The Interactive Role of Hydrocarbon Seeps, Hydrothermal Vents and Intermediate Antarctic/Mediterranean Water Masses on the Distribution of Some Vulnerable Deep-Sea Habitats in Mid Latitude NE Atlantic Ocean

In this work, we integrate five case studies harboring vulnerable deep-sea benthic habitats in different geological settings from mid latitude NE Atlantic Ocean (24–42° N). Data and images of specific deep-sea habitats were acquired with Remoted Operated Vehicle (ROV) sensors (temperature, salinity, potential density, O2, CO2, and CH4). Besides documenting some key vulnerable deep-sea habitats, this study shows that the distribution of some deep-sea coral aggregations (including scleractinians, gorgonians, and antipatharians), deep-sea sponge aggregations and other deep-sea habitats are influenced by water masses’ properties. Our data support that the distribution of scleractinian reefs and aggregations of other deep-sea corals, from subtropical to north Atlantic could be dependent of the latitudinal extents of the Antarctic Intermediate Waters (AAIW) and the Mediterranean Outflow Waters (MOW). Otherwise, the distribution of some vulnerable deep-sea habitats is influenced, at the local scale, by active hydrocarbon seeps (Gulf of Cádiz) and hydrothermal vents (El Hierro, Canary Island). The co-occurrence of deep-sea corals and chemosynthesis-based communities has been identified in methane seeps of the Gulf of Cádiz. Extensive beds of living deep-sea mussels (Bathymodiolus mauritanicus) and other chemosymbiotic bivalves occur closely to deep-sea coral aggregations (e.g., gorgonians, black corals) that colonize methane-derived authigenic carbonates.


Introduction
Maintaining the sustainable functioning of the global biosphere requires protection of deep-sea ecosystems, particularly because they face major changes related to human and climate-induced impacts [1]. For an effective protection, an improvement in knowledge  [8][9][10][11][12] are labelled as: North Atlantic Curren (NAC), Azores Current (AC). Regional bathymetric map extracted from the EMODnet Project (http://www.emodnet.eu/bathymetry, accessed on 1 December 2020).

Gulf of Cádiz and Moroccan Atlantic Margin
The second case study refers to chemosynthesis-based habitats and other vulnerable deep-sea habitats (aggregations of sponges, gorgonians, antipatharians, among others) in mud volcanoes (MVs) located in the Moroccan Atlantic margin of the Gulf of Cádiz (GoC) between 34 • and 35 • N (Figures 1 and 2B). In the GoC, extensive geophysical research and seabed sampling have resulted in the discovery of 84 MVs and MVs-mud diapir complexes since 2000 [13][14][15][16][17][18][19][20][21]. Mud volcanism in the GoC is primarily associated with high concentrations of thermogenically-derived methane [22]. Different sources have been invoked for mud volcanism in the GoC: Pliocene and Late Miocene shales, the so-called Allochthonous Unit of the GoC and even deeper sources of Mesozoic age [23,24]. Carbonates and ferromanganese rocks such as methane-derived authigenic carbonates (MDACs) [25,26] formed by microbial-mediated anaerobic oxidation of methane (AOM) [27] and Fe-rich nodules formed by later exhumation, oxidation and diagenesis of buried AOM products [28]. Three types of intermediate water masses are currently considered in the case study of the GoC (Figure 1): the Eastern North Atlantic Central Water current (ENACW), the Mediterranean Outflow Water (MOW), the North Atlantic Deep Water current (NADW), and the Subarctic Intermediate Water current (SAIW).

The Passage of Lanzarote-Canary Islands-NW African Margin
The third case study focuses on the Passage of Lanzarote (PoL), between the Canary Islands (Fuerteventura-Lanzarote Islands) and the West African Continental Margin (Figure 1). The bathymetric profile transverse to the PoL is asymmetrical with the passage narrowing

The Passage of Lanzarote-Canary Islands-NW African Margin
The third case study focuses on the Passage of Lanzarote (PoL), between the Canary Islands (Fuerteventura-Lanzarote Islands) and the West African Continental Margin (Figure 1). The bathymetric profile transverse to the PoL is asymmetrical with the passage narrowing towards the south, showing a steeper western flank ( Figure 2C). The PoL has maximum water depths at its center, ranging between 1240 and 1460 mbsl (Figures 1 and 2C). Two groups of seafloor morphologies stand out in the submarine relief of this passage [30,31]: (a) seamounts and hills related to volcanic ridges and salt domes and (b) bottom current-related features. Three main types of water masses have been identified circulating through the PoL (Figure 1) [10,32,33]: The upper thermocline North Atlantic Central Water current (NACW), which spans from the surface to the neutral density (Υn) value of 27.3 kg/m 3 (approximately 600 mbsl); and the Antarctic Intermediate Water current (AAIW) reflected by a clear S minimum and found below the NACW (roughly 700-1600 mbsl).The AAIW is well identified along the African continental margin with a predominantly northward flow which often exceed 0.02 m s −1 , appearing particularly intense (up to 0.06 m s −1 near the bottom) during the summer seasons [33]; the third, the Mediterranean Modified Water current (MW), a modified branch of the MOW identified in individual profiles by high-salinity peaks flowing southwards between 900 mbsl to the bottom with a mean southward flow of −0.05 Sv [33]. In winter and spring, the formation of active meddies (Mediterranean Outflow Water eddies) have been reported at the north of the PoL between 12 • W and 15 • W [33]. The occurrence of submarine mounds along this deep-water passage promotes the intensification of the turbulence at the interface between the AAIW and MW bottom currents [31,32].

El Hierro Island, Canary Islands
The fourth case study highlights the natural successional changes in newly formed volcanic substrates and habitats related to recent submarine eruptions that occurred in 2011-2012, south of El Hierro Island, Canary Islands (Figures 1 and 2D). Dead fish and patches of pale colored water at the sea surface indicated the onset of a submarine eruption on 10 October 2011 at 5 km distance from the town of La Restinga. The El Hierro eruption continued during late February, when seismicity decreased drastically until 6 March 2012. As a result of this shallow submarine eruption, a new submarine volcano grew from 375 to 89 mbsl [34]. Since 2016, the new volcano appears on the official hydrographic charts as "Tagoro" (meaning "stone circle for meeting place" in the aboriginal language of Canary Islands). The eruption consisted of two main phases of edifice construction intercalated with collapse events. After the cessation of the volcanic eruption, emissions of large quantities of iron and carbon dioxide from submarine hydrothermal vents were reported [35,36]. Several oceanographic expeditions were carried out during and after the eruption of the Tagoro volcano (Supplementary Table S1). These expeditions have allowed the identification of the development of new habitats after the eruption, associated with the emission of large quantities of iron and carbon dioxide from hydrothermal submarine vents.

The Canary Island Seamounts
The fifth case study comprises the southern seamounts of the Canary Island Seamount Province (CISP), located southwest of the Canary Islands and 100 km west off the African coast (Figures 1 and 2E). The CISP is composed of more than 100 seamounts and submarine hills rising from~5000 to 200 mbsl [37]. The CISP extends from the Lars-Essauira seamount, approximately 400 km from the north of Lanzarote (32.7 • N, 13.2 • W) to the Tropic seamount, 500 km at the southwest of the archipelago (23.8 • N, 20.7 • W). This case study focuses on the southern CISP area which is characterized by the presence of several large seamounts, including The Paps, Echo, Drago and Tropic, rising from~5000 m to 200 mbsl (Figures 1 and 2E). These are the oldest seamounts of the CISP, dated between 91 and 119 Ma [38]. The seabed of these seamounts is mainly composed of ferromanganese crusts and nodules growing on basalt-sedimentary rock substrates containing high average amounts of Fe (23.5 wt%), Mn (16.1 wt%), and trace elements like Co (4700 µg/g), Ni (2800 µg/g), V (2400 µg/g), and Pb (1600 µg/g) [39][40][41]. The oldest age of initiation of the ferromanganese crusts growth was estimated at 90 Ma [40]. The CISP seamounts are located beneath the northern end of the Oxygen Minimum Zone (OMZ), which extends from 100 to 700 mbsl, from near the equator to 25 • N [42]. The core of the OMZ is located at 400-500 mbsl, reaching very low oxygen values (<50 µmol/kg). The dissolved oxygen is also depleted by the high biological productivity in proximity to the Canary Islands due to upwelling and nutrient-rich currents [42]. At intermediate depths, the low oxygen waters are ventilated by the ENACW and by the South Atlantic Central Water current (SACW) above~700 mbsl and by the AAIW at~1000 mbsl. The North Atlantic Deep-Water current (NADW) flows at depths below 1500 mbsl and the Antarctic Bottom Water current (AABW) flows below~4000 mbsl [33] (Figure 1). These deep bottom currents accelerate around the seamounts, increasing the supply of nutrients related to high inputs of Fe and P sourced from the Sahara dust [39].

Materials and Methods
Mapping the seafloor and its specific habitats (and Vulnerable Marine Ecosystems, VMEs) at regional scale requires interdisciplinary research teams using a wide suite of surveying techniques. Data of this work were collected mainly during the SUBVENT-2 cruise aboard RV Sarmiento de Gamboa [43]. Other data included in this work were collected during a set of extensive scientific expeditions listed in the Supplementary Table S1. A summary of the cruise details for each of the five case studies including data sets collected, MBES systems and ground truthing data sets are listed in Supplementary Table S1.
The multibeam bathymetry echosounder (MBES) Atlas DS 1 × 1 on board the RV Sarmiento de Gamboa has been used for seabed mapping of the distinct habitats and to plan ROV tracks (see Supplementary Table S1 for further details on MBES systems). MBES data were processed using CARIS HIPS&SIPS™ version 9 software (Teledyne CARIS, Frederiction, NB, Canada). The MBES data were used to generate Digital Terrain Models (DTM) at spatial resolutions of 30-50 m (depending on water depth). The multi-resolution DTM was used to produce regional sun-shaded image renders, perspective views and to extract margin-wide bathymetric profiles using Fledermaus™ version 7 software (QPS, Porstmouth, NH, USA) to interpret the submarine landscapes. It was also used to generate derivative products such as slope angle maps by means of ArcGIS™ desktop v. 12.4.
The ATLAS P-35 used aboard the RV Sarmiento de Gamboa is a parasound echosounder with two frequencies: a Primary High Frequency (PHF) at 20 kHz and a Secondary Low Frequency (SLF) at 4.5 kHz. PHF was used to record anomalies within the water column, whereas SLF was used as a sub-bottom profiler to record sediment/rock features (Supplementary Table S1).
Submersible observations and sampling of the seafloor were carried out with the ROV Luso (from Estructura de Missão para a Extensão da Plataforma Continental, Portugal), equipped with a high definition video camera Argus HD-SDI Camera (ARGUS Remote Systems AS, Laksevag, Norway), two robotic manipulators to recover biological and geological samples, a CTD (conductivity, temperature, and depth measurements) with fluorescence, turbidity and CO 2 -, CH 4 -and O 2 -sensors, and four Niskin bottles for water sampling (Supplementary Table S1). Water samples (two replicates of 20 mL) were taken for methane determination using a gas chromatograph in cold seep areas. Rock-mineralization samples and associated biota were taken by means of conventional rectangular benthic dredges (0.8 m in width by 0.6 m in height) towed on the seafloor during 10 to 20 min at 1 knot speed. ROV tracks were planned after analysis and interpretation of previous MBES mapping (DTM of the bathymetry) and backscatter models. Gravity cores with a maximum length of 300 cm were taken on the summits and/or slopes of the mud volcanoes. The cores were photographed and a visual lithostratigraphic description was made in each case.

Description of Vulnerable Deep-Sea Habitats of Each Case Study
In this section, the morphology and the type of habitats and communities in the five case studies from the north Atlantic (42 • N) to subtropical Atlantic (23 • N) have been described. Full details of substrate types, water depth ranges, geomorphology, habitat types, and the associated biota for each specific site are listed in the Supplementary A large number of live scleractinian colonies of Desmophyllum pertusum (previously named as Lophelia pertusa) and Madrepora oculata have been identified conforming reefs on the summit and flanks of the Galicia Bank at water depths between 620 and 1175 mbsl ( Figure 3). The distribution of these scleractinian reefs has been mapped by means of MBES backscatter mosaic images, ultra-high resolution and high-resolution multichannel seismic reflection data and seabed sampling ( Figure 3). A complete sequence of stepped elongated reefs (M1 to M5 in Figure 3), known as Breogham mounds and characterized by high backscatter strengths with a seabed expression, were identified on multibeam bathymetry along the western flank of the Galicia Bank ( Figure 3A Figure 3C). We interpret their low acoustic response (~1520 ms −1 ) close to values for the water column, as due to the high contents of seawater within their skeletons, as well as the open space created by the skeletal growth patterns. Samples of these still thriving scleractinian reefs yielded living D. pertusum and M. oculata ( Figure 3D,E). In contrast, older and semi-buried scleractinian reefs were partially cemented forming elongated mounds along the flanks of the bank, being characterized by higher backscatter responses [46]. In some cases, scleractinians, mollusc monoplacophora (Laevipilina rolani), and bryozoans [47] occurred on encrusted phosphorites and ferromanganese nodules substrates at 750-1400 mbsl in the southeast Galicia Bank. Six MVs located between 350 and 3000 mbsl (Mercator, Algacel, Yuma, Madrid, Las Negras, and Bonjardim), were explored with the ROV "Luso" during the oceanographic expedition SUBVENT-2 [43] (Location shown in Figure 4A). Chemosynthesis-based communities and high methane concentrations were detected in these explored MVs. Reduced grey mud breccias were recovered by gravity cores in all cases, when testing the nature of extrusion of these cones. Ridges and mounds with abundant scleractinian skeletons (mainly D. pertusum and M. oculata), but with scarce living D. pertusum colonies and stony octocoral colonies (e.g., C. tricolor) were detected westwards of the Algacel MV in the Pompeia Coral Mound Province ( Figure 4). Patches of chemosymbiotic bivalve shells (mainly L. asapheus with some Thyasiravulcolutre), and scattered bacterial mats (Beggiatoa-like sulfur oxidizers) were also detected ( Figure 6E,H). Ultra-high-resolution profiles below the scleractinian skeletons show that they represent the top of giant buried mounds that reach up to 42 m in height (equivalent to 50 ms two-way travel time, TWT, assuming an average sonic velocity of 1750 m s −1 for recent sediments) ( Figure 4E). The potential causes of the regression of these giant coral mounds in the GoC will be considered in the Section 5. Methane concentrations on the seafloor of the ridge at the Pompeia Coral Mound Province range from 41.93 to The type of habitats identified in these MVs can be resumed into seven types (See details in Supplementary Table S2): (1) Active methane seeps with chemosynthesis-based communities.
(2) Non-active pockmarks colonized by Cerianthids (3) Aggregations of sponges, gorgonians, black corals, soft corals and bamboo corals colonizing methane-derived authigenic carbonates (MDACs) (4) Hexactinellid sponge aggregations on muddy sediments and coral graveyards.  Chemosynthesis-based communities were mainly detected on the summits and sometimes on the flanks (e.g., Algacel MV), of the surveyed MVs ( Figure 5) and contained different types of taxa and rates of methane flux. Regarding this, in MVs with high methane fluxes such as Algacel MV (methane concentrations up to 97.60 nM) ( Figure 5A-C), harbored living deep-sea mussel Bathymodiolus mauritanicus beds, containing both small-and large-size specimens were found. These beds formed large linear and circular mussel clumps (up to 10 m in diameter) surrounding emissions of intermittent gas bubbling with methane concentrations of 97.60 nM ( Figure 6A-E).
2, FOR PEER REVIEW 11 43.24 nM, indicating the occurrence of moderate seepage. The E-W orientation of these ridges at the westward side of the Algacel MV ( Figure 5A) points to the influence of strong bottom currents causing strong turbulences on their lee face.     Sulfur-oxidizing bacterial (SOB) mats forming macroscopically visible cohesive white patches of 10-30 cm in diameter were also detected ( Figure 6A).
In MVs with low methane fluxes such as the Bonjardim MV (20.18-28.12 nM), the past occurrence of chemosynthesis-based communities is revealed by abundant shells of the chemosymbiotic bivalve I. megadesmus ( Figure 6B).
Ridges and mounds with abundant scleractinian skeletons (mainly D. pertusum and M. oculata), but with scarce living D. pertusum colonies and stony octocoral colonies (e.g., C. tricolor) were detected westwards of the Algacel MV in the Pompeia Coral Mound Province ( Figure 4). Patches of chemosymbiotic bivalve shells (mainly L. asapheus with some Thyasiravulcolutre), and scattered bacterial mats (Beggiatoa-like sulfur oxidizers) were also detected ( Figure 6E,H). Ultra-high-resolution profiles below the scleractinian skeletons show that they represent the top of giant buried mounds that reach up to 42 m in height (equivalent to 50 ms two-way travel time, TWT, assuming an average sonic velocity of 1750 m s −1 for recent sediments) ( Figure 4E). The potential causes of the regression of these giant coral mounds in the GoC will be considered in the Section 5. Methane concentrations on the seafloor of the ridge at the Pompeia Coral Mound Province range from 41.93 to 43.24 nM, indicating the occurrence of moderate seepage. The E-W orientation of these ridges at the westward side of the Algacel MV ( Figure 5A) points to the influence of strong bottom currents causing strong turbulences on their lee face. spectively in Figure 7). Otherwise, the basin morphology of the PoL is dominated by channels and moats related to the interaction of the strong bottom currents with the seabed (Figure7). Therefore, a NE-SW central channel 100 km in length and 1-5 km in width is located at 1290 mbsl in the central sector and deepens toward the NE (1460 mbsl) and towards the SW (1320 mbsl). Rimmed depressions around the mounds classified as moats are 0.5-2 km widths incising to 180 m depth. Moats are better developed along the east and south sides of the mounds reaching up to 1270-1530 mbsl at their bases. (1) Deep-Sea hexactinellid sponge aggregations intermixed with Actiniarian communities covering the soft, muddy sea floor of the summit of some mounds (e.g., M1 mound) at 830-850 mbsl. (2) Sea-pens communities and aggregations of bamboo corals covering soft muddy bottoms with some coral rubble along the flanks of some mounds (e.g., M1 mound) at 1020-1100 mbsl. Mounds are cylindrical or sub-rounded highs, 2-10 km in diameter with flat summits (e.g., M1 in Figure 7). The base of the mounds along the PoL ranges between 1225 and 1530 mbsl and their summits between 828 and 1336 mbsl. The volcanic ridges are 6 km long, 150 m high, E-W trending linear ridges detached from the mounds (e.g., the Volcanic Ridge in Figure 7). Volcanic cones are single structures 15-70 m height and 350-700 m in diameter crossing the flat summits of the mounds (e.g., the Volcancito in Figure 7). Six circular or slightly elliptical depressions have also been identified in the continental slope of the West African continental margin at the PoL [48]. They are located between 750 and 1415 mbsl, and their reliefs vary between 40 and 240 m. The length and width of their axes range from 2 and 4.5 km to 2 and 3.3 km, respectively. The surveyed deep depressions have named as the Twin Pools [48] (Western and Eastern Twin Pool, WTP and ETP respectively in Figure 7). Otherwise, the basin morphology of the PoL is dominated by channels and moats related to the interaction of the strong bottom currents with the seabed (Figure 7). Therefore, a NE-SW central channel 100 km in length and 1-5 km in width is located at 1290 mbsl in the central sector and deepens toward the NE (1460 mbsl) and towards the SW (1320 mbsl). Rimmed depressions around the mounds classified as moats are 0.5-2 km widths incising to 180 m depth. Moats are better developed along the east and south sides of the mounds reaching up to 1270-1530 mbsl at their bases.
The volcanic ridges and volcanic cones are colonized by a wide variety of suspensionfeeding species, such as stony octocorals (mainly C. tricolor and C. niobe), black corals (Leiopathes glaberrima), bamboo corals (A. arbuscula), and small and large gorgonians (Swiftia, Plexaurid gorgonians), together with crinoids and hexactinellid and lithistid sponges, among a wide variety of benthic species. Some areas covered by abundant coral rubble were colonized by isolated bamboo corals (A. arbuscula). The occurrence of strong bottom currents supports the fact that tree-like branches of some octocorals are oriented along an E-W direction ( Figure 8E) Giant circular depressions, such as WTP and ETP (Figure 7), contain a mixed seabed with soft and carbonated flagstones. The sandy and muddy substrates are colonized by typical sedimentary bathyal species such as sponges (Thenea), cerianthids, sea-pens (Pennatula), echinoderms (Ceramaster, Mesothuria, Araeosoma), decapods (A. foliacea, P. edwardsianus, Plesionika spp.) and large scalpellid barnacles. The rocky substrates are covered by a layer of sediment that is poorly colonized by fauna, including some massive demosponges (Pachastrellid-like sponges), small encrusting sponges, scattered hydroids and solitary scleractinians (Caryophyllia). ROV observations in 2014 showed that the base of the Tagoro volcano is dominated by an area with extensive accumulations of scoriaceous bombs at 280 to 380 mbsl formed from basanitic lava emissions ( Figure 9C,E,F). When observed closely, these bombs appeared to be either whole intact lava balloons or broken fragments of larger balloons. These bombs correspond to lava balloons floating on the sea surface during the eruption ( Figure 9E). Echosounder images of the water column taken during the eruption overlie on the 3D multibeam bathymetry model showed high-reflective bright spots interpreted as these floating bombs sank along the flanks of the volcano ( Figure 9A).
Two main habitats were recognized after two years of the cessation of the eruption (see details in Supplementary Table S2): (1) Chemosynthesis-based habitats composed by a great proliferation of orange-brown Fe-oxidising bacteria draped the whole seafloor of the summit. (2) Volcanic caves communities along the flanks of the volcano composed by small oysters and serpulids, shrimps and eels.
ROV images of the summit of the volcano show 5 m-high chimneys or hornitos with numerous degassing conduits punctuating their walls and marked by yellow mats, linked to sulfur-related bacteria ( Figure 9D). Temperatures measured during the 2014 survey (Supplementary Table S1) showed abrupt increases in temperature up to~2.69 • C, related to active hydrothermal chimneys or hornitos located at the volcano summit [50]. Peaks of CO 2 emissions were detected with the ROV sensors around these hornitos [50]. On the contrary, the flanks of the volcano showed recolonization of fauna such as small oysters (Neopycnodonte cochlear) and serpulids, shrimps (mainly Plesionika), and eels (Conger conger, Gymnothorax) living on caves and crevices generated by the cooling of the plastic bulbous lavas flowing downslope at 250-300 mbsl.  In this fifth case study, we present the data from four ferromanganese crust-bearing seamounts (Echo, The Paps, Drago, and Tropic) located in the west-southwest region of the CISP at water depths ranging from 300 to 4300 ( Figure 10). The Echo Seamount is a sub-circular seamount of 10 km in diameter with the flat shallow summit located at only 300 mbsl and the base at −3700 mbsl ( Figure 10A). The Paps seamount has the shape of a NW-SE ridge, 40 km length in the SE direction with the summit at 1600 mbsl and the base at 4300 mbsl ( Figure 10B). The Tropic seamount is a star-shaped guyot, with its base located at 4200 mbsl and its summit at about 1000 mbsl ( Figure 10C). The Drago Seamount is elliptical in shape with major axis NW-SE oriented. The summit is situated at 2200, whereas the base at 3000 mbsl ( Figure 10D).

Potential Drivers of Deep-Sea Habitat Distribution from Subtropical North Atlantic
This section discusses the potential drivers affecting the distribution and biodiversity of vulnerable deep-sea habitats, including both chemosynthesis and non-chemosynthesisbased habitats. Some of these drivers are: (a) the seafloor water mass properties as temperature, salinity, dissolved oxygen and potential density [12]; and (b) the active geological processes affecting the seafloor such as (i) methane seeps [51][52][53][54][55] and (ii) submarine volcanic eruptions followed by low-T hydrothermal degasification [50]. Furthermore, an overview of the effects of methane seeps and low-T hydrothermal vents following recent submarine eruptions on the distribution of deep-sea habitats at regional scale along the northeast Atlantic Ocean from 24 • N to 42 • N is provided.

Influence of Water Mass Properties on Vulnerable Deep-Sea Habitats
The relationships between water depths and water mass properties (temperature, salinity, dissolved oxygen, and potential density) for specific vulnerable deep-sea habitats highlight important considerations on suitable environmental conditions for them. The distribution of undercurrents along the NE Atlantic from the NW African Margin and Canary Islands to the north Iberian Margin is mainly driven by the outflow of the MOW at the Gibraltar Strait and by the intrusions of the Antarctic-derived AAIW currents at intermediate waters ( Figure 12). The ROV-mounted CTDs data are in-situ measurements of the benthic layer, where the deep-sea habitats allow us to compare the regional distribution of water masses ( Figure 12) with the local variables affecting the specific habitats (Figures 13-15). A full list of oceanographic measures in-situ for each site surveyed with the ROV-mounted CTD is shown in Supplementary Table S3. Oceans 2021, 2, FOR PEER REVIEW 20

Potential Drivers of Deep-Sea Habitat Distribution from Subtropical North Atlantic
This section discusses the potential drivers affecting the distribution and biodiversity of vulnerable deep-sea habitats, including both chemosynthesis and non-chemosynthesisbased habitats. Some of these drivers are: (a) the seafloor water mass properties as temperature, salinity, dissolved oxygen and potential density [12]; and (b) the active geological processes affecting the seafloor such as (i) methane seeps [51][52][53][54][55] and (ii) submarine volcanic eruptions followed by low-T hydrothermal degasification [50]. Furthermore, an overview of the effects of methane seeps and low-T hydrothermal vents following recent submarine eruptions on the distribution of deep-sea habitats at regional scale along the northeast Atlantic Ocean from 24° N to 42° N is provided.

Influence of Water Mass Properties on Vulnerable Deep-Sea Habitats
The relationships between water depths and water mass properties (temperature, salinity, dissolved oxygen, and potential density) for specific vulnerable deep-sea habitats highlight important considerations on suitable environmental conditions for them. The distribution of undercurrents along the NE Atlantic from the NW African Margin and Canary Islands to the north Iberian Margin is mainly driven by the outflow of the MOW at the Gibraltar Strait and by the intrusions of the Antarctic-derived AAIW currents at intermediate waters ( Figure 12). The ROV-mounted CTDs data are in-situ measurements of the benthic layer, where the deep-sea habitats allow us to compare the regional distribution of water masses ( Figure 12) with the local variables affecting the specific habitats (Figures 13-15). A full list of oceanographic measures in-situ for each site surveyed with the ROV-mounted CTD is shown in Supplementary Table S3.     [33]: NACW, AAIW, MOW and NADW defined by [33]. Legend: FAO Taxa Classification and Codes for Vulnerable Marine Ecosystems (VMEs) (http://www.fao.org/in-action/vulnerable-marineecosystems/vme-database, accessed 1 December 2020). Figure 13 shows the T-S diagram for the in-situ water mass conditions measured for each type of habitat (data can be found in Supplementary Table S3 Supplementary Table S3. Further explanation in the text. Figure 13 shows the T-S diagram for the in-situ water mass conditions measured for each type of habitat (data can be found in Supplementary Table S3   Chemosynthesis-based habitats of the GoC are also located under the influence of the MOW, except for the deepest mud volcano (e.g., Bomjardim MV), which is located under the influence of the NADW. The values for low-T hydrothermal habitats of the summit of the Tagoro volcano with high S and T are disturbed by the influence of hydrothermal fluids not reflecting its location at the thermocline. In contrast, benthic habitats of volcanic caves at the flanks of Tagoro are bathed by the NACW reflecting the major influence of water masses (Figure 13).

Water Mass Temperatures
Water temperature has been traditionally considered as one of the most important factors influencing the distribution of deep-sea organisms due to their different physiological tolerances [12,56]. Thermal thresholds for deep-sea coral habitats (including those conformed by scleractinians, stony octocorals, gorgonians, and black corals) are well constrained to temperature ranges of 7.3 and 11.5 • C within the depth range of 800-1400 m ( Figure 13A). Within this threshold, all these deep-sea corals appear distributed into three levels of seafloor temperatures: (i) scleractinians conforming reefs (Desmophyllum pertusum, and Madrepora oculata) located at the maximum temperature tolerance of 11-11.5 • C; (ii) Gorgonians, scleractinian and antipatharians conforming aggregations at intermediate temperatures of 8.8-10 • C; and finally iii) Stony octocoral aggregations at the lowest temperatures of 7.3-7.7 • C ( Figure 14A).
The temperature range of the distribution of the reef-forming scleractinians D. pertusum and M. oculata (4-12 • C) across the five case studies matches the temperature range of cold North Atlantic Intermediate waters and the temperature range where those reefforming species have been detected in the past [56,57].
On the other hand, some aggregations of fragile octocorals (Acanella, Radicipes) appear at the lowest temperatures of 7.3-7.7 • C ( Figure 14A) in the case studies but at a higher temperature range (1.5-6.1 • C) than that detected previously for the North Atlantic, so the present study provides new data for case studies located southwards of those considered [58]. Moreover, the low temperature values could point out that stony octocoral gardens living along the PoL are somehow influenced by the cold Antarctic Intermediate Waters (AAIW) that flows between the easternmost Canary Islands and the African margin (Figures 12 and 13), which was totally unexpected previously in this study.
Otherwise, desmosponges aggregations dominated by Geodia sp. and Phakellia sp., occurring within the crater of Mercator MV ( Figure 5D) at shallow depths of 350-370 mbsl, tolerate high sea-floor temperatures up to 12.5 • C ( Figure 14A) as also detected in the northern sector of the GoC, where the MOW influence is higher [54]. On the contrary, hexactinellid sponge aggregations with Pheronema and Hyalonema detected along the flanks of the Algacel MV at 820-840 mbsl ( Figure 5E) live within the thresholds of the aggregations of gorgonians, scleractinians, and antipatharians, colonizing MDACs around methane seeps ( Figure 14A). Indeed, these sponges were found at similar depths and environmental conditions in the northern part of the GoC [59,60]. On the other hand, deep-sea chemosynthesis-based habitats do not show seafloor temperature constraints, varying from 3.2 to 12.5 • C, as function of the seeps location. In the case of the large mussels Bathymodiolus mauritanicus, the seafloor temperature of 10.1 • C may fluctuate as function of intensification of the hydrocarbon seeps. No information on the effect of temperature on the distribution of methane seeps fauna has been found, but the fact that the same chemosymbiotic-species may occur in cold seeps with different oceanographic conditions in methane seeps of the northern and southern GoC may indicate a lower dependence on water mass properties for these chemosymbiotic organisms than for the above mentioned cnidarians and sponges [60,61]. In the case of the hydrothermal-related habitats (V1 = hornitos-like hydrothermal chimneys and V2 = lava cavities in Figure 14A), temperatures reflect thermal anomalies associated with venting hydrothermal fluids. Therefore, maximum measured temperature of expelled fluids in Tagoro volcano was 39 • C, while the ambient seawater range between 15 and 19 • C with local temperature anomalies of +2.7 • C associated with CO 2 emissions [50].

Salinity and Potential Density
Although salinity variations are very low in the deep sea, the distribution of deep-sea scleractinians and octocorals in some areas of the NE Atlantic has been related to potential density, which represents a parameter defined by salinity and temperature [62]. Indeed, reef-forming scleractinians of the selected sites are controlled by a narrow salinity range of 35.35-36.1 psu ( Figure 14B). As seafloor temperatures, habitats conformed by deep-sea corals appear also distributed into three levels of salinity: (i) Scleractinian reefs (D. pertusum and M. oculata) occurred at salinity ranges between 35.8 and 36.1 psu; (ii) Gorgonian aggregations at salinity ranges between 35.6 and 36.1 psu; and (iii) Stony octocoral aggregations at the lowest salinity values between 35 and 35.2 psu. These data point out that there is an influence of the MOW waters bathing the scleractinian reefs, and of the mixing between the saltier MOW waters and the lower salinity AAIW waters for some gorgonian and stony octocoral aggregations ( Figure 13). Indeed, the MOW flow seems to play an important role in the distribution and connectivity of deep-sea corals across the NE Atlantic, with a high diversity of deep-sea corals along the MOW pathway [63].
Deep-sea desmosponges aggregations at 1400 mbsl appear associated with salty water masses of 36 psu ( Figure 13B) related to the export of bathyal benthos to the Atlantic through the MOW outflow as detected in other areas of the GoC [60]. On the contrary, shallow water desmosponges grounds associated with methane seeps of the Mercator MV ( Figure 5C), located at 350 mbsl above the MOW influence, show the lowest levels of salinity of 35.75 psu ( Figure 14B). As occurred for temperature values, large hexactinellid sponge aggregations occurred within the same salinity range as for deep-sea corals ( Figure 14B). The role of the MOW exporting deep-sea sponge larvae from the Mediterranean to the Atlantic Ocean and some NE locations close to the GoC has been demonstrated recently, and this may partly explain the occurrence of some sponges in salty water masses related to the MOW [64].
The occurrence of scleractinian reefs along the NE Atlantic margins has been related to values of potential density, a parameter defined by salinity and temperature. Thus, D. pertusum and M. oculata reefs, were firstly constrained to a narrow potential density range (potential density; δ θ = 27.35-27.65 kg m −3 ) [62] which further, in other North Atlantic regions, proved to be larger than initially suggested as ranging δ θ = 27.10-27.84 kg m −3 [63]. This range is similar for the D. pertusum and M. oculata reefs identified in the Galicia Bank, which falls within this suggested range with values of δ θ = 27.353-27.431 kg m −3 ( Figure 14C). In the case of the Galicia Bank, these conditions seem to be caused by the turbulent mixing between the MOW and the ENACW water masses promoted by the MOW current impinging the topography of the Galicia Bank [46]. The formation of turbulent eddies of MOW flow facilitates the downward transport of nutrients, influencing the present distribution of the scleractinian reefs and mounds mapped along its flanks and on the summit ( Figure 3B).
On the contrary, the gorgonian and stony octocorals aggregations do not fit with this potential density threshold ( Figure 14C). Thus, stony octocoral aggregations in the subtropical latitudes occur at potential density values δ θ = 32.725 kg m −3 , whereas gorgoniandominated aggregations occur at values of δ θ = 32.050-34.900 kg m −3 , much higher than those for scleractinian reefs. Thus, according our data, the potential density range proposed for scleractinian reefs [62,63,65] would be only valid for the northernmost NE Atlantic margins, and more data on the presence of these species southwards is then needed for estimating the appropriate density range. One explanation is the potential influence of intrusion of AAIW flow along the NW Africa margin towards the GoC (Figure 12).
Desmosponges and hexactillenid aggregations also show different potential densities. Therefore, desmosponge aggregations show higher potential density ranges (δ θ = 32.050-34.900 kg m −3 ) than the studied hexactillenid sponge aggregations (δ θ = 31.058 kg m −3 ) ( Figure 14C) Hydrography plays an important role in shaping the distribution of sponge aggregations in the Atlantic, and several authors have noted the association of sponges with particular water masses due to their temperature and salinity characteristics or hydrodynamic conditions, such as tides or internal waves which enhance the food supply. Thus, the influence of the NACW (Figure 13) in the study area allows the presence of desmosponges assemblages with a wide Atlanto-Mediterranean distribution [60,64].

Dissolved Oxygen Concentrations
Dissolved oxygen (DO) values are close to saturation in most deep-sea areas, ranging from 2.5 mL·L −1 off SW Africa to 6 mL·L −1 in the NW Atlantic [65]. The values of DO for deep-sea corals in the study area are limited to values ranging from 4.3 to 5.5 mL·L −1 ( Figure 14D Figure 14D). Deep-sea corals and sponges, like other organisms, are not very sensitive to small variations in DO unless it drops a certain threshold [12].
Otherwise, hypoxic or anoxia conditions are mainly related to submarine areas with methane seeps or hydrothermal vents. Seafloor anoxic conditions may be generated by intense activity of methane seeps, hydrothermal vents or submarine eruption plumes. Fluid emissions are not continuos but may be reactivated periodically on focused submarine vents or remain diffuse during long time [66]. Very low DO values of 0.64 mL·L −1 observed on deep-water mud volcanoes as Bonjardim in the GoC are closely to anoxia suggesting the intense activity of methane seeps ( Figure 14D). If methane seeps are intense and/or undercurrents are weak in such deep waters, then low oxygen conditions prevail above seafloor and chemosynthesis-based habitats are only composed by colonies of Siboglinidae tubes [67]. However, in areas of methane seeps influenced by strong intermediate undercurrents ( Figure 14D), co-occurrence of chemosynthesis-based and scleractinian-gorgonian aggregations has been detected as in this study and other MVs of the Gulf of Mexico [68]. This is the case for the extensive beds of deep-sea mussels Bathymodiulus mauritanicus beds living around bubbling methane seeps ( Figure 5D) and MDACs patches colonyzed by gorgonians, antipatharians, and scleractinians in Algacel MV ( Figure 5D). In such methane seeps, the siboglinids tubeworms play an important role in the connectivity between methane seeps and deep-sea corals by filtering sulphur reducing bacteria (SRB) allowing the predominance of anaerobic oxidation of methane (AOM) by archaeas building up carbonates patches and allows deep-sea coral larvae to grow isolated from the surrounding highly acidic methane muds [69].

Distribution of Vulnerable Deep-Sea Habitats from Subtropical to North Latitudes
The biodiversity of deep-sea habitats and their biogeographical affinities can vary over space and time due to regional and basin-scale changes in the oceanographic conditions [65]. However, active geological process affecting the ocean s seafloor such as methane seeps, hydrothermal vents or submarine eruptions can modulate the spatial distribution of deepsea habitats as detected in this study. The water properties for deep-sea habitats show trends with latitude which are related to oceanographic conditions, but also anomalous values associated with methane seeps and hydrothermal vents ( Figure 15). Therefore, deep-sea coral habitats show a notable decreasing trend in the suitable temperatures from north to south ( Figure 15A): (i) 11-11.5 • C for scleractinian reefs habitats in the Galicia Bank; (ii) 8.8-10 • C for gorgonian and scleractinian aggregations associated with mud volcanoes of the GoC; and (ii) 7.4-7.7 • C for stony octocoral gardens of the PoL. Otherwise, the sponge grounds show a similar decreasing trend but at higher temperature ranges.
Thus, desmosponges habitats of the GoC are related to temperatures thresholds as high as 12.5 • C, whereas hexactillined sponge grounds of the Pol show lower temperatures of 7.3-7.33 • C ( Figure 15A). This negative trend identified in the sensitive temperatures for these habitats may be caused by the cooling of the AAIW intermediate waters and it may affect the composition of these communities as identified on T-S diagram ( Figure 13). The AAIW flows along the NW African coast and extends to the GoC, where it interacts with the MOW outflow, perhaps restricting the spreading of the later [70].
The values of salinity from 24 • to 44 • N show a different trend than the temperature ones ( Figure 15B). In this case, the deep-sea habitats supporting maximum salinity values are located on the mud volcanoes of the GoC, that are strongly influenced by the MOW undercurrent (Figures 12 and 13). Therefore, gorgonian and scleractinian aggregations growing on MDACs around methane seeps show maximum salinity values up 36 psu. Both to the north and to the south, the salinity threshold for deep-sea corals diminishes.  Figure 15B). Considering this, the low salinity and temperature values bathing the stony octocoral aggregations of the PoL are due to the influence of the AAIW flowing along the NW African (Figures 12 and 13).
The salinity threshold for the sponge aggregations follows the same descending trend from 34 to 28 • N at regional scale ( Figure 15B). Desmosponge grounds living close to methane seeps in the GoC are living under similar high salinity values to gorgonian and scleractinian aggregations ( Figure 15B). However, hexactillenid sponge grounds living at shallower depths on the summits of the PoL mounds support higher salinity values than stony octocoral habitats ( Figure 15B). This is interpreted as a result of the influence of periodic southwards intrusions of salty MOW waters into the PoL at water depths shallower than the AAIW undercurrents which may influence the development of those habitats.  (Figure 4), pointing to a massive mortality of scleractinian reefs off northwest Moroccan [69,[71][72][73] and along the Mauritanian margins [74].
Based on radiocarbon data of scleractinians along the Western Mediterranean Sea during the last deglaciation times [75], we hypothesize that the beginning of intrusion of AAIW waters into the GoC during the last deglacial times may have been one of the causes of a massive mortality of scleractinians by shifting northwards the biogeographical boundary between some scleractinians and stony octocoral aggregations ( Figure 15B). This point out that stony octocorals (Corallium tricolor and C. niobe), antipatharians, and gorgonians are more suitable to AAIW conditions than the scleractinians D. pertusum and M. oculata.

The role of Methane Seeps Driving Distribution of Chemosynthesis and Non-Chemosynthesis-Based Habitats
Seabed features formed by seafloor venting of hydrocarbon-enriched fluids are generically termed cold seeps, which are associated with high geological, geochemical and, biological activity [51,52]. Submarine MVs are one of the main seabed morphological expressions of cold seeps formed by violent eruptions, followed by progressive degassing of hydrocarbon-enriched fluids and sediments onto the seafloor [66].

Drivers Controlling Distribution of Habitats in Methane Seeps: Acidic Muds vs. Carbonates
Based on the habitat types identified, ROV-mounted CTD parameters and CH 4 water analyses along MVs of the GoC, two main drivers controlling their formation and distribution should be highlighted: (i) the rate of release of deep-seated methane-enriched fluids, and (ii) the formation of hard substrates such as MDACs (chimneys, slabs or pavements) by AOM processes [27].
The upward migration of methane is transformed by AOM into large amounts of sulphide on the surface [76]. This extremely acid seafloor is buffered by large populations of sulphur-oxidizing siboglinid tubeworms and sulphur-oxidizing bacterial mats, allowing formation of hotspots on the surface by consuming the AOM-sourced sulphur [69]. The occurrence of siboglinid tubeworms in the anoxic-oxic zone seems to be essential for the formation and the non-dissolution of carbonates at the seabed and, moreover for the progressive colonization by deep-sea corals and other suspension feeders on these hard carbonated substrates. Thus, some scleractinians, gorgonians, antipatharians, bamboo corals, and demosponges can colonize the upper parts of MDACs blocks, slabs and pavements, up to 1 m in diameter. In areas with extensive hydrocarbon seeps, massive MDACs are the dominant substrate for coral colonization and reef formation as detected in other MVs of the GoC [54,59].

CWC Mounds and Methane Seeps
The formation of giant carbonate mounds up to 30 m high built up by colonial scleractinians has been identified related to methane seeps in the GoC [69,71,72,77]. In the case of the Northern Pompeia Coral Ridge (westwards Algacel MV), we identified values of methane ranging from 41.93 to 43.24 nM and patches of shells of chemosymbiotic bivalves, mainly L. asapheus with some Thyasira vulcolutre, and scattered bacterial mats (sulfur-oxidizing-like Beggiatoa) indicating active methane seeps throughout the carbonate mounds. It has been proposed a direct relationship between carbonate reefs and fluid seepages by fertilizing waters sourced from methane seeps [78]. Recently, a new hypothesis on the formation of carbonate mounds conformed by scleractinians has been proposed in relation to methane seeps [69]. Thus, scleractinian larvae may colonize MDACs hotspots only if siboglinid tubeworms previously reduce the concentration of sulfide in the anoxicoxic zone allowing skeletal calcification of scleractinians in MDACs surrounded by the highly acidic muds of methane seeps. Transition from active methane seeps, carbonate mounds and deep-sea coral colonization stages has also been proposed as evolutionary stages of MVs in the GoC [79].
Deep-sea coral colonizing MDACs hard substrates in areas of methane seeps have been reported throughout all margins of the world: The Gulf of México [80,81], Hikurangi Margin in New Zealand [82], Brazilian margin [83], the Darwin Mounds in the northern Rockall Trough [63], the Norwegian shelf [78], and the Porcupine Basin, west of Ireland [84]. Furthermore, the co-existence of chemosymbiotic vestimentiferan worms and bacterial mats with deep-sea corals in cold seeps has been reported in the Gulf of Mexico [81]. The co-occurrence of MDACs with annelids has also been reported from hydrocarbon seeps along the US northern and mid-Atlantic margin [85]. Both MDACs and chemosymbiotic deep-sea mussels in the U.S. Atlantic margin seeps shows average δ 13 C signature of −47‰, a value consistent with microbially driven anaerobic oxidation of methane-rich fluids occurring at or near the sediment-water interface [85]. In these seep areas, macrofaunal densities dominated by annelid families Dorvilleidae, Capitellidae, and Tubificidae were four times greater than those present in deep-sea mussel beds habitats. These differences between chemosynthesis-based habitats have also been observed in the GoC [59,61]. In this way, it has been suggested that the difference between habitats in such extremophile environments is driven by quality and source of organic matter [86].
The influence of strong undercurrents bathing the flanks of the MVs favours the occurrence of non-chemosymbiotic fauna such as large sponge grounds (Geodia sp., Phakellia sp.) that colonize the scattered MDAC slabs, as well as sea-pens (Funiculina quadrangularis), cerianthids and annelids (Hyalinoeciatubicola) on the soft, muddy sediments.

Potential Ecological Restoration of Deep-Sea Habitats after Submarine Eruptions in the Macaronesia Region
Volcanism and associated hydrothermal systems are relevant processes for the evolution of the ocean basins, due to their impact on the geochemistry of the oceans and their potential to form significant deposits [87]. Low-T hydrothermal vents after violent submarine volcanic eruptions generate long-term CO 2 inputs to oceans due to the continuous degasification of the magmatic systems mainly placed on hot-spot volcanic islands like Hawaii or Canary Islands. This is due to the high contents in C bearing in the thick oceanic sediments below the submarine volcanoes that are expulsed by low-T hydrothermal vent systems [88].
In the Tagoro volcano, recolonization of pioneering fauna such as small oysters, serpulids and mobile species (e.g., shrimps, eels) was detected, representing first colonizers of the newly formed substrates in this volcanic environment. Newly formed habitats were also detected [89] together with the burial of extensive areas with aggregations of antipatharians and some deep-sea corals. Some authors indicated that the first colonizers at Tagoro volcano included a large proportion of common suspension feeders and predators of circalittoral and bathyal hard bottoms of the Macaronesian fauna, which could have exploited the uncolonized hard bottoms and the post eruptive fertilization of water masses [35,36]. Along the flanks of this volcano, caves show high values up 6.44 mL·L −1 of DO related to active CO 2 degasification two years after the volcanic eruption [50]. The trend representing the DO range for deep-sea complex habitats from 40 • N to 26 • N ( Figure 16) shows the potential pathway from the present parameters to reach suitable DO conditions for the settlement and development of slow-growing organisms such as octocorals (gorgonians and soft corals) as well as antipatharians as detected in other areas of El Hierro Island [89].
We suggest that the comparison between habitats growing after submarine eruptions at different ages might be used to infer the rate of biological colonization and the natural ecological succession of habitats after a violent submarine eruption. Previously, a similar approach has been successfully done for understanding geological and biological evolutionary stages in methane seeps displaying different scenarios of rates of fluid venting [79] and hydrodynamics [21]. Therefore, within the Macaronesia volcanic archipelagos, several recent submarine eruptions have taken place in Capelinhos (west Faial Island, Azores) in 1958-59 or south of El Hierro Island (Canary Islands) in 2011-2012 [34]. The recent discovery of soft coral gardens dominated by Alcyonacea in the Azores Archipelago [90] colonizing the volcanic substrate created from the eruption of Capelinhos in 19581-959, opens new studies of succession and survivorship of habitat-forming species in the Macaronesia volcanic areas as they have already been developed in the Hawaiian Islands [91]. eral recent submarine eruptions have taken place in Capelinhos (west Faial Island Azores) in 1958-59 or south of El Hierro Island (Canary Islands) in 2011-2012 [34]. The recent discovery of soft coral gardens dominated by Alcyonacea in the Azores Archipelago [90] colonizing the volcanic substrate created from the eruption of Capelinhos in 19581-959, opens new studies of succession and survivorship of habitat-forming species in the Macaronesia volcanic areas as they have already been developed in the Hawaiian Islands [91].   Supplementary Table S3. This fact would support the hypothesis that the type of seabed substrate and the occurrence of fluid flow (CO 2 , methane, sulfide, iron) together with some water mass properties (e.g., current speed, salinity, and temperature) might control the evolution of the type of habitats in such volcanic environments, i.e., (i) soft octocoral gardens developed after recent volcanic eruptions (~50 years ago) with latent hydrothermal CO 2 degassing and Fe fertilization but causing seabed acidification unsuitable for carbonates; (ii) Coral gardens and sponge aggregations with a wide variety of sessile species (e.g., octocorals, hexactinellid and lithistid sponges, black corals, bamboo corals and large gorgonians) supported by non-degassing volcanic rocks (up thousands of years old) as the submarine ridges of PoL allowing occurrence of carbonate-bearing benthic fauna.

Tools for Future Management of Vulnerable Marine Ecosystems
The integration of high-resolution bathymetry, measurements of in-situ water mass properties, and identification of deep-sea habitats ground truthing by ROV at regional scale represents an important tool for increasing the knowledge and protection of deep-water marine ecosystems, especially those areas with VMEs, affected by the ongoing climate changes and/or contemporary anthropogenic impacts. The future scenario for the impact in deep-sea species and habitats, such as scleractinian reefs, coral gardens or deep-sea sponge aggregations, with potential increases in CO 2 and CH 4 emissions or rising in the seawater temperature of the oceans at global scale, might be compared with the changes produced, at local scale, by natural emissions of methane in cold seeps or carbon dioxide in recent submarine eruptions.
Otherwise, these integrated studies are also of paramount importance for the efficient management of natural marine resources, such as the ferromanganese crusts bearing seamounts with high contents in Co, Ni, and other Rare Earth Elements (REE), which are presently targets for mineral exploration in the Area under contracts with the Inter-national Seabed Authority (ISA). These seamounts host VMEs, as detected in this and previous studies [92] as well as mineral resources [93] and, thus, spatial management plans are needed to address potential conflicts between deep seabed mining interests and the conservation of the deep-sea biodiversity presented in this study. The same applies for the hydrocarbon-bearing fluid habitats of the studied methane seeps, which are potential target areas for hydrocarbon exploitation in the subsurface and contain singular habitats with endemic species such as the chemosymbiotic bivalves of the GoC.
The five case studies presented here might be considered Ecologically or Biologically Significant Marine Areas (EBSAs) as considered by the United Nations Convention of Biological Diversity (according to different criteria of Annex I, decision IX/20). Unfortunately, significant ecosystem components of those areas (mainly benthic ones) may be threatened by human activities (e.g., fishing activities, hydrocarbon exploitation, or seabed mining), at present or in a near future. Therefore, these selected areas comprising a wide variety of deep-sea habitats in the North Atlantic should be protected and used as pilot areas for further mapping and monitoring of habitats and VMEs, contributing to the environmental management of the North Atlantic Ocean seafloor.

Conclusions
Five case studies located between 90 and 2500 mbsl depth, along the NE and Central Atlantic Ocean from 23 • N to 42 • N latitudes, are presented in this work. These were targeted with MBES mapping, ROV-mounted CTD data of the benthic layer (temperatures, salinity, potential density, dissolved oxygen, potential density, CO 2 , CH 4 concentration) and identification and sampling of deep-sea habitats. Based on these datasets, we conclude that: (1) The distribution of deep-sea habitats along the northeastern Atlantic Ocean is somehow influenced by the water mass properties of the benthic layer at basin scale. However, the water mass properties drivers are modulated by the effects, at regional and local scale, of methane seeps or low-temperature hydrothermal fields after submarine eruptions. (5) The co-occurrence of deep-sea coral and sponge habitats and chemosynthesis-based habitats was detected in methane seeps of the Gulf of Cádiz. Thus, extensive beds of living deep-sea mussels Bathymodiolus mauritanicus and other chemosymbiotic bivalves around focused bubbling CH 4 vents are placed close to aggregations of sponges, scleractinians, gorgonians, and antipatharians colonizing newly formed MDACs carbonates. Colonies of Sibloginid sp. tubeworms play an important role in the connectivity between seeps and some of these suspension feeders by generating pavement patches of MDACs and allowing them to be isolated from the acidic seafloor [69]. (6) Our data support that some deep-sea habitats can be very sensitive to local variations in dissolved oxygen (DO) concentrations within the benthic layer.

Data Availability Statement:
The data presented in this study are available on request from the corresponding author.