appearance of many ichnogenera during the Ordovician (Kobluk et al. 1978; Mángano and Droser 2004). This trend holds especially true for borings in lithic substrates, where the “Ordovician Bioerosion Revolution” led to the appearance of many new ichnogenera in concert with a significant increase in the intensity of bioerosion (Ekdale and Bromley 2001; Bromley 2004; Wilson and Palmer 2006). However, even though the density of bioerosion was greatly enhanced, most macroborings were comparatively shallow, only rarely reaching 50 mm in penetration depth. In this context, we would like to present the unexpected finding of unusually large and deeply penetrating macroborings—a new ichnogenus presumably produced by a cavity-boring worm in a Silurian stromatoporoid.

Institutional abbreviation.

  • NRM, Naturhistoriska Riksmuseet, Stockholm, Sweden.

Material and methods

The stromatoporoid host.—One piece of the stromatoporoid Densastroma pexisum (Yavorsky, 1929) was found in the locality “Halls Huk 3” (see Laufeld 1974) on Gotland, Sweden (Fig. 1). This locality is situated ca. 4 km NE of the Hall church (Swedish Grid: 6425681/1674742, topographical map 66C Tingstäde). The specimen is in the collections of the Naturhistoriska Riksmuseet, Stockholm, Sweden (inventory number NRM-Cn 69062). The colony is 240 mm in diameter and with a maximal height of 175 mm in the central part of its coenosteum. The surface of the coenosteum is smooth but exhibits a high number of small pit holes filled with carbonate mud. The colony is high dome-shaped (sensu Kershaw 1990), and is broken along the vertical middle axis. Furthermore, the surface is partly broken off along the laminae. The fracture zones expose several endolithic traces of different size, all filled with fine carbonate mud.

CT scan analysis.—Computer Tomography (CT) was chosen for its direct, non-destructive characteristics and for analysing the spatial distribution of bodies with different densities and shapes within the stromatoporoid. A Siemens SOMATOM Sensation 64® in the Medical Solution Centre Forchheim, Germany, was used in this study. The data acquisition occurred at 140kV, 545 eff. mAs, 0.6 pitch and with an isotropic resolution of 1 mm. The spiral data set was visualised in syngo® CT.3D with 2D and 3D post-processing tools at the Institute for Medical Physics in Erlangen, Germany. The common view of acquired slices on a monitor is from caudal, resulting in a mirrored view. For the analysis of the borings, only the density range of the micritic fillings was imaged. CT scan analysis figures of this study were taken by Screenshots from the monitor and were not mirrored. For printable 3D visualisation, the stereoscopic technique was applied on selected images. Therefore, two images were superimposed intergrading in a perspective angle of 6°, were coloured in Adobe Photoshop® (red/blue) and one image was given a transparency of 50% for examination with anaglyph glasses (red-blue glasses). Additionally, three types of movies were produced: serial sections in 2D throughout the entire specimen were created from individual section images with an interval of 1 mm; rotating 3D sample movies were created from 360 serially produced images within syngo® CT.3D, showing the object from all possible angles in a defined rotation axis and movies created for anaglyph glasses were produced from the dataset of the latter by superimposing two movies with a six frame offset (equal to 6°). The conversion from images to movies was done with the software VideoMach® 3.1.7. The anaglyph technique for the 3D movies was undertaken in Adobe Premiere® 1.5 by colouring the individual movies (red/blue) and rendering the compound movie with a transparency of 50% of the upper one (see also Beuck et al. 2007). The movies are stored in the data repository of Acta Palaeontologica Polonica (see Supplementary Online Material at  http://app.pan.pl/acta53/app53-Beuck_etal_SOM.pdf).

Fig. 1.

Study area. A Overview showing the position of Gotland in the Baltic Sea. B. Geographic position of the “Halls Huk 3” locality. C. Field photograph indicating where the stromatoporoid specimen was found (arrow).

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Stable carbon isotope analysis.—In order to stratigraphically date the sample, δ13C carb analyses have been carried out on 5 micrite samples drilled from the fillings of three different borings. Carbonate powders were reacted with 100% phosphoric acid (density >1.9, Wachter and Hayes 1985) at 75°C using a Kiel III online carbonate preparation line connected to a ThermoFinnigan 252 mass-spectrometer at the Geological Institute in Erlangen (Germany). All values are reported in per mil relative to V-PDB by assigning a δ13C carb value of+1.95‰ to NBS19. Reproducibility was checked by replicate analysis of laboratory standards and is better than ± 0.02 (1s).

Results

Stratigraphie position.—The stromatoporoid was found at the locality termed “Halls Huk 3” (Fig. 1). This locality is characterised by an up to 30 m high cliff section. Just below modern sea level the Lower Visby Formation (uppermost Llandovery to lowermost Wenlock) crops out. The cliff itself comprises the Upper Visby Formation (lowermost Wenlock) in the lower part, and the Högklint Formation in the upper part (lower Wenlock). The Lower and Upper Visby Formations represent the oldest rocks on Gotland. They developed as a prograding limestone-marl alternation. The Lower Visby Formation was deposited below storm-wave base and below the photic zone in a distal shelf environment, whereas the overlying Upper Visby Formation was deposited in shallower water, probably between storm-wave base and fairweather wave base as indicated by an increased abundance of packstones and grainstones, ripple marks, and the occurrence of calcareous algae (Samtleben et al. 1996; Calner et al. 2004). The Upper Visby Formation contains numerous small decimeter-sized reef-mounds. The main reef builders are tabulate corals and stromatoporoids, but also rugose corals. The overlying Högklint Formation consists of coarse-grained bioclastic limestones rich in crinoids, trilobites, brachiopods, and molluscs. Abundant oncolites and oncolitic crusts indicate deposition well within the photic zone.

Since the stromatoporoid was found as a loose specimen at the foot of the cliff, the exact stratigraphic position was unknown. However, on Gotland—but also on a global scale—the Llandovery—Wenlock boundary is characterised by a pronounced positive shift in δ13Ccarb values (Samtleben et al. 1996), which can be correlated exactly with the conodont stratigraphy (Fig. 2; Jeppsson 1997; Munnecke et al. 2003). The mean δ13C carb value of+4.18‰ indicates a stratigraphic position within the upper part of the Lower Kockelella ranuliformis Conodont Zone, i.e., in the upper part of the Upper Visby Formation (Fig. 2).

Fig. 2.

A. Stable carbon isotope stratigraphy across the Silurian Lower/Upper Visby Formation boundary (metres according to the Ireviken type section; after Munnecke et al. 2003). B. Conodont stratigraphy after Jeppsson (1997). C. Formations on Gotland. D. Series. 513C carb data from micritic material indicate a stratigraphic position within the upper part of the Lower Kockelella ranuliformis Conodont Zone.

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Characterisation of the ichnocoenosis.—The surface of the investigated Densastroma pexisum is highly pitted by circular holes between 1 and 4 mm in diameter (Figs. 3, 4C). These are the apertures of borings referred to as ichnogenera Palaeosabella and Trypanites (see also Kershaw 1980). Both are cylindrical boring traces of up to few centimetres in length as seen in the fracture surface (Fig. 4D). Surface-boring density is very high and increases towards the apex of the host. Although most of these borings originated from the surface of the stromatoporoid, some traces were recognised deep within the host as revealed by CT scan analysis (Figs. 5B, D, F, 6C–F, 7C). Most prominent are, however, exceptionally large traces (Figs. 38), which we describe below as a new ichnospecies.

Systematic ichnology

(L. Beuck and M. Wisshak)

Ichnogenus Osprioneides Beuck and Wisshak, nov.

  • Type and only ichnospecies: Osprioneides kampto nov.

  • Derivation of the name: From Greek osprion, legume; -eides, alike.

  • Diagnosis.—Unbranched, elongate boring in lithic substrate with oval cross-section, single-entrance and straight, curved or irregular course.

  • Discussion.—The morphological characteristics of Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. are distinguished from the emended diagnosis of Trypanites Mägdefrau, 1932 as given by Bromley and D'Alessandro (1987) by being oval in cross-section and by being somewhat variable in width. In addition, Trypanites is generally smaller in dimension (the diameter of Trypanites weisei is usually only about 1 mm; Mägdefrau 1932; Bromley 1972), and the only ichnospecies reaching comparable penetration depths is T. fosteryeomani which is, however, always oriented vertical and has a smaller diameter (3.9–4.9 mm; Cole and Palmer 1999). The related ichnogenus Palaeosabella Clarke, 1921 is distinguished from Trypanites and Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. by widening towards its distal limit. Furthermore, Palaeosabella features a circular cross-section and is also commonly much smaller (e.g., Bromley 2004). The ichnogenus Gastrochaenolites Leymarie, 1842 is a clavate boring that may reach comparable penetration depths but exhibits an aperture size always significantly smaller than the traces maximum width, and it additionally shows lower length/width ratios (Kelly and Bromley 1984). There is some apparent affinity to Petroxestes pera Wilson and Palmer, 1988 where traces of O. kampto Beuck and Wisshak, igen, et isp. nov. are uncovered by erosion. Petroxestes is, in contrast, much longer than deep and is usually connected to the substrate surface along its entire length forming an elongated groove rather than a tubeshaped boring (Wilson and Palmer 1988; Tapanila and Copper 2002).

  • Fig. 3.

    Large stromatoporoid Densastroma pexisum from the Upper Visby Formation at “Halls Huk 3” of Gotland, Sweden, with multiple macroborings (dashed rectangles indicate close-ups illustrated in Fig. 4). A. Transverse fracture surface showing dense host skeleton with concentric growth laminae, and large Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. macroborings filled with a fine micrite matrix. B. Densely pitted, partly eroded surface of the stromatoporoid with numerous unroofed O. kampto Beuck and Wisshak, igen, et isp. nov. macroborings, occasionally truncating each other.

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    Fig. 4.

    Close-ups of the bored Densastroma pexisum stromatoporoid (positions indicated by dashed lines in Fig. 3). A. Undulating course of a deeply penetrating Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. in longitudinal section. B. Two unroofed O. kampto Beuck and Wisshak, igen, et isp. nov. specimen, one of which showing the growth increments of the host stromatoporoid on the boring walls where the micritic infill is eroded. Boring direction was from the eroded aperture at the right towards the left hand side. C. The densely pitted outer surface of the stromatoporoid showing circular apertures of Trypanites and Palaeosabella of various size. D. The nearby fracture surface, exposing longitudinal to oblique sections of small Trypanites and Palaeosabella borings. Scale bars 10 mm.

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    Osprioneides kampto Beuck and Wisshak, isp. nov. Fig. 38.

  • 1982 “Gekronkelde boring”; Stel and Stoep 1982:22–23, text-figs. 11, 12.

    1970 “Macroscopic borings”; Newall 1970: 337, pl. 1; 341, pl. 2.

    2001 Petroxestes pera Wilson and Palmer, 1988; Tapanila 2001: 90–91, pi. 3: 1–4.

    2001 Trypanites Mägdefrau, 1932; Tapanila 2001: 86–87, pl. 1: 3.

  • Derivation of the name: From Greek kampto, bent.

  • Holotype: Boring trace within the stromatoporoid Densastroma pexisum (NRM-Cn 69062) revealed by computer tomography (see Figs. 6G, 7B).

  • Type locality: “Halls Huk 3”, Gotland, Sweden.

  • Type horizon: Lower Kockelella ranuliformis Conodont Zone, Upper Visby Formation, lower Sheinwoodian, Wenlock, Gotland, Sweden.

  • Material.—Large Densastroma pexisum specimen (NRM-Cn 69062) with multiple borings including the holotype (Figs. 3, 4). Section of a small Densastroma cf. pexisum stromatoporoid (NRM-Cn 69063) found in the upper part of the Slite Group (locality “Odvalds 1”, “Pentamerus gothlandicus Beds”, Ozarkodina sagitta sagitta Conodont Zone, lower Homerian, Wenlock) in the Silurian of Gotland (Sweden) exhibiting one oblique oval cross-section of a boring (21 × 10 mm).

  • Diagnosis.—Large, straight to irregularly bent, unlined boring of variable length entering the substrate perpendicular to subparallel; cross-section oval; roughly constant oval diameter; terminus tapered to rounded.

  • Description.—From a single oval aperture, the unbranched borings are sharply incised in the dense host skeleton, showing no deflections of the host growth increments (Fig. 4A, B), and are filled with a micritic matrix (Figs. 3,4). The borings enter the substrate in a perpendicular to subparallel manner and follow primarily a straight course but may as well slightly curve or undulate (e.g., Fig 6C). Individual traces measure up to 120 mm in length (Fig. 5B) with an oval cross-section of averaging 7 (min. 5) × 13 (max. 17) mm in diameter, with a max/min ratio in excess of ½ (Fig. 6, 7). Individual borings have a tapered to rounded terminus (Fig. 6D, E). Due to the high-abundance of traces within the sample analysed, borings occasionally truncate each other, occasionally resembling a branching pattern (Figs. 5A, C–F, 6F). Neither scratch marks nor any internal lining were observed. An idealised schematic drawing of the trace is given in Fig. 8.

  • Discussion.—As for genus.

  • Stratigraphic and geographic range.—In the tabulate coral Heliolites interstinctus from the Aymestry Limestone in the Upper Silurian (Ludlow) of the Welsh Borderlands, Newall (1970: pls. 1, 2) describes a similar boring under the informal name “Macroscopic borings” having corresponding diameters but a maximum penetration depth of 42 mm (due to substrate limitation). Another occurrence was reported among other boring traces by Stel and Stoep (1982: fig. 12A, D) under the informal name “gekronkelde boring” found in the stromatoporoid Densastroma pexisum from the Visby Formation (Wenlock, Lower Silurian) at Ireviken on Gotland, Sweden. From the Lower Silurian (Llandovery) of Anticosti Island, eastern Canada, Tapanila (2001) and Tapanila et al. (2004) report large, vertical Trypanites borings in the tabulate coral ?Propora conferta and in stromatoporoids. The latter authors give a size range with a maximum length of 52.8 mm at a diameter of 9.5 mm, indicating an affinity to the present material. In addition, Tapanila (2001: pl. 3: 1–3) depicts large Petroxestes pera borings in the stromatoporoid Clathrodictyon which closely mirror unroofed Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. A boring tentatively attributed as ?Gastrochaenolithes (Tapanila 2001: pl. 3:4) possibly represents an obliquely sectioned specimen of the new ichnospecies. Furthermore, similar borings are found from the Silurian of Estonia by Olev Vinn (Mark Wilson, personal communication 2007).

    In summary, the known stratigraphical range of Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. is currently restricted to the Silurian (Llandovery—Ludlow), and the known host substrates comprise stromatoporoids and tabulate corals.

  • Fig. 5.

    Spatial distribution of traces (CT scan analysis). Cubes indicating the spatial orientation of sample based on medical terms; grey-dashed lines indicate further virtual sections that have been visualised parallel but are not pictured. A. 3D reconstruction of Densastroma pexisum with semi-transparent adjustment of it's skeleton, exposing trace fillings. White lines indicate the section planes of C–F. Cutting sites of C/D and E/F show meeting points of individual Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. B. Virtual section partially exposing a 120 mm long trace of O. kampto Beuck and Wisshak, igen, et isp. nov. C. White line indicating section plane of B. C-F. O. kampto Beuck and Wisshak, igen, et isp. nov. traces feigning ramification (see arrows).

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    Discussion

    CT scan analysis as visualisation tool.—When investigating boring trace fossils, one is often confronted with the problem of proper three-dimensional visualisation of the structures in question. As a result, destructive methods such as serial thin-sectioning (Van der Pers 1978) or epoxy-cast embedding techniques (Golubic et al. 1970) were utilised. For relatively thin substrates, such as mollusc shells, this problem was partly solved by applying x-ray analysis, allowing a two-dimensional visualisation of boring traces where significant density contrasts are present between cavity and substrate (Bromley 1970; Bromley and Tendal 1973; Schönberg 2001). Only with the advent of sophisticated (micro-) Computer Tomography (CT), it is now possible to produce three-dimensional views, not only of empty Recent and/or fossil borings (Schönberg 2001; Beuck 2002; Beuck et al. 2007; Bromley et al. in press; Schönberg and Shields in press) but even of filled cavities (see also Tapanila in press). In the present study the borings are filled with a dense matrix, which contains clay minerals and has a slightly higher density than calcite. With the aid of new image analysis software, the raw data can be processed and visualised in form of virtual sections, x-ray simulations, three-dimensional views and animations (see Figs. 57 and Supplementary Online Material at  http://app.pan.pl/acta53/app53-Beuck_etal_SOM.pdf). Additional application of the anaglyph technique on CT images and movies clearly shows the shape and spatial orientation of the traces. Even subtle density contrasts are sufficient for distinguishing between substrate (pure calcite) and boring (calcite plus clay), providing adequate settings are chosen. However, some of the Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. borings show unclear, blurred termini (Figs. 6G, 7). This might be an indicator of traces that are only partly filled by fine-grained sediment (geopetal fillings), because the sparite fillings at the end of such traces would be indistinguishable in terms of density from the surrounding stromatoporoid since both are composed of pure calcite. In addition, as the soft sediment inside the borings was protected from mechanical compaction prior to lithification by the rigid stromatoporoid framework, the distal part of the sedimentary fillings was characterised by very high initial porosity with probably up to 80% water in the pore space. During the cementation of the sediment, this pore space was filled by calcite, resulting in comparatively high carbonate contents of the micritic filling close to the sediment-sparite boundary, and consequently producing low density contrasts, which might be the reason for the blurred termini.

    This study is a successful attempt to use this non-destructive method to characterise lithified boring patterns with low density differences in fossil material. We consider CT scan analysis to be of high potential for future bioerosion studies on both fossil and Recent material. With increasing hardware performance it can be expected that the resolution of the method will be further enhanced, as will be the image analysis software, which might soon contain also stereoscopic features and become more affordable as a standard tool for bioerosion analyses.

    Fig. 6.

    3D reconstruction of Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. (CT scan analysis). Cubes indicating the spatial orientation of sample based on medical terms. A. Semi-transparent visualisation of the of stromatoporoid's surface and the micritic matrix of its boring infill. Grey-dashed lines indicate virtual sections that have been visualised parallel but are not pictured. B. O. kampto Beuck and Wisshak, igen, et isp. nov. mainly located in the upper part of host substrate. C. O. kampto Beuck and Wisshak, igen, et isp. nov. gently curved and presumably secondarily settled by Trypanites weisei. D. Tapered and rounded terminus of O. kampto Beuck and Wisshak, igen, et isp. nov. E. O. kampto Beuck and Wisshak, igen, et isp. nov. interwoven with Trypanites isp. F. Three traces of O. kampto Beuck and Wisshak, igen, et isp. nov. meet. G. Holotype of O. kampto Beuck and Wisshak, igen, et isp. nov. showing a strongly oval cross-section and a slightly bent course (arrow). Scale bars 10 mm.

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    Fig. 7.

    3D reconstruction of traces visualised for observation with anaglyph glasses (red/blue). A. Borings filled by micritic material within Densastroma pexisum. Arrow indicating holotype. B. Holotype of Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. showing a maximal diameter of 17 mm. C. Micritic matrix of boring infills with interfering micritic compounds augmented in the host skeleton. D. Holotype of O. kampto Beuck and Wisshak, igen, et isp. nov. indicated by arrow. Scale bars 10 mm.

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    Fig. 8.

    Idealised schematic drawing of Osprioneides kampto Beuck and Wisshak, igen, et isp. nov.

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    The identity of the trace maker.—Traces of Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. are sharply incised in the substratum and did not affect the growth of host laminae indicating that the producer penetrated the coenosteum post-mortem and are thus true borings as opposed to embedment structures (e.g., Tapanila et al. 2004). The length of O. kampto Beuck and Wisshak, igen, et isp. nov. seems to be only limited by the substrate size (see also Newall 1970). Inside corresponding borings, Newall (1970) detected fossil lingulids. He concluded that Lingula occupied preformed sediment filled borings, which in some cases may have lived in symbiosis with Heliolites. Our CT scan analysis, however, showed that the boring fills of Densastroma pexisum lack any faunal evidence. The occasionally curved to slightly undulating course of the trace, its variable length and sometimes slightly enlarging diameter in central parts as well as the absence of any lining or scratch marks let us presume a soft bodied organism with a primarily chemical mode of penetration—most likely a boring worm—as the potential trace maker. These characters also rule out a bivalve producer such as inferred for Gastrochaenolites (Kelly and Bromley 1984) and Petroxestes pera (Pojeta and Palmer 1976; Wilson and Palmer 1988). Stel and Stoep (1982) and Newall (1970) came to a corresponding conclusion for the synonymous material. Recent Trypanites is known to be produced by sipunculids (Rice 1969) and polychaetes (Bromley 1978), and both bioerosion agents range amongst the most important bioeroders in Recent tropical reefs (Hutchings and Peyrot-Clausade 2002). Corresponding fossil borings were interpreted accordingly (e.g., James et al. 1977 for the oldest Trypanites discovered in the Lower Cambrian of Labrador, and Pemberton et al. 1980 from Silurian—Devonian strata in southern Ontario). Moreover, Kobluk and Nemscok (1982) found direct evidence for a polychaete producer in form of scolecodonts detected within the boring infill of Trypanites from the Middle Ordovician Verulam Formation at Kirkfield, Ontario.

    Temporal pattern of ichnocoenosis development.—It is presumed that Densastroma pexisum preferred a marly bottom in calm water (Mori 1969). According to Tapanila et al. (2004), Palaeozoic corals and stromatoporids were also more likely to be bored in muddy facies than in sandy facies with highest boring frequency in high domical host shapes because massive forms are less prone to breakage and burial (see also Kershaw 1984). In addition, shapes that provide optimal water currents, while reducing sediment accumulation, influence the distribution of suspension feeding macroborers (Kobluk and Nemcsok 1982; Nield 1984). Most small Trypanites and Palaeosabella borings are located in the superficial zone of the coenosteum indicating a post-mortem infestation with the strongest concentration on the higher raised regions of the substrate (see also Kobluk and Nemcsok 1982), which was interpreted by Kershaw (1980) as a larval preference for enhanced current flows. Borings deep inside the host, however, are interpreted to represent either synvivo borings overgrown by the recovery of the host bio-substrate (see Tapanila et al. 2004) or, as secondary settlers within abandoned O. kampto Beuck and Wisshak, igen, et isp. nov. borings. The latter borings exclusively originate from the host surface and thus represent a post-mortem settlement as well.

    Evolution of penetration capabilities.—Both the deeply penetrating nature of the Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. as well as the high density of common Trypanites and Palaeosabella show a considerable degree of ecospace competition among hardground dwelling organisms during the Silurian. This can be interpreted as a direct result of the “Ordovician Bioerosion Revolution” which led to the appearance of many new ichnogenera in concert with a significant increase in the intensity of bioerosion, peaking in the Late Ordovician and Early Silurian (Tylor and Wilson 2003; Wilson and Palmer 2006). However, a penetration depth of 120 mm is a unique finding for the Palaeozoic (Fig. 9). Even traces exceeding 50 mm did not become abundant before the “Mesozoic Marine Revolution” as demonstrated by an evaluation of animal classes with endolithic representatives throughout the Phanerozoic by Vermeij (1993; see also Fig. 9), even though more recent investigations indicate that some Ordovician to Silurian Trypanites and Gastrochaenolithes may reach 40 to 60 mm in boring depth (Ekdale and Bromley 2001; Tapanila 2001; Mark A. Wilson, personal communication 2006). During the major Mesozoic evolutionary turnover, enhanced predation and grazing pressure (Vermeij 1977) led to a significant increase in bioerosion intensity reflected for instance in the Palaeo-Reef database (Kiessling et al. 1999; Kiessling 2002; see Fig. 9). The first ichnospecies reaching comparable and even superior penetration depth is Trypanites fosteryeomani, reported from a Middle Jurassic (Bajocian) hardground community by Cole and Palmer (1999). Hence, the present material predates the oldest finding of such a pronounced penetration capability by more than 260 million years, during which this adaptive strategy was abandoned before renewed enhanced ecospace pressure during Mesozoic times led to convergent reinventions.

    Fig. 9.

    Evolution of bioerosion intensity and boring depth throughout the Phanerozoic. The line graph (scale at left hand side) illustrates the percentage of reefs with evidence of macroborings, based on the PaleoReefs database (after Kiessling 2002). The shaded columns (scale on right hand side) shows the number of classes with endolithic representatives (light grey) and those reaching penetration depths in excess of 50 mm (dark grey) (after Vermeij 1993). Note the significant increase of boring intensity and penetration depth during the “Mesozoic Marine Revolution”.

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    Conclusions

    • Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. is an exceptionally large, straight to irregularly bent, unlined boring of variable length entering the lithic substrate perpendicular to subparallel and with a tapered to rounded terminus. The boring has a constant oval diameter in cross-section. This new ichnospecies represents the deepest boring trace known from the Palaeozoic.

    • We presume a soft-bodied organism with a primarily chemical mode of penetration (most likely a boring worm) was the potential tracemaker.

    • Both, the deeply penetrating nature of Osprioneides kampto Beuck and Wisshak, igen, et isp. nov. as well as the high density of common Trypanites and Palaeosabella including potential secondary settlement indicate a considerable degree of ecospace competition among hardground dwelling organisms already in the Silurian.

    • A penetration depth of 120 mm is a unique finding for the Palaeozoic and was not exceeded until some 260 million years later (Bajocian, Middle Jurassic), when enhanced predation and grazing pressure during the “Mesozoic Marine Revolution” led to convergent reinventions (e.g., Trypanites fosteryeomani).

    • We consider CT scan analysis, especially in combination with stereoscopic techniques, to be of high potential for future bioerosion studies on both fossil and Recent material.

    Acknowledgements

    We are indebted to Leif Tapanila (Department of Geosciences, Idaho State University, USA), Richard G. Bromley (Geologisk Institut, Copenhagen, Denmark), and Mark A. Wilson (Department of Geology, The College of Wooster, USA) for valuable discussions. Furthermore, we would like to express our gratitude to Wolfgang Maxlmoser (Siemens Medical Solutions, Magnetic Resonance, Erlangen, Germany) and Werner Schmidt (Siemens Medical Solutions, Computed Tomography, Forchheim, Germany) for their support in obtaining the CT data. The working group of Willi A. Kalender (Institute of Medical Physics, Erlangen, Germany), especially Elizaveta Stepina and Marek Karolczak, we are beholden for the provision of syngo® CT.3D and their help. We thank Lydia Schäfer (Tübingen, Germany) for solving the etymology of the new ichnospecies, and Michael Joachimski (Institute of Geologie, Erlangen, Germany) for stable isotope analyses. The study was funded by the Deutsche Forschungsgemeinschaft (Grant No. Fr 1134/6). This paper is a contribution to IGCP 503. Mark A. Wilson (Department of Geology, The College of Wooster, Wooster, USA) and Jordi M. De Gibert (Departament d'Estratigrafia, Paleontologia i Geociències Marines, Universitat de Barcelona, Spain) are thanked for their thorough reviews and constructive comments.

    References

    1.

    L. Beuck 2002. Biodegradation und Ichnodiversität postmortaler Stadien der Tiefwasserkoralle Lophelia pertusa am Propeller Mound (Porcupine Seabight). 11 pp. Unpublished Masters Thesis, Eberhard-KarlsUniversität, Tübingen, Germany. Google Scholar

    2.

    L. Beuck , A. Vertino , E. Stepina , M. Karolczak , and O. Pfannkuche 2007. Skeletal response of Lophelia pertusa (Scleractinia) to bioeroding sponge infestation visualised with micro-computed tomography. Facies 53: 157–176. Google Scholar

    3.

    R.G. Bromley 1970. Borings as trace fossils and Entobia cretacea Portlock, as an example. In : T.P. Crimes and J.C. Harper (eds.), Trace Fossils.Geological Journal Special Issue 3: 49–90. Google Scholar

    4.

    R.G. Bromley 1972. On some ichnotaxa in hard substrates, with a redefinition of Trypanites Mägdefrau. Paläontologische Zeitschrift 46: 93–98. Google Scholar

    5.

    R.G. Bromley 1978. Bioerosion of Bermuda reefs. Palaeogeography, Palaeoclimatology, Palaeoecology 23: 169–197. Google Scholar

    6.

    R.G. Bromley 2004. A stratigraphy of marine bioerosion. In: D. McIlroy (ed.), The Application of Ichnology to Palaeoenvironmental and Stratigraphic Analysis. Geological Society of London, Special Publications 228: 455–481. Google Scholar

    7.

    R.G. Bromley and A. D'Alessandro 1987. Bioerosion of the Plio-Pleistocene transgression of southern Italy. Rivista Italiana di Paleontologia e Stratigrafia 93: 379–442. Google Scholar

    8.

    R.G. Bromley and O.S. Tendal 1973. Example of substrate competition and phototrophism between two clionid sponges. Journal of Zoology 169: 151–155. Google Scholar

    9.

    R.G. Bromley , L. Beuck , and E. Taddei Ruggiero (in press). Endolithic sponge versus terebratulid brachiopod, Pleistocene, Italy: accidental symbiosis, bioclaustration and deformity. In : M. Wisshak and L. Tapanila (eds.), Current Developments in Bioerosion , 361–368. Springer, Berlin. Google Scholar

    10.

    M. Calner , L. Jeppsson , and A. Munnecke 2004. The Silurian of Gotland —Part I: Review of the stratigraphic framework, event stratigraphy, and stable carbon and oxygen isotope development. Erlanger geologische Abhandlungen Sonderband 5: 113–131. Google Scholar

    11.

    J.M. Clarke 1921. Organic dependence and disease: their origin and significance. Bulletin of New York State Museum of Natural History 221–222: 1–113. Google Scholar

    12.

    A.R. Cole and T.J. Palmer 1999. Middle Jurassic worm borings, and a new giant ichnospecies of Trypanites from the Bajocian/Dinantian unconformity, southern England. Proceedings of the Geologists ' Association 110: 203–209. Google Scholar

    13.

    A.A. Ekdale and R.G. Bromley 2001. Bioerosional innovation for living in carbonate hardgrounds in the Early Ordovician of Sweden. Lethaia 34: 1–12. Google Scholar

    14.

    S. Golubic , G. Brent , and T. LeCampion 1970. Scanning electron microscopy of endolithic algae and fungi using a multipurpose casting-embedding technique. Lethaia 3: 203–209. Google Scholar

    15.

    S.J. Gould 1989. Wonderful Life: The Burgess Shale and the Nature of History. 347 pp. W.W. Norton and Co, New York. Google Scholar

    16.

    D.A.T. Harper . 2006. The Ordovician biodiversification: Setting an agenda for marine life. Palaeogeography, Palaeoclimatology, Palaeoecology 232: 148–166. Google Scholar

    17.

    P.A. Hutchings and M. Peyrot-Clausade 2002. The distribution and abundance of boring species of polychaetes and sipunculans in coral substrates in French Polynesia. Journal of Experimental Marine Biology and Ecology 269: 101–121. Google Scholar

    18.

    N.P. James , D.R. Kobluk , and S.G. Pemberton 1977. The oldest macroborers: Lower Cambrian of Labrador. Science 197: 980–983. Google Scholar

    19.

    L. Jeppsson 1997. A new latest Telychian, Sheinwoodian and Early Homerian (Early Silurian) Standard Conodont Zonation. Transactions of the Royal Society of Edinburgh: Earth Sciences 88: 91–114. Google Scholar

    20.

    S.R.A. Kelly and R.G. Bromley 1984. Ichnological nomenclature of clavate borings. Palaeontology 27: 793–807. Google Scholar

    21.

    S. Kershaw 1980. Cavities and cryptic faunas beneath non-reef stromatoporoids. Lethaia 13: 327–338. Google Scholar

    22.

    S. Kershaw 1984. Patterns of stromatoporoid growth in level-bottom environments. Palaeontology 27: 113–130. Google Scholar

    23.

    S. Kershaw 1990. Stromatoporoid palaeobiology and taphonomy in a Silurian biostrome on Gotland, Sweden. Palaeontology 33: 681–705. Google Scholar

    24.

    W. Kiessling 2002. Secular variations in the Phanerozoic reef ecosystem. In : E. Flügel , W. Kiessling , and J. Golonka (eds.), Phanerozoic Reef Patterns. Tulsa, SEPM Special Publications 72: 625–690. Google Scholar

    25.

    W. Kiessling , E. Flügel , and J. Golonka 1999. Paleoreef maps: Evaluation of a comprehensive database on Phanerozoic reefs. AAPG Bulletin 83: 1552–1587. Google Scholar

    26.

    D.R. Kobluk and S. Nemcsok 1982. The macroboring ichnofossil Trypanites in colonies of the Middle Ordovician bryozoan Prasopora: population behaviour and reaction to environmental influences. Canadian Journal of Earth Science 19: 679–688. Google Scholar

    27.

    D.R. Kobluk , N.P. James , and S.G. Pemberton 1978. Initial diversification of macroboring ichnofossils and exploitation of the macroboring niche in the Lower Paleozoic. Paleobiology 4: 163–170. Google Scholar

    28.

    S. Laufeld 1974. Reference localities for palaeontology and geology in the Silurian of Gotland. Sveriges Geologiska Undersökning C705: 1–172. Google Scholar

    29.

    M.A. Leymarie 1842. Suite du mémoire sur le terrain Crétacé du Département de l'Aube. Mémoires de la Société Géologique de France 5:1–34. Google Scholar

    30.

    K. Mägdefrau 1932. Über einige Bohrgänge aus dem Unteren Muschelkalk von Jena. Paläontologische Zeitschrift 14: 150–160. Google Scholar

    31.

    M.G. Mángano and M.L. Droser 2004. The ichnological record of the Ordovician Radiation. In: B.D. Webby , F. Paris , M. Droser , and I.G. Percival (eds.), The Great Ordovician Biodiversification Event , 369–379. Columbia University Press, New York. Google Scholar

    32.

    K. Mori 1969. Stromatoporoids from the Silurian of Gotland. Part 1. Stockholm Contributions in Geology 19: 1–100. Google Scholar

    33.

    A. Munnecke , C. Samtleben , and T. Bickert 2003. The Ireviken Event in the lower Silurian of Gotland, Sweden—relation to similar Palaeozoic and Proterozoic events. Palaeogeography, Palaeoclimatology, Palaeoecology 195: 99–124. Google Scholar

    34.

    G. Newall 1970. A symbiotic relationship between Lingula and the coral Heliolites in the Silurian. Geological Journal, Special Issue 3: 335–344. Google Scholar

    35.

    E.W. Nield 1984. The boring of Silurian stromatoporoids—towards an understanding of larval behaviour in the Trypanites organism. Palaeogeography, Palaeoclimatology, Palaeoecology 48: 229–243. Google Scholar

    36.

    S.G. Pemberton , D.R. Kobluk , R.K. Yeo , and M.J. Risk 1980. The boring Trypanites at the Silurian—Devonian disconformity in southern Ontario. Journal of Paleontology 54: 1258–1266. Google Scholar

    37.

    J. Pojeta and T.J. Palmer 1976. The origin of rock boring in mytilacean pelecypods. Alcheringa 1: 167–179. Google Scholar

    38.

    M.E. Rice 1969. Possible boring structures of sipunculids. American Zoologist 9: 803–812. Google Scholar

    39.

    C. Samtleben , A. Munnecke , T. Bickert , and J. Pätzold 1996. The Silurian of Gotland (Sweden): Facies interpretation based on stable isotopes in brachiopod shells. Geologische Rundschau 85: 278–292. Google Scholar

    40.

    C.H.L. Schönberg 2001. Estimating the extent of endolithic tissue of a Great Barrier Reef clionid sponge. Senckenbergiana maritima 31: 29–39. Google Scholar

    41.

    C.H.L. Schönberg and G. Shields (in press). Micro-computed tomography for studies on Entobia: transparent substrate versus modern technology. In : M. Wisshak and L. Tapanila (eds.), Current Developments in Bioerosion , 147–164. Springer, Berlin. Google Scholar

    42.

    J.H. Stel and E. van de Stoep 1982. Interspecifieke relaties en boringen in enige Silurische stromatoporen. Grondboor en Hamer 1: 11–23. Google Scholar

    43.

    L. Tapanila 2001. Bioerosion in Late Ordovician and Early Silurian tropical carbonate settings of Anticosti Island, Québec, Canada. 152 pp. Unpublished Masters Thesis, School of Graduate Studies, Laurentian University, Sudbury. Google Scholar

    44.

    L. Tapanila (in press). The medium is the message: imaging a complex microboring (Pyrodendrina cupra igen, and isp. n.) from the early Paleozoic of Anticosti Island, Canada. In : M. Wisshak and L. Tapanila (eds.), Current Developments in Bioerosion , 123–146. Springer, Berlin. Google Scholar

    45.

    L. Tapanila and P. Copper 2002. Endolithic trace fossils in Ordovician—Silurian corals and stromatoporoids, Anticosti Island, eastern Canada. Acta Geologica Hispanica 37: 15–20. Google Scholar

    46.

    L. Tapanila , P. Copper , and E. Edinger 2004. Environmental and substrate control on Paleozoic bioerosion in corals and stromatoporoids, Anticosti Island, Eastern Canada. Palaios 19: 292–306. Google Scholar

    47.

    P.D. Taylor and M.A. Wilson 2003. Palaeoecology and evolution of marine hard substrate communities. Earth-Science Reviews 62: 1–103. Google Scholar

    48.

    J.N.C. Van der Pers 1978. Bioerosion by Polydora (Polychaeta, Sedentaria, Vermes) off Helgoland, Germany. Geologie en Mijnbouw 57: 465–478. Google Scholar

    49.

    G.J. Vermeij 1977. The Mesozoic marine revolution: evidence from snails, predators and grazers. Paleobiology 3: 245–258. Google Scholar

    50.

    G.J. Vermeij 1993. Evolution and EscalationAn Ecological History of Life. 544 pp. Princeton University Press, Princeton. Google Scholar

    51.

    E. Wachter and J.M. Hayes 1985. Exchange of oxygen isotopes in carbon-dioxide—phosphoric acid systems. Chemical Geology 52: 365–374. Google Scholar

    52.

    B.D. Webby , F. Paris , M. Droser , and I.G. Percival (eds.) 2004. The Great Ordovician Biodiversification Event. 484 pp. Columbia University Press, New York. Google Scholar

    53.

    M.A. Wilson and T.J. Palmer 1988. Nomenclature of a bivalve boring from the Upper Ordovician of the Midwestern United States. Journal of Paleontology 62: 306–308. Google Scholar

    54.

    M.A. Wilson and T.J. Palmer 2006. Patterns and processes in the Ordovician Bioerosion Revolution. Ichnos 13: 109–112. Google Scholar

    55.

    V.I Yavorsky. [Âvorski, V.I.] 1929. Silurian Stromatoporoidea [in Russian]. Izvestiâ Geologˆeskogo Komiteta 48: 77–114. Google Scholar
    Lydia Beuck, Max Wisshak, Axel Munnecke, and Andrá Freiwald "A Giant Boring in a Silurian Stromatoporoid Analysed by Computer Tomography," Acta Palaeontologica Polonica 53(1), 149-160, (1 January 2008). https://doi.org/10.4202/app.2008.0111
    Published: 1 January 2008
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