Coincident wide-angle and multi-channel seismic data acquired within the scope of the PAMELA Moz3-5 project allow to reconsider the formation mechanism of East-African margins offshore southern Mozambique. This study most specifically focuses on the sedimentary and deep crustal architecture of the Limpopo margin (LM) that fringes the eastern edge of the Mozambique’s Coastal Plain (MCP) and its offshore southern prolongation the North Natal Valley (NNV). It relies primarily on the MZ3 profile that runs obliquely from the northeastern NNV towards the Mozambique basin (MB) with additional inputs from a tectono-stratigraphy analysis of industrial onshore-offshore seismic lines and nearby or crossing velocity models from companion studies. Over its entire N-S extension the LM appears segmented in (1) a western domain that shows the progressive eastward crustal thinning and termination of the MCP/NNV continental crust and its overlying pre-Neocomien volcano-sedimentary basement; and (2) a central corridor of anomalous crust bounded to the east by the Mozambique fracture zone (MFZ) and the oceanic crust of the MB. A prominent basement high marks the boundary between these two domains. Its development was most probably controlled by a steep and deeply rooted fault, i.e. the Limpopo fault. We infer that strike-slip or slightly trans-tensional rifting occurred along the LM and was accommodated along this Limpopo fault. At depth we propose that ductile shearing was responsible for the thinning of the continental crust and an oceanward flow of lower crustal material. This process was accompanied by intense magmatism that extruded to form the volcanic basement and gave to the corridor its peculiar structure and mixed nature. The whole region remained at a relative high level during the rifting period and a shallow marine environment dominated the pre-Neocomien period during the early phase of continent-ocean interaction. It is only some times after break-up in the MB and the initiation of the MFZ that decoupling occurred between the MCP/NNV and the corridor allowing for the latter to subside and being covered by deep marine sediments. A scenario for the early evolution and formation of the LM is proposed taking into account both recent kinematic and geological constraints. It implies that no or little changes in extensional direction occurred between the intra-continental rifting and subsequent phase of continent-ocean interaction.

This archive includes wide-angle seismic data from profiles 1, 2, 3 and 2 of the MARGATS cruise offshore French Guyana and Surinam including navigation files. The objective is more precisely to characterize the crustal structure and evolution of marginal plateaux, sub-marine reliefs that are associated to 30 % of the transform margins in the world. These reliefs are systematically observed at the junction of different ages in relay zones between divergent and transform segments. Their building remains enigmatic although they represent reliefs established in geodynamical nubs that are keys ton understand the localisation of transform margins. This project MARGATS intend to image the deep structure of the marginal plateau (wide angle seismic and multichannel seismic MCS). The experimental site proposed is the Demerara plateau offshore French Guyana and Surinam and located at the junction between Central Atlantic locally opened in a divergent mode and Equatorial Atlantic opened mainly in transform mode in the area. Hence, this plateau has recorded at its different borders the divergent opening of the central Atlantic and the tranform opening of the Equatorial Atlantic. It may be this situation itself that leads to the formation of the plateau, but it requires to precisely constraint its deep internal structure. Finally the Demerara plateau is one of the more studied with petroleum seismic data and high resolution seismic data. It is then one of the ideal place to conduct a high resolution wide-angle deep seismic survey.

Pialassa Baiona is a temperate coastal lagoon connected with the Northwestern Adriatic Sea (44° 280 N and 44°310 E). Sediment cores and surface sediments were collected in two habitats within Pialassa Baiona: a) a salt marsh habitat characterized by the presence of saltmarsh vegetation, and b) a human impacted habitat close to anthropogenic source inputs. Cores were sampled by inserting one cylindrical Plexiglas hand corer (5-cm diameter, 50 cm long) into the sediment to a depth of 20-25 cm, and surface sediment samples (0–5 cm) were collected with a stainless-steel grab sampler. The cores were extruded in the field, sectioned into 1‐2 cm intervals, and analyzed for total organic carbon (OC), total nitrogen (TN), carbon isotope ratio (δ13C) and dry bulk density (upper 20 – 25 cm) and analyzed for organic carbon (OC), total nitrogen (TN), carbon isotope ratio (δ13C) and dry bulk density. Organic carbon (OC), total nitrogen (TN), and carbon isotopes (δ13C = [(13C/12C)sample/(13C/12C)standard − 1] × 1,000) were measured in sediment cores and surface sediments using a using a FINNIGAN Delta Plus XP mass spectrometer directly coupled to Thermo Fisher FLASH 2000 CHNS Elemental Analyzer. OC and TN content was expressed as the weight percentage of dried sediment, and carbon isotope results were reported in the standard delta notation with respect to the Vienna Pee Dee Belemnite. A ‘three-end member’ mixing model was used to estimate the relative contribution of the different organic matter (OM) sources: marine phytoplankton (FM), riverine-estuarine phytoplankton (FRE), and C3 saltmarsh plant material (FSM): δ13Csample = δ13CM x FM + δ13CFE x FFE + δ13CSM x FSM C/Nsample = C/NM x FM + C/NFE x FFE + C/NSM x FSM 1 = FM + FRE + FSM where FM, FRE and FSM are the relative contributions of marine phytoplankton, riverine-estuarine phytoplankton, and saltmarsh plant material, respectively. δ13CM (-18.97‰) and C/NM (4.95), and δ13CRE (-30.70‰,) and C/NRE (6.63) represent the end member POC signature recorded during distinct marine and estuarine phytoplankton blooms in the coastal lagoon (Guerra et al., 2013).The C3 saltmarsh plant end-member was selected on the basis of typical δ13CSM (-20.2‰) and C/NSM (15.35) values for Juncus spp. (Gebrehiwet et al., 2008; Hughes and Sherr, 1983; J. I. Kelleway et al., 2017; Kemp et al., 2012, 2010; Lamb et al., 2006). References Gebrehiwet, T., Koretsky, C.M., Krishnamurthy, R. V., 2008. Influence of Spartina and Juncus on saltmarsh sediments. III. Organic geochemistry. Chem. Geol. 255, 114–119. https://doi.org/10.1016/j.chemgeo.2008.06.015 Guerra, R., Pistocchi, R., Vanucci, S., 2013. Dynamics and sources of organic carbon in suspended particulate matter and sediments in Pialassa Baiona lagoon (NW Adriatic Sea, Italy). Estuar. Coast. Shelf Sci. 135, 24–32. https://doi.org/10.1016/j.ecss.2013.06.022 Kelleway, J.I., Saintilan, N., Macreadie, P.I., Baldock, J.A., Ralph, P.J., 2017. Sediment and carbon deposition vary among vegetation assemblages in a coastal salt marsh. Biogeosciences 14, 3763–3779. https://doi.org/10.5194/bg-14-3763-2017 Kemp, A.C., Vane, C.H., Horton, B.P., Culver, S.J., 2010. Stable carbon isotopes as potential sea-level indicators in salt marshes, North Carolina, USA. Holocene 20, 623–636. https://doi.org/10.1177/0959683609354302 Kemp, A.C., Vane, C.H., Horton, B.P., Engelhart, S.E., Nikitina, D., 2012. Application of stable carbon isotopes for reconstructing salt-marsh floral zones and relative sea level, New Jersey, USA. J. Quat. Sci. 27, 404–414. https://doi.org/10.1002/jqs.1561

Harmonised WFS Download service for Maltese Agglomeration Maltese Zone and PAHs Zone According to the requirements of Directives 2008/50/EC and 2004/107/EC with respect to the minimum number of sampling points and the assessment regimes, the data set consists of two zones in the Maltese territory, the Air Monitoring Agglomeration and the Air Quality Monitoring Zone in which all main pollutants are being monitored. A third zone covering the monitoring of Polycyclic Aromatic Hydrocarbons (PAHs) is also included in the data set.

Six large grids were obtained by merging multibeam bathymetric data from several international cruises along the Southwest Indian Ridge from the Gallieni Transform Fault (54°E) to the Rodrigues Triple Junction (70°E). The spatial resolution is about 150 m. This dataset was used in several scientific papers.

ODEMAR AUV Abyss (GEOMAR) + shipboard Pourquoi Pas? multibeam bathymetry - 13deg20minN Oceanic Core Complex, Mid Atlantic Ridge Microbathymetry acquired with AUV REMOS 6000 with a SeaBat RESON 7125 multibeam system. Bathymetry data gridded at 2 m (GMT grdfile) - one grid for 13deg20'N Oceanic Core Complex, and one grid for 13deg30'N Oceanic Core Complex - DM_OCC1320_AUV_SHI.grd: Title: ODM_OCC1320_AUV2.grd - ODM_OCC1320_AUV_SHI.grd: Command: grdmath ODM_OCC1320_AUV2.grd ODM_OCC1320_SHI2.grd AND = ODM_OCC1320_AUV_SHI.grd - ODM_OCC1320_AUV_SHI.grd: Remark:  - ODM_OCC1320_AUV_SHI.grd: Gridline node registration used [Cartesian grid] - ODM_OCC1320_AUV_SHI.grd: Grid file format: nf = GMT netCDF format (32-bit float), COARDS, CF-1.5 - ODM_OCC1320_AUV_SHI.grd: x_min: -44.97115 x_max: -44.86795 x_inc: 1.7947826087e-05 name: x nx: 5751 - ODM_OCC1320_AUV_SHI.grd: y_min: 13.27915 y_max: 13.34155 y_inc: 1.79361885599e-05 name: y ny: 3480 - ODM_OCC1320_AUV_SHI.grd: z_min: -3924.5378418 z_max: -1905.49023438 name: z - ODM_OCC1320_AUV_SHI.grd: scale_factor: 1 add_offset: 0 - ODM_OCC1320_AUV_SHI.grd: format: classic - ODM_OCC1330_AUV_SHI.grd: Command: grdmath ODM_OCC1330_AUV2.grd ODM_OCC1330_SHI2.grd AND = ODM_OCC1330_AUV_SHI.grd - ODM_OCC1330_AUV_SHI.grd: Remark:  - ODM_OCC1330_AUV_SHI.grd: Gridline node registration used [Cartesian grid] - ODM_OCC1330_AUV_SHI.grd: Grid file format: nf = GMT netCDF format (32-bit float), COARDS, CF-1.5 - ODM_OCC1330_AUV_SHI.grd: x_min: -45.00965 x_max: -44.88125 x_inc: 1.79454926625e-05 name: x nx: 7156 - ODM_OCC1330_AUV_SHI.grd: y_min: 13.48665 y_max: 13.52225 y_inc: 1.79254783484e-05 name: y ny: 1987 - ODM_OCC1330_AUV_SHI.grd: z_min: -3244.60083008 z_max: -2087.49829102 name: z - ODM_OCC1330_AUV_SHI.grd: scale_factor: 1 add_offset: 0 - ODM_OCC1330_AUV_SHI.grd: format: classic  

Pre-Quaternary - Lithology. This web map service shows the geological units of the seafloor originated earlier than 2,588 Ma from now (pre-Quaternary). International Geological Map of Europe and Adjacent Areas (Asch, 2005). The scale varies between 25,000 and 5 000 000.The data were compiled by BGR from the EMODnet geology partner organisations in the EMODnet Geology project between 2009 and 2021

Pre-Quaternary -age This web map service shows the chronostratigraphic age of geological units of the seafloor originated earlier than 2,588 Ma from now (pre-Quaternary). International Geological Map of Europe and Adjacent Areas (Asch, 2005). The scale varies between 25,000 and 5 000 000. The data were compiled by BGR from the EMODnet geology partner organisations in the EMODnet Geology project phases I, II and III between 2009 and 2019. Pre-Quaternary -lithology This web map service shows the rock type (lithology) of geological units of the seafloor originated earlier than 2,588 Ma from now (pre-Quaternary). International Geological Map of Europe and Adjacent Areas (Asch, 2005). The scale varies between 25 000 and 5 000 000. The data were compiled by BGR from the EMODnet geology partner organisations in the EMODnet Geology project phases I, II and III between 2009 and 2019. The scale varies between 25 000 and 5 000 000.

The SeaExplorer glider Sea028 was deployed from the research vessel R/V Lance on the 15 September 2017 at 79.5°N, 8.6°E, on the western slope of Svalbard. The glider was recovered on 23 September 2017 at 80.62°N, 13.83°E.The glider was equipped with a GPCTD (Glider Payload Conductivity Temperature Depth from SeaBird), a dissolved oxygen sensor (Sea Bird SBE43F), and an optical sensor measuring Chlorophyll a (470/695 nm), Colored Dissolved Organic Matter (CDOM, 370/460 nm), and the total particle concentration or backscatter (backscattering at 700 nm) (EcoPuck from Wetlabs). The dataset is composed of the data corrected from the thermal lag and the sensor lag, despiked and interpolated every 1m. The profiles are separated.