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ATLAS OF THE MEDITERRANEAN AND –LIKE STRUCTURES

226 5. Seamounts and Seamount-like Structures of the

Bayram Öztürk Univesity, Faculty of Ordu Caddesi 200, Laleli, Istanbul and Turkish Marine Research Foundation

Marzia Rovere Istituto di Scienze Marine, Consiglio Nazionale delle Ricerche Via P. Gobetti 101, 40129 Bologna, and

Maurizio Würtz DISTAV, Università di Genova Corso Europa 26, 16132 Genova, Italy

Acknowledgements: The Authors are indebted to Dr. Nur Eda Topçu for her valuable help.

227 OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

Table 5: Seamounts and Seamount-Like Structures of the East Mediterranean.

Seamout name Lat. ° Long. ° Peak depth (m) Base depth (m) Page Alkyoni Bank 38.22130 25.56280 60-70 410-420 230

Anamur-Kormakiti Ridge ND ND ND ND 231

Anaxagoras Seamount 35.67566 30.51171 920-930 1510-1520 233

Anaximander- Seamount 35.50840 29.78160 1110-1120 2000-2010 234

Anaximenes Seamount 35.43070 30.16420 690-700 1500-1510 235

Aphroditi Bank 39.70040 24.53820 150-160 290-300 236

Balıkçı Bank 37.91021 25.99832 40-50 330-340 237

Bilim Bank 36.36251 34.44887 40-50 250-260 238

Brouker and Stokes Banks 38.87820 25.39500 70-80 200-210 239

Danaos-2007 Seamount 34.66586 25.54216 450-460 780-790 240

Eratosthenes Seamount 33.74444 32.73362 780-790 1920-1930 241

Florence Rise 34.82090 31.69151 1560-1570 2100-2110 243

Glavki Bank 39.61340 24.45670 110-120 320-330 236

Gűzelyurt Seamount 35.67092 32.76268 1410-1420 ND 231

Hecataeus Rise 34.44201 34.34533 1090-1100 1510-1520 244

Hecataeus Knoll 34.44025 33.61840 190-200 690-700 244

Ira and Navtilos Banks 38.67146 24.24609 40-50 260-270 245

Karpas Ridge 35.88444 34.88554 50-60 360-370 246

Kaş Bank 35.58756 29.33301 91 ND 247

Kolumbo 36.52070 25.47170 10-20 280-290 248

Larnaka Ridge 35.27495 35.09294 840-850 ND 249

Latakia Ridge 35.13782 35.54911 890-900 ND 250

Literi Bank 38.81486 24.85928 70-80 210-220 251

Mansel and Johnston Banks 39.29600 25.38780 30-40 190-200 252

West Mediterranean Ridge 33.77267 22.70907 1150-1160 2190-2200 253

East Mediterranean Ridge 34.95354 27.46288 350-360 1240-1250 253

Ptolemy Seamount 34.62513 24.56142 1050-1060 1820-1830 255

Sinaya Bank 38.86362 25.78698 70-80 210-220 256

Turgut Reis Bank 35.02200 35.01300 1110-1120 1350-1360 257

Venus Bank 40.23870 25.02910 150-160 350-360 258

Yunus Bank 37.14237 26.25719 100-110 300-310 259

228 EASTERN MEDITERRANEAN

East Mediterranean Seamounts and Banks: general map.

Venus

40 Aphroditi Glavki Mansel-Johnston

Brouker-Stokes Literi Sinaya Ira-Navtilos

Alkyoni Balikçi 38

Yunus

Kolumbo Bilim Karpas 36

Anaxagoras Anamur-Kornakiti -Finike Larnaka Florence Turgut Reis Latakia East Mediterranean rdg Danaos-2007 (Nameless) Ptolemy Hecataeus knoll Hecataeus rise 34

West Mediterranean rdg Eratosthenes

32

24 26 28 30 32 34 36

180 km

The Eastern Mediterranean comprises the Cretan , the Aegean The Messinian Salinity Crisis led to the deposition of 1.5 km of Sea and the Levantine Sea. The Eastern formed evaporites in the Levantine Basin, which overall contains up to 10 during the tectonic break-up of the Pangea Supercontinent starting km of . During the Pliocene, accretionary activity along the about 270 Ma to 180 Ma, that led to stretching and external front, due the ongoing convergence of towards the thinning, with the formation of several , where very thick Aegean Arc, led to the formation of the Mediterranean Ridge (Finetti, sedimentary sequences deposited (Biju-Duval and Montadert, 1976), with active mud diapirism. Huge piles of containing 1977). When Africa and started to converge, the evaporites, strike-slip movements and compression, , salt experienced strike-slip faulting and of those previously and gravitational processes are all concurrent causes for formed grabens. When 18-14 Ma started in the Aegean the formation of seamounts in this sea region. region, the Hellenic Arc formed and extension began in its -arc region, due to tearing (Jolivet et al., 1994). The external non- now consists of a raised topographic feature running the full length of the Hellenic arc, forming the uplifted of and Rhodes. The inner southern volcanic arc consists of a series of dormant or active volcanoes, including the Kolumbo Seamount.

229 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Alkyoni Bank Location: 38.22130°N – 25.56280°E Peak depth (m): 60-70 Base depth (m): 410-420

DESCRIPTION:

Geology

No specific geological or geographical information is available on this structure, which is depicted in this map: http://highsea.cz/map/GM06.JPG

Life on and around the Seamount

Some coralligenous have been detected such as the sponge Spongia of- ficinalis, and the and Homarus vulgaris. Besides, Scillarus arctus was also reported during the summer 2007 cruises in the . This bank offers a suitable for lobsters due to the occurrence of patchy and fragmented rocky substrates (Ozturk, 2007).

No information about the Alkyoni Bank pelagic communities has been found in the scientific literature.

18 km

230 EASTERN MEDITERRANEAN

STRUCTURE: Anamur Kormakiti Ridge and Güzelyurt Seamount Anamur Kormakiti Ridge (ANM) Location: ND Peak depth (m): ND Base depth (m): ND

Güzelyurt Seamount (GZL)* Location: 35.67092°N – 32.76268°E Peak depth (m): 1410-1420 Base depth (m): ND

* Source: http://www.geomapapp.org/database/GEBCO/GEBCO_gazetteer.htm

DESCRIPTION:

Geology

The Anamur-Kormakiti Ridge is a prominent N-S oriented structural high with a thick cover of Plio-Quaternary sediment: it is probably a lineament, which bounds the -Adana Basin, to the east, and the Antalya Basin, to the west (Robertson, 1998b). The Anamur–Kormakiti Ridge is characterized by an imbri- GZL cate -thrust system. The older structures appear to be truncated by a promi- nent E-W trending normal fault system, which at least locally affects the Plio- Quaternary sequences along much of the Turkish slope of the Cilicia Basin. West of Anamur–Kormakiti Ridge, the thick Plio-Quaternary sediments, on the strongly dissected slope, have been affected by N–S trending normal faults and display a block and morphology (Ozel et al., 2007).

ANM Life on and around the Seamount

Large unexploited commercial sponge communities (mainly Spongia officinalis) have been discovered during two summer surveys (2007 and 2008) conducted in these sites. Scillarus arctus and Scillarus latus were also reported. A lot of pur- seiner fishing nets have been found in these areas as a ghost fishing.

The area of the Güzelyurt Seamount is represented by the submarine between and , it is located on migratory routes of large and small in the Levantine Basin (Öztürk, 2009a). Besides, it is a spawning ground of bullet (Auxis rochei) and Atlantic skipjack (Euthynnus allettera- tus). Along the Turkish , nestling of the endangered loggerhead turtle (Caretta caretta) and green turtle (Chelonia mydas) are present (Gücü and Öztürk, 2010). Bluefin tuna spawning area has been demonstrated to be located 9 km between Turkey and Cyprus islands (Karakulak et al., 2004). This area was pro- posed as High MPA (Öztürk, 2009a) and remains within the determined EBSAs (UNEP-MAP-RAC/SPA, 2010).

231 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Anaximander Complex (Anaxagoras, Anaximander, Anaximenes Seamounts)

The Anaximander Mountains Complex (Anaxagoras, Anaximander or Finike and This area was suggested as a High Seas MPA Anaximenes Seamounts) is located between the Hellenic and Cyprus arcs and (Öztürk, 2009a) and later as a potential SPAMI was formed in large part due to the ongoing convergence of the African and (Öztürk et al., 2012b). Turkish government has de- Anatolian plates. A protracted interval of contraction in the Miocene created a clared as Special Protected Area on 16th August series of broadly east-west trending and predominantly south-verging structures 2013 (official gazetteer number 28737: http://www. across the entire eastern Mediterranean, among them there are the Anaximander resmigazete.gov.tr/eskiler/2013/08/20130816-3. Mountains. The absence of the Messinian evaporites in the Anaximander htm). OCEANA cited the area among the EBSAs in Mountains and in the adjacent deep basins, Rhodes Basin (more than 4000 the Mediterranean due to the above cited character- m-deep) and Finike Basin (3000 m-deep), indicates that the southward thrust- istics as well as the presence of large migratory fish ing of the Anaximander Mountains occurred in post-Messinian time (Dimitrov and cetaceans (OCEANA, 2014). and Woodside, 2003; Zitter, 2004). During the mid-Tortonian, the last phase of thrusting coincided with the onset of a different kinematic regime related to the westward rotation of the . This Late Miocene change marked the start of differential subsidence that resulted in the formation of the Anaximander Mountains, which are thus characterized by strong contractional/transpressional deformation (ten Veen et al., 2004). During the Plio–Quaternary, the Anaximander Seamount and the Anaximenes Seamount developed as the result of uplift and rotation of a thrust fan. At this time, the Anaximenes Seamount experienced a progressive counterclockwise rotation, while the Anaxagoras Seamount and the Florence Rise experienced a clockwise rotation creating the present-day arrowhead-shaped morphology of the Anaximander Mountains. An arcuate fault separates the Anaximenes and Anaxagoras Seamounts from the Anaximander Seamount (Aksu et al., 2009). Between the Anaximander and Anaximenes Seamounts a 2200 km2-large debris flow called ‘‘the Great Slide” is present (Lykousis et al., 2009). Pockmarks are found in the slide area, they are generally small, no more than about 30 m across, and aligned with faulting; however, in a few cases they can be rather large with diameters up to 1000 m and depths of 300 m.

232 EASTERN MEDITERRANEAN

DESCRIPTION: Anaxagoras Seamount Geology Location: 35.67565°N – 30.51171°E Peak depth (m): 920-930 Base depth (m): 1510-1520 The Anaxagoras Seamount exhibits a very rough topography with a rather summit area in the north and central part. Its shape suggests that it is controlled by major faults. The relatively steep eastern flank separates the summit , lying at about 1200 m water depth, from the Antalya Basin and it is rather linear with a NW-SE trend, roughly parallel to the western flank. From north to south, the seamount can be subdivided into three main blocks. The northern part has the greatest relief rising up to 930 m water depth in the north-central part of the plateau. It is bounded to the south by a ridge extending southwestward towards the Anaximenes Seamount. This ridge has a pronounced bathymetric expression with a vertical scarp of about 500 m. The southern part of the seamount shows slightly greater relief in its eastern region, while the south- western part merges with the Florence Rise further south. The numerous linear ridges and scarps indicate that the area is crosscut by a very dense network of sub-vertical faults, which fall into two main groups, one trending NW-SE and the other NE-SW. In length, the faults with an orientation ranging from 140°N to 150°N are dominant and correspond to the general elon- gation of the Anaxagoras Seamount. The other family of faults cut across the seamount with a 60°N to 70°N orientation, they appear to be the youngest ones since they cut across the other features. These faults also show some continuity from Anaxagoras to Anaximenes, in spite of the different origin of the two sea- mounts (Zitter et al., 2005).

Life on and around the Seamount

This seamount hosts three mud volcanoes (Kazan, Kula and San Remo) where chemosynthetic communities dominated by bivalves were discovered (Olu- Le Roy et al., 2004; Lykousis et al., 2009). The abundance and richness of the observed chemosynthetic fauna and the size of some of the species contrast with the usual poverty of the eastern Mediterranean (Gönenç et al., 2004; Olu- Le Roy et al., 2004; Salas and Woodside, 2002). The communities of Eastern Mediterranean mud volcanoes actually seem to host a higher diversity with re- spect to similar communities found in other , including also neo-endemic species and differing for the smaller size of the bivalves (Olu-Le Roy et al., 2004). A new deep-water bivalve species of Lucinidae, Lucinoma kazani, was described from the Kazan (Salas and Woodside, 2002). In September 2010, a ROV study was performed over three mud volcanoes: Kazan, Amsterdam and Tessaloniki (Shank et al., 2011). Diverse seep in more than two dozen localized seep sites were found. Siboglinid tubeworms (Lamellabrachia sp.), am- phipods, brachyuran , echinoid sea urchins, galatheid squat lobsters, myti- lid mussels, and lucinid, vesicomyid, and thyasirid clams were observed. Active seepage on the northern of the Kazan mud volcano’s summit, at ~ 1720 m 18 km water depth, fueled aggregations of tubeworms and bivalves in an area more than a 300 m2.

A recent study by Tserpes et al. (2008) exhibited density distribution maps of the (Woodside et al., 2006). In fact the gouge marks that swordfish (Xiphias gladius) that migrates toward the eastern Levantine for - were found on mud volcanoes were suggested to be ing and suggested the existence of a major spawning ground that seems to be created by Cuvier’s beaked (Ziphius caviro- located near the Anaximander seamounts, at an area between the Anaximander stris) during foraging dives (Woodside et al., 2006). , the Antalya eddy and the Rhodes Gyre, which is one of the most distinct The area is within the sperm (Physeter cato- features of the Levantine Basin (Öztürk et al., 2012a). don) distribution area in the Eastern Mediterranean This area is important for marine mammals since such environments have rich and (Öztürk et al., 2013). diverse benthic ecology associated with methane-rich fluid seeps and thus could be the base of food chains that reach top predators like the deep-diving whales

233 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

Anaximander - Finike Seamount Location: 35.50840°N – 29.78160°E Peak depth (m): 1110-1120 Base depth (m): 2000-2010

18 km

DESCRIPTION:

Geology

The Anaximander Seamount is a sharply asymmetrical high, roughly NNE-SSW oriented, with an elongated summit and with the shallowest part lying at around 1120 m water depth.

Life on and around the Seamount

Between 1700 and 2000 m water depth, in the Anaximander mud field, high methane concentrations were measured. A new species of lamellibrachiid ves- timentiferan (Lamellibrachia anaximandri) has been discovered. This species showed a different spatial distribution and a variable density in the two mud volcano fields (on Anaxagoras and Anaximenes), apparently related with higher methane fluxes.

Many fish species of which the status are not yet evaluated by IUCN and including the vulnerable Squalus acanthias were sampled from this area, together with highly commercial deep-sea shrimps (Öztürk et al., 2010). Abralia veranyi, a deep sea and a preferable prey of the striped and Risso’s was also sampled from the area (Öztürk et al., 2010). Besides, the Anaximander Seamount is within the sperm whale (Physeter catodon) distri- bution area in the Eastern Mediterranean (Öztürk et al., 2013).

234 EASTERN MEDITERRANEAN

Anaximenes Seamount Location: 35.43070°N – 30.16420°E Peak depth (m): 690-700 Base depth (m): 1500-1510

18 km

DESCRIPTION: Life on and around the Seamount

Geology Chemosynthetic communities dominated by bivalves were discovered surround- ing the Amsterdam mud volcano (Olu-Le Roy et al., 2004). The Amsterdam mud The Anaximenes Seamount, with a slightly north- volcano (summit near 2050 m water depth) hosted local patches of cold-water westward concave shape, has the smallest area, but octocorals and scleractinian . Other organisms observed thriving on these shows the largest relief, rising up to 690 m depth hard substrates included actinarians and solitary scleractinian corals (Shank et from the basin floor. The Anaximenes Seamount al., 2011). Recently, two new species of Harpacticoid were described is a curved ridge of steeply dipping sedimentary from the seamount (Gheerardyn and George, 2010). strata. Locally, northeastward compression of the Anaximenes against the Anaxagoras Seamount has Denda and Christiansen (2011) studied the possible effects of steep topography resulted in the tilting and bending of Anaximenes to on the zooplankton community in the oligotrophic eastern Mediterranean at two the northwest and the development of a fold belt in site: the Anaximenes Seamount and the deep Rhodes Basin. In general, biomass the Antalya Basin to the northeast of Anaxagoras. and abundance of zooplankton were low, reflecting the oligotrophic character of Because of resistance of northeastward movement the area, but zooplankton standing stocks were higher in the Rhodes Basin than of the mountains, deformation of the Anaximenes at the Anaximenes Seamount. The taxonomic composition above the seamount Seamount is accompanied by underthrusting of summit did not differ markedly from the slope region or the reference station. this block beneath the Anaximander Seamount, The zooplankton community in the Anaximenes Seamount region seems not to which is being uplifted as a consequence. Detrital be influenced by a local seamount effect, but differences in standing stocks be- limestones, green-gray siltstones and tween the seamount and the Rhodes Basin are more likely driven by larger-scale and claystones and marlstones, attributed to and structures of cyclonic and anticyclonic eddies and a Middle Miocene flysch, as well as Eocene rocks, gyres, which dominate the circulation in the area. This area is important for sharks have been sampled from the seamount slope (Zitter, (e.g. Prionace glauca) and for marine mammals since such environments have 2004; Lykousis et al., 2008). There are three mud vol- rich and diverse benthic ecology associated with methane-rich fluid seeps and canoes (Amsterdam, Athina and Thessaloniki) lying thus could be the base of food chains that reach top predators like the deep- on top and in the southern side of the Anaximenes diving whales (Woodside et al., 2006). Seamount (Bohrmann et al., 2013).

235 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Aphroditi and Glavki Banks Aphroditi bank Location: 39.70040°N – 24.53820°E Peak depth (m): 150-160 Base depth (m): 290-300

Glavki bank Location: 39.61340°N – 24.45670°E Peak depth (m): 110-120 Base depth (m): 320-330

DESCRIPTION:

Geology

No specific geological or geographical informa- tion is available on this structure which is depicted in this map: http://highsea.cz/map/GM06.JPG and this name is present in the IOC-IHO GEBCO SCUFN (Sub-Committee on Undersea Feature Names) Gazetteer database: http://www.geomapapp.org/ 9 km database/GEBCO/GEBCO_gazetteer.htm

Life on and around the Seamount

The site harbours cold water corals (Lophelia per- tusa and Madrepora oculata). Corals occurrence is likely related to the circulation patterns regime in the area.

The area, which is located in the Northern Aegean Sea, is within the distribution range of the monk seal (Monachus monachus) (Hoyt and Notarbartolo di Sciara, 2008) and of the blue (Prionace glauca) (Megalofonou et al., 2009). It is also consid- ered a spawning area for pelagic fishes like Xiphias gladius, Euthynnus alletteratus or Auxis rochei (Vassilopoulou et al., 2008). The Glavki Bank is cited among the critical habitats for cetaceans by Hoyt and Notarbartolo di Sciara (2008). The area was suggested to meet the crite- 9 km for EBSAs by OCEANA (2014) and is part of the area proposed to be designated as a SPAMI (UNEP- MAP-RAC/SPA, 2010).

236 EASTERN MEDITERRANEAN

STRUCTURE: Balıkçı Bank Location: 37.91021°N – 25.99832°E Peak depth (m): 40-50 Base depth (m): 330-340

18 km

DESCRIPTION:

Geology

No specific geological or geographical information is available on this structure which is depicted in this map: http://highsea.cz/map/GM06.JPG

Life on and around the Seamount

No information about the Balıkçı Bank benthic and pelagic communities has been found in the scientific literature.

237 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Bilim Seamount Location: 36.36251°N – 34.44887°E Peak depth (m): 40-50 Base depth (m): 250-260

18 km DESCRIPTION:

Geology

No specific geological or geographical information is available on this structure which is depicted in this map: http://highsea.cz/map/GM06.JPG. There are also unpublished studies in the area (Öztürk, 2007), which contain the scientific re- sults of the Eastern Mediterranean Campaign (2007-2008).

Life on and around the Seamount

This area hosts large sponge fields of commercial species such as Spongia officinalis, as well as the anthozoans Antipathella subpinnata and Caryophyllia sp. and the Calocaris macandreae. Lesser-spotted dogfish(Scyliorhinus canicula), the rough ray (Raja radula) and the common stingray (Dasyatis pastin- aca) have been also found in the area.

It is known that this seamount is bluefin tuna Thunnus( thynnus) spawning ground and very rich in eggs and larvae of other Scombridae.

238 EASTERN MEDITERRANEAN

STRUCTURE: Brouker and Stokes Banks Location: 38.87820°N – 25.39500°E Peak depth (m): 70-80 Base depth (m): 200-210

18 km

DESCRIPTION:

Geology

No specific geological or geographical information is available on these struc- tures which are depicted in this map: http://highsea.cz/map/GM06.JPG and these names are present in the IOC-IHO GEBCO SCUFN (Sub-Committee on Undersea Feature Names) Gazetteer database: http://www.geomapapp.org/da- tabase/GEBCO/GEBCO_gazetteer.htm

Life on and around the Seamount

These banks host a large variety of coralligenous assemblages probably representing unique habitats in the Aegean Sea in terms of size and species rich- ness (Öztürk, unpublished data). The Bruker Bank has already been studied by Kisseleve (1983) and 42 benthic species were identified at the time. These sensi- tive areas are also under the threat due to bottom , purse seining, marine litter and marine transportation (Öztürk, 2009a). Kara et al. (2000) mentioned heavy fishing pressure in the area.

No information about the pelagic communities of the Brouker and Stokes Banks has been found in the scientific literature.

239 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Danaos-2007 (Nameless) Seamount Location: 34.66586°N – 25.54216°E Peak depth (m): 450-460 Base depth (m): 780-790

18 km

DESCRIPTION:

Geology

This nameless bank is located to the SSW of Chryssi , approximately 12 nm south of Ieraptera along the south of Crete. This bank was previously unknown and consists of a raising structure formed between the Ptolemy and Pliny Trenches, with its summit lying at 450 m water depth and dropping off to in excess of 1000 m to the south (Smith et al., 2009). Due to the recent studies car- ried out in the area, it is worth to be mentioned in this Atlas compilation.

Life on and around the Seamount

Under the DANAOS project a nameless Seamount South of Crete was surveyed with manned and unmanned underwater vehicles at depths of 550-650 m. The seafloor is featured by soft silty sediments inhabited by a quite scarce fauna as suggested by the poor faunal traces (burrow openings, feeding pits, echinoid feeding tracks). The fauna observed on the soft sediments accounted for the shortnose greeneye fish Chloropthalmus ( agassizi), rare colonies of the isidid alcyonacean Isidella elongata and some unidentified red shrimps. Most of the observed rocky outcrops were populated by extremely large numbers (hundreds per square metre) of shrimps (Plesionika spp.) and small colonies of the yellow scleractinian Dendrophyllia cornigera, which was observed in at least 5-6 different sites at depths between 520-620 m, in small aggregates often associat- ed with dead coral rubble. On wider rocky outcrops the large wreckfish Polyprion( americanus), the black-spot bream (Pagellus bogaraveo) and the conger eel (Conger conger) have been observed (Smith et al., 2009).

No information about the Danaos-2007 (Nameless) Seamount pelagic communi- ties has been found in the scientific literature.

240 EASTERN MEDITERRANEAN

STRUCTURE: Eratosthenes Seamount Location: 33.74444°N – 32.73362°E Peak depth (m): 780-790 Base depth (m): 1920-1930

47 km

DESCRIPTION: flexure, induced by southward overthrusting of the Cyprus active margin. The Eratosthenes Seamount sits atop the which is being pushed toward Geology Cyprus. Tectonic subsidence of the Eratosthenes Seamount was approximately The Eratosthenes Seamount is located about 95 km synchronous with rapid surface uplift of the overriding plate. This uplift is ex- south of Cyprus and is a large (120 x 70 km) elliptical plained in terms of incipient collision of the Eratosthenes submarine plateau rising about 1300 m above the with the subduction trench (Robertson, 1998a). The Eratosthenes Seamount is surrounding that lies at depths deeper thus interpreted as a crustal continental block in the process of break up in re- than 2000 m. Its very flat, -like top lies 700 me- sponse to subduction and incipient collision of the African and Eurasian Plates. ters below at its shallowest point, and 2000 As the feature is being forced into subduction, chemical rich fluids are being meters at its deepest, and is about 30 km-wide and squeezed out of cracks in the southern part of the seamount. Shimmering water 50 km-long. The Eratosthenes Seamount is foremost was observed there with a ROV, but most of the seeps are not very hot, being the most studied seamount in the Mediterranean within 1°C of the ambient water temperature. More than 40 pockmarks were sug- Sea (Emery et al., 1966; Ben-Avraham et al., 1976; gested to be present on top of the structure, based on side-scan data Krasheninnikov et al., 1994; Mart and Robertson, (Dimitrov and Woodside, 2003), but the pockmarks turned out to be sinkholes 1998; Mascle et al., 2000; Feld et al., 2013). Several (collapsed sub-aerial caves) when inspected with a ROV system (Mayer et al., ODP sites were drilled here (Robertson, 1998a). The 2011). seamount, although being flat-topped, is slightly tilt- ed northward and sliced by a series of E-W-trending normal faults. The upper part of the Eratosthenes Seamount hosts both shallow and deep water car- bonates dating back to Early Cretaceous time. The seamount underwent several episodes of submer- gence and uplift during the geologic times. The platform was exposed during the Messinian salinity crisis (5 Ma). Global sea level changes also played a role in the deepening of the seamount from the Miocene/Pliocene to the present (Spezzaferri and Tamburini, 2007). Subsidence accelerated in the Late Pliocene–Early Pleistocene. Deformation of the Eratosthenes Seamount resulted from crustal

241 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

Life on and around the Seamount

Despite so many geological researches, the biology of this is limited to a few studies. The first benthic characterization of the seamount (Galil and Zibrowius, 1998), based on remotely collected material, reported two species of scleractinian corals (Caryophyllia calveri and Desmophyllum dianthus) (now Dendrophyllia dianthus), two species of encrusting foraminiferans, two species of encrusting sponges, abundant scyphozoan polyps, many individuals of the small actiniarian Kadophellia bathyalis, seven species of bivalves, one sipuncu- lan, one asteroid, one fish and various unidentified zoantharians and antipathar- ians. A recent study revealed concentrations of vent-like communities, including small tube worms (Siboglinidae), clams, sea urchins, and small crabs (Mayer et al., 2011). GFCM has already banned demersal fishing activities in the area of the Seamount according to the recommendation number 2006/3 and the fishing restricted areas have been established in order to protect the deep-sea sensitive . IUU fisheries, ship-originated pollution and offshore drilling carried out in recent years were stated as main threats for the pristine habitats of the Seamount and the ban of oil and gas exploration was proposed as well as the designation of the area as a SPAMI (Specially Protected Areas of Mediterranean Importance) (Öztürk et al., 2012). OCEANA cited the area among the EBSAs (Ecologically or Biologically Significant Marine Areas) in the Mediterranean Sea due to the above-cited characteristics as well as the presence of slow maturing fish species such as the Mediterranean Hoplostethus( mediterraneus), sea turtles (Chelonia mydas and Caretta caretta) and commercially important shrimps, such as Aristaeomorpha foliacea and Aristeus antennatus (OCEANA, 2014). The Eratosthenes Seamount is one of the most relevant features of the eastern Mediterranean seafloor, it is evident that international cooperation, compromise, consensus and concerted actions are needed for the sustainable exploitation of the living resources and protection of such a vulnerable environment (Öztürk and Başeren, 2008).

No information about the Eratosthenes Seamount pelagic communities has been found in the scientific literature.

242 EASTERN MEDITERRANEAN

STRUCTURE: Florence Rise Location: 34.82090°N – 31.69151°E Peak depth (m): 1560-1570 Base depth (m): 2100-2110

18 km

DESCRIPTION: correspond to mud breccias (Zitter et al., 2006). Along the Florence Rise, the relative motion between the Anatolian and African plates is sinistral, and here, Geology most characteristics of subduction zones are lacking: there is no volcanic arc, no The Florence Rise is a submarine feature extend- trench, no accretionary and low and dispersed seismicity (Woodside et al., ing from the island of Cyprus to the Anaximander 2002). The whole rise is now subsiding northward together with the Antalya Basin Mountains and is also referred to, more appropri- (Zitter, 2004). To the south of the Florence Rise, lies a 15 to 20 km-high bathymet- ately, as the Florence Ridge, it was first name by ric zone, characterized by subvertical faulting with anastomosing fault branches Biju-Duval et al. (1974). This is a very well known and positive flower structures affecting post-Messinian sediments, which is be- structure, where 2 DSDP sites were performed down lieved to be one of the most active area of the region (Hall et al., 2009). This to the thin Messinian gypsum and marlstones (Hsü typical transpressive deformation is responsible for the construction of the relief and Shipboard Scientific Party, 1978). The Florence (about 200 m) of the central part of the Florence Rise. In contrast, the core of the Rise is not part of the , but it is rise displays relatively low relief and it deepen towards the northwest . a compressional relief that was eroded during the Furthermore, the eastern deep-sea fan, subjected to extremely vigorous salt Messinian salinity crisis (Özer et al., 2009), while tectonics, seems to have collided with the Florence Ridge fold belt and to have massive deposition of salt occurred to the North generated a “salt extrusion” zone (Sellier et al., 2013). (Antalya basin) and to the South (Herodotus abyssal The area remains within the one proposed as a SPAMI by UNEP-MAP-RAC/SPA plain). On the Florence Ridge itself, the base of salt (2010). evolves laterally to a Messinian erosional surface that erodes a series of stacked . This surface Life on and around the Seamount is involved in recent faulting (Sellier et al., 2013). No information about the benthic and pelagic communities of the Florence Rise The eastern Florence Rise includes a topographic has been found in the scientific literature. high near Cyprus, rising from the Antalya Basin for about 600 m. The eastern high shows a rhombohe- dral shape delimited by two major trends, roughly 130°N and 70°N near-vertical faults, with a relief ex- pression on the seafloor of about 150 m (Woodside et al., 2002). Several mud volcanoes exist along the Florence Ridge and are related to N°150 transpres- sive faults or secondary transcurrent N-S oriented faults. Sediments along those mud volcanoes

243 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Hecataeus Rise and Hecataeus Knoll Hecataeus Rise (HCT-1) Location: 34.44201°N – 34.34533°E Peak depth (m): 1090-1100 Base depth (m): 1510-1520

Hecataeus Knoll (HCT-2) Location: 34.44025°N – 33.61840°E Peak depth (m): 190-200 Base depth (m): 690-700

HCT-1 HCT-2

47 km

DESCRIPTION:

Geology

The Hecataeus Knoll rises to about 200 m below sea-level and comprises twin highs in its central, shallowest part. The Hecataeus Rise is located directly south of Cyprus and forms a broad ridge with a steep southern slope rising ~ 1800 m from the seafloor of the Levantine Basin. This feature is arguably continental crust or part of an ophiolite suite, as indicated by a weak positive magnetic anomaly over the rise (Robertson, 1998b). The Hecataeus Rise is separated from the Island of Cyprus by the Cyprus Basin, which is ~ 50 km-wide and 2 km-deep and contains about 1 km of post-Miocene sediments (Ben-Avraham et al., 1995). Seismic profiles of the Hecataeus Rise reveal a relatively thin, nearly transparent Pliocene–Pleistocene sediment suc- cession, underlain by a relatively steeply dipping, folded lower unit. Messinian evaporites are absent from both the Hecataeus Rise and the Latakia Ridge fur- ther east, suggesting that these areas were raised, emergent features during the Messinian Salinity Crisis. The southern side of the Hecataeus Rise is folded and cut by southward-dipping steep faults (Robertson, 1998b; Rahimi et al., 2013).

Life on and around the Seamount

No information about the benthic and pelagic communities of the Hecataeus Knoll has been found in the scientific literature.

244 EASTERN MEDITERRANEAN

STRUCTURE: Ira and Navtilos Banks Location: 38.67146°N – 24.24609°E Peak depth (m): 40-50 Base depth (m): 260-270

17 km

DESCRIPTION:

Geology

No specific geological or geographical information is available on this structure which is depicted in this map: http://highsea.cz/map/GM06.JPG

Life on and around the Seamount

No information about the benthic and pelagic communities of the Ira and Navtilos Banks has been found in the scientific literature.

245 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Karpas Ridge Location: 35.88444°N – 34.88554°E Peak depth (m): 50-60 Base depth (m): 360-370

18 km

DESCRIPTION:

Geology

No specific geological or geographical information is available on this struc- ture, which is present at this database: http://www.marineregions.org/gazetteer. php?p=details&id=4171

Life on and around the Seamount

The site is located in the northern Levantine Sea, NE of Cyprus and close to Turkey and . The sea bottom hosts mixed habitats including rocky outcrops, muddy beds, shell fragments, cobbles, etc. and important communities of sea- grass (Posidonia oceanica) and algae (Cystoseira crinita, Sargassum vulgare, Padina pavonica, Flabelia petiolata, etc.) with the presence of diverse species of , sponges, bryozoans, sipunculids, etc. (Açik et al., 2005; Çinar, 2005; Kocak et al., 2002).

This area is under the influence of the Latakia Eddy. As for the Latakia escarp- ment proposal, this area is of high interest because it is one of the most impor- tant spawning grounds for bluefin tuna Thunnus( thynnus). Furthermore, it is also within the distribution range of loggerhead and green turtle (Caretta caretta and Chelonia mydas). This area is under intense fishing pressure because of the rela- tively high presence of large pelagic fish (OCEANA, 2014).

246 EASTERN MEDITERRANEAN

STRUCTURE: Kaş Bank Location: 35.58756°N – 29.33301°E Peak depth (m): 91 Base depth (m): ND

45 km

DESCRIPTION:

Geology

No specific geological or geographical information is available on this structure, which is depicted in this map: http://highsea.cz/map/INT302.JPG .

Life on and around the Seamount

Many years ago this bank harbored large quantities of commercial sponges.

The Kaş Bank is a rich fishing ground for swordfishXiphias ( gladius) and scom- brids. Besides, red coral (Corallium rubrum) colonies have been reported in 1990’s (Öztürk, 2009b).

247 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Kolumbo Volcano Location: 36.52070°N – 25.47170°E Peak depth (m): 10-20 Base depth (m): 280-290

9 km

DESCRIPTION: -10 m above the crater floor (500 m below sea level). Dissolution of the gas likely causes local increases Geology in water density that result in sequestration of CO2 Kolumbo is a located in the Aegean Sea and is the largest within the enclosed crater, and the accumulation of one among a series of submarine centers that extend 20 km to the northeast of acidic . Lack of macrofauna at the Kolumbo the island of ( Island). The volcanoes lie within a which ends in hydrothermal vents, occurrence of carbonate-poor the southwest as normal faults that dissect the northern wall of the island sediment in the crater, and pH values as low as 5.0 of Thera. The “Kameni-Kolumbo Line” is an active, 40 km-long, strike-slip fault in recovered water samples point to acidic condi- zone and runs through the volcanoes of Nea Kameni (a small island inside the tions within the crater (Carey et al., 2013). The site collapsed Santorini caldera) and Kolumbo and controls the spatial distribution is a remarkable example of extreme acidifica- of the volcanic cones along the axis of the Anyhdros Basin, located northeast tion and its challenge to marine life (Brewer, 2013). of the Thera Island (Sakellariou et al., 2010). Kolumbo consists of a 3 km-wide cone with a 1500 m-wide crater, a rim as shallow as 10 m below sea level in Life on and around the Seamount the southwest, and a crater floor located about 500 m below sea level (Carey et Marine ecosystems in which nitrifying Archaea bac- al., 2011). It was last active in 1650 CE, when an explosive eruption produced teria are important were recently discovered on the hot surges that spread over the sea surface and caused 70 deaths on Thera hydrothermal vents of the Kolumbo Volcano consid- and other extensive damage caused by the inundation (Fouqué, 1879). ered a geologically, mineralogically and biologically During the 1650 CE eruption, the volcano broke the surface and produced an unique place (Kilias et al., 2013). The volcano has ephemeral bank that was subsequently eroded below the surface. The a cone that rises up to 18 m, which makes it reach- submarine crater wall consists of a spectacular sequence of well-bedded able and vulnerable to potential anthropic threats. pumice deposits. A large part of the upper cone consists almost exclusively of Besides, this area is known to be frequented by very loose pyroclastic material that is actively slumping into the caldera. Recent the Monachus monachus marine geological investigations of the Kolumbo volcano using ROVs revealed a (Marchessaux and Duguy, 1977). Due to the pres- very active high-temperature field that is about 25,000 m2 in ence of gas hydrates, highly migratory fish species area in the northeastern part of the crater floor. Vent chimneys up to 4 m-high are and seamount benthic communities, this area was vigorously emitting colorless gas plumes up to 10 m-high in the . suggested by OCEANA (2014) to meet the EBSAs Temperatures as high as 220°C were recorded in vent fluids. Some vents are criteria. located in crater-like depressions that contain debris from collapsed extinct chim- neys (Carey and Sigurdsson, 2007; and Fuller, 2011). Acoustic imaging of the ascending bubbles suggests that the gas is being dissolved into seawater within

248 EASTERN MEDITERRANEAN

STRUCTURE: Larnaka Ridge Location: 35.27495°N – 35.09294°E Peak depth (m): 840-850 Base depth (m): ND

46 km

DESCRIPTION:

Geology

The Larnaka Ridge is a broad arcuate ENE-WSW oriented structure, extending from southeastern Cyprus toward southeast Turkey. It forms the southern bound- ary of the Latakia Basin and merges in the southeast with the northern portion of the Tartus Ridge of the Latakia Ridge, very close to the Syrian coast (Hall et al., 2005). Ophiolitic basement rocks are believed to form the core of the Larnaka Ridge (Robertson, 1998b).

Life on and around the Seamount

No information about the benthic and pelagic communities of the Larnaka Ridge has been found in the scientific literature.

249 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Latakia Ridge Location: 35.13782°N – 35.54911°E Peak depth (m): 890-900 Base depth (m): ND

46 km

DESCRIPTION: Life on and around the Seamount

Geology This area is ecologically important because it is one of the spawning grounds for the bluefin tunaThunnus The Latakia Ridge is a prominent arcuate NE trending bathymetric feature which thynnus (Karakulak et al., 2004). Besides, it harbors stands 100-500 m above the adjacent seafloor, linking the Hecataeus Rise with the endangered sea turtle species Caretta caretta the Latakia region of the northern Levantine coast. The northeastern part of the and Chelonia mydas and was therefore suggested to Latakia Ridge is characterised by a prominent NNE-trending narrow ridge less meet the criteria for EBSAs (OCEANA, 2014). Also, than 20 km in width with maximum height of approximately 3600 m and steep the designation of this area as a High Seas Marine slopes (Tartus Ridge). There are several smaller ridges with lower relief which Protected Area was previously proposed due to un- follow the general trend of the Latakia Ridge and merge with the Tartus Ridge. exploited commercially important deep-sea shrimps Towards the southwest, the Latakia Ridge merges gradually with the Hecataeus stocks (Öztürk, 2009a). Some sparse information on Rise and displays very little topographic relief with uniform and conformable dep- the Cetacean fauna in the area are found in Kerem osition of Oligocene – Miocene sediments (Robertson, 1998b; Bowman, 2011). et al. (2012). The Plio-Quaternary structure of the Latakia Ridge is interpreted as a positive No information about the benthic communities of flower structure (Hall et al., 2005). Ben-Avraham et al. (1995) showed that the the Latakia Ridge has been found in the scientific Latakia Ridge is a young and active feature which delineates the present-day literature. plate boundary between the African and Anatolian plates, along the eastern Cyprus Arc. They suggested that the ridge probably originated as a large thrust sheet during the southward migration of the plate boundary, and that became a zone of wrench faulting when the convergence direction changed. They noted that wrench faulting is more pronounced in the Tartus Ridge.

250 EASTERN MEDITERRANEAN

STRUCTURE: Literi Bank Location: 38.81486°N – 24.85928°E Peak depth (m): 70-80 Base depth (m): 210-220

17 km

DESCRIPTION:

Geology

No specific geological or geographical information is available on this structure which is depicted in this map: http://highsea.cz/map/GM06.JPG

Life on and around the Seamount

No information about the benthic and pelagic communities of the Literi Bank has been found in the scientific literature.

251 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Mansel and Johnston Banks Location: 39.29600°N – 25.38780°E Peak depth (m): 30-40 Base depth (m): 190-200

17 km

DESCRIPTION:

Geology

No specific geological or geographical information is available on this structure except for the study of Banolessy et al. (1978), which is no more available for reading. The structure is depicted in this map: http://highsea.cz/map/GM06.JPG

Life on and around the Seamount

The Johnston Bank is covered by maërl beds that are among the most valuable Mediterranean coralligenous communities (Aktan, 2010). The bank seems to be a nursery ground for several taxa. In total, 2288 individuals belonging to 51 taxa have been reported on the bank (Topaloğlu et al., 2010) and has been suggested to be designated as a protected area (Öztürk, 2009a).

No information about the pelagic communities of the Mansel and Johnston Banks has been found in the scientific literature.

252 EASTERN MEDITERRANEAN

STRUCTURE: Mediterranean Ridge W. Mediterranean Ridge (W-MRG) Location: 33.77267°N – 22.70907°E Peak depth (m): 1150-1160 Base depth (m): 2190-2200

E. Mediterranean Ridge (E-MRG) Location: 34.95354°N – 27.46288°E Peak depth (m): 350-360 Base depth (m): 1240-1250

94 km

91 km

DESCRIPTION:

Geology

The Mediterranean Ridge is the most prominent topographic feature and the foremost studied morpho-structural unit in the Eastern Mediterranean Sea (see Limonov et al., 1996 for a review of the initial research activities carried on the ridge). The Mediterranean Ridge is of course more than a seamount, because it stretches from the Calabrian Arc in the northwest to the Cyprus Arc in the east, a distance of about 1500 km, with a width ranging from about 150 to 300 km.

253 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

Notwithstanding, we have decided to include it as a unique structure in this Atlas. evaporites by seawater (Corselli and Basso, 1996). The ridge has an arcuate southward-convex shape, almost parallel to the Hellenic Since they were first discovered and described Arc, and lies at an average water depth of about 2100-2200 m. Because of its (Camerlenghi, 1990), these anoxic basins have at- large width the general slope angles rarely exceed 2° (Limonov et al., 1996). It can tracted many scientists especially microbiologists, be divided in the Western Mediterannean Ridge, which roughly trends NNW-SSE who have now provided evidence that these extreme and the Eastern Mediterranean Ridge, which roughly trends ENE-WSW (Huguen ecosystems are in-habited by prokaryotes, proto- et al., 2001). The Western Mediterranean Ridge topography is dominated by zoa and some metazoans ( et al., 2009; small, closely spaced depressions and ridges, with a relief of 50-100 m, mostly Danovaro et al., 2010; Edgcomb et al., 2011). parallel to the overall ridge trend. This kind of seafloor morphology is broadly known as the ‘cobblestone topography’. The Mediterranean Ridge is considered Life on and around the Seamount to be the Neogene to Recent accretionary prism created by the scraping and ac- The outstanding geology of this area ensures the oc- cumulation of the upper part of the sediments deposited on the top of the down- currence of a variety of biologically and ecologically going African plate (Le Pichon et al., 1995). An estimated 40-60% of the avail- significant structures. There are several mud volca- able sedimentary input was accreted in the Western Mediterannean Ridge, where noes on the ridge (Olu-Le Roy et al., 2004) and these the collision between Europe and Africa is less accentuated (Kopf et al., 2003). volcanoes, which are cold seeps, harbour chemos- Compressional deformation intensively disturbs the sediment cover and the ynthetic communities (Corselli and Basso 1996; Olu- basement, creating folds, reverse faults, thrust and strike-slip faults (Westbrook Le Roy et al., 2004) that constitute oases and Reston, 2002). Beneath most of the accretionary complex, the subducting in the otherwise “desertic” deep Mediterranean Sea. crust of the African plate is oceanic, but along its southern margin in its central The Napoli mud volcano is prominent among others sector, the accretionary complex is colliding with the continental margin of Africa, by the diversity of higher taxa (Ritt et al., 2012). The off (Chaumillon and Mascle, 1997). The southern margin is in fact shown communities of the Eastern Mediterranean mud vol- by a positive gravity anomaly (Le Pichon et al., 2002). The sedimentary cover canoes seem to host a higher diversity with respect of the ridge is composed of about 200-700 m of Plio-Quaternary hemipelagic to similar communities found in other oceans includ- and turbiditic deposits, over 1 km of Messinian evaporites on the deeper flanks, ing also neo-endemic species and differing for the and several kilometers of pre-Messinian and Cretaceous sediments. The core smaller size of the bivalves (Olu-Le Roy et al., 2004). of the Mediterranean Ridge backstop consists of a pile of Hellenic nappes that migrated outward from the Aegean within the adjacent Mediterranean This area is important for marine mammals since basins during late middle Miocene, about 15 Ma, and the present Mediterranean such environments have rich and diverse benthic Ridge has developed since that time by of a new wedge (Le Pichon et ecology associated with methane-rich fluid seeps al., 2002). and thus could be the base of food chains that The Mediterranean Ridge is densely marked by pockmarks and mud volcanoes, reach top predators like the deep-diving whales these latter being the real seamounts of this structure. The mud volcano fields, (Woodside et al., 2006) such as Cuvier’s beaked from west to east, are: the Cobblestone area, Pan di Zucchero, Prometheus II, whales, (Ziphius cavirostris) and sperm whales Olimpi field, the Southern Belt and the United Nations Rise mud fields (Akhmanov (Physeter catodon). and Woodside, 1998; Huguen et al., 2004; Chamot-Rooke et al., 2005). Some Although very limited information is available from of the mud volcanoes are: Novorossiysk, Aros, Prometheus in the Cobblestone the eastern Mediterranean Ridge, it was presented area; Toronto, Maidstone, Moscow, Napoli, Milano, Milford Haven, Leipzig, Nice as a high area due to upwelling process and Gelendzhik in the Olimpi-Prometheus area; Stoke-on-Trent, Dublin on the and was suggested by OCEANA (2014) as an EBSA United Nation Rise (Dimitrov, 2002; Dimitrov and Woodside, 2003; Huguen et al., in the Mediterranean due mainly to the presence 2004). The Napoli and Milano mud volcanoes have been drilled during the ODP of highly migratory species including marine mam- Leg 160 (Robertson and Shipboard Scientific Party, 1996). All these names, like mals, sharks and pelagic fish (OCEANA, 2014). all the names given by marine scientists to mud volcanoes around the world, are to be considered unofficial and you will not find them for now in any undersea feature name compilations. Mud volcanoes slowly release hydrogen sulfide, methane and other hydrocar- bon-rich fluids in the water column and, for this reason, they are considered pos- sible players in the global greenhouse gas emission budget and the consumption of oxygen at the seafloor (Boetius and Wenzhöfer, 2013). Uncertainties remain regarding the quantity of free methane that is emitted from deep-water seeps into the water column, with several authors showing that, at least in deep-sea gas hydrates scenarios, most of the methane emitted per year within the gas hydrate stability zone remain trapped in the deep ocean (e.g. Römer et al., 2012), with a more optimistic vision in respect to previous, probably oversimplified, studies (e.g. Kopf, 2003). Brine lakes are present near the front of the accretionary complex and first pro- vided evidence of interaction between tectonics, fluid flow and dissolution of the

254 EASTERN MEDITERRANEAN

STRUCTURE: Ptolemy Seamount Location: 34.62513°N – 24.56142°E Peak depth (m): 1050-1060 Base depth (m): 1820-1830

18 km

DESCRIPTION: Life on and around the Seamount

Geology This area is subject to seasonal strong upwelling which greatly increases primary productivity and it A large plateau occurs on the eastern Mediterranean sea floor south of cen- was cited by OCEANA among the Mediterranean tral and eastern Crete Island. The western E-W elongated portion is known as areas meeting scientific criteria for Ecologically and the Ptolemy Mountains, here we name it seamount. The larger eastern portion Biologically Significant Areas (EBSAs according to (DANAOS 2007-Nameless Seamount in this Atlas) was surveyed for the first time Convention on Biological Diversity) due mainly to the in 2007 by the DANAOS project for archaeological purposes (http://nautica- presence of large cetaceans and sharks (OCEANA, larch.org/danaos/Geological.html). The overall plateau is bordered to the north 2014). Although no study specific to the area was by the Ptolemy Trench, to the south by the Pliny Trench, and to the east by the carried out, the area is known to harbour important Cretan-Rhodos Ridge. This plateau represents a tectonic block created by the populations of the blue shark (Megalofonou et al., African-Aegean plate convergence. Its boundaries are active faults: the northern 2009) and it is a longline fishing ground for pelagic boundary (Ptolemy trench) is a left-lateral strike-slip fault extending onto Crete species such as albacore tuna (Thunnus alalunga) as the Ierapetra normal fault. The southern boundary (Pliny trench) consists of and swordfish Xiphias ( gladius) with blue shark an en-echelon series of elongated depocenters, whose geometry reflects left- (Prionace galuca) as bycatch. This area is also lateral transform motion along the trench axis. Continental rocks form the alpine known for the regular presence of sperm whales basement of Late Cenozoic deposits on both sides of the Pliny trench and are (Physeter catodon) and of the Cuvier’s Beaked locally outcropping along the steep walls. Thus deformation takes place within Whales (Ziphius cavirostris) (Würtz, 2010; OCEANA the Aegean continental margin, which demonstrates that former or present-day 2014). subduction along this trench is improbable. The thinned continental margin can be interpreted to function as a crustal wedge in the deformation zone at No information about the benthic communities of the the African-Eurasian , leading to the formation of an ac- Ptolemy Seamount has been found in the scientific cretionary prism of tectonized sediments, the Mediterranean Ridge (Peters and literature. Huson, 1985). Notwithstanding the occurrence of strike-slip motion parallel with the Pliny–Strabo “trenches”, trench-normal thrusting is not observed so far and it is more likely ascribable to a zone between the Aegean in the NW and the African lithosphere in the SE (Özbakır et al., 2013). The western boundary of the plateau is a series of normal faults (Galanopoulos, 1974).

255 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Sinaya Bank Location: 38.86362°N – 25.78698°E Peak depth (m): 70-80 Base depth (m): 210-220

17 km

DESCRIPTION:

Geology

No specific geological or geographical information is available on this structure which is depicted in this map: http://highsea.cz/map/GM06.JPG

Life on and around the Seamount

The most represented habitats of the Sinaya Bank are sandy and muddy sea- floors. A 2010 study reported 17 benthic species and several (Topaloğlu et al., 2010). In addition, 490 individuals belonging to 17 taxa were successively found on the Bank. The Sinaya Bank also need protection from harmful fishing activities and various types of pollution.

No information about the Sinaya Bank pelagic communities has been found in the scientific literature.

256 EASTERN MEDITERRANEAN

STRUCTURE: Turgut Reis Bank Location: 35.02200°N – 35.01300°E Peak depth (m): 1110-1120 Base depth (m): 1350-1360

9 km

DESCRIPTION:

Geology

Very little knowledge is available over the Turgut Reis Bank, located between Turkey, Cyprus and Syria. It is believed that the area is underlain by streched continental crust.

Life on and around the Seamount

Although very limited information is available for the area, some data account for the presence of sharks (the blackmouth dogfish Galeus melastomus and the spiny dogfish Squalus acanthias), fish, such as the greater forkbeard Phycis ( blennoides) and commercially important deep-sea shrimps (Plesionika martia, Aristaeomorpha foliacea and Aristeus antennatus) (Öztürk et al., 2010). Besides, live and dead communities of polychaetes, bivalves and sponges were found associated with cold seeps. The area was suggested to be designated as a High Sea or sensitive deep-sea habitat (GFCM Fisheries Restricted Area) due to its fragil- ity and vulnerability to deep-sea trawling activities (Öztürk, 2009a; Öztürk et al., 2010). Furthermore, the bank is within the area proposed to be designated as a SPAMI (UNEP-MAP-RAC/SPA, 2010).

No information about the pelagic communities of the Turgut Reis Bank has been found in the scientific literature.

257 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

STRUCTURE: Venus Bank Location: 40.23870°N – 25.02910°E Peak depth (m): 150-160 Base depth (m): 350-360

DESCRIPTION:

Geology

The Venus Bank lies very close to the Gökçeada Island in the northern Aegean Sea in proximity of the Saroz Trough, along the seismically active North Anatolian Fault (NAF). The NAF, accommodates the strike-slip movement of the Anatolian Plate, and continues through northern Turkey into the Marmara Sea and the of Saroz. The Gökçeada Island with its high and rough topography, underwent strong uplift. The island is characterized by a variety of morphological and coast- al features such as paleo-coastal notches, hanging valleys, waterfalls, springs and travertine formation (Koral et al., 2007). No specific geological or geographical information is available on this structure which is depicted in this map: http://highsea.cz/map/GM06.JPG and this name is present in the IOC-IHO GEBCO SCUFN (Sub-Committee on Undersea Feature Names) Gazetteer database: http://www.geomapapp.org/database/GEBCO/ GEBCO_gazetteer.htm

Life on and around the Seamount

The site harbours cold water corals (Lophelia pertusa and Madrepora oculata) (OCEANA, 2014). Corals occurrence is likely related to the regime of circulation patterns in the area.

The area, located in the Northern Aegean Sea, is within the distribution range of the monk seals (Monachus monachus) (Hoyt and Notarbartolo di Sciara, 2008) and that of the blue sharks (Prionace glauca) (Megalofonou et al., 2009). It is cited among the critical habitats for cetaceans by Hoyt and Notarbartolo di Sciara (2008). The area was suggested to meet the criteria for EBSAs by OCEANA 17 km (2014) and is part of the area proposed to be designated as a SPAMI (UNEP- MAP-RAC/SPA, 2010).

258 EASTERN MEDITERRANEAN

STRUCTURE: Yunus Bank Location: 37.14237°N – 26.25719°E Peak depth (m): 100-110 Base depth (m): 300-310

18 km

DESCRIPTION:

Geology

No specific geological or geographical information is available on this structure.

Life on and around the Seamount

Coralligenous communities constitute the most important ‘hot-spot’ of species diversity of the Yunus Bank (Öztürk, 2011). The macrozoobenthic invertebrate fauna of the bank includes several sponges such as the commercial species Spongia officinalis and the non-commercial Axinella polypoides and Agelas oroides. Besides, gorgonians Eunicella singularis and Paramuricea clavata were also reported. The spiny lobsters (Palinurus elephas) were also found in the caves of the bank.

No information about the pelagic communities of the Yunus Bank has been found in the scientific literature.

259 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

References Bohrmann G., Aljuhne A., Dehning K., Ferreira C., Feseker T., Gür- can E.S., Hacioğlu E., Leymann T., Meinecke G., Pape T., Ren- ken J., Roemer M., Spiesecke U. and T.vV. Wahl, 2013. Report and Preliminary Results of R/V POSEIDON Cruise P462. Izmir Açik S., Murina G.V., Çinar M.E. and Z. Ergen, 2005. Cyprus Sipun- – Izmir, 28 October – 21 November, 2013. Gas Hydrate Dynam- culans from the coast of (eastern Mediterranean ics of Mud Volcanoes in the Submarine Anaximander Mountains Sea). Zootaxa, 1077, 1–23. (Eastern Mediterranean). Berichte, MARUM – Zentrum für Marine Umweltwissenschaften, Fachbereich Geowissenschaften, Uni- Akhmanov G.G. and J.M. Woodside, 1998. Mud Volcanic Samples versität Bremen, No. 300, 51 pp. Bremen. ISSN 2195-9633. in The Context Of The Mediterranean Ridge Mud Diapiric Belt. In: Robertson A.H.F., Emeis K.-C., Richter C. and A. Camerlenghi Bowman S.A., 2011. Regional seismic interpretation of the hydrocar- (eds.), Proceedings of the Ocean Drilling Program, Scientific Re- bon prospectivity of offshore Syria. GeoArabia, 16 (3), 95-124. sults, 160, pp. 596-605

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Fouqué, F., 1879. Santorin et ses éruptions. G. Masson, Paris. Karakulak S., Oray I., Corriero A., Aprea A., Spedicato D., Zubani Galanopoulos A.G., 1974. On the tectonic processes along the Hel- D., Santamaria N. and G. De Metrio, 2004. First Information on lenic Arc. Annals. Geophys., 27 (3-4), 429-442. the Reproductive Biology of the Bluefin Tuna Thunnus( Thynnus) in the Eastern Mediterranean. Col. Vol. Sci. Pap. ICCAT, 56 (3): Galil B. and H. Zibrowius, 1998. First benthos samples from Erato- 1158-1162. sthenes Seamount, eastern Mediterranean. Senckenb. Marit., 28 (4- 6), 111-121. Kerem D., Hadar N., Goffman O., Scheinin A., Kent R., Boisseau O. and U. Schattner, 2012. Update on the Cetacean Fauna of the Gheerardyn H. and K.H. George, 2010. New representatives of the Mediterranean Levantine Basin. Open. Mar. Biol. J., 6, 6 -27. genus Ancorabolina George, 2006 (Copepoda, Harpacticoida, Ancorabolidae) including remarks on ancorabolid phylogeny. Zool. J. Linn. Soc., 158 (1), 1096-3642. Kilias S. P., Nomikou P., Papanikolaou D., Polymenakou P.N., Godel- itsas A., Argyraki A., Carey S. Gamaletsos P., Mertzimekis T.J., G onenc T., Ergun M. and E.Z. Oral, 2004. Structure Anaximander Stathopoulou E., Goettlicher J., Steininger R., Betzelou K., Liva- Mountains with the system of the Eastern Mediterranean. Rapp. nos I., Christakis C., Bell K.C. and M. Scoullos, 2013. New in- Comm. int. Mer Mèdit., 37, 33. sights into hydrothermal vent processes in the unique shallow- submarine arc-volcano, Kolumbo (Santorini), Greece. Sci. Rep., Gücü A.C. and B. Öztürk, 2010. Scientific rationale for the proposed 3, Article number: 2421. CİESM North Marine Peace Park. Marine Peace Parks in the Mediterranean a CIESM Proposal. CIESM Workshop, 41, 61- Kocak F., Balduzzi A. and H.A. Benli, 2002. Epiphytic bryozoan com- 68. munity of Posidonia oceanica (L.) Delile meadow in the northern Cyprus (Eastern Mediterranean). Indian J. Mar. Sci., 31 (3), 235- Hall J., Calon T. J., Aksu A.E. and S.R. Meade, 2005. Structural evo- 238. lution of the Latakia Ridge and Cyprus Basin at the front of the Cyprus Arc, eastern Mediterranean Sea. Mar.. Geol., 221 (1), 261- 297. Kopf A., 2003. Global methane emission through mud volcanoes and its past and present impact on the Earth’s climate. Int. J. Hall J., Aksu A.E., Yaltırak C. and J.D. Winsor, 2009. Structural ar- Earth. Sci. (Geol Rundsch), 92, 806-816. chitecture of the Rhodes Basin: A deep depocentre that evolved since the Pliocene at the junction of Hellenic and Cyprus Arcs, Kopf A., Mascle J. and D. Klaeschen, 2003. The Mediterranean eastern Mediterranean. Mar. Geol., 258, 1-23. Ridge: A mass balance across the fastest growing accretionary complex on Earth. J. Geophys. Res., 108, 2372-2402. Hoyt E. and G. Notarbartolo di Sciara, 2008. Distribution and overlap of critical habitats of Mediterranean top marine predators. Work- shop: “Species information for designing and managing marine Koral H., Öztürk H. and N. Hanilci, 2007. Modes of Tectonics in protected areas: improving access and integration”, World Con- Gökçeada Island, Northern Aegean Sea: Implications for the servation Congress, Barcelona, 6 October 2008. North Anatolian Fault. Rapp. Comm. int. Mer Medit., 38, 101.

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Krasheninnikov V.A., Udintsev G.B., Mouraviov V. and J.K. Hall, Olu-Le Roy K., Sibuet M., Fiala-Médioni A., Gofas S., Salas C., Mari- 1994. Geological structure of the Eratosthenes Seamount. In: otti A., Foucher J.P. and J. Woodside, 2004. communi- Krasheninnikov, V.A., and J.K. Hall (eds.), Geological Structure of ties in the deep Eastern Mediterranean Sea: composition, sym- the Northeastern Mediterranean (Cruise 5 of the Research Vessel biosis and spatial distribution on mud volcanoes. Deep-Sea Res. Akademik Nokolaj Strakhov). Jerusalem (Historical Productions- Part I, 51, 1915-1936. Hall Ltd.), pp. 113-130.

Özbakır A.D., Şengör A.M.C., Wortel M.J.R. and R. Govers, 2013. Le Pichon X., Chamot-Rooke N. and S. Lallemant, 1995. Geodetic The Pliny–Strabo trench region: A large shear zone resulting from determination of the kinematics of central Greece with respect slab tearing. Earth Plan. Sci. Lett., 375, 188–195. to Europe: Implications for Eastern Mediterranean tectonics. J. Geophys. Res., 100, 12675-12690. Ozel E., Ulug A. and B. Pekcetino, 2007. Neotectonic aspects of the northern margin of the Adana-Cilicia submarine basin, NE Medi- Le Pichon X., Lallemant S. J., Chamot-Rooke N., Lemeur D. and G. terranean. J. Earth Syst. Sci., 116 (2), 113-124. Pascal, 2002. The Mediterranean Ridge backstop and the Hel- lenic nappes. Mar. Geol., 186 (1-2), 111-125. Özer P., Hall J., Çifçi G., Aksu A., Dondurur D. and C. Yaltirak, 2009. Neogene history of the Florence Rise at the paleo- of the Limonov A.F., Woodside J.M., Cita M.B. and M.K. Ivanov, 1996. The African plate with the Aegean-Anatolian microplate in the eastern Mediterranean Ridge and related mud diapirism: a background. Mediterranean: results from recent seismic reflection profiling. Mar. Geol., 132, 7-19. EGU General Assembly Conference Abstracts, 11, 4871.

Lykousis V., Alexandri S., Woodside J., De Lange G., Dählmann A., Öztürk A.A., Tonay A.M. and A. Dede, 2013. Sperm whale (Physeter Perissoratis C., Heeschen K., Ioakim C., Sakellariou D., Nomikou macrocephalus) sightings in the Aegean and Mediterranean part P., Rousakis G., Casas D., Ballas D. and G. Ercilla, 2009. Mud vol- of Turkish waters. J. Black Sea/Mediterranean Environment, canoes and gas hydrates in the Anaximander mountains (Eastern 19 (2), 169 -177. Mediterranean Sea). Mar. Pet. Geol., 26 (6), 854-872.

Marchessaux D. and R. Duguy, 1977. Le phoque moine, Monachus Öztürk B., 2007. Results of the Aegean Sea expedition, Unpublished report, Istanbul Univeristy, 45 pp. (in Turkish). monachus (Hermann, 1779) en Grece. Mammalia, 41 (4), 419- 439. Öztürk B., 2009a. Marine protected areas in the high seas of the Ae- Mart Y. and A.H.F. Robertson, 1998. Eratosthenes Seamount: an gean and Eastern Mediterranean Seas, some proposals. J. Black oceanographic yardstick recording the Late Mesozoic-Tertiary Sea/Mediterranean Environment, 15, 69-82. geological history of the Eastern Mediterranean. In: Robertson A.H.F., Emeis K.-C., Richter C. and A. Camerlenghi (eds.), Pro- Öztürk B., 2009b. Red coral and its actual situation in Turkey. In: ceedings of the Ocean Drilling Program, Scientific Results, , 160 Bussoletti E., Cottingham D., Bruckner A., Roberts G., Sandulli R. pp. 701-708. (eds.), Proceedings of the International Workshop on Red Coral Science, Management and Trade: Lessons from the Mediterra- Mascle J., Benkhelil J., Bellaiche G., Zitter T., Woodside J. and L. nean, 23-26 September, 2009, Naples, Italy, p. 119. Loncke, 2000. Marine geologic evidence for a Levantine-Sinai plate, a new piece of the Mediterranean puzzle. Geology, 28, Öztürk B., 2011. Marine Essays, İlke Kitap. Istanbul. Turkey, 378 pp. 779-782. (in Turkish).

Mayer L., Bell K.L.C., Ballard R., Nicolaides S., Konnaris K., Hall J., Tibor G., Austin Jr. J.A. and T.M. Shank, 2011. Discovery of sink- Öztürk B. and S.H. Başeren, 2008. The exclusive economic zone holes and seeps on Eratosthenes Seamount. In: New Frontiers in debates in the Eastern Mediterranean Sea and fisheries.J. Black : The E/V Nautilus 2010 field season. Ocean- Sea/Mediterranean Environment, 14, 77-83. ography, 24, 28-29. Öztürk B., Topçu E.N. and B. Topaloğlu, 2010. A preliminary study on Megalofonou P., Damalas D. and G. De Metrio, 2009. Biological two seamounts in the Eastern Mediterranean Sea. Rapp. Comm. characteristics of blue shark, Prionace glauca, in the Mediterra- int. Mer Médit., 39, 620. nean Sea. J. Mar. Biol. Assoc. U. K., 89 (6), 1233-1242. Öztürk B., Topcu E.N. and B. Topaloğlu, 2012a. The submarine can- OCEANA, 2014. Scientific Information to Describe Areas Meeting yons of the Rhodes basin and the Mediterranean coast of Turkey. Scientific Criteria for Mediterranean EBSAs.(Information provided In: Würtz M. (ed.), Mediterranean Submarine Canyons: Ecology by OCEANA to CBD and UNEP/MAP for the Mediterranean EBSA and Governance. Gland, Switzerland and Málaga, : IUCN, Workshop, March 2014), Madrid, 144 pp. pp. 65-71.

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Öztürk B., Topçu E.N. and Ç. Keskin, 2012b. SPAMI Proposals For Sellier N.C., Loncke L., Vendeville B.C., Mascle J., Zitter T., Wood- Finike (Anaximander) and Mediterranean (Eratosthenes) Sea- side J. and B. Loubrieu, 2013. Post-Messinian evolution of the mounts in the Eastern Mediterranean Sea. The 2012 Forum of Florence Ridge area (Western Cyprus Arc), Part I: Morphostruc- Marine Protected Areas in the Mediterranean, 25-28 November tural analysis. Tectonophysics, 591, 131-142. 2012, Antalya, Turkey. Shank T.M., Herrera S., Cho W., Roman C.N. and K.L.C. Bell, 2011. Peters J.M. and W.J. Huson, 1985. The Pliny and Strabo trenches Exploration of the Anaximander mud volcanoes. In: Bell K.L.C. (eastern Mediterranean): Integration of seismic reflection data and S.A. Fuller (eds.), New Frontiers in Ocean Exploration: The and SeaBeam bathymetric maps. Mar. Geol., 64 (1-2), 1-17. E/V Nautilus 2010 Field Season. Oceanography, 24 (1), supple- ment, pp. 22-23.

Rahimi A., Welford K., Hall J., Hübscher C., Louden K. and A. Ehrhardt, 2013. A wide-angle seismic survey of the Hecataeus Smith C., Sakellariou D., McCoy F. and S. Wachsmann, 2009. Deep Ridge, south of Cyprus: a microcontinental block from the African coral environments south of Crete. 9th Symposium on Oceanog- plate docked in a subduction zone? EGU General Assembly Con- raphy & Fisheries, 2009 - Proceedings, Ι, 665-668. ference Abstracts, 15, 2663. Spezzaferri S. and F. Tamburini, 2007. Paleodepth variations on Reston T.J., von Huene R., Dickmann T., Klaeschen D. and H. Kopp, the Eratosthenes Seamount (Eastern Mediterranean): sea-level 2002. Frontal accretion along the western Mediterranean Ridge: changes or subsidence? eEarth Discussions, 2, 115-132. the effect of Messinian evaporites on wedge mechanics and structural style. Mar. Geol., 186 (1), 59-82. ten Veen J.H., Woodside J.M., Zitter T.A.C., Dumont J.F., Mascle J. and A. Volkonskaia, 2004. Neotectonic evolution of the Anaxi- Ritt B., Desbruyeres D., Caprais J.C, Gauthier O., Ruffine L., Buscail mander Mountains at the junction of the Hellenic and Cyprus R., Olu-Le Roy K. and J. Sarrazin, 2012. Seep communities from arcs. Tectonophysics, 391, 35-65. two mud volcanoes in the deep eastern Mediterranean Sea: fau- nal composition, spatial patterns and environmental control. Mar. Tserpes G., Peristeraki P. and V.D. Valavanis, 2008. Distribution of Ecol. Prog. Ser., 466, 93-143. swordfish in the eastern Mediterranean, in relation to environmen- tal factors and the species biology. Hydrobiologia, 612, 241-250. Robertson A.H.F. and Shipboard Scientific Party, 1996. Mud volcan- ism on the Mediterranean Ridge: initial results of Ocean Drilling Topaloğlu B., Öztürk B., Topçu E.N. and O. Gönülal, 2010. A Pre- Program Leg 160. Geology, 24, 239-242. liminary Study on the Macrozoobenthic Invertebrate Fauna of two Banks in the North Aegean Sea. Rapp. Comm. int. Mer Médit., Robertson A.H.F., 1998a. Formation and destruction of the Eratos- 39, 682. thenes Seamount, Eastern Mediterranean Sea, and implications for collisional processes. Proceedings of the Ocean Drilling Pro- UNEP-MAP-RAC/SPA. 2010. Overview of scientific findings and gram, Scientific Results, 160, 681-699. criteria relevant to identifying SPAMIs in the Mediterranean open seas, including the deep sea. Notarbartolo di Sciara, G. and T. Robertson A.H.F., 1998b. Mesozoic-Tertiary tectonic evolution of the Agardy (ed.). RAC/SPA, Tunis: 71 pp. easternmost Mediterranean area: integration of marine and land evidence. Proceedings of the Ocean Drilling Program, Scientific Vassilopoulou V., Siapatis A., Papaconstantinou C. and E. Caragit- Results, 160, 723-782. sou, 2008. Annotated records of scombroid larvae distribution in northeastern Mediterranean waters. Med. Mar. Sci., 9 (1), 21-29. Römer M., Sahling H., Pape T., Bohrmann G. and V. Spieß, 2012. Quantification of gas bubble emissions from submarine hydrocar- Westbrook G.K. and T.J. Reston, 2002. The accretionary complex of bon seeps at the Makran continental margin (offshore Pakistan). the Mediterranean Ridge: tectonics, fluid flow and the formation J. Geophys. Res., 117, C10015. of brine lakes: an introduction to the special issue of Marine Geol- ogy. Mar. Geol., 186, 1-8. Sakellariou D., Sigurdsson H., Alexandri M., Carey S., Rousakis G., Nomikou P., Georgiou P. and D. Ballas, 2010. Active Tectonics Woodside J.M., Mascle J., Zitter T.A.C., Limonov A.F., Ergun M., in the Hellenic Volcanic Arc: The Kolumbo Submarine Volcanic Volkonskaia A. and Shipboard scientists of the PRISMED II expe- Zone. Bulletin of the Geological Society of Greece, Proceedings dition, 2002. The Florence Rise, the western bend of the Cyprus of the 12th International Congress, 43 (2), 1056-1063. Arc. Mar. Geol., 185, 177-194.

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263 ATLAS OF THE MEDITERRANEAN SEAMOUNTS AND SEAMOUNT–LIKE STRUCTURES

Würtz M., 2010. Mediterranean Pelagic Habitat: Oceanographic and Biological Processes, An Overview. Gland, Switzerland and Malaga, Spain: IUCN, 89 pp.

Zitter T.A.C., 2004. Mud volcanism and fluid emissions in Eastern Mediterranean neotectonic zones. (Doctoral dissertation, Vrije Universiteit), Amsterdam. 140 pp.

Zitter T.A.C., Huguen C. and J.M. Woodside, 2005. Geology of mud volcanoes in the eastern Mediterranean from combined sidescan sonar and submersible surveys. Deep Sea Res. Part I, 52 (3), 457-475.

Zitter T.A.C., Huguen C., ten Veen and J.M. Woodside, 2006. Tectonic control on mud volcanoes and fluid seeps in the Anaximander Mountains, eastern Mediterranean Sea. Geol. Soc. America Spec. Pub., 409, 615-631.

264 Plates

265 PLATES

A B

C D

E F

G H

Plate 1: (A-B, courtesy OCEANA; C, courtesy D. Palomino, J.T. Vasquez and DEEPER Team; D-H, courtesy OCEANA).

Avempace Seamount: Cabliers Bank: A) Palinurus mauritanicus; D) Anthomastus sp.; B) Zoanthid; E) Bathynectes maravigna; C) Leptometra celtica. F) Lophelia pertusa; G) Parantipathes larix; H) Sympagella sp.

266 PLATES

A B

C D

E F

G H

Plate 2: (A-H, courtesy OCEANA).

Chella Bank: A) Conger conger; E) Oxynotus centrina; B) Dendrophyllia ramea; F) Paramuricea clavata; C) glaberrima; G) Placogorgia coronata; D) Astropecten sp.; H) Scillarus arctus.

267 PLATES

A B

C D

E F

G H

Plate 3: (A-D, courtesy C. Lo Iacono; E, courtesy D. Palomino, J.T. Vasquez and MONTERA team; F-H, courtesy D. Palomino, J.T. Vasquez and DEEPER Team).

Chella Bank: F) Common , Delphinus delphis; A) Asconema setubalense; Djibouti Ville Bank: B) Callogorgia verticillata; G) Dendrophyllia ramea; C) Dendrophyllia cornigera; Djibouti Bank: D) Paramuricea sp., Helicolenus dactylopterus; H) Various crustacean species. Alboran Ridge: E) Long finned pilot whale, Globicephala melas;

268 PLATES

A B

C D

E F

G H

Plate 4: (A-H, courtesy OCEANA).

Ausiàs March Seamount: Emile Baudot Seamount: A) Raja clavata on Ampeliscidae garden; C) Histioteuthis reversa; B) Schilderia achatidea; D) Leiodermatium pffeiferae; E) Paromola cuvieri; F) Phakelia robusta; G) Tretodyction tubulosum on coral framework; Bell Seamount: H) sponsalis.

269 PLATES

A B

C D

E F

G H

Plate 5: (A-H, courtesy OCEANA).

Bell Guyot Seamount: Ses Olives Seamount: A) Bathypterois dubius; F) Acanthogorgia hirsuta and Cidaris cidaris on coral framework; B) Schedophilus medusophagus; G) Callogorgia verticillata and Acanthogorgia hirsuta; Seco de Palos Seamount: H) Leiopathes glaberrima and Acanthogorgia hirsuta. C) ; D) Alcyonacea; E) Paramuricea macrospina;

270 PLATES

A B

C D

E F

G H

Plate 6: (A-C, courtesy OCEANA; D-H, courtesy M. Bo).

Ses Olives Seamount: Santa Lucia Bank: A) Molva dypetrigia; D) Entangled Antipathes dichotoma; B) Plesionika narval; E) Antipathella subpinnata; C) Polyprion americanus; F) Leiopathes glaberrima; G) Damaged colony of L. glaberrima; H) Dendrophyllia cornigera tanatocoenosis.

271 PLATES

A B

C D

E F

G H

Plate 7: (A-H, courtesy M. Bo)

Santa Lucia Bank: A) Parantipathes larix; E) Mixed forest; B) Pachastrella monilifera; F) Conger conger; C) Acanthogorgia hirsuta; G) Leiopathes glaberrima forest; D) Conger conger; H) Viminella flagellum.

272 PLATES

A B

C D

E F

G H

Plate 8: (A-B, courtesy Artescienza s.a.s.; C, courtesy E. Lovece; D-H, courtesy M. Bo).

Nameless Seamount (Janua High): E) Denrophyllia cornigera, northern flank; A) Cuvier’s , Ziphius cavirostris, 8 August 2014; F) Sponge ground, western flank; Spinola Spur: G) Corallium rubrum, southern flank; B) , Balaenoptera physalus, 10 July 2013; H) Rocky hardground, pinnacle osting hosting Dendrophyllia cornigera. Ulisse Seamount: C) Deep sea long line catch (Pagellus bogaraveo), June 2009; Palinuro Seamount: D) Diazona violacea, top pinnacle;

273 PLATES

A B

C D

E F

G H

Plate 9: (A-H, courtesy M. Bo).

Palinuro Seamount: Vercelli Seamount: A) Denrophyllia cornigera and Bebryce mollis; C) Sperm whales, Physeter catodon, 20 August 2013; B) Leiopathes glaberrima: D) Merluccius merluccius, plateau; E) Callogorgia verticillata, peak; F) Laminaria rodriguezii, pinnacle; G) Leptometra phalangium bed, pinnacle; H) A. subpinnata, pinnacle.

274 PLATES

A B

C D

E F

G H

Plate 10: (A-G, courtesy Greenpeace/ISPRA; H, courtesy Artescienza s.a.s.)

Adventure Bank: Empedocle Seamount (Graham Bank): A) Alcyonacea and sponge community; E) Antipathella subpinnata; B) Anthias anthias; F) Andresia parthenopea; C) Cliona sp.; G) Viminella flagellum; D) Paramuricea clavata; H) Scorpaena scrofa, about 20 m depth, August 1977.

275 Printed in Spain by I.G. Solprint, S.L. P.I. La Vega. c/Archidona,56 29651 Mijas-Costa (Málaga)

http://www.solprint.com SARDINIA CHANNEL, OF SICILY, ,

Seamounts and Banks of the Sardinia Channel-Sicily Strait – Ionian Sea – Adriatic Sea: general map.

Dauno

Amendolara 40 Rossano Cariati

Resgui Sentinelle (Skerki) 38 Biddlecombe Silvia Keith Hecate Estafette Adventure Talbot Tetide Anfitrite Empedocle Pantelleria Galatea Anteo 2 Foerstner Cimotoe Pinne Anteo 3 Nameless Alfeo Pnt CB Pnt E Anteo 1 Pnt SW Angelina Madrepore Bannock bank Birsa Pnt SE Linosa III Linosa I Linosa II 36 Alfil V.Hensen Fonkal

Bouri smt V.Hensen 2

Medina Medina-Malte rdg

Melita Bannock smt Epicharmos Conrad 34

Battos Herodotus-Cyrene

Akhdar

32

10 12 14 16 18 20 22

180 km Disambiguation

In early studies, the Sardinia Channel, the sea region comprised between Sardinia and Sicily and bordered to the south by the northern Tunisian continental shelf, has been termed Sardinia Valley. The Tunisian Plateau was identified as a broad sector of the northern Tunisian INTERNATIONAL UNION upper slope/shelf around Bon (Gennesseaux and Stanley, 1983). FOR CONSERVATION OF In Budillon et al. (2009), the Plateau corresponds with a small sector of the northern Tunisian continental shelf, close to the Galite IUCN Centre for Mediterranean Cooperation Island. The term Tunisian Plateau actually corresponds to another marine region in Spalding et al. (2007), from which it has been adopted Parque Tecnológico de Andalucia in http://www.marineregions.org/gazetteer.php?p=details&id=21898, where it is identified with the (Sirte), between Tunisia and Marie Curie, 22 Lybia. 29590 - Campanillas (Malaga), Spain [email protected] Moreover at http://www.marineregions.org/gazetteer.php?p=details&id=4095, citing the IHO-IOC GEBCO Gazetteer of Undersea Feature Tel +34 95 202 84 30 Names (2002-10-01), the Tunisian Plateau is decribed as part of the . Fax +34 95 202 81 45 www.iucn.org/mediterranean Since the term Tunisia Plateau is also used for Tunisian terrestrial territories, we will stick to the term Sardinia Channel, considering this one the most reliable definition.

Notwithstanding, we will use the term Tunisian Plateau (sensu Gennesseaux and Stanley, 1983) for the Estafette, Resgui and Sentinelle Banks.

Core support to the IUCN Centre for 189189 Mediterranean Cooperation is provided by: