Bioerosion describes the erosion of hard ocean substrates – and less often terrestrial substrates – by living organisms. Marine bioerosion can be caused by mollusks, polychaete worms, phoronids, sponges, crustaceans, echinoids, and fish; it can occur on coastlines, on coral reefs, and on ships; its mechanisms include biotic boring, drilling, rasping, and scraping. On dry land, bioerosion is typically performed by pioneer plants or plant-like organisms such as lichen, and mostly chemical (e.g. by acidic secretions on limestone) or mechanical (e.g. by roots growing into cracks) in nature.
Bioerosion of coral reefs generates the fine and white coral sand characteristic of tropical islands. The coral is converted to sand by internal bioeroders such as algae, fungi, bacteria (microborers) and sponges (Clionaidae), bivalves (including Lithophaga), sipunculans, polychaetes, acrothoracican barnacles and phoronids, generating extremely fine sediment with diameters of 10 to 100 micrometres. External bioeroders include sea urchins (such as Diadema) and chitons. These forces in concert produce a great deal of erosion. Sea urchin erosion of calcium carbonate has been reported in some reefs at annual rates exceeding 20 kg/m².
Fish also erode coral while eating algae. Parrotfish cause a great deal of bioerosion using well developed jaw muscles, tooth armature, and a pharyngeal mill, to grind ingested material into sand-sized particles. Bioerosion of coral reef aragonite by parrotfish can range from 1017.7±186.3 kg/yr (0.41±0.07 m³/yr) for Chlorurus gibbus and 23.6±3.4 kg/yr (9.7 10-³±1.3 10-³ m²/yr) for Chlorurus sordidus (Bellwood, 1995).
Bioerosion is also well known in the fossil record on shells and hardgrounds (Bromley, 1970), with traces of this activity stretching back well into the Precambrian (Taylor & Wilson, 2003). Macrobioerosion, which produces borings visible to the naked eye, shows two distinct evolutionary radiations. One was in the Middle Ordovician (the Ordovician Bioerosion Revolution; see Wilson & Palmer, 2006) and the other in the Jurassic (see Taylor & Wilson, 2003; Bromley, 2004; Wilson, 2007). Microbioerosion also has a long fossil record and its own radiations (see Glaub & Vogel, 2004; Glaub et al., 2007).
- Petroxestes borings Ordovician.jpg
Petroxestes borings in an Upper Ordovician hardground, southern Ohio; see Wilson and Palmer (2006).
Teredolites borings in a modern wharf piling; the work of bivalves known as "shipworms".
- Geopetal Structure.jpg
Geopetal structure in bivalve boring in coral; bivalve shell visible; Matmor Formation (Middle Jurassic), southern Israel.
- "Terminology for biorelated polymers and applications (IUPAC Recommendations 2012)" (PDF). Pure and Applied Chemistry 84 (2): 377–410. 2012. doi:10.1351/PAC-REC-10-12-04.
- Bellwood, D. R. (1995). "Direct estimate of bioerosion by two parrotfish species, Chlorurus gibbus and C. sordidus, on the Great Barrier Reef, Australia". Marine Biology 121 (3): 419–429. doi:10.1007/BF00349451.
- Bromley, R. G (1970). "Borings as trace fossils and Entobia cretacea Portlock as an example". In Crimes, T.P. and Harper, J.C. (eds.). Trace Fossils. Geological Journal Special Issue 3. pp. 49–90.
- Bromley, R. G. (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. London: Geological Society. pp. 455–481. ISBN 1-86239-154-8.
- Glaub, I.; Golubic, S., Gektidis, M., Radtke, G. and Vogel, K. (2007). "Microborings and microbial endoliths: geological implications". In Miller III, W (ed). Trace fossils: concepts, problems, prospects. Amsterdam: Elsevier. pp. 368–381. ISBN 0-444-52949-7.
- Glaub, I.; Vogel, K. (2004). "The stratigraphic record of microborings". Fossils & Strata 51: 126–135. ISSN 0300-9491.
- Palmer, T. J. (1982). "Cambrian to Cretaceous changes in hardground communities". Lethaia 15 (4): 309–323. doi:10.1111/j.1502-3931.1982.tb01696.x.
- Taylor, P. D.; Wilson, M. A. (2003). "Palaeoecology and evolution of marine hard substrate communities" (PDF). Earth-Science Reviews 62 (1-2): 1–103. Bibcode:2003ESRv...62....1T. doi:10.1016/S0012-8252(02)00131-9.
- Vinn, O.; Wilson, M. A.; Mõtus, M.-A. (2014). "The Earliest Giant Osprioneides Borings from the Sandbian (Late Ordovician) of Estonia". PLoS ONE 9(6) (e99455). doi:10.1371/journal.pone.0099455.
- Wilson, M. A. (1986). "Coelobites and spatial refuges in a Lower Cretaceous cobble-dwelling hardground fauna". Palaeontology 29: 691–703. ISSN 0031-0239.
- Wilson, M. A. (2007). "Macroborings and the evolution of bioerosion". In Miller III, W (ed). Trace fossils: concepts, problems, prospects. Amsterdam: Elsevier. pp. 356–367. ISBN 0-444-52949-7.
- Wilson, M. A.; Palmer, T. J. (1994). "A carbonate hardground in the Carmel Formation (Middle Jurassic, SW Utah, USA) and its associated encrusters, borers and nestlers". Ichnos 3 (2): 79–87. doi:10.1080/10420949409386375.
- Wilson, M. A.; Palmer, T. J. (2001). "Domiciles, not predatory borings: a simpler explanation of the holes in Ordovician shells analyzed by Kaplan and Baumiller, 2000". PALAIOS 16 (5): 524–525. doi:10.1669/0883-1351(2001)016<0524:DNPBAS>2.0.CO;2.
- Wilson, M. A.; Palmer, T. J. (2006). "Patterns and processes in the Ordovician Bioerosion Revolution" (PDF). Ichnos 13 (3): 109–112. doi:10.1080/10420940600850505.
- Vinn, O.; Wilson, M.A. (2010). "Occurrence of giant borings of Osprioneides kampto in the lower Silurian (Sheinwoodian) stromatoporoids of Saaremaa, Estonia". Ichnos 17: 166–171. doi:10.1080/10420940.2010.502478. Retrieved 2014-06-10.
- Vinn, O.; Wilson, M.A. (2010). "Early large borings from a hardground of Floian-Dapingian age (Early and Middle Ordovician) in northeastern Estonia (Baltica)". Carnets de Géologie 2010: CG2010_L04. doi:10.4267/2042/35594. Retrieved 2014-06-10.
|40x40px||Wikimedia Commons has media related to Bioerosion.|