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This data set belongs to "21st-century environmental change decreases habitat overlap of Antarctic toothfish (Dissostichus mawsoni) and its prey" by Cara Nissen, Jilda Alicia Caccavo and Anne L. Moree (to be submitted to "Frontiers in Marine Science") Contact: cara.nissen@colorado.edu The data provided here are post-processed from the raw FESOM1.4-REcoM2 model output which can be obtained at the World Data Center for Climate (WDCC): https://www.wdc-climate.de/ui/project?acronym=HighRes_highLat_SO simA (historical simulation): https://doi.org/10.26050/WDCC/FESOM14-REcoM2_A_hist_vA_vCsimA-ssp126: https://doi.org/10.26050/WDCC/FESOM14-REcoM2_A_s126_vA_vCsimA-ssp245: https://doi.org/10.26050/WDCC/FESOM14-REcoM2_A_s245_vA_vCsimA-ssp370: https://doi.org/10.26050/WDCC/FESOM14-REcoM2_A_s370_vA_vCsimA-ssp585: https://doi.org/10.26050/WDCC/FESOM14-REcoM2_A_s585_vA_vCsimB (control simulation): https://doi.org/10.26050/WDCC/FESOM14-REcoM2_B_1921_cA_cC The raw model output was first post-processed with MASTER_toothfish_postprocessing_AGI_save_netcdf_files_monthly_with_drift_correction.ipynb to get fields of in-situ temperature (t_insitu) and partial pressure of oxygen (pO2) on the regular grid used in this study (see Mesh_ancillary_information_v20220919.nc). Subsequently, these data are post-processed with reduce_depth_levels_drift_corr_files.sh. 2-dimensional distribution data of Antarctic Toothfish prey used in this study can be accessed viahttps://doi.org/10.5281/zenodo.10598488 The following files are provided here: Monthly climatological pO2 and t_insitu 1995-2014 (used to compute preferred temperature, pO2 threshold and critical AGI of each species):- pO2_fesom_simA_monthly_clim_1995_2014_v2.nc- t_insitu_fesom_simA_monthly_clim_1995_2014_v2.nc Annual pO2 and t_insitu for the historical period 1995-2014:- pO2_fesom_historical_1995_2014_annual_mean_AGImesh.tar.gz- t_insitu_historical_1995_2014_annual_mean_AGImesh.tar.gz Drift-corrected annual pO2 and t_insitu 2091-2100 for four emission scenarios: - pO2_fesom_ssp126_2091_2100_drift_corrected_annual_mean_AGImesh.tar.gz- pO2_fesom_ssp245_2091_2100_drift_corrected_annual_mean_AGImesh.tar.gz- pO2_fesom_ssp370_2091_2100_drift_corrected_annual_mean_AGImesh.tar.gz- pO2_fesom_ssp585_2091_2100_drift_corrected_annual_mean_AGImesh.tar.gz- t_insitu_fesom_ssp126_2091_2100_drift_corrected_annual_mean_AGImesh.tar.gz- t_insitu_fesom_ssp245_2091_2100_drift_corrected_annual_mean_AGImesh.tar.gz- t_insitu_fesom_ssp370_2091_2100_drift_corrected_annual_mean_AGImesh.tar.gz- t_insitu_fesom_ssp585_2091_2100_drift_corrected_annual_mean_AGImesh.tar.gz Sensitivity to chosen future time period / Drift-corrected annual pO2 and t_insitu 2081-2100 and 2098-2100 for the highest-emission scenario SSP5-8.5: - pO2_fesom_ssp585_2081_2100_drift_corrected_annual_mean_AGImesh.tar.gz- pO2_fesom_ssp585_2098_2100_drift_corrected_annual_mean_AGImesh.tar.gz- t_insitu_fesom_ssp585_2081_2100_drift_corrected_annual_mean_AGImesh.tar.gz- t_insitu_fesom_ssp585_2098_2100_drift_corrected_annual_mean_AGImesh.tar.gz Attributing change to warming and deoxygenation / Drift-corrected annual pO2 2091-2100 at clim. t_insitu for the highest-emission scenario SSP5-8.5:- pO2_fesom_ssp585_2091_2100_drift_corrected_at_clim_t_insitu_annual_mean_AGImesh.tar.gz Information on model drift (used to correct the above files): - oxygen_fesom_simB_1995_2014_2091_2100_monthly.tar.gz- pO2_fesom_simB_1995_2014_2091_2100_monthly.tar.gz- salinity_fesom_simB_1995_2014_2091_2100_monthly.tar.gz- t_insitu_fesom_simB_1995_2014_2091_2100_monthly.tar.gz

Habitat files of 28 Antarctic Toothfish (Dissostichus mawsoni) prey species and the Antarctic Toothfish itself, regridded to the FESOM-REcoM model grid, in NetCDF format. For use in article '21st-century environmental change decreases habitat overlap of Antarctic toothfish (Dissostichus mawsoni) and its prey'. This dataset is a collection of the following: 1) 2-dimensional distribution data for 3 squid species, derived from Raymond et al. (2015) 2) 2-dimensional distribution data for 25 prey species and the Antarctic Toothfish, derived from AquaMaps distribution data 3) the model grid file. A species is present in a certain gridcell when its value is 1, elsewhere the species is considered absent. 1) Original files for the 3 squid species galiteuthis glacialis, kondakovia longimana and mesonychoteuthis hamiltoni are taken from previously published data of Raymond et al. (2015) and regridded to the FESOM-REcoM model grid. These squid species are considered to have their habitat anywhere where habitat suitability in the original Raymond et al. (2015) dataset exceeds the habitat suitability thresholds of 0.228 for Galiteuthis glacialis, 0.281 for Kondakovia longimana and 0.121 for Mesonychoteuthis hamiltoni (threshold values as in Xavier et al. (2016), personal communication with Ben Raymond 16.01.2023 to get exact values). These data have an original resolution of 0.1x0.1 degrees (regular longitude-latitude grid). 2) The 25 files taken from AquaMaps start with Default_* or Reviewed_* and are the native predicted range data as provided by Kaschner et al. (2019). They were shared by Kathleen Kesner-Reyes from AquaMaps in March and April 2023 after being reviewed by her for correctness and actuality. The files that start with Reviewed_* have had adjustments made to the original Default_* based on this review, which is described in more detail on the AquaMaps website. These data have an original resolution of 0.5x0.5 degrees (regular longitude-latitude grid). 3) The model grid file 'Mesh_ancillary_information_v20220919.nc' contains the longitude and latitude data needed for regridding to the FESOM-REcoM model grid. Regridding was done using CDO version 1.9.6 (http://mpimet.mpg.de/cdo; developed by U. Schulzweida) and CDO function 'remaplaf', which performs largest area fraction remapping. References Xavier, J.C., Raymond, B., Jones, D.C. et al. Biogeography of Cephalopods in the Southern Ocean Using Habitat Suitability Prediction Models. Ecosystems 19, 220–247 (2016). https://doi.org/10.1007/s10021-015-9926-1 Raymond, B., Xavier, J., Griffiths, H., Jones, D. (2015) Habitat suitability predictions for 15 species of cephalopods in the Southern Ocean, Ver. 1, Australian Antarctic Data Centre - doi:10.4225/15/563AC33450A28, Accessed: 2023-01-16 Kaschner, K., Kesner-Reyes, K., Garilao, C., Segschneider, J., Rius-Barile, J. Rees, T., & Froese, R. (2019, October). AquaMaps: Predicted range maps for aquatic species. Retrieved from https://www.aquamaps.org.

Ocean Alkalinity Enhancement (OAE) could augment long-term carbon storage and mitigate ocean acidification by increasing the bicarbonate ion concentration in ocean water. However, the side effects and/or potential co-benefits of OAE on natural planktonic communities remain poorly understood. To address this knowledge gap, 9 mesocosms were deployed in the oligotrophic waters of Gran Canaria, from September 14th to October 16th, 2021. A CO2-equilibrated Total Alkalinity (TA) gradient was employed in increments of 300 µmol·L-1, ranging from ~2400 to ~4800 µmol·L-1. The carbonate chemistry conditions in terms of TA and Dissolved Inorganic Carbon (DIC), which were then used to calculate pCO2 and pH, and the nitrate+nitrite, phosphate and silicate concentrations were measured every two days over the course of the 33-day experiment alongside the following biotic parameters. Net Community Production (NCP), Gross Production (GP), Community Respiration (CR) rates, as well as the metabolic balance (GP:CR), were monitored every two days through oxygen production and consumption using the winkler method. Fractionated 14C uptake and chlorophyll a were also determined every four days although, initially, the total PO14C and DO14C production were also measured every 4 days, in between, up to day 13. Finally, flow cytometry was also carried out every two days and synecococcus, picoeukaryote and nanophytoplankton abundances were obtained. No damaging effect of CO2-equilibrated OAE in the range applied here, on phytoplankton primary production, community metabolism and composition could be inferred from our results. In fact, a potential co-benefit to OAE was observed in the form of the positive curvilinear response to the DIC gradient up to the ∆TA1800 treatment. Further experimental research at this scale is key to gain a better understanding of the short and long-term effects of OAE on planktonic communities.

Second-year sea-ice thickness, draft, salinity, temperature, and density were measured during near-weekly surveys at the main second-year ice coring site (MCS-SYI) during the MOSAiC expedition (legs 1 to 3) and new second-year ice coring site leg 4, since the earlier site was not accessible any longer. The ice cores were extracted either with a 9-cm (Mark II) or 7.25-cm (Mark III) internal diameter ice corers (Kovacs Enterprise, US). This data set includes data from 18 coring site visits and were performed from 28 October 2019 to 20 July 2020 at coring locations within 50 m to each other in the MOSAiC Central Observatory. During each coring event, ice temperature was measured in situ from a separate temperature core, using Testo 720 thermometers in drill holes with a length of half-core-diameter at 5-cm vertical resolution. Ice bulk practical salinity was measured from melted core sections at 5-cm resolution using a YSI 30 conductivity meter. Ice density was measured using the hydrostatic weighing method (Pustogvar and Kulyakhtin, 2016) from a density core in the freezer laboratory onboard Polarstern at the temperature of –15°C. Relative volumes of brine and gas were estimated from ice salinity, temperature and density using Cox and Weeks (1983) for cold ice and Leppäranta and Manninen (1988) for ice warmer than –2°C. The data contains the event label (1), time (2), and global coordinates (3,4) of each coring measurement and sample IDs (13, 15). Each salinity core has its manually measured ice thickness (5), ice draft (6), core length (7), and mean snow height (22). Each core section has the total length of its top (8) and bottom (9) measured in situ, as well estimated depth of section top (10), bottom (11), and middle (12). The depth estimates assume that the total length of all core sections is equal to the measured ice thickness. Each core section has the value of its practical salinity (14), isotopic values (16, 17, 18) (Meyer et al., 2000), as well as sea ice temperature (19) and ice density (20) interpolated to the depth of salinity measurements. The global coordinates of coring sites were measured directly. When it was not possible, coordinates of the nearby temperature buoy 2019T62 (legs 1-3) or 2019T61 (leg 4) were used. Ice mass balance buoy 2019T62 installation is described in doi:10.1594/PANGAEA.940231, ice mass balance buoy 2020T61 installation is described in doi: 10.1594/PANGAEA.926580. Brine volume (21) fraction estimates are presented only for fraction values from 0 to 30%. Each core section also has comments (23) describing if the sample is from a new coring site or has any other special characteristics. Macronutrients from the salinity core will be published in a subsequent version of this data set.

Biological nitrogen fixation is a key process balancing the loss of combined nitrogen in the marine nitrogen cycle. Its relevance in upwelling systems is not fully resolved. This dataset contains rates of nitrogen fixation through the euphotic layer in two size fractions measured following Montoya et al (1996) technique. It also contains the stable isotopes of carbon in seston expressed in delta notation (δ13C, ‰, VPDB). We sampled in the region of the Guinea Dome and Equatorial Atlantic Ocean along 23°W during Meteor cruise M119 in September 2015. Water samples were collected by niskin bottles attached to a rosette equipped with CTD sensors. Incubations were done in on-deck incubators refrigerated by running surface water continuously and simulating the light intensity of each depth by neutral density filters or meshes.

The Knapps Narrows core was drilled at 38.72129N, -76.33162W on the Eastern Shore of Maryland. The cored target interval lies between 84-102 meters in the Nanjemoy Formation. Calcareous nannofossil biozonation was established in conjunction with paleomagnetic data, allowing us to date the interval to approximately 53.7 mya. Benthic foraminiferal and bulk carbon isotope data allowed for further refinement of the dating of this interval, allowing us to identify ETM2 and H2 on the basis of carbon isotope stratigraphy. For analyses of benthic foraminifera 4-6 Anomalinoides acutus specimens were picked from the 180-250 μm size fraction at each interval. Dinoflagellate cyst assemblages were counted in order to allow for paleo-environmental analysis. Benthic foraminiferal δ18O and TEX86 temperature proxies were compiled over the interval of interest. Semi-quantitative clay mineral assemblages were used to test for changes in the weathering response over hyperthermal intervals. There is excellent agreement between the δ18O and TEX86 temperature proxies, although the highest temperatures do not correspond to either hyperthermal event. There is a noticeable increase in illite content during the ETM2 interval, and an absence of kaolinite. Dinoflagellate assemblages suggest changes in marine paleo-environmental conditions were driven by long-term trends rather than immediate responses to the hyperthermal events.

This data is part of the BMBF project CUSCO (Coastal Upwelling Systems in a Changing Ocean). Here we report biogenic Silica concentrations in the watercolumn collected during a 35-day experiment, where we enclosed natural plankton communities in in-situ mesocosms off Peru. The experiment investigated the interactive effects of light and upwelling on the Humboldt upwelling ecosystem by mimicking a gradient of upwelling intensities (0%, 15%, 30%, 45% and 60%) under summer-time high light and winter-time low light. Integrated seawater samples from a depth between 0 and 10m were collected using a 5L Integrating Water sampler (IWS; Hydro-Bios, Kiel). Samples (0.15-1L) were filtered onto polycarbonate filters (0.65 µm pore size, Whatman). The filters were then dried in the oven at 60 °C for 24 hours and measured following a modified procedure by DeMaster (1981, doi:10.1016/0016-7037(81)90006-5). A standard water bath (Fisher Scientific Isotemp Water Bath, Thermo Fisher Scientific, Waltham, US) was used to digest BSi samples at 85°C. The BSi analysis was carried out with a 4.5-hour time course alkaline digestion (0.1N Na2CO3) to dissolve the BSi followed by a 48 hour HF acid digestion (2.0M) to release the remaining lithogenic silica (LSi). Spectrophotometric analysis of the solubilized silica was done using a Thermo Scientific Genesys 10 UV- VIS Spectrophotometer (Thermo Fisher Scientific, Waltham, US). Model I linear regression was performed to calculate the concentrations of BSi while accounting for the amount of LSi that leached out during the alkaline digestion. Due to restrictions caused by the COVID-19 pandemic BSi data is only available for day 1 until day 17 and for day 31 until day 35. Mesocosm 10 describes the control sample from the Pacificvalues marked with #: analytically undetectable

Fossil scleractinian corals were collected from the Galápagos platform in the East Equatorial Pacific (0°N, 90°E) on cruises MV1007 and NA064 from water depths between 419 and 650 m. Equatorial Atlantic corals (taxa Caryophyllia, Enallopsammia, Desmophyllum) were collected from a depth range of 749 to 2814 m during Cruise JC094 from Carter Seamount (9.2°N, 21.3°W), Knipovich Seamount (5.6°N, 26.9°W), Vema Fracture Zone (10.7°N, 44.6°W), Vayda Seamount (14.9°N, 48.2°W) and Gramberg Seamount (15.4°N, 51.1°W). Southern Ocean samples were obtained from Burdwood Bank (54.7°S, 62.2°W; taxa Caryophyllia, Balanophyllia, Flabellum, Desmophyllum) and Cape Horn (57.2°S, 67.1°W; taxa Caryophyllia, Balanophyllia, Flabellum) in the Subantarctic Zone and the Sars and Interim Seamounts in the Polar Front Zone (59.7°S, 68.8°W and 60.6°S, 66.0°W; taxa Caryophyllia, Desmophyllum) on cruises NBP0805 and NBP1103 in the Drake Passage. These proximal Sars and Interim sites are grouped as simply "Sars". The shallowest coral samples come from depths of 334 m on Burdwood Bank however the majority are from 700 to 1520 m, at water depths corresponding to modern Antarctic Intermediate Water. Corals recovered from the depth of 1012 m from Cape Horn and further south from Sars Seamount at depths of 695 to 1200 m are currently bathed in Upper Circumpolar Deep Water. Deeper samples at the Sars Seamount site sit within Lower Circumpolar Deep Water (1300 to 1750 m). We use published U-series dates for all samples (Burke and Robinson, 2012; Chen et al., 2020; Chen et al., 2015; Li et al., 2020; Margolin et al., 2014; Stewart et al., 2021). Reported age uncertainties are typically ±1% (2 SD). Whole "S1" septa and attached theca were taken from cup corals while whole calyxes were taken from branching specimens using a rotary cutting tool. This tool was further used to remove surficial oxide coatings and any chalky altered carbonate. Where sufficient sample material allowed, multiple sub-samples were measured to minimize microstructural bias (typically duplicates). Coral fragments were crushed and cleaned using warm 1% H2O2 (buffered in NH4OH) oxidative cleaning and a weak acid polish (0.0005 M HNO3). Samples were dissolved in 0.5 M HNO3 and analysed by ICP-MS to yield Li/Mg ratios. Repeat analysis of NIST RM 8301 (Coral) (n=19) yielded analytical precision of <± 1.5%. Coral Li/Mg was converted to temperature using a calibration applicable to all aragonitic corals (Li/Mg = 5.42 exp(−0.050×T(°C)); (Stewart et al., 2020). The quoted uncertainty on this calibration based on prediction intervals is ± 1.7 °C (1σ). This uncertainty is significantly reduced however at extremely low temperatures close to the freezing point of seawater (~ −2 °C). Corals could not survive in frozen seawater, therefore, where proxy estimated temperature falls below this minimum a value of −2 °C is reported instead. For Li/Mg averages of each coral sample and conversion to bottom water temperature, see the xlsx version of the dataset under Further details.