The water vapour isotopic composition (1H216O, H218O and 1H2H16O) of the Atlantic marine boundary layer has been measured from 5 research vessels between 2012 and 2015. Using laser spectroscopy analysers, measurements have been carried out continuously on samples collected 10–20 meter above sea level. All the datasets have been carefully calibrated against the international VSMOW-SLAP scale following the same protocol to build a homogeneous dataset covering the Atlantic Ocean between 4°S to 63°N. In addition, standard meteorological variables have been measured continuously, including sea surface temperatures using calibrated Thermo-Salinograph for most cruises. All calibrated observations are provided with 15-minute resolution. We also provide 6-hourly data to allow easier comparisons with simulations from the isotope-enabled Global Circulation Models. In addition, backwards trajectories from the HYSPLIT model are supplied every 6-hours for the position of our measurements.
|Design Type(s)||observation design|
|Measurement Type(s)||stable isotope analysis|
|Technology Type(s)||cavity ring-down spectroscopy|
|Sample Characteristic(s)||Gulf of Guinea • Northeast Atlantic Ocean • North Atlantic Ocean • Northwest Atlantic Ocean • atmospheric water vapour|
Machine-accessible metadata file describing the reported data (ISA-Tab format)
Background & Summary
The water vapour in the lower atmosphere is a key component of earth’s climate system. It is expected that the recent warming of the earth surface will strongly influence sea surface evaporation and precipitation patterns1–3. Hence in order to accurately project future changes in the atmospheric hydrological cycle, it is necessary to improve our understanding of the physical processes influencing the atmospheric hydrological cycle. Due to the molecular properties of water stable isotopes, isotopic fractionation occurs during phase transitions. This means that the isotopic composition of water vapour thus provides an integrated perspective on the hydrological history of an air mass. Comparisons between these observations and GCM simulations with isotope tracers can be used to test how accurate key processes such as evaporation, condensation and air mixing are captured by climate model simulations4–6. Evaporation is the starting point of the atmospheric hydrological cycle. The processes at play during evaporation are the main focus, which this dataset of marine boundary layer water vapor isotopes is applicable to.
Currently, the available datasets of isotope measurements of the atmospheric water vapor over the ocean are very limited7–12. Most of the measurements of atmospheric vapor isotopes were collected using traditional methods, involving collection of vapor samples by cryogenic trapping methods. Thanks to development of commercial water vapor isotope spectroscopy analyzers, it is now possible to provide continuous in-situ measurements. We provide here a combined new dataset of water vapor isotope measurements over the ocean with both large spatial and temporal resolution.
This compilation of measurements covers a large part of the Atlantic Ocean, from 4° S to 63° N (see data distribution on Fig. 1). During five cruises, the atmospheric water vapor isotopic composition has been continuously measured with laser spectroscopy analyzers between 10 to 17 meters above the sea surface (Table 1). A weather station was installed on each vessel to continuously measure the standard meteorological variables (atmospheric sea level pressure, relative humidity, air temperature, wind speed and direction). In addition, during most cruises, near-surface ocean temperature measurements have been carried out at a depth between 3.5 and 1.5 m below the surface with a calibrated temperature probe (see Table 1).
The calibration of the raw Picarro data has been carefully performed against the international VSMOW-SLAP scale to obtain a homogeneous dataset for the five cruises, as described in the method section. All observations (Picarro and weather station measurements) have been averaged over 15 min and we also provide 6-hourly data for easy comparison with simulation outputs using isotope-enabled General Circulation Models. To facilitate interpretation of the dataset, we also provide relative humidity (RHS) normalized to sea surface temperature (SST) and backwards trajectories (120 h backwards) from the position of the measurements every 6 h using the HYSPLIT model13. Furthermore, we supply an averaged SST value, by using the OSTIA remote sensing product, over an area of 200 km by 200 km centred on the position of the ship.
We expect that this unique combined dataset for the Atlantic Ocean will contribute to:
We describe here the protocol for producing the presented data in the following order:
Standard meteorological variables
Atmospheric water vapour isotope measurements
Calculated backwards trajectories
Standard meteorological variables
Standard meteorological variables such as air temperature, relative humidity, wind speed, wind direction, and atmospheric sea level pressure were obtained from weather stations installed on the vessels. Furthermore, sea surface temperature (SST) has been continuously measured at a depth between 3.5 and 1.5 m below the surface with a calibrated temperature probe. The SST sensor placement was chosen to minimize the influence on the measurement from thermal heating caused by the research vessels. The heights and depths of sampling are presented in Table 1. The sensor names and their uncertainties are indicated in Table 2. The following subsections describe the measurement for each cruise.
The STRASSE cruise
A BATOS (French Met Office) weather station was installed at 18 m above the sea surface. The weather station was installed close to the centre of the ship, along the mast and above the bridge. The station consists of a contact protective housing (fan-aspired radiation shield) and was calibrated beforehand (for relative humidity, air temperature, wind, and pressure. During STRASSE, we also had at our disposal a dedicated instrumented mast near the bow (for turbulence measurements and also bulk measurements (Young Propeller 05106 anemometers and Vaisala HMP233 for humidity), which was used to check the consistency of the measurements. We found a discrepancy in the relative humidity, which we established with 10 measurements using a manual psychrometer. The applied correction is RHPsychro=0.9795×RHBatos−0.5263. The RH in the datafiles is the correct RHPsychro. The SST has been continuously measured by a calibrated temperature probe SBE35 at 3.50 m depth. The SST sensor has been calibrated before and after the cruise, with no indication of drift between successive calibrations larger than 0.01 °C. During the cruise, we have noticed occasional events of warming of less than 0.05 °C during stops at CTD cast stations (based on comparison with CTD cast data). We expect that the measurement of SST is accurate to within 0.05 °C.
The PIRATA FR24 cruise
A BATOS (French Met Office) weather station was installed at 12 m above the sea surface. The weather station was located portside above the bridge. The anemometer was installed above the weather station at a height of 18 m above the ocean surface. The BATOS weather station consists of contact protective housing (fan-aspired radiation shield) and has been calibrated beforehand (for relative humidity, air temperature, wind, and pressure. The SST has been continuously measured by a calibrated temperature probe SBE3S at 3.33 m depth. The SST sensors have been calibrated before and after the cruise, with no indication of drift between successive calibrations larger than 0.01 °C. We expect that the measurement of SST is accurate to within 0.05 °C.
The RARA cruise
A MetPak Pro weather station from Gill Instruments was installed at 4 m above the ocean surface. The weather station was located portside on the mizzenmast. The anemometer was installed above the weather station and the height of the wind measurement was 15 m. The Metpak Pro measurements are carried out in a fan-aspired radiation shield. The instrumentation consists of WindSonic ultrasonic wind speed and direction sensor, a highly accurate barometric pressure sensor, a Rotronic Hygroclip temperature/humidity probe, and a Pt100 probe for air temperature. During RARA AVIS cruise, the station was installed directly from the manufacturer and the conditions at sea on a sailing vessel precluded sophisticated calibration procedures. The near-surface seawater temperature has been continuously measured by a calibrated temperature probe SBE38 at 1.50 m depth. The temperature sensors have been calibrated before and after the cruise, with no indication of drift between successive calibrations larger than 0.01 °C. The measurement of SST is accurate to within 0.05 °C.
The ACTIV cruise
A DAVIS Vantage Pro 2 weather station was installed at 3 m above the sea surface. The weather station was located portside along the railing. The Davis measurements onboard ACTIV consists of a fan-aspirated radiation shield. The wind speed and direction could not be retrieved during the ACTIV cruise. We have instead used 6-hourly outputs from the ERA-interim reanalysis product26. No continuous SST measurements have been carried out during the ACTIV cruise. Instead we use estimates from the daily OSTIA product retrieved at the ship position27. However, no SST is reported close to the coast of Greenland for the period 15 July–5 September 2014, as they are not correctly estimated in the OSTIA products due to the size of the footprint. However, regular sampling of the sea surface temperature has been carried out throughout the campaign using a PT-100 thermistor submerged in ocean water immediately after sampling using a 10-litre bucket. These measurements are reported in the file SST_Activ_Bucket.txt. The good agreement (difference less than 0.1 °C) with the OSTIA estimations over the open ocean validated the measurement from the bucket, which can be used close to the coast of Greenland, where OSTIA estimations are not correct. In short, the measurement of surface water temperature is accurate to within 0.1 °C for the bucket measurement during the ACTIV cruise.
The BERMUDA cruise
A RM Young weather station was installed at 11 m above the sea surface, close to the centre of the ship, above the bridge. The anemometer was installed above the weather station and the height of the wind measurement was 15 m. The temperature and humidity sensors used for the BERMUDA system is obtained using a multi-plated radiation shield housing. The near-surface seawater temperature has been continuously measured by a calibrated temperature probe SBE3S (2 m depth). The measurement of surface water temperature is accurate to within 0.05 °C. We notice that the meteorological observations onboard the BERMUDA cruise are part of the permanent observational system on R/V Atlantic Explorer. The research vessel and operation is in compliance with the University National Oceanography Laboratory System.
The uncertainties on the meteorological data are given in Table 2 (factory values). It is possible that for some of the cruises, the accuracy is better, but we cannot guarantee it for all cruises. Notice that an observed constant difference between the Picarro measurements and the humidity measured by the weather stations for each cruise suggests that no significant change in the meteorological station measurements occured.
The meteorological station measurements can be influenced by the ship structure, both due to flow distortion, turbulent mixing, and heating/radiative influence from the ship itself. This is expected to contribute to the errors at least as much as the instrumental errors. Nevertheless, the comparison during the STRASSE cruise between the BATOS measurements, a dedicated mast near the prow and measurements 2-m above the sea surface suggested that the profile (of humidity, air temperature and wind) was consistent with the expected height of the BATOS measurements. Meteorological observations onboard R/V Atlantic Explorer were carried out both in starboard and portside, and the two sets of observations were not significantly different. Because RARA and ACTIV measurements were done on much smaller sailing vessels, it is expected that flow distortion is much less. However, during RARA and ACTIV, the presence of the sails nearby would certainly have modified the relative wind measurements. Nevertheless, we don’t notice major absolute wind changes when the RARA sailing vessel changed direction. No wind measurements are reported from ACTIV.
The larger issue is how to compare the measured seawater temperature with surface skin temperature. Tests done with COARE-Met flux algorithms suggest that the difference between measured temperature and the skin temperature is usually within 0.3 °C for those cruises due to near surface stratification and skin radiative cooling effects. Notice that there are however a few mid-day situations with very large near-surface stratification, when difference between the temperatures measured from the TSG and the radiative infrared temperature sensor that was installed for the STRASSE cruise was larger (caused by very weak winds during mid-day and early afternoon).
We have also calculated the relative humidity with respect to the sea surface temperature (RHS_10m) following equation 1.
With qair being the specific humidity at 10 m, estimated from the Picarro measurement assuming that profiles follow the logarithmic profiles expected from the Monin-Obukhov similitude theory in a constant stress layer, qsat(SST) the specific humidity at saturation for a temperature equal to SST. qsat is calculated for sea water at salinity 35, thus 2% lower than for freshwater28.
As for the ACTIV cruise, we also provide OSTIA measurements for the 4 other cruises (Resolution 1/20°). Then, to estimate horizontal heterogeneity of SST, we provide an average SST value over a square of 200 km by 200 km centred on the ship position (from OSTIA daily SST products).
Data collected by the Picarro laser spectrometer
Cavity-Ring-Down-Spectroscopy analyzers from Picarro Inc. were installed on each research vessel to measure the stable isotopic composition of the atmospheric water vapor and the specific humidity. The instrument versions of the different analyzers are presented in Table 1, as well as the main characteristic of the experimental setup. All the sampling inlets are located between 10 and 17 m above the sea surface. A protective inlet was installed at the beginning of the tube on all setups to prevent rain from being sucked into the tube and affecting the vapor measurements. The water isotopic composition is given in per mil following the definition by McKinney et al.29 and Craig30 whereas the humidity is reported in ppmv.
The STRASSE cruise. For the STRASSE cruise, the Picarro water vapor isotope instrument type was L2130i. The air is sampled from the atmosphere using ~10 m perfluolkoxy (PFA) tubing (outer diameter 13 mm, inner diameter 9 mm) with a 6 l/min airflow. The PFA tube was permanently heated to 40 °C or above to avoid condensation. The air has been sampled at ~17 m above the sea surface, just below the weather station BATOS.
The PIRATA FR24 cruise. For the PIRATA FR24 cruise, the Picarro water vapor isotope instrument type was L2130i. The air is sampled from the atmosphere using ~10 m perfluolkoxy (PFA) tubing (outer diameter 13 mm, inner diameter 9 mm) with a 6 l min−1 airflow. The PFA tube was permanently heated to 40 °C or above to avoid condensation. The air has been sampled at ~12 m above the sea surface, portside above the bridge, next to the weather station.
The RARA cruise. For the RARA cruise, the instrument type was L2130i. The air is sampled from the atmosphere using ~10 m perfluolkoxy (PFA) tubing (outer diameter 13 mm, inner diameter 9 mm) with a 6 l min−1 airflow. The air has been sampled at ~10 m above the sea surface from the fore mast. No heating was applied to the tube used on the RARA campaign. To check whether the lack of heating on the RARA cruise had any effect on the results we tested the setup at the beginning of the cruise by comparing the specific humidity measured by the Picarro analyzer with the measurements from the weather station, alternating periods of heating of the sampling tube with periods with no heating. In both situations we observe a consistent agreement with the humidity weather station measurements, indicating no condensation processes in the PFA tube. Moreover, at no time during the RARA cruise was the temperature in the tube below the dew point temperature.
The ACTIV cruise. For the ACTIV cruise, the instrument type was L1102i. The air is sampled using ~25 meter copper tubing (outer diameter ¼ inch) with a 6 l min−1 airflow. The copper tube was permanently heated to 40 °C or above to avoid condensation. The Picarro analyzer L1102 was situated in a PID temperature controlled enclosure. The air has been sampled at ~15 m above the sea surface, at the top of the mizzen mast.
The BERMUDA cruise. For the BERMUDA cruise, the instrument type was L2120i. The air is sampled using a ~20 meter stainless steel tube (outer diameter ¼ inch) with a 10 l/min airflow. Similar tube length (25 m) was used in the study of Steen-Larsen et al.16, in which the authors discussed the smoothing of the signal due do tubing length. No heating was applied to the tube used on the BERMUDA campaign, but an orifice was installed in the beginning of the tube to lower the pressure inside the tube and hence decrease the dew point temperature. The air has been sampled at ~11 m above the sea surface, along a mast located in front of the boat31.
Notes. It is not expected that sea spray affects the measurements as we did not find significant sea spray deposits on the tube and inlet at the end of the cruise. Moreover, conditions were never stormy enough to have major sea spray input during STRASSE, PIRATA FR24 and BERMUDA cruises. The good consistency between the humidity measured by the Picarro analyzer onboard and the humidity measured by the weather station suggests that no strong input of sea spray affected the measurement. Furthermore, if sea spray droplets were to be drawn into the inlet lines we would expect to see spikes in the humidity signal as the droplet evaporated. However, we cannot disregard the possibility that small sea spray droplets are drawn into the inlet and contribute to the water vapor measurements. If this were the case, we would expect that the measured isotopic composition to be more enriched than the ambient water vapor as the evaporation of sea spray would add vapor equivalent to the ocean isotopic composition.
Foam was placed underneath the instruments to dampen the vibrations and movements of the vessel on the Picarro instruments. No influence of the ship movements was observed during the STRASSE, PIRATA FR24, and BERMUDA cruise. However, since the RARA and ACTIV cruises took place on a sailing boat more significant vibration and movement was encountered. During those cruises, we observed that the cavity pressure fluctuated more during conditions with stong winds/high waves. Although it is difficult to precisely evaluate the effect of these variations on the isotopic measurement, we did not notice specific problems (e.g. changes in s.d. during calibration) during these periods of higher-pressure fluctuations. We furthermore notice that the cavity pressure variations are within the deviations approved by the Picarro manufacturer.
Finally, no influence of ambient room temperature variations on the water vapor isotope observations was observed during any of the cruises. The PID temperature-controlled enclosure, which housed the Picarro analyzer (model L1102i) during the ACTIV cruise minimized the temperature fluctuations to within 1 K. During the other cruises, the analyzers used (L2130i and L2120i) are much less sensitive to the temperature fluctuations, and did therefore not need a temperature regulated enclosure under these conditions.
The temporal resolution of the Picarro measurements depends on the instrument used. For the L1102i analyser the temporal resolution is about 20 s, while for the L2120/2130 analyser the temporal resolution is about 1 to 3 s depending on the instrument. We average these measurements for 15 min to obtain the high-temporal resolution dataset.
Calibration of the raw data
For the calibration of the raw data, we follow the protocol elaborated by Steen-Larsen et al.32 i. The first step is to correct the raw measurements of the concentration effect. ii. The second step is to convert the measurements to the international VSMOW-SLAP scale by using at least 2 different references of known isotopic composition. iii. Then, the measurements must be corrected for the instrumental drift by regularly injecting a reference standard to the analyzer.
As described in Steen-Larsen et al.32 it is necessary to perform a humidity-isotope response calibration of the analyzer, and correct the raw measurements. The principle is to introduce a reference with a constant isotopic composition into the instrument at different humidity levels. Multiple humidity-isotope response calibrations were carried out before, during, and/or after each cruise. To correct the raw data from the concentration effect, we chose 20,000 ppmv humidity level as a reference similar to other studies18,19,32,33. The results of the humidity-isotope calibrations are shown in Fig. 2.
Then, we reference the measurements against the International Atomic Energy Agency (IAEA) VSMOW-SLAP scale. We used at least 3 internal references bracketing the range of values encountered during the cruises. The values of the references used are reported in Table 3. The internal standards used to calibrate the water vapour isotope data have a typical uncertainty of (1 σ) of +/−0.03‰ for δ18O and 0.5‰ for δD. At least 2 calibration curves were established before or during each cruise to confirm the calibration in the VSMOW-SLAP scale. During each cruise, the slope of calibration curves did not evolve significantly during the period of the cruise.
Finally, we regularly measured a reference standard to correct the instrumental drift through time. The evolution of the instrumental drift for each cruise is presented in Fig. 3 and the main characteristics of the protocol are described in Table 4.
The Picarro un-calibrated humidity measurements (in ppmv) have been calibrated against the specific humidity measured by the local weather stations on each of the cruises (see Table 2 for overview on instrument and uncertainty). For the five cruises, very high (R>0.95) correlation is obtained between the calibration curve and the measurements (the correction formula are reported in the Table 5). We report the calibrated Picarro humidity data in the data files supplied (in g kg−1 dry air).
The STRASSE cruise. We used a Picarro autosampler and vaporizer with compressed dry air (50 ppmv). The humidity-isotope response calibrations were done in the middle and at the end of the cruise. No shift in the humidity-isotope calibration was observed during the cruise. The drift of the instrument was measured by injecting a liquid reference every 6 h during the first 2 weeks. Later on we reduced the frequency of the reference injections, as the system proved to be very stable.
The PIRATA cruise. We used a Picarro autosampler and vaporizer with compressed dry air (50 ppmv). The humidity-isotope response calibrations were done in the middle and at the end of the cruise. No shift in the humidity-isotope calibration was observed during the cruise. To evaluate the instrumental drift, the measurements of the reference standard were carried out every 12-hour.
The RARA cruise. We used a custom-made calibration system described previously by Steen-Larsen et al. and Gkinis et al.16,34. We used ambient air, which was dried using Drierite (less than 200 ppmv). For this cruise, we did 3 humidity-isotope response calibrations carried out after the cruise when the instrument was back in the LOCEAN laboratory in Paris. To evaluate the instrumental drift, the measurements of the reference standard were carried out every 24–48 h.
The ACTIV cruise. We used a custom-made calibration system described previously by Steen-Larsen et al. and Gkinis et al.16,34. We used ambient air, which was dried using Drierite (less than 200 ppmv). The humidity-isotope calibration for the instrument used during the ACTIV cruise was carried out five times during the cruise and the combined dataset was used to correct the complete dataset. No shift in the humidity-isotope calibration was observed during the cruise. To evaluate the instrumental drift, the measurements of the reference standard were carried out every 24 h.
The BERMUDA cruise. We used a custom-made calibration system described previously by Steen-Larsen et al.16. We used ambient air, which was dried using Drierite® (less than 200 ppmv). This cruise was calibrated using a humidity-isotope response calibration carried out a few days before the cruise. As documented in Steen-Larsen et al.15, this instrument has been stable over multiple years. This was also supported by a humidity-isotope calibration carried out several months after the cruise. Unfortunately for the Bermuda cruise our calibration system failed during the period at sea and we therefore rely on the stability and knowledge of the long-term variability before and after the cruise from June 2013 to August 2015 (Fig. 3e). Linear interpolation is used across the period where no calibration was performed and lower accuracy of the Bermuda measurements is anticipated.
Notes. Besides a single short-term event during the ACTIV cruise, the ambient humidity level is never below 4,000 ppmv for the five cruises and we assume that the influence of the residual water in the dry air (<200 ppmv) on the Picarro measurement is insignificant35. In the following, each step of the calibration is described.
A recent study comparing directly water vapor isotope observations from two independently calibrated spectroscopy analyzers from Picarro documented an uncertainty on 10-minute average data of 0.14‰, 0.85‰, and 1.1‰ for δ18O, δD, and d-excess respectively16. Except for the data collected during the BERMUDA cruise, we expect this uncertainty to be representative of the data presented here. For the data collected as part of the Bermuda cruise we expect the uncertainty to be larger due to issues with the calibration system. However, we still expect, based on the long-term stability of the analyzer used for the Bermuda cruise, the combined accuracy and precision for the d-excess to be better than 2‰. We note the risk of overfitting both the humidity-isotope response relationship and the instrumental drift if too few measurements are used compared to the measurement precision. It is therefore important to always assess if the fitted trend is significant or not.
Calculated backwards trajectories
Backwards trajectories have been calculated using the HYSPLIT—Hybrid Single Particle Lagrangian Integrated Trajectory Model (HYSPLIT OCTOBER 2014 release version) from the Air Resources Laboratory, NOAA13,36. Meteorological fields for the backwards trajectories have been obtained from NCEP’s Global Data Assimilation System 1-degree latitude-longitude resolution. Trajectories have been calculated backwards for 120 h from the 6-hour resolution position of the vessels. Trajectories were started 100 m above sea level. Elevation (m), air pressure (mb), air temperature (K), rainfall rate (mm/hour), marine boundary layer mixing depth (m), relative humidity (%), humidity mixing ratio (g/kg dry air), height of terrain (m), and solar insulation (W/m2) are given along the trajectory with a 1-hour resolution. Meteorological data along the back trajectory was obtained from the NCEP GDAS output.
The surface data are recorded in ascii-format in the .txt-file and in matlab-format in the .mat-file. The variables are described in the Table 7. For each cruise (each vessel), two different files are created: one with a 15-minutes time scale resolution (average over 15 min) and another one with a 6-hours time scale resolution (average over 45 min centred on time stamp). The average is calculated for a given time stamp, only if 80% of the data are available. The naming convention is as follows: CRUISENAME_15_min.txt (.mat) or CRUISENAME_6_hour.txt (.mat). The columns of the .txt files are separated by a comma.
The additional file SST_Activ_Bucket.txt records the discrete SST measured using the 10-litre bucket (No interpolation on a equal time step is carried out). The variables are: Day Month Year Hour Min SST Latitude Longitude.
Calculated backwards trajectories
The calculated backwards trajectories for each cruise (each vessel) are given in ascii-format in the .txt-file and in matlab-format in the .mat-file. The variables in the files are described in Table 8. The Matlab-format is the format of a structure array. The .txt-file is organized in blocks of 128 lines separated by 3 empty lines. The first 6 lines of each block give the starting time (year, month, day, hour UTC) and position (latitude and longitude). Line 7 of the block gives the header (see Table 8 for the description of the variables) of the output position and meteorological data along the individual trajectories. Each column is separated by a space.
All the internal water standards used have been calibrated against the IAEA water standards (VSMOW, SLAP). Notice, however, that the internal water standards used to calibrate the isotopic Picarro measurement to the VSMOW-SLAP scale were not always the same for the different cruises.
In the following, we present a brief description of the general weather conditions and discuss the general large-scale variability pattern of the surface conditions. The spatial variability of the main parameters discussed below is presented in Figs 4 and 5. The time series of the same parameters are presented in Supplementary Materials (Supplementary Figs S1).
This cruise took place in the eastern part of the subtropical North Atlantic gyre during the summer of 201218,19. It can be separated in to three main parts: 1) From the Canary Islands to 26°N ; 35°W (survey area), 2) the survey area (26° N ; 35° W), 3) from 26° N ; 35° W to Ponta Delgada (Azores). The atmospheric sea level pressure increased from the Canary Islands to the study area, which is close to the Azores High pressure system (HP). During the survey, the atmospheric pressure fluctuated around 1,020 hPa, a mean value indicating the proximity of the HP (its core value was often close to 1,025 hPa). The surface winds usually came from the East or North-East, as expected for a trade wind regime. A small event of convection occurred around September 1st, with a 5 mb atmospheric pressure drop, and a small rain event as well as some isolated cumulonimbus were observed from the ship. Closer to the Azores Islands on the return leg, the atmospheric pressure decreased and rainfall events occurred with varying wind regimes. The largest air temperature (28 °C) was observed at the end of leg 1 and during the survey, but air temperature was more commonly near 26 °C with a slight diurnal cycle of 0.5 °C. Close to the Canary and Azores Islands, air temperature was lower (23 °C near the Canary Islands and 19 °C in Ponta Delgada). Specific humidity during the whole cruise ranged from 11 to 18 g kg−1 and RHS from 56 to 85%. The isotopic composition in the water vapour decreased during the two days of shallow convection and close to the Azores Islands.
This cruise took place in the Gulf of Guinea from 9 April to 22 May 2014, with Picarro measurements during the 2nd leg from 1 to 20 May 2014. SST and Tair were generally higher than for the other cruises (27–30 °C) indicating warm surface conditions associated with the large solar fluxes close to the equator in late spring. A SST decrease around May 2 was associated with a weak equatorial upwelling event. The atmospheric sea level pressure did not change much during the cruise (from 1,008 to 1,014 hPa) as expected in the equatorial region. The mean value near 1,010 hPa is typical for this low-pressure region associated with the ascending branch of the Hadley cell. A period of deep convection occurred from May 3–7, close to the Intertropical Convergence Zone (ITCZ). At this time, the wind direction was variable, including some northerly winds at time. Another convection event was observed close to Abidjan (Ivory Coast) during the last day of the cruise. During these convection events, sudden air temperature decreases occurred. Except for these periods of convection, the region was dominated by a trade wind regime with winds coming mostly from the S-SE (135°–170°). During the whole cruise, specific humidity ranged between 15 and 20 g kg−1 and RHS between 60 and 83%. The most enriched water vapour isotope values were observed during periods dominated by the trade wind regime with limited atmospheric convection. The most depleted isotopic values were recorded during periods of strong convective activity when they dropped to −19‰ for δ18O and −140‰ for δD.
The RARA cruise is divided into two main legs.
Leg 1 was from Brittany (Brest) to Martinique Island in the Antilles region during late winter 2015. Air temperature and SST progressively increased during the cruise from 10.5 to 26 °C and from 11.5 to 26.5 °C. This increase corresponds to the climatological latitudinal winter meridional gradient from Brittany to Cape Verde and zonal gradient from Cape Verde to Martinique. In the first part of the cruise, the ship crosses some of the cold waters carried by the winter upwelling off North West Africa. Closer to the Antilles, it encountered warmer and fresher waters of the western Atlantic. No deep atmospheric convection event was observed during this leg with specific humidity ranging from 5.6 to 15 g.kg−1and RHS from 51 to 100%. The driest air conditions were observed at the departure from Brest (clear sky), followed by a period of wet conditions in the Bay of Biscay associated with mist/fog over the sea surface. South of the Canary Islands, the wind direction was mostly NE veering to E after the Cape Verde Islands, which is characteristic of trade winds. SST/Tair measured in February in the South-Eastern part of the subtropical gyre was nearly 3 °C lower than during the summer STRASSE cruise, as expected from the seasonal cycle. The isotopic composition of the atmospheric water vapour ranged from −15 to −10‰ for δ18O and for −110 to −70‰ for δD.
Leg 2 from Martinique to Brittany occurred in May and June 2015. The Picarro instrument was stopped during a week when the sailing boat was around the Azores Islands (by request of the ship’s master). The atmospheric sea level pressure increased from Martinique to the Azores Islands (except close to Bermuda, see discussion below), as the ship came closer to the center of the high-pressure system. At the Azores Islands, the highest pressure was 1,038 hPa. The temperature (air and sea surface) decreased during the crossing between the Antilles and towards Brittany, following the expected meridional gradient. Close to Bermuda, the ship encountered a strong convective event with atmospheric pressure dropping by 15 mb (on 12 May at 09 am, in the vicinity of 32.5°N and 64°W). The 15 min average wind speed reached 36 knots with sudden changes of directions. Estimated maximum wave height reached 8 m, and air temperature became much lower than SST (with the largest difference of 3.5 °C), suggesting unstable surface conditions.
The ACTIV cruise took place in the northern part of the North Atlantic between Scandinavia and Greenland throughout the summer of 2014. The cruise covers a large variability in atmospheric and oceanic conditions from the outer Baltic region to the fjords of south-east Greenland. This large variability also gave rise to a large span in d-excess values. Atmospheric specific humidity was most of the time lower than during the 4 other cruises and ranged from 1.3 to 10.3 g.kg−1. d-excess reached the highest value recorded by the 5 cruises (ranging from −6.3 to 25.7‰). The most depleted values of the isotopic composition, compared to the four other cruises has been observed during the voyage of ACTIV with values of −34.65‰ for δ18O and −255.49‰ for δD. During the cruise between Scandinavia and Greenland and for the return the large variability in water vapor isotope observations was governed by varying synoptic conditions. When the ship was near or in the fjords of south-east Greenland the varying water vapor isotope observations was governed by episodic katabatic winds coming off the Greenland Ice Sheet.
The Bermuda-cruise took place in the autumn of 2014 between Bermuda and Puerto Rico and back as part of the Bermuda Atlantic Time-series Study validation cruise. Besides shorter periods of convective activity giving rise to heavy rain and rough sea near Bermuda at the beginning and the end of the cruise, the water vapor isotope composition (δ18O and δ D) is characterized by being very stable with values above −12‰ in δ18O. However, significant variations in the d-excess are observed throughout the entire cruise ranging between ~10 and 25 ‰. In agreement with the climatology, the SST latitudinal variability is less pronounced in October compared to this one measured in May in the same region with the RARA cruise (Fig. 4e).
Isotopic measurement problems during the PIRATA FR24 cruise
Due to high winds, the inlet cap protecting the tube from sucking in rain drops fell off during period from May 04th at 04:50 am to May 07th at 03:30 pm. This meant that during heavy rain events drops were sucked into the inlet line where it evaporated and influenced the water vapor isotope measurements. For this period, we have removed the data during and immediately after each rain event. We identified this issue from the differences between the weather station humidity measurements and the Picarro humidity measurements (the difference was always less than 0.7 g kg−1).
How to cite this article: Benetti, M. et al. Stable isotopes in the atmospheric marine boundary layer water vapour over the Atlantic Ocean, 2012–2015. Sci. Data 4:160128 doi: 10.1038/sdata.2016.128 (2017).
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HCSL acknowledge support from AXA Research Fund, the Carlsberg Foundation, and the Danish Council for Independent Research–Natural Sciences grant number 10–092850. AKF acknowledges support from the Danish National Research Foundation. Fieldwork carried out onboard the ACTIV cruise was part of the X_Centuries project funded by the Danish Council for Independent Research (FNU) (grant number DFF-0602-02526B) and the Centre for GeoGenetics supported by the Danish National Research Foundation (DNRF94). The authors thank the captain and crew of the ACTIV cruise. Work during Strasse on R/V Thalassa and Pirata FR24 on R/V Suroit was supported by three LEFE/IMAGO grants (Strasse, Strasse/SPURS and PIRATA), with additional support for equipment from IPSL and from OSU Ecce Terra. The authors gratefully acknowledge the help of the association ‘Les Amis du Jeudi et du Dimanche’ for the installation of the scientific instrumentation on the RARA AVIS. The authors also thank the PIRATA program for providing free precious data sets to the whole scientific community. The authors thank the TOSCA-SMOS program which founding was used for installing the SBE45 onboard the RaRa Avis Vessel. The authors thank Floriane Desprez de Gézincourt (LOPS) for her help setting up the TSG on the RaRa Avis and for her contribution in analyzing salinity of the water samples. The authors also gratefully acknowledge the NOAA Air Resources Laboratory (ARL) for the provision of the HYSPLIT transport and dispersion model and/or READY website (http://www.ready.noaa.gov) used in this publication. ERA-Interim data provided by courtesy of ECMWF.
The authors declare no competing financial interests.
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Benetti, M., Steen-Larsen, H., Reverdin, G. et al. Stable isotopes in the atmospheric marine boundary layer water vapour over the Atlantic Ocean, 2012–2015. Sci Data 4, 160128 (2017). https://doi.org/10.1038/sdata.2016.128
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