1. Introduction
Carbonate mounds are sedimentary seafloor elevations that have been detected worldwide, rise up to a few meters and up to 380 m [1] (above the surrounding seabed) and displaying different shapes (e.g., round, elongated), sizes (spanning from 10 s to 1000 s m in diameter) and sedimentary composition [2,3,4,5,6]. They often cluster as extended fields along continental shelves and slopes (from 100 to 1000 m water depth) comprising tens and even <1000 mounds [7,8]. Carbonate mounds are formed by framework-building calcareous organisms distributed according to various transport, depositional and erosive processes [2,4,5]. Hence, they are firstly dependent on the biological activity of their reef-forming organisms, which include colonial suspension feeding invertebrates, such as cnidarians (e.g., scleractinians, stony hydrozoans and octocorals) [9,10], sponges [11], serpulids [12] and bryozoans [13]. These framework-building organisms sometimes have branching forms, increasing the complexity and diversity of substrates, food sources and associated sessile and mobile organisms, including those with calcareous skeletons (e.g., encrusting coralline algae, mollusks, cirripeds, etc.) [14,15,16,17]). Indeed, these associated organisms with calcareous skeletons may also contribute to the accretion of the carbonate mound. Thus, the heterogeneous composition of carbonate mounds includes fragments of the habitat-forming species as well as other parautochthonous bioclasts, embedded in hemipelagic and contouritic sediments [15,16,17,18].
One of the most common and dominant faunal groups forming carbonate mounds are colonial cold-water corals (CWCs), which are dependent on different physicochemical parameters, such as temperature, salinity, dissolved oxygen concentrations, aragonite saturation and water mass density [10,19,20,21,22,23,24,25]. Nevertheless, CWC growth is also linked to the food availability (phytoplankton, zooplankton, particulate organic material), promoted by enhanced surface productivity and by the local hydrodynamic regime (including geostrophic currents, internal tides and waves, cascading and down-welling processes) supporting the lateral advection of food particles to the sessile CWC [26,27,28,29,30,31]). In general, CWCs develop reefs in areas with vigorous bottom currents (sometimes >50 cm s−1), preventing them from smothering by sediments [10,27,28,32,33]. The three-dimensional structure of CWCs can baffle suspended sediments entering their framework over time, and the continuous interplay between this sediment baffling and CWC growth leads to the formation of CWC mounds [18,20,33,34]. In general, CWC mounds maintain sustained development through time if there is equilibrium between sediment and food supply; often CWC mounds display an internal structure related to recurring periods of CWC colonization, decline and renewed colonization related to environmental changes induced by the Late Quaternary climatic cycles [18,35,36,37,38,39]. Periods of growth and/or decline of CWCs have been linked to changes in the physicochemical properties and productivity of the water masses [35,38,40,41,42,43,44,45,46]. Bottom currents can also create small erosional and depositional sedimentary structures and modulate the shape of the mound [47]), resulting in flattened top mounds (within the storm wave base), cone-shaped mounds (quiet and deeper waters) [4], elongated mound shapes (due to the preferred growth of the reef-forming organisms towards the main current) [48]), and mounds with current scours and moats around them (in strong bottom deep water along slope bottom currents) [35,41,49,50,51]. Active CWC mounds are covered by thriving CWC reefs and background sedimentation rate is generally lower than CWCs growth rate, however, contouritic and/or hemipelagic sediments have generally been found as major structural components contributing to the accretion of the CWC mounds (sometimes representing up to two-thirds of the mound deposits) [18,52,53]. Favorable environmental conditions for CWC growth or increases of background sedimentation in specific areas or time periods (e.g., sediment outputs from meltwater during deglaciation, changes in bottom current regimes, sediment extrusion in mud volcanoes, etc.) may promote the collapse and burial of the CWC reefs and their associated biota, resulting in the stagnation of the CWC mounds [7,38,43,54,55].
The analysis of high-resolution geomorphological and sedimentary data obtained by geophysical techniques since the 2000s has improved the knowledge about Quaternary sedimentation in the Alboran Sea. Some of these studies highlighted the role of contourite erosional and depositional processes in the formation of contourite terraces and drifts along the Spanish and Moroccan continental slopes [6,56]. These contouritic terraces that shape the continental slope are formed by turbulent processes (i.e., internal waves) occurring at the interfaces between the Atlantic and Mediterranean waters through the Quaternary glacio-eustatic sea-level changes [56,57]. In addition, other studies revealed a large scale distribution of clustered mounds with circular to elongated footprints along the Alboran Sea margins [43,55,58,59,60,61]. The clustering of mounds in extensive fields, especially along the upper and middle slopes, has been recently documented in the southern and central Alboran Sea, especially in the East [43,61] and West Melilla CWC mound provinces [46,55], as well as in the Cabliers bank [62,63] (Figure 1A). Furthermore, three mound fields have been located within the contouritic terraces of the northern Alboran Sea margin (south-eastern Spain), in front of Marbella (around the Torrenueva submarine canyon), in front of Málaga and southwest off Almería [6,58,59,64]. Sampling and direct observations of the southern Alboran Sea carbonate mounds (East and West Melilla CWC mound provinces) confirmed that CWCs were the main organism involved in their formation [15,43,46,55]. Nevertheless, some of those CWC mounds are nowadays partly or even completely buried by contouritic and hemipelagic sediments [55,56,65]. The distribution and burial state of the observed CWC mounds were explained by changes in water mass dynamics during the Late Quaternary climatic cycles [15,43,46].
The northern Alboran Sea mounds were initially identified on high-resolution bathymetric maps during the analysis of the main morphotectonic characteristics of this margin [58,59]. Subsequently, some of the mounds located in front of Málaga were investigated using a Remotely Operated Vehicle (ROV) during a German expedition with the R/V POSEIDON (POS385, led by MARUM) [60]. Later on, two multidisciplinary projects (MONCARAL and RIGEL) from the Instituto Español de Oceanografía (IEO) provided a new opportunity for exploring the different mounds of the northern Alboran Sea margin during two expeditions with the R/V ÁngelesAlvariño (MONCARAL 0516 and RIGEL 1116). Both geological and biological sampling was carried out, together with the acquisition of high-resolution acoustic datasets (bathymetry and parametric seismic profiles) and of underwater images using a ROV.
The main aim of the present study is to provide a detailed analysis of the morphosedimentary features, internal structure and contemporary and past benthic and subordinate organisms, including some habitat-forming species, of the three different mound fields located in the contouritic terrace, developed along the upper continental slope of the northern Alboran Sea [56,57,58]. The new datasets improve the knowledge of the morphology, distribution and the present-day and past evolution of these mounds in relation to some geological and oceanographic processes.
2. Regional Setting
The tectonic evolution of the Alboran Sea Basin (western Mediterranean Sea), linked to the Betics-Rif orogeny, has generated a basin characterized by narrow continental shelves and irregular, steep to gentle slopes, and a series of ridges and seamounts, of volcanic and/or tectonic origin, such as Xauen, Djibouti Ville and Avempace, which increase the seafloor complexity of the basin (Figure 1A) [6,66]. As mentioned previously, the upper continental slope is characterized by a contouritic terrace [56].
In the Alboran Sea, intermediate and deep Mediterranean waters migrate to the west through the Strait of Gibraltar, through which surficial Modified Atlantic Water (MAW) enters and flows to the east [67]. The MAW forms two anticyclonic gyres in the Alboran Sea (Western and Eastern Alboran Gyres) that extend to maximum depths of 150 to 200 m [68]. The Mediterranean water masses have been grouped by density [69] into two large groups [56]: (i) Light Mediterranean Water (LMW) comprising the less dense and salty intermediate waters that include the Western Intermediate Water (WIW), which flows at depths between 150 and 200 mbsl, the Levantine Intermediate Water (LIW), between 200 and 500 m water depth, and the lighter top of the Tyrrhenian Deep Water which flows below 500 m; and (ii) Dense Mediterranean Waters (DMW) including the lower part of the Tyrrhenian Deep Water and the Western Mediterranean Deep Water that flow below 600 m water depth. Both, the LMW and the DMW interact with the bottom of the basin: the LMW flows preferentially along the northern Alboran margin generating an erosive terrace at its interface with the MAW (around 150–300 m water depth) and a series of attached drifts along the slope or around the seamount-like banks and ridges; while the DMW circulates throughout the basin but ascends to shallower depths along the southern Alboran Sea margin, controlling the formation of the Ceuta Drift [56].
The Alboran Sea is one of the most productive areas within the generally oligotrophic Mediterranean Sea and its productivity is partially driven by local nutrient-rich upwellings that occur along the edge of the Western Alboran Gyre and at the eastern limb of the Eastern Alboran Gyre [68,70,71]. Some rivers discharge into the Alboran Sea, with the large Moulouya river at the Moroccan margin and the Guadiaro, Guadalhorce, Guadalfeo and Andarax rivers at the Spanish margin being the most important ones.
Due to the oceanographic and geological complexity of the Alboran Sea, a large variety of habitats and associated species from different biogeographical regions occur in the basin, representing a biodiversity hotspot for the European and northern African margins [72]. One of the most biodiverse habitats in bathyal depths of the basin is represented by reefs dominated by CWCs, which have been detected on various seafloor structures including seamounts (e.g., Seco de los Olivos (Chella Bank), East and West Cabliers, Djibouti Ville), mud volcanoes, submarine canyons and carbonate mounds [15,43,54,60,62,73,74]). Only rare occurrences of CWCs are reported for the Alboran Sea during the Last Glacial, but during the last deglaciation since the onset of the Bølling-Allerød warm interval, CWCs experienced a marked proliferation, which resulted in enhanced mound aggradation as indicated for several CWC mounds in the southern Alboran Sea [15,43,46]. The deglacial proliferation of CWCs coincided with enhanced surface ocean productivity and a peak in meltwater discharge originating from the northern Mediterranean borderlands, which caused a major re-organization of the Mediterranean thermohaline circulation [43,75]. Enhanced mound formation in the southern Alboran Sea lasted until the Early Holocene [15,43,46], which was likely controlled by strong hydrodynamic conditions caused by internal waves that developed along the density gradient between the Atlantic and Mediterranean waters [43,46]. Internal waves generally promote the resuspension and transport of recently deposited and/or fresh food particles at an increased velocity to the CWCs thriving on the mounds and, thus, enhance the chance of the CWC polyps to capture these particles [18,27]. Since the late Early to Mid-Holocene mound formation significantly slowed-down due to relatively weak hydrodynamics and oligotrophic conditions, and eventually stagnated until today with some of them becoming (partially to completely) buried by sediments [46].
3. Materials and Methods
In May 2009, during the expedition POS-385 on board the German R/V Poseidon [60]; two video transects (Dives 02 and 03 in Figure 1C) were performed crossing some of the mounds off Málaga with the MARUM ROV Cherokee. The ROV was equipped with four video cameras including a color video zoom camera and a digital still camera. The cameras were further equipped with three laser pointers for scaling adjusted to 19.5 cm in the horizontal direction and 12 cm in the vertical direction, and a hydraulically operated manipulator for collecting fauna and rock samples. A total of 3.5 h of video footage were recorded along more than 3000 m of seafloor tracks (Table 1). The ROV transects were carried out at low speed and close to the seafloor.
In May 2016, the expedition MONCARAL 0516 on board R/V Ángeles Alvariño (IEO, Spain) explored three mound fields of the northern continental slope of the Alboran Sea. These three fields have been named in the present study, from west to east, as Alcántara, Málaga and Aceitunas mound fields. Bathymetric data were obtained with a Kongsberg EM710 multibeam echosounder system, covering a total area of 102 km2 between 142 and 408 m water depth (Figure 1B–D). At the same time, high-resolution parametric profiles were acquired using a TOPAS PS018. Multibeam data were imported in a single project using CARIS HIPS and SIPS V. 11.1 software (© Teledyne) and were georeferenced to create a gridded base surface of 5 m cell size. After that, it was integrated into an ArcGIS v.10.8 (© ESRI) project where the geomorphological analyses were made. These geomorphological analyses include morphometric characterization after computing main size, slope and shape parameters, such as height, axis length and irregularity of the mounds (Iri), which represents the contour complexity of the polygon of each mound [76] (Table 2), as well as mound counting and Kernel density of the fields (mounds per km2). Parametric profiles were loaded in Kingdom IHS Markit software for the interpretation of seafloor and subseafloor structures.
Eight video transects (Dives 01 to 08) were recorded using the ROV Liropus 2000 at the three carbonate mound fields (Figure 1B–D) providing a total of 10 h of high-resolution underwater imagery along almost 12,000 m of seafloor tracks (Table 1). The ROV transects were carried out at low speed and close to the seafloor. This ROV was equipped with a full HD camera, two laser pointers for scaling (10 cm between them) and two hydraulic manipulators for collecting samples of rocks, sediment, fauna and remains of organisms. Samples collected during the ROV dives were used for identifying seafloor features and organisms observed in the underwater images. Qualitative analysis of video transects was carried out using VLC Media Player 3.0.16 for Windows software. The video fragments were viewed for identification of benthic and demersal species, substrate type categories (i.e., mud, sand, gravel, bioclasts and consolidated rocks) and sedimentary bedforms (i.e., moats). Furthermore, eleven surface sediment samples (VV01-VV11) were recovered from the three mound fields and adjacent bottoms between 173 and 317 m depth using a Van Veen grab sampler (Appendix A).
Finally, in November 2016, the expedition RIGEL 1116 on board R/V Ángeles Alvariño sampled the top and flanks of some of the mounds detected during the previous expeditions. Nine surface sediment samples (VV16-VV24) using a Van Veen grab sampler and nine sediment cores (TG16-TG24) using a gravity corer were obtained from the Málaga and Aceitunas mound fields between 188 and 255 m and 171 and 248 m depth. The maximum recovery of the gravity cores was 38 cm at the mounds and 260 cm at the adjacent seafloor. These samples were only used for in situ characterization of the top subseafloor sediments/structures (Appendix A).
4. Results
4.1. Alcántara Mound Field
The Alcántara mound field in the west is located at the western side of the Torrenueva canyon system, 11 km off the coast, between 239 to 297 m water depth (Figure 1B). It is the smallest mound field of the northern Alboran Sea and it is composed of 18 mainly elongated mounds stretching NW-SE, NE-SW and N-S with a mean Irregularity index (Iri) of 1.7. The mounds have heights of up to 14 m, with maximum slopes up to 18° and diameters between 131 to 966 m (Figure 2). This field contains the most elongated mounds of the northern Alboran Sea, and often these elongated mounds display higher reliefs (up to 14 m) than the circular ones that are generally lower and smoother (Table 2). In plain view, this field shows a random spatial distribution of individual mounds. In general, the mounds are highly separated with a low mound density (ca. 1 mound per km2) although the central sector of the field contains a cluster of mounds with a higher density (up to 8) (Figure 2D). Furthermore, the most elongated mounds seem to be composed of merged smaller mounds and occasionally, those elongated mounds are surrounded by moats down to 3 m in relation to the surrounding seabed (e.g., at the eastern sector of the Alcántara mound field) (Figure 2A and Figure 3).
The three surface sediment samples VV01-04 recovered with the Van Veen grab from some of the Alcántara mounds are overall characterized by mud and muddy sands with high bioclastic content corresponding to the shells of dominant mollusks of bathyal muddy bottoms, such as Nucula sulcata, Nassarius ovoideus, Abra spp., among others (Appendix A). The main bottom sediments and benthic communities detected in Alcántara mound field were bathyal muds and muddy sands with burrowing megafauna, mainly displaying a low-moderate number of burrows (1–5 burrows m−2) of large decapods, such as Munida spp. and the Norway lobster (Nephrops norvegicus) (Dive 1; Figure 4 and Figure 5). Small reducts of bathyal muds with seapens (mostly Veretillum cynomorium), cerianthiids (Cerianthus spp., Arachnanthus sp.) and sabellids (Sabella pavonina) have also been detected in specific areas of the mound field (Dive 3). Other benthic organisms detected at such sediment-covered bottoms were the hydrozoan Nemertesia ramosa, the sedentary polychate Spiochaetopterus sp., hermit crabs (Dardanus sp. and Pagurus sp.) and some pandalid shrimps (Plesionika spp.) as well as the gastropods Fusiturris similis and Aporrhais serresiana. Common fishes in this field are unidentified species of Myctophids, the horse mackerel Trachurus spp., the dogfish Scyliorhinus canicula, the Mediterranean silver scabbardfish Lepidopus caudatus and the boar fish Capros aper. Remains of solitary scleractinians (mainly Caryophyllia spp.) were also detected in the sediment. The main indicators of human anthropic activities were bottom-trawling marks on the seafloor of different sectors of the Alcántara mound field.
4.2. Malága Mound Field
The central Málaga mound field is located 35 km southeast off Málaga, between 220 and 273 m water depth (Figure 1C). This field consists of 64 mounds with mainly circular to elongated shapes, with the elongated mounds mainly displaying NW to SE extensions and a mean Iri of 2.1. The mounds have heights of 2 to 18 m, and diameters between 79 and 831 m with maximum slopes of 14°. The most elongated mounds generally display the largest heights (up to 18 m) as well as the steepest flanks and a mean Iri of 1.8 (Table 2). This field contains the largest number of mounds with the largest basal area (Table 2).
The spatial distribution of the mounds shows two different trends: mounds clustered in the western sector of the field with mound density values of 11 per km2, and scattered mounds with much lower mound densities (less than 2) in the eastern sector (Figure 2E). In addition, even further to the west, another cluster of mounds could be identified on the hillshade map (Figure 1C) but the scarce data resolution did not allow its detailed and comparative analysis.
The sediment surface samples VV05-08 and VV22-24 taken from the Málaga mound field consisted of mud and muddy sand with some bioclasts, mainly rhodoliths and fragmented bivalves and polychaete tubes, such as Aporrhais serresianus, Nassarius ovoideus, Neopycnodonte cochlear, among others, together with fossilized shells of Modiolus modiolus and debris of scleractinian corals (e.g., Caryophyllia) (Appendix A). Three cores were taken from this mound field with one core (TG22) collected from the top of a mound revealing a very low recovery of ~5–38 cm and only containing rhodoliths, while the two gravity cores (TG23-24) collected from the seabed adjacent to the Málaga mounds yielded core recoveries of more than 2 m only containing soft muddy sediments (Appendix A).
The bottom sediments and benthic and demersal communities of the Málaga mound field were similar to the ones detected in the Alcántara mound field, and included bathyal muds with burrowing megafauna (mainly Munida spp.), intermixed with seapens (mainly V. cynomorium and Virgularia mirabilis) and soft octocorals (Alcyonum palmatum), together with cerianthiids (Cerianthus spp.) and sabellid polychaetes (Sabella pavonina) (Dive 4; Dive 6) (Figure 4 and Figure 5). Other benthic organisms detected were the hydrozoan N. ramosa and the soft bottom gorgonian Spinimuricea sp., the polychate Spiochaetopterus sp., decapods (Dardanus arrosor, Monodaeus couchii, Macropodia sp. and Plesionika spp.) as well as the gastropod Xenophora crispa and cephalopods (Illexcoindetti). Common fishes in this field are also similar to the ones detected in the Alcántara mound field and included unidentified species of Myctophids, the horse mackerel Trachurus spp., the dogfish S. canicula, small gobiids (Lesueurigobius spp.) and the monk fish Lophius sp. The fossil record included remains of solitary (mainly Caryophyllia spp.) and colonial scleractinians (Dendrophyllia cornigera), abundant remains of fossilized rhodoliths and of some bivalves (mainly Glycymeris glycymeris and Modiolus modiolus) (Figure 4 and Figure 5). Bottom-trawling marks in this mound field represent human activities.
4.3. Aceitunas Mound Field
The Aceitunas mound field in the east has the largest extension and is located 10.5 km off Almería (north-westwards of Chella Bank), between 155 and 401 m water depth (Figure 1D and Figure 2C). It is the most heterogeneous field and is composed of 243 mounds (Table 2). Most mounds have circular to subcircular shapes, but few of them have also elongated shapes (Iri > 1.8) showing a NW-SE orientation (Table 2). The mounds have heights up to 15 m and diameters between 6 to 630 m (Table 2), with maximum slopes of 20°. The mounds with steep flanks are located at the base of Chella Bank, developed on the flank of the rim depression surrounding the seamount (Figure 2C). In general, the circular mounds of this field are smaller (mean diameters: 123 m) and are generally located deeper (224 to 366 m) compared to the elongated mounds (lengths: 280 to 630 m; water depth: below 210 m). In the Aceitunas mound field, the distribution of the individual mounds follows a scallop pattern, with the largest mounds located at the western sector of the field (with a mound density of 18 mounds per km2) and the smallest ones located in the easternmost sector (with mound densities between one and five mounds per km2).
The sediment surface samples VV09-21 were collected from different mounds in the Aceitunas mound field and consisted of fine muddy bioclastic sand with some pebbles, including some remains of bivalves and polychaetes. At the northernmost part of the Aceitunas mound field, the sediment contains more sand, showing diverse bioclastic fragments. Six gravity cores (TG16-21, with recoveries of 2 to 30 cm) retrieved from the top and flanks of the mounds of the Aceitunas field are characterized by bioclastic muddy sands, with some fragments of scleractinian corals (i.e., Caryophyllia spp.) (Appendix A).
In the Aceitunas mound field, the main bottom sediments were bathyal sandy muds and muddy sands and benthic and demersal communities were dominated by burrowing megafauna (mainly Munida spp.), intermixed with seapens (mainly V. cynomorium and Virgularia mirabilis) and octocorals (Alcyonumpalmatum), as well as with cerianthiids (Cerianthus sp.) (Dive 7). Other benthic organisms include unidentified hydrozoans, decapods (Dardanus sp. and Plesionika spp.) as well as the gastropod Xenophora crispa. Common fishes in this field are also similar to the ones detected in the Alcántara and Málaga mound fields and included unidentified species of flatfishes and gobiids, the dogfish S. canicula and the blackbelly rosefish Helicolenus dactylopterus. In some mounds, remains of rhodoliths and of the seagrass Posidonia oceanica were commonly observed on the underwater images and were also detected in the collected sediment samples. Anthropic activity indicators were represented by several bottom-trawling marks, some of them being very well defined, as well as by remains of plastics and fabrics.
4.4. Subseafloor Features and Seismic Facies of the Mound Fields
The high-resolution seismic profiles revealed that the mounds are embedded in the Quaternary contouritic terrace deposits of the northern Alboran Sea margin. These deposits are made up of the vertical stacking of seaward tilted subparallel stratified facies with reflections of variable acoustic amplitude. These deposits show seismic discontinuities of wide lateral continuity that represent irregular erosive surfaces outstanding by their high acoustic reflectivity (Figure 3). These unconformities are sharp surfaces and are locally covered by an extensive (<80 km long) but thin (few millisecond (ms) thick) layers of transparent and chaotic reflections, whose top forms a surface of high reflectivity with irregular morphology. Locally, terrace deposits are affected by some ancient faults (Late Pleistocene in age, [77] that in the Alcántara mound field are sealed by the most recent erosive surface (Figure 3A).
The seismic sections of the mounds protruding at the seafloor show conical shapes with two main types of morphologies: single mounds with gently inclined flanks and clusters of mounds of different heights. Their basal parts are >300 m to <2 km long, with total heights varying from >5 to about 30 ms. These mounds root on at least three different erosive surfaces (i.e., with different ages; named lower, middle and upper in Figure 3). The transparent and chaotic level overlying the lower erosive surface resembles levels of similar, but much smaller within the mounds (Figure 3B). Some mounds continued to form since their initiation at the lower erosive surface, while others disappeared and new ones formed at the middle and upper erosive surfaces. The hummocky level overlying the lower erosive surface resembles levels of similar, but much smaller mounds due to their facies and morphology (Figure 3B). This suggests that the larger mounds build up as isolated features rooted on the erosive surfaces and also grew on extensive patches with multiple smaller mounds where locally, prominent mounds stand out and eventually protrude at the seafloor. In both cases, below the prominent mounds, acoustic anomalies, such as velocity pull-up (Figure 3B) and column-shaped blanking that mask completely or partially the underlying deposits (Figure 3) are observed. The mounds rooted on the most ancient surface are commonly those with the highest dimensions.
In general, the irregular topography created by the mounds elevating from the seafloor is infilled by stratified deposits (Figure 3). Their reflections seem to continue along the sides of the mounds suggesting that most of them are at least covered by a variable thin (a few meters) layer of recent sediments. The mounds are internally defined by transparent facies. High reflectivity internal surfaces, vertically and laterally stacked are identified in some single cases. In the mound clusters, those surfaces are grouped with complex patterns (Figure 3B, C). Mounds with asymmetric cross sections are characterized by a relatively longer and steeper side with prolonged echoes, and a gentler flank showing wedges of stratified deposits at their foot (Figure 3A). Additionally, at the basal part of some Alcántara mounds, contourite moats (tens of meters wide, few ms in height) or moat-drift systems (few hundred meters in length) could be identified (Figure 3A).
Mounds are not exclusively found on the present seafloor. Seismic profiles from the Alcántara and Málaga mound fields show buried features similar in morphology and dimensions to the seafloor mounds (Figure 3B), pointing to additional, older mound formation periods. These older buried mounds and their surrounding contouritic sediments appear seismically very similar to the younger ones and, thus, indicate that mounds have been developed intermittently in the same areas during a long time period. The buried mounds also root on (at least up to 4) erosive surfaces (Figure 3B). The Alcántara and Aceitunas fields comprise 26 to 58 identified buried mounds, respectively, whilst in the Málaga field, more than 120 buried mounds are identified, which may represent the most ancient ones as some of them root on the deepest erosive surface (Figure 3).
5. Discussion
5.1. Potential Main Framework-Building Organisms of the Mounds
The present study could not confirm which framework-building organisms induced the formation and further development of the mounds of the northern Alboran Sea, but samples collected in the mound fields included remains of solitary and colonial scleractinians (e.g., Caryophyllia spp., Dendrophyllia cornigera), rhodoliths and large bivalves, with subordinate organisms. Organisms inducing mound formation generally include different groups with different biological traits, ranging from cyanobacteria and calcareous algae (mostly in mounds built in photic areas during ancient times) to heterozoans (mostly colonial scleractinians) without photoautotrophic symbionts (during past and modern times) but dependent on external food particles transported by bottom currents [2,4,5,26,30,33,78]. The morphologies and internal structures of the studied mounds in the northern Alboran Sea are similar to those reported for mounds detected in the southern Alboran Sea (East and West Melilla CWC mound Provinces) [43,46,55,61]. These southern Alboran Sea mounds are clear examples of carbonate mounds built by framework forming cold-water corals (CWCs) (mainly Madrepora oculata and Desmophyllum pertusum, the latter known as Lophelia pertusa until [79], so it is likely that CWCs could represent the dominating contributors for mound development in the northern Alboran Sea mounds. CWC mounds, either active (covered by thriving CWC reefs) or buried in soft sediments have been previously reported from many parts of the Mediterranean Sea (e.g., Apulian margin in the Ionian Sea -Santa Maria di Leuca CWC province, Corsica Channel-Tuscan Archipelago slope) [17,80,81,82,83,84,85] and the adjacent Gulf of Cádiz (e.g., [7,85,86,87,88,89]). Seismostratigraphic analysis and radiometric dating suggested that some of these mounds (e.g., EMP, WMP) experienced their most recent formation period during the last deglaciation until the Early Holocene most likely related to enhanced marine productivity [43] while older mound formation periods are placed (e.g., during the last interglacial [63]. The demise and subsequent burial of some Mediterranean CWC mounds since the Early to Mid-Holocene generally coincided with substantial changes in the environmental conditions driven by changes in climate water mass distribution [44,55,79,90], and water mass interfaces sculpting the regional contouritic erosive terraces [56]. These terraces have been created through time by turbulent oceanographic processes (e.g., internal waves) related to the water mass interfaces, and their vertical and lateral variations during the Late Quaternary sea-level variations [56,91].
In this sense, some southern Alboran Sea CWC mounds (e.g., WMP) significantly slowed down their aggradation during the Mid-Holocene due to relatively weak hydrodynamics and oligotrophic conditions and, finally, stagnated until today with some mounds becoming buried and/or partially buried by sediments [46]. This contrasts with the high proliferation and aggradation rates of the southern Alboran Sea CWC mounds during the Bølling–Allerød interval, possibly related to enhanced surface ocean productivity and a peak in meltwater discharge originating from the northern Mediterranean borderlands, which caused a major reorganization of the Mediterranean thermohaline circulation [43,75]. Indeed, significant environmental changes on the continental slope decrease onshore sediment inputs to the continental slope due to landward migration of the coastline [6,92,93]. Hence, the mounds could be controlled by changes in the sediment focusing, resulting in lateral sediment supply and changing deposition on the mounds, as supported in [53] and also changes in the current bottom-current regimes. Considering all these observations, it is possible that changes in the water mass circulation and water column structure, productivity, near-bottom currents and sediment supply may also have induced the demise of the studied northern Alboran Sea mounds as detected in the southern Alboran Sea CWC mounds.
The studied carbonate mounds from the northern Alboran Sea are mostly buried by mud and muddy sands, over a thick layer of calcareous algae (mainly rhodoliths), with subordinate remains of solitary and colonial scleractinian (e.g., Dendrophyllia cornigera) and bivalve shells, including the horse mussels (Modiolus modiolus). In fact, several gravity cores were recovered from the mounds but they could just retrieve a maximum length of 38 cm of sediment, with the lowest 5 cm section of the cores containing rhodoliths, while gravity cores collected from the adjacent seabed only recovered soft sediments. Rhodolith beds occur commonly in the photic and mesophotic zones, generally at less than ca. 40 m water depth in the NE Atlantic and above ca. 120 m in the Mediterranean Sea in different coastal and offshore environmental settings [16,94]. Rhodolith beds can display considerable variation in thickness, with thicker beds occurring in settings with strong hydrodynamics [14]. In these settings, rhodolith beds can even display wave ripples or mega ripples (e.g., in Galway Bay, Stravanan Bay) [95,96]. In low energy settings, rhodoliths can conform minireefs made of the fusion of rhodoliths with other sessile organisms (e.g., Fernando de Noronha Island, Rocas Atol, Vitoria Trindade Chain, Brazil) [97,98]. Furthermore, some mobile organisms (e.g., the tilefish Malacanthus plumieri) can create small mounds of rhodoliths [97,98]. Nevertheless, no records of large mounds built by rhodoliths have been found in the literature, thus, it is more plausible that the rhodoliths developed just on top of the already existing carbonate mounds and, therefore, contributed to a minor extent to their aggradation. Rhodolith beds occur nowadays in the Alboran Sea (20–120 m) on the summits of Chella Bank (75–120 m) and of the Alboran ridge (20–100 m) [99,100]. Considering that rhodoliths may have been formed on top of the carbonate mounds when sea level was minimal during the Last Glacial because some of the studied carbonate mounds were located at suitable depth for rhodolith growth (ca. 53–110 m) during that period (Appendix A).
Together with the rhodoliths, remains of horse mussels (M. modiolus) were collected in some surface samples and were also detected in some underwater ROV images from the Málaga mound field. Graveyards of this mytilid have been found in other parts of the Alboran Sea, mainly at Chella Bank [96] and at the Alboran ridge (between 100–120 m) [99]. Graveyards of other mytilids have been detected in upper Miocene out cropped carbonates in a NE–SW trending belt (42 km long and 1.5–8 km wide) along the so-called El Alcor topographic high (Guadalquivir Basin, S Spain) [101]. In the M. modiolus graveyards of the Alboran Sea, remains of other bivalve species were detected, including Panomya norvegica and large individuals of Mytilus edulis [99]. The former species, together with M. modiolus, represent examples of boreal guests that occurred in the Alboran Sea during the Last Glacial, while today the distribution of these species is restricted to latitudes north of the English Channel in the NE Atlantic. A study [102] indicated that M. modiolus occurred intermittently in the Western Mediterranean Sea and adjacent Gulf of Cádiz from the late Pleistocene until the substantial warming accompanying Termination l of the Last Glacial (ca. 13,000 years B.P.). Individuals of M. modiolus are best described as being adapted to live semi-infaunally with endobyssate attachment to the substrate, which ranges from soft or coarse sediments to rhodolith beds and hard substrata [103,104,105]. Generally, M. modiolus can be found on the lower shore in rock pools or in laminarian holdfasts but more common subtidally down to ca. 280 m depth [105]. This bivalve occurs singularly, in clumps, or in high-density and species-rich biogenic reefs in boreal and temperate regions around the world [106,107]. Some of the M. modiolus beds can extend ca. 349 ha (e.g., The North Lleyn reef, in the UK) and display undulating reliefs up to 1–2 m high, which are generally orientated perpendicular to the current [108]. Considering this, it is very unlikely that the carbonate mounds of the northern Alboran Sea, with heights of up to 18 m, would have been built up solely by the aggradation of M. modiolus beds, which generally are less than 2 m high, and no records of large mounds formed by this mytilid have been found in the literature. So, it is likely that these bivalves lived on top of some carbonate mounds together with the rhodoliths before they declined during Termination 1a of the Last Glacial, in accordance with [102].
5.2. Carbonate Mound Location and Environmental Setting
A large number of mound structures with acoustically transparent features presented in this study are interpreted as carbonate mounds, probably built by CWCs, considering the striking morphological and seismic similarities, such as their conical shape and the rooting on different seismic horizons, with other similar exposed and/or buried CWC mounds previously described in the Gulf of Cádiz [7,89], in the Porcupine Seabight [109,110] and in the southern Alboran Sea [55,61].
In general, larger and elongated mounds were detected in the shallowest areas whereas smaller mounds were detected in the deepest areas of the northern Alboran Sea mound fields. This is in accordance with the observations made by [55] for the WMP in the southern Alboran Sea, where smaller mounds were more frequent along the distal and deeper sectors of the mound field. The authors attributed this depth-related distribution pattern to a lower hydrodynamic energy setting and reduced food supply for CWCs in those deeper waters. Moreover, [46] detected stagnation of the southern Alboran Sea CWC mounds with the onset of the Mid Holocene, because they were located in an oligotrophic setting. This contrasts with the strong hydrodynamic setting promoted by internal waves developed along the water mass interface between the MAW and the LIW during the Bølling–Allerød (B/A) interstadial and the Early Holocene [46]. If water mass properties and internal waves (developed along the water mass interface) controlled the proliferation of CWCs and hence the development of CWC mounds, it is likely that the larger elongated mounds were more exposed to these internal waves with an efficient food delivery than the small mounds located deeper. Since for the northern and central Alboran Sea, the interval waves are currently reported from the interface between MAW and LIW at ~250 m water depth [111], the studied mounds, which occur in a relatively narrow depth range, should be influenced by internal waves in the same way. The elongated mounds located in the shallowest sectors of the studied fields could also have been benefitted more from food particles generated through the nutrient-rich coastal upwelling waters of the northern Alboran Sea [68]. Thus, the interaction between enhanced productivity and hydrodynamic energy settings in the shallowest areas probably has provided more suitable conditions for CWC growth and carbonate mound aggradation, allowing individual small mounds to merge to more complex structures conforming to larger, elongated CWC mounds as also found in other areas [112,113,114].
In the northern Alboran Sea, the carbonate mounds of the shallowest sectors are elongated with a predominant downslope extension of their length axis, mainly following NW-SE directions rather than parallel to the bathymetric contours of the continental slope. This probably might be related to the activity of internal waves developed along the water mass interface between the MAW and the LIW which could influence the shape and orientation of the mounds as assumed for carbonate mounds of the Gulf of Cádiz [7]. Furthermore, these internal waves and the generated strong hydrodynamic energy setting could also have played a big role in shaping the contourite terraces where the studied mound fields are located [56]. The sustained effect of a strong hydrodynamic energy setting, as observed by extended contourite deposition at several sites in the Alboran Sea [56,115], is clearly displayed in the present-day topography of the studied carbonate mound fields with many of the mounds being aligned by extensive moats, which are more pronounced around the Alcántara mounds, implying a more vigorous bottom current regime there (Figure 2A). This fact can be related to the constriction and acceleration of Mediterranean water masses near the Strait of Gibraltar [116].
The morphometric analysis of the studied carbonate mounds at the upper slope of the northern Alboran Sea revealed a total of 325 exposed carbonate mounds and 204 buried ones, extending over the three areas of almost 5.5 km2 and resulting in a mean mound density of 62 mounds per km2 for the northern Alboran Sea. In the Aceitunas mound field, the mean mound density reaches up to 78 mounds per km2, hence being much larger than in the Málaga and Alcántara mound fields (Figure 2D–F). Such mound densities are much higher than the ones detected for other CWC mound fields from the Mediterranean Sea, with 3–5 mounds per km2 were observed [55], and from the Moroccan margin, with 2–12 mounds per km2 [89,117]. The high number of carbonate mounds observed for various mound provinces in the Atlantic and Mediterranean [4,7,8,50,81,118], and now, in the Alboran Sea, point to their role as common seafloor morphological features usually occurring in intermediate water depths, which should be considered for future seafloor classification studies.
Furthermore, the high-resolution seismic investigations provide evidence that striking regional and high acoustic amplitude erosional surfaces represent the base of the mounds, as has been also observed in the Gulf of Cádiz [88]. Based on seismic stratigraphy works using high-resolution seismic profiles in the Alboran Sea, we can tentatively suggest that those surfaces formed from latest Pleistocene to Holocene [56,93,119]. Their formation would have formed during phases of erosion shaping the contouritic terrace and during periods of relatively higher energetic bottom currents, related with climatic variability [56]. Consequently, these erosional surfaces likely provided hard substrates (e.g., lag deposits) that could have allowed initial colonization by CWC and subsequent reef formation, favored by topography-enhanced bottom currents.
5.3. Current and Past Sedimentary Environment Affecting the Mound Fields
Nowadays, the studied carbonate mounds can be considered inactive mound fields with no living CWCs and with most of the mounds buried in soft sediments as detected in other carbonate mounds of the NE Atlantic and Mediterranean Sea [33,55,120]. The associated communities in all three fields are very similar regarding their megafauna, mainly due to the fact that there are no extreme changes in the sediment type and depth among them, which generally represent two of the most important factors inducing species replacements in megabenthic communities. The detected megabenthic communities are very widespread in the northern Alboran Sea and are often exposed to bottom trawling activities because they attract valuable commercial fisheries resources [72]. Indeed, several trawling marks were detected in the underwater images obtained from the studied carbonate mounds. The bottom sediments and associated benthic communities on the mounds are similar to those detected on the seafloor adjacent to the mounds, indicating a very low present-day benthic heterogeneity between the studied mounds and the surrounding seabed. Generally, mound formation requires mound growth to be faster than background sedimentation, and baffling of hemipelagic sediment is a major component contributing to mound growth (especially in branching mound-forming organisms; [5,18,20,33,34,53]. Thus, the burial of carbonate mounds appears to be a consequence of the cessation of active reefs and, thus, mound growth induced by the deterioration of living conditions for the respective mound-forming organisms [5]. In the southern Alboran Sea, stagnation in mound formation occurred since the Mid-Holocene and some of these mounds became buried by sediments. In the present study, it is not possible to place the development of the northern Alboran Sea mounds into any temporal framework or know precisely when the burial of the mounds took place. The burial induced extreme changes in the seabed and associated communities, from complex and highly diverse CWC and rhodolith bed communities, which probably formed since/during the Last Glacial Maximum, to current soft sediments with burrowing organisms and the specialized soft-bottom suspension feeders of the typical bathyal communities of the northern Alboran Sea [17].
The arrangements of the three erosive surfaces observed in the sub-bottom profiles (Figure 3), as well as on the stratigraphic relationships between the buried mounds and the stratification of the sedimentary deposits allow us to conclude that active sedimentation generated stratified deposits overlying the carbonate mounds. Laterally, the continuity of the deposits seems to be interrupted by the mounds themselves, once they are inactive. This suggests that the mounds were formed shortly after the major erosional event that created the hardground mound base common for the three fields and developed quickly, likely promoted by favorable oceanographic and climatic conditions, before strong drift sedimentation started [109]. Such mound-controlled processes have already been suggested for other CWC mound provinces off Ireland [113,120]. The inferred age of the lower rooted surface at the base of the mounds is late Pliocene to early Quaternary, so the stage of formation of the mounds would date from the early Quaternary.
6. Conclusions
Based on these observations, we consider that the occurrence pattern of the northern Alboran Sea mounds could be related to favorable climatic conditions for CWC mound formation, possibly during the Quaternary and before Termination 1a of the Last Glacial due to the occurrence of boreal guest fauna on top of the mounds. This contrasts with the findings of [15,43,46] who detected that the most recent mound formation period started during the last deglaciation in some southern Alboran Sea mounds (e.g., WMP). Although direct observation of the typical CWCs involved in mound formation (e.g., Madrepora oculata, Desmophyllum pertusum) could not be carried out in the present study, it is very plausible that CWCs represented the main mound-building organisms due to the morphological similarities and internal structure of the studied mounds. Further studies may focus on obtaining long cores using extracting methods (e.g., drilling) that are more efficient than gravity coring in order to improve the knowledge on the internal composition of the mounds as well as in performing seismostratigraphic analyses and radiocarbon dating of the rhodolith outer surface. In addition, bathymetry and high-resolution seismic profiles could be obtained with equipment operating closer to the seafloor, such as autonomous underwater vehicles (AUVs). This would allow us to obtain detailed bathymetry, backscatter and seismic profiles to study the internal structure of the mounds and to correlate their morphostructure with long sediment corers in order to advance the knowledge of the formation and evolution of the northern Alboran Sea mounds.
Conceptualization, O.S.-G., M.G.-B. and J.L.R.; Funding acquisition, M.G.-B., G.E., C.W. and D.H.; Methodology, O.S.-G., M.G.-B., J.L.R., J.U. and J.T.V.; Species identification, J.L.R., J.U., E.M.-U., C.W. and D.H.; Formal analysis, O.S.-G., J.L.R., C.W., D.H., M.G.-B., J.T.V., F.E. and G.E.; Data curation, All authors; Writing—original draft, review & editing, All authors; Supervision, O.S.-G., J.L.R., C.W. and D.H. All authors have read and agreed to the published version of the manuscript.
This research was performed in the scope of MONCARAL and RIGEL projects, funded by the Instituto Español de Oceanografía (IEO), and the AGORA project (P18-RT-3275) (funded by Junta de Andalucía).
Not applicable.
Not applicable.
Datasets are stored in the database of the Instituto Español de Oceanografía (IEO) for the MONCARAL and RIGEL projects, some of which is available at the IEO marine geospatial information viewers and services:
This work is a contribution from “Contraste de la actividad geológica entre el sector este y oeste del mar de Alborán y cordilleras adyacentes”: AGORA (P18-RT-3275 (Junta de Andalucía), “Estudio y caracterización de montículos carbonatados en el Mar de Alborán”: MONCARAL (IEO) funded projects as well to a contribution of the ESMARES 2 (MITERD and Instituto Español de Oceanografía) project for improving the knowledge on the circalitoral and bathyal habitats of the northern Alboran Sea (Demarcación Estrecho-Alboran) (18ESMARES2-CIRCA). We appreciate all the valuable help made by the captains, crews and scientific teams during the POS-385, MONCARAL 0516 and RIGEL 1116 expeditions on board R/V Poseidon and R/V Ángeles Alvariño. This work acknowledges to the `Severo Ochoa of Excellence’accreditation (CEX2019-000928-S).
The authors declare any conflict of interest.
Publisher’s Note: MDPI stays neutral with regard to jurisdictional claims in published maps and institutional affiliations.
![View Image - Figure 1. (A) Overview map showing the three carbonate mound fields (B–D) on the northern margin of the Alboran Sea described in this study and the location of cold-water corals (CWC) mound provinces detected in the southern Alboran Sea (Cabliers, West Melilla (WMP) and East Melilla (EMP) mound provinces [55,61,62,63]. The water mass circulation scheme is adapted from [56] based on Legend: MAW, Atlantic Water; WIW, Western Intermediate Water; LIW, Levantine Intermediate Water; WMDW, Western Mediterranean Deep Water; ShW, Shelf Water. Bathymetric map of (B) Alcántara carbonate mound field; (C) Málaga carbonate mound field and (D) Aceitunas carbonate mound field showing the location of dive tracks and sub-bottom parametric profiles (lines). Extension of the mound fields are marked by white dotted contours. The black scales represent 2.5 km. Bathymetric contours with 25 m spacing are shown as white lines.](https://media.proquest.com/media/hms/THUM/2/dCFNM?_a=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%2BgIBWYIDA1dlYooDHENJRDoyMDI1MDcyNjIyMjEzMTA3OTo0NzUzMzE%3D&_s=9W0IvCVe6Xy1FvaOmtQobiuKrII%3D "View Image - Figure 1. (A) Overview map showing the three carbonate mound fields (B–D) on the northern margin of the Alboran Sea described in this study and the location of cold-water corals (CWC) mound provinces detected in the southern Alboran Sea (Cabliers, West Melilla (WMP) and East Melilla (EMP) mound provinces [55,61,62,63]. The water mass circulation scheme is adapted from [56] based on Legend: MAW, Atlantic Water; WIW, Western Intermediate Water; LIW, Levantine Intermediate Water; WMDW, Western Mediterranean Deep Water; ShW, Shelf Water. Bathymetric map of (B) Alcántara carbonate mound field; (C) Málaga carbonate mound field and (D) Aceitunas carbonate mound field showing the location of dive tracks and sub-bottom parametric profiles (lines). Extension of the mound fields are marked by white dotted contours. The black scales represent 2.5 km. Bathymetric contours with 25 m spacing are shown as white lines.")
Enlarge this image.Figure 1. (A) Overview map showing the three carbonate mound fields (B–D) on the northern margin of the Alboran Sea described in this study and the location of cold-water corals (CWC) mound provinces detected in the southern Alboran Sea (Cabliers, West Melilla (WMP) and East Melilla (EMP) mound provinces [55,61,62,63]. The water mass circulation scheme is adapted from [56] based on Legend: MAW, Atlantic Water; WIW, Western Intermediate Water; LIW, Levantine Intermediate Water; WMDW, Western Mediterranean Deep Water; ShW, Shelf Water. Bathymetric map of (B) Alcántara carbonate mound field; (C) Málaga carbonate mound field and (D) Aceitunas carbonate mound field showing the location of dive tracks and sub-bottom parametric profiles (lines). Extension of the mound fields are marked by white dotted contours. The black scales represent 2.5 km. Bathymetric contours with 25 m spacing are shown as white lines.
Enlarge this image.Figure 2. Spatial distribution and main morphological variables of the 325 carbonate mounds detected in the three mound fields of the northern Alboran Sea. (A–C) 3D bathymetric images of the carbonate mound fields with a vertical exaggeration of 6. (A) Alcántara mound field; (B) Málaga mound field and (C) Aceitunas mound field. (D–F) Kernel density maps (mound per km2) of the mound fields based on mound contours. The black scales represent 2.5 km. (G–J) Morphometric data of the analyzed geomorphological features: (G) Bathymetric distribution of carbonate mounds in terms of the number of mounds; (H) Main trends of length axes orientation of the carbonate mounds. Histograms show (I) the length and (J) the basal area covered by the mounds.
Enlarge this image.Figure 3. High-resolution sub-bottom parametric profiles showing some carbonate mounds and contourite drift sequences of the (A) Alcántara mound field; (B) Málaga mound field and (C) Aceitunas mound field in the northern Alboran Sea. Location of the profiles is shown in Figure 1B–D.
Enlarge this image.Figure 4. Some examples of present-day bottom sediments and benthic and demersal fauna detected at the Alcántara (M), Málaga (A–E,L,N) and Aceitunas (F–K) carbonate mound fields of the northern Alboran Sea. (A) the burrowing decapod Munida sp.; (B) the pandalid shrimp Plesionika heterocarpus; (C) Hermit crabs using Xenophora crispa shells; (D,E) Cerianthus sp. (Ce) individuals, with one of them located close to two sabellidpolychaete tubes (Sa) and the decapods Munida sp. (Mu) and Macropodia sp. (Ma); (F,G) the seapen Virgularia mirabilis; (H) the soft bottom octocoral Alcyonum palmatum; (I,J) an aggregation of an unidentified solitary anthozoan, including a close-up of one individual; (K,M) tubes of the polychaete Spiochaetopterus sp. colonized by small hydrozoans; (L) the sabellid polychaete Sabella pavonina; (N) the squid Illex coindetii. All underwater images obtained with ROV LIROPUS 2000, Instituto Español de Oceanografía (Spain).
Enlarge this image.Figure 5. Some examples of present-day bottom sediments, fossil remains and anthropic activity indicators detected for the Alcántara (A,B), Málaga (C–H) and Aceitunas (I,J) carbonate mound fields of the northern Alboran Sea. (A,B) Muddy bottoms with some typical bathyal species, such as the gastropod Aporrhais serresiana (Ap) and the polychaete Lanice conchilega (La); (C) Bathyal muddy bottoms with burrowing megafauna (mainly Munida spp. and Nephrops norvegicus); (D–H) rhodoliths and bivalve remains detected in several mounds; (I) a cloth sack over Spiochaetopterus sp. tubes and (J) a bottom-trawling mark. All underwater images obtained with ROV LIROPUS 2000, Instituto Español de Oceanografía (Spain), except figure E obtained with ROV CHEROKEE, Marum, Bremen (Germany).
Metadata of the ROV video transects recorded during POS-385 (ROV Cherokke) and MONCARAL 0516 (ROV Liropus 2000) expeditions in the northern Alboran Sea.
| Expedition | Mound Field | Dive | Track Length (m) | Water Depth (m) | Start |
End |
|---|---|---|---|---|---|---|
| POS-385 | Málaga | 02 | 1128 | 243–233 | 36°37.35′ N |
36°37.72′ N |
| POS-385 | Málaga | 03 | 1931 | 236–218 | 36°37.48′ N |
36°37.78′ N |
| MONCARAL | Alcántara | 01 | 2512 | 309–317 | 36°19.83′ N |
36°20.17′ N |
| MONCARAL | Alcántara | 02 | 353 | 291–297 | 36°20.40′ N |
36°20.46′ N |
| MONCARAL | Alcántara | 03 | 1452 | 243–253 | 36°21.35′ N |
36°21.56′ N |
| MONCARAL | Málaga | 04 | 1307 | 238–261 | 36°37.20′ N |
36°37.34′ N |
| MONCARAL | Málaga | 05 | 1895 | 271–276 | 36°36.90′ N |
36°37.06′ N |
| MONCARAL | Málaga | 06 | 1586 | 225–230 | 36°37.61′ N |
36°37.83′ N |
| MONCARAL | Aceitunas | 07 | 1348 | 180 | 36°36.94′ N |
36°37.06′ N |
| MONCARAL | Aceitunas | 08 | 1192 | 194–200 | 36°36.18′ N |
36°36.37′ N |
Location, number (N°) and morphological features of the mounds and mound fields detected in the northern Alboran Sea (Iri: Irregularity index, BA: Basal Area, H: Height).
| Mound Field | Location | Depth Range (m) | N° of Exposed Mounds | N° of Buried Mounds | Length Range (m) | Width Range (m) | Iri Range | BA (km2) | H Range (m) | Mean Slope (°) |
|---|---|---|---|---|---|---|---|---|---|---|
| Alcántara | North-western Alboran Sea | 239–297 | 18 | 26 | 131–966 | 84–361 | 1.3–3.1 | 0.82 | 3–14 | 2.5–6 |
| Málaga | North-central Alboran Sea | 220–273 | 64 | 58 | 79–831 | 57–313 | 1.03–4.7 | 1.33 | 2–18 | 2.5–16 |
| Aceitunas | North-eastern Alboran Sea | 155–401 | 243 | 120 | 6–630 | 5–295 | 1.03–3.5 | 3.08 | 1–15 | 2–20 |
| All mound fields | 155–401 | 325 | 204 | 6–966 | 5–361 | 1.03–4.7 | 5.23 | 1–18 | 2–20 |
Appendix A
Metadata of the surface sediment Van veen grab samples (VV) and gravity cores (TG) recovered during MONCARAL_0516 and RIGEL_1116 expeditions in the northern Alboran Sea.
| Expedition | Mound Field | Sample Code | Core Length (cm) | Water Depth (m) | Latitude N (°) | Longitude W (°) | Description |
|---|---|---|---|---|---|---|---|
| MONCARAL | Alcántara | VV01 | 241 | 36°21.52′ | 05°01.40′ | Muddy sand with Nucula sulcata and Nassarius ovoideus shells | |
| MONCARAL | Alcántara | VV02 | 251 | 36°21.36′ | 05°01.45′ | Muddy sand with Nucula sulcata and Euspira fusca shells | |
| MONCARAL | Alcántara | VV03 | 317 | 36°19.83′ | 04°59.86′ | Sandy mud with Abra spp. and Nassarius ovoideus | |
| MONCARAL | Alcántara | VV04 | 313 | 36°19.85′ | 04°59.80′ | Muddy sand | |
| MONCARAL | Málaga | VV05 | 231 | 36°37.70′ | 04°12.90′ | Bioclastic sandy mud with rhodoliths and Modiolus modiolus shells fragments | |
| MONCARAL | Málaga | VV06 | 260 | 36°37.20′ | 04°12.10′ | Bioclastic sandy mud with Neopycnodonte cochlear shells and Caryophyllia spp. fragments | |
| MONCARAL | Málaga | VV07/08 | 271 | 36°37.01′ | 04°11.60′ | Sandy mud with Nassarius ovoideus and Aporrhais serresiana shells | |
| MONCARAL | Aceitunas | VV09 | 192 | 36°36.50′ | 02°54.50′ | Muddy fine sand with Posidonia oceanica remains | |
| MONCARAL | Aceitunas | VV10 | 201 | 36°36.20′ | 02°54.30′ | Bioclastic sand with rhodoliths fragments | |
| MONCARAL | Aceitunas | VV11 | 173 | 36°37.00′ | 02°56.20′ | Bioclastic sand with rhodoliths fragments | |
| RIGEL | Aceitunas | VV16 | 223 | 36°36.37′ | 2°56.61′ | Bioclastic muddy sand | |
| RIGEL | Aceitunas | VV17 | 233 | 36°35.36′ | 2°53.61′ | Bioclastic muddy sand with Caryophyllia spp. fragments | |
| RIGEL | Aceitunas | VV18 | 244 | 36°35.14′ | 2°52.79′ | Sandy mud | |
| RIGEL | Aceitunas | VV19 | 188 | 36°36.20′ | 2°53.48′ | Sandy mud | |
| RIGEL | Aceitunas | VV20 | 196 | 36°36.31′ | 2°54.88′ | Sandy mud | |
| RIGEL | Aceitunas | VV21 | 231 | 36°38.52′ | 4°10.16′ | Sandy mud | |
| RIGEL | Málaga | VV22 | 238 | 36°37.66′ | 4°11.94′ | Bioclastic sandy mud | |
| RIGEL | Málaga | VV23 | 255 | 36°37.59′ | 4°11.17′ | Sandy mud with polychaetes | |
| RIGEL | Málaga | VV24 | 232 | 36°37.82′ | 4°12.85′ | Sandy mud | |
| RIGEL | Aceitunas | TG16 | 7 | 171 | 36°37.04′ | 2°56.18′ | Bioclastic muddy sand |
| RIGEL | Aceitunas | TG17 | 5 | 172 | 36°37.05′ | 2°56.19′ | Bioclastic muddy sand |
| RIGEL | Aceitunas | TG18 | 30 | 191 | 36°36.25′ | 2°54.46′ | Bioclastic muddy sand |
| RIGEL | Aceitunas | TG19 | 5 | 194 | 36°36.19′ | 2°54.38′ | Bioclastic muddy sand with Caryophyllia spp. fragments |
| RIGEL | Aceitunas | TG20 | 26 | 193 | 36°36.38′ | 2°54.78′ | Bioclastic muddy sand with Caryophyllia spp. fragments |
| RIGEL | Aceitunas | TG21 | 2 | 233 | 36°35.36′ | 2°53.61′ | Bioclastic sandy mud |
| RIGEL | Málaga | TG22 | 38 | 231 | 36°38.52′ | 4°10.16′ | Sandy mud with N. cochlear shells fragments and rhodoliths |
| RIGEL | Málaga | TG23 | 260 | 248 | 36°37.34′ | 4°12.12′ | Bioclastic sandy mud |
| RIGEL | Málaga | TG24 | 105 | 231 | 36°37.82′ | 4°12.85′ | Bioclastic sandy mud |
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; Rueda, Jose L 1
; Wienberg, Claudia 2
; Ercilla, Gemma 3 ; Juan Tomás Vázquez 1
; Gómez-Ballesteros, Maria 4 ; Urra, Javier 1 ; Moya-Urbano, Elena 5 ; Estrada, Ferran 3
; Hebbeln, Dierk 2 1 Centro Oceanográfico de Málaga, Instituto Español de Oceanografía (IEO-CSIC), 29640 Fuengirola, Spain;
2 MARUM—Center for Marine Environmental Sciences, University of Bremen, LeobenerStraße 8, 28359 Bremen, Germany;
3 Continental Margins Group, Institut de Ciencies del Mar-CSIC, Passeig Marítim de la Barceloneta 37-49, 08003 Barcelona, Spain;
4 Servicios Centrales de Madrid, Instituto Español de Oceanografía (IEO-CSIC), 28002 Madrid, Spain;
5 Departamento de Biología Animal, Universidad de Málaga, 29071 Málaga, Spain;