Description: Water temperature, salinity and density were obtained in melt ponds within the MOSAiC Leg 5 ice camp between 23 August and 14 September 2020. A Rinko handheld CTD (JFE Advantech Co., Ltd., Japan) was carefully lowered into the melt ponds on a regular basis to determine the spatial distribution and temporal evolution of the stratification. A fresh meltwater layer was detected within the melt ponds. As part of a dedicated study, the present dataset documents the evolution of this layer.

Description: The temperatures at water depths of 0.015, 0.05, 0.1, and 0.2 m were measured by thermistor probe (TR-5120, T&D Corp., Nagano, Japan) and temperature data were stored in a data logger (TR-52i, T&D Corp.) at St. 1 melt pond during expedition PS122/5 (MOSAiC Leg 5) to the central Arctic in August-September 2020. In order to install the thermistor probe, we used stick longer than the diameter of the pond.

Description: The CO2 fluxes were measured over the surfaces of snow, ice, water with LI-COR 8100-104 chambers connected to a LI-8100A soil CO2 flux system (LI-COR Inc., USA) during expedition PS122 (MOSAiC Legs 1−5) to the central Arctic in October 2019−September 2020. A chamber was connected via a closed loop to an infrared gas analyzer (LI-8100A, LI-COR Inc., USA) to measure CO2 concentrations with an air pump at a rate of 3 L min−1 during 20-minute intervals. Power was supplied by a battery (8012−254, Optima Batteries Inc., USA). We also used a Teflon-coated metal chamber (0.50 m in diameter and 0.30 m high with a serrated bottom edge) (Nomura et al., 2010, 2012). Every 5 or 10 minutes during an experiment, about 500 mL of air was collected from the chamber using a 50-mL glass syringe with a three-way valve and then transferred to a 3000-mL Tedlar bag (AAK 3L, GL Sciences Inc., Japan). After collection, air samples were quickly transported in a dark container to a laboratory onboard the R/V Polarstern, which was moored near our sampling site. The CO2 concentrations were measured with a CO2 analyzer (Picarro 2132-i, Los Gatos Research Inc., USA) used for continuous measurements of atmospheric CO2/CH4 concentrations on board. The CO2 fluxes (in mmol C m−2 day−1) (a negative value indicates CO2 being absorbed from the atmosphere) were calculated with LI-COR software (model: LI8100PC Client v.3.0.1.) based on the changes of the CO2 concentrations within the headspace of the LI-COR 8100−104 chambers. For the metal chamber, we took into account the changes of CO2 concentrations and the volume of the chamber (Nomura et al., 2010, 2012) to calculate the CO2 fluxes. The detection limit of this system was about +0.1 mmol C m−2 day−1 (Nomura et al., 2010; 2018). An inter-comparison experiment between the metal chamber and the LI-COR 8100−104 chamber in the home laboratory indicated good agreement (Nomura et al., 2022). Data obtained with both methods were therefore comparable. When the surface of the melt ponds/leads was frozen, flux measurements were made over the frozen surface. Then, a 1 m x 1 m hole was cut with a hand saw, and chambers were installed over the water surface with buoyant material (Nomura et al., 2020; 2022). In addition, chambers were installed over snow/slush/frost flower surface, and ice surface after removing snow by shovel. We conducted water mixing experiments at St. 4 (melt pond) on September 2, 2020 and at the ROV lead site on September 5, 2020 to understand how the carbonate chemistry and CO2 fluxes responded to changes in the marine environment caused by agitation in the melt pond and lead by wind and movement of sea ice. We measured the fluxes between the atmosphere and the surfaces of the melt ponds and leads using a floating metal chamber. After the measurements, the water in the melt ponds or leads was mixed for 30 minutes by two persons using a shovel and an oar. After mixing, the pre-mixing measurements were repeated.

Description: Melt ponds water sampling for biogeochemical parameters such as dissolved inorganic carbon (DIC), total alkalinity (TA), oxygen isotopes were examined from August to September 2020. To obtain discrete water samples from the melt ponds and leads, we checked the vertical structure and depth of the meltwater layer from the same hole used for the RINKO Profiler by attaching a conductivity sensor (Cond 315i, WTW GmbH, Germany) to a 2-m-long ruler and inserting the ruler into the lead water until the salinity measured with the Cond 315i increased at the meltwater–seawater interface (Nomura et al., 2024) . Water was pumped up with a peristaltic pump through a 2-m-long PTFE tube (L/S Pump Tubing, Masterflex, USA) at depths corresponding to meltwater (surface), the interface between meltwater and seawater (interface), and seawater (bottom). Salinity was measured at each depth by attaching a Cond 315i conductivity sensor to the bottom of the ruler. The tube intake was likewise attached to the bottom of the ruler. Seawater was subsampled into a 250-mL glass vial (Duran Co., Ltd., Germany) for measurement of dissolved inorganic carbon (DIC) and total alkalinity (TA) and a 50-mL glass, screw-cap, narrow-neck vial (VWR international LLC, Germany) for measurement of the oxygen isotopic ratio (δ18O) of the water. Immediately after subsampling for measurement of DIC and TA, a 6.0% (wt.) mercuric chloride (HgCl2) solution (100 µL) was added to stop biological activity. Samples for DIC and TA were stored at +4°C on the R/V Polarstern. Samples for δ18O were stored at room temperature (20°C). During the discrete water sampling, the CO2 concentration in the water column was measured directly on site by passing the water through an equilibrator Liqui-Cel® (G542, S/N: 132462, 3M Company, USA) connected to an infrared gas analyzer (LI-8100A, LI-COR Inc., USA). The analyzer was calibrated with standard gases containing 0.0, 299.3, and 501.3 ppm CO2 before MOSAiC Leg 5. RMS (root means square) noise at 370 ppm with 1 sec signal averaging is 〈1 ppm (https://www.licor.com/env/products/soil-flux/LI-8100a). The equilibrator was connected in the loop for water sampling (vide supra), and a 2-m-long ruler was inserted into the water and kept at that depth until the CO2 was equilibrated with air (about 1 minute) by monitoring the CO2 values. The CO2 concentration was measured at each depth (i.e., surface, interface, and bottom). At the ROV lead sites, vertical CO2 measurements were made every 0.05 m for detailed profiles. The DIC of water was determined by coulometry (Johnson et al., 1985; Johnson, 1992) using a home-made CO2 extraction system (Ono et al., 1998) and a coulometer (CM5012, UIC, Inc., Binghamton, NY, USA). The TA of water was determined by titration (Dickson et al., 2007) using a TA analyzer (ATT-05, Kimoto Electric Co., Ltd., Japan). Both DIC and TA measurements were calibrated with reference seawater materials (Batch AR, AU, and AV; KANSO Technos Co., Ltd., Osaka, Japan) traceable to the Certified Reference Material distributed by Prof. A. G. Dickson (Scripps Institution of Oceanography, La Jolla, CA, USA). Oxygen isotope analyses were carried out at the ISOLAB Facility at AWI Potsdam (hdl:10013/sensor.ddc92f54-4c63-492d-81c7-696260694001) with mass spectrometers (DELTA-S Finnigan MAT, USA): hdl:10013/sensor.af148dea-fe65-4c87-9744-50dc4c81f7c9 and hdl:10013/sensor.62e86761-9fae-4f12-9c10-9b245028ea4c employing the equilibration method (details in Meyer et al., 2000). δ18O values were given in per mil (‰) vs. Vienna standard mean ocean water (V-SMOW) as the standard.

Description: Recently, long-acting injection (LAI) of second-generation antipsychotics has become a valuable strategy for the treatment of schizophrenia. However, few studies have compared the effects of different LAI anti...

Description: Generation of a novel transgenic rat model for tracing extracellular vesicles in body fluids Scientific Reports, Published online: 19 August 2016; doi:10.1038/srep31172