## Introduction

Over the last 50 years, the global ocean has lost around 2% of the dissolved oxygen inventory1. Climate-model projections predict that the current deoxygenation trend will continue1,2, and even intensify over the next century3. The observed global-ocean deoxygenation trend over the past decades has been attributed to a combination of a warming-induced decline in oxygen due to a lower solubility1 (25% in the first 1000 m depth), and reduced ocean ventilation due to increased upper ocean stratification1,4,5. However, the uncertainties of those projections are still important because the regional and interannual-to-decadal variability of the ocean oxygen content are poorly documented4,6. This is particularly true in the main ventilation areas of subtropical and subpolar latitudes, which play a crucial role for the oxygen supply into the ocean interior, and for the present and the future ocean deoxygenation7,8.

In the North Atlantic Ocean (Fig. 1), the Labrador and Irminger seas are recognized as important regions for ocean ventilation and oxygen uptake9,10,11. There, the massive mixing between mixed-layer waters, nearly saturated in oxygen, and undersaturated subsurface waters take place during winter deep convection12,13. This process is responsible for the formation of the weakly stratified Labrador Sea Water (LSW), which conveys oxygenated waters into the deep ocean. Then, ocean circulation transports those oxygen-rich waters away from their sources across the entire Atlantic Basin14. For instance, in deep convection regions as the Irminger Sea, the oxygen concentration within the mixed layer is close to saturation12,13,15,16 (i.e. around 93%). Local mixing and consumption, as well as remote oxygen advection, can also modulate the local oxygen concentration, but the role of these mechanisms in setting the oxygen content in the Irminger Sea remains unclear.

In this context, the Irminger basin is of special interest since recent observations have suggested a return of deep convection there in the last years, with a potential impact on oxygen ventilation11,15,17,18. For instance, stronger convection was attributed to stronger westerly winds and intense heat loss from the ocean during the positive North Atlantic Oscillation (NAO) phase19. At interannual scale, the occurrence of intense wind stress events, the Greenland tip jets, also favors deep convection in the Irminger Sea15. In some of these studies, oxygen concentration has been used to investigate deep convection and ventilation processes at seasonal to interannual scales11,13,15,18,20,21,22. At decadal scale, the subpolar gyre is also subjected to strong variability. Cooling and freshening (warming and salinification) of the subpolar gyre has been associated with a gyre strengthening23 (weakening) . Cold and fresh conditions also play a role in the preconditioning of the water column for deep convection events through changes in circulation and stratification18,24.

In this study, we investigate the decadal variability of the dissolved oxygen of the LSW in the Irminger Sea and its driving processes over the period 1991–2018. The most updated Argo dataset, combined with the available hydrographic sections, provide us with a unique time series of physical variables and oxygen concentration to address this question. Particularly, we focus on: (i) describing the change in oxygen concentration in the Irminger Sea over the last three decades, and (ii) attributing the observed oxygen variability within the LSW layer in the Irminger Sea to the driving physical processes.

The article is organized as follows: “Results” section describes the variability of the dissolved oxygen concentration in the Irminger Sea with a focus on the LSW. Results are then discussed and conclusions drawn in the section “Discussion and conclusion”. “Methods” section describes the datasets and methods used in this study.

## Results

Over the whole sampling period, the LSW density varies between 27.7 and 27.8 kg m−3 (Fig. 2), and its mean properties are θ = 3.5 ± 0.1 C, S = 34.88 ± 0.02, and oxygen concentration of 292.9 ± 2.1 μmol kg−1 (Figs. 3 and 4). However, LSW properties exhibit strong interannual to decadal variability that allows to roughly distinguish three different periods: P1: 1991-1997, P2: 2002–2014, and P3: 2015–2018. These three periods are highlighted as in Fig. 2.

Between 1991 and 1997 (P1), the LSW is relatively cold (3.2 ± 0.02 C), fresh (34.86), and dense (σ0 ≈ 27.77 kg m−3). The weak stratification during this period results in a thick LSW layer (around 870 m) that extends down to 1500 m (Fig. 3). This thick LSW is characterized by high oxygen concentration (297.8 ± 3.10 μmol kg−1), and low apparent oxygen utilization (AOU; 25 ± 3 μmol kg−1) (Figs. 2b, c and 3b). During this period, the hydrographic properties and oxygen concentration showed little variability with no changes in AOU and oxygen at saturation $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$.

Over the period 2002–2014 (P2), the LSW was, on average, warmer (3.8 ± 0.22 C), saltier (34.90 ± 0.01), and lighter (27.74 ± 0.02 kg m−3) than during the previous period. The LSW layer was also thinner, more stratified (thickness < 500 m), and shallower, with maximum depth around 1000 m (Figs. 3 and 4). These changes in LSW properties are accompanied by a decrease in the oxygen concentration as compared to the previous P1 period (287.2 ± 3.8 μmol kg−1). During the first half of P2 (between 2002 and 2008), we observe a progressive decrease of both, $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$ and AOU, while the oxygen concentration slightly increases (Fig. 2). AOU increases again during the second half of P2 (2010–2014) while $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$ remains low and nearly constant.

Finally, from 2015 to 2018 (P3), the Argo data reveal an abrupt increase of oxygen concentration in the LSW of about 15 μmol kg−1 (from <280 μmol kg−1 in 2015 to around 295 μmol kg−1 in 2018, Figs. 2 and 4). The latter is accompanied by a dramatic shallowing of the 27.75 kg m−3 isopycnal of ≈800 m from 2016 to 2018 (Fig. 2). The LSW layer was slightly thinner (700 m) and shallower (maximum depth ≈ 1300 m) than in the 90’s (Fig. 3). During P3, the upper stratification in the Irminger Sea diminished in comparison with the previous P2 period, which is consistent with the observed increase of the LSW thickness (Figs. 2 and 4). The strong oxygenation of the LSW (289.6 ± 5.3 μmol  kg−1) is accompanied by a recovering of cold (3.6 ± 0.1 C), fresh (34.9) and dense (27.75 ± 0.01 kg m−3) properties comparable to those of the 90s (P1) (Fig. 3). Over the whole 1991–2018 period, the variance of the LSW oxygen concentration was 41.8 μmol2 kg−2, while that of the oxygen solubility and AOU were 7.0 μmol2 kg−2 and 30.6 μmol2 kg−2, respectively. Changes in solubility ($${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$) account for only about 17% of the total oxygen variability and cannot explain most of the decadal variability of the oxygen concentration in the LSW. In contrast, processes related to AOU changes account for about 73% of the O2 variability (Fig. 2c). This reveals that mixing, advection and consumption are important drivers of the observed oxygen variability.

During 1991–1997 (P1) and 2017–2018 (last years of P3), the oxygen concentration of the LSW is close to the 93% of $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$, i.e the typical saturation of fairly recently ventilated LSW (Fig. 2b). Over these periods, the estimated AOU is relatively low, and can mainly be attributed to convective mixing between young, oxygen-rich waters in the mixed layer, and less oxygenated waters below. In contrast, during the 2002–2014 period (P2), as well as in 2015–2016 (first years of P3), the observed oxygen concentration is lower than the 93% of $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$. Interestingly both, the solubility and AOU, diminish during the P2 period, which exhibits important variability. LSW is oldest at the beginning of the period while the LSW starts to get warmer. During P2, the decrease in AOU also coincides with a strong decrease in the LSW core density, from 27.78 in 2002 to 27.73 after 2004. Part of this might be due to the presence of two different types of LSW, i.e., the 1987–1994 LSW and the 2000–2003 LSW with the former being much older10. During this period, given the weak convection in the Irminger Sea, the presence of older water could be explained by a combination of an advection of LSW from the Labrador Sea and a slow drainage of the available LSW volume, rather than by local ventilation through winter convection. However, from 2002 to 2014 (P2), the interannual variability in the oxygen concentration of LSW as well as in its age (AOU) can be partly explained by convective events visible in 2008, 2009, and 2012 (Figs. 2 and 4) and reported in previous studies11,15,18,21,25.

As suggested by the important variability of the AOU over the sampling record, changes in the oxygen concentration of the LSW are strongly related to mixing and advection processes. The contribution of biological respiration, also possible although unlikely to have a major role in this region, is beyond the scope of the present study. Therefore, we investigated the temporal variability of three processes that could contribute to the observed changes in the oxygen concentration of the LSW: (i) the convection depth (given by the MLD), that accounts for the direct ventilation of the LSW during the boreal winter; (ii) the wind stress curl, that spins up/down the subpolar gyre, and influences temperature, salinity, stratification and advection26 (Fig. 5), and (iii) the mixed layer temperature that controls oxygen solubility. All three processes are linked to the NAO index (i.e. positive/negative NAO anomalies, Fig. 5a).

We first investigated the link between the changes in oxygen concentration and the change in the circulation at 1000 m depth (approximately the mean depth of the LSW) within the extended region of the Irminger Sea (see the dashed black rectangle in Fig. 1). We used the anomaly of the relative vorticity of the velocity field at 1000 m depth as a proxy of the intensity of the gyre (Fig. 5c, horizontal black lines). From 2002 to 2014 (P2), when oxygen concentration was low in the LSW, we observed that the circulation of the subpolar gyre at 1000 m depth is weaker. Then, during the transition to the periods of high oxygen concentration (P2 to P3), the circulation has intensified in about 1.2 × 10−7 s−1. Since we do not have Argo data available in P1, we complemented the gyre intensity by an other proxy: the Sea Level Anomaly (SLA). The variability of the SLA is consistently anticorrelated with the anomaly of the relative vorticity at 1000 m, suggesting a mostly barotropic gyre circulation. Between 2002 and 2014 (P2) when the gyre is less intense, the SLA is positive, and the opposite occurs during the period 2015–2018 (P3). Despite satellite data are only available from 1993, the SLA anomaly suggests that the slowdown of the subpolar gyre is likely to occur during the second half of the 90s, when the SLA anomaly transitions from negative to positive. The intensity of the subpolar gyre near 1000 m depth is in general agreement with the enhancement of the winter Wind Stress Curl (WSC) in the Irminger Sea (Fig. 5a). We observe that the strength of the gyre is significantly anti-correlated (at 95% confidence level), with a 2 year-lag, with the annual WSC (r = − 0.5, WSC leading). During P1 and P3, the NAO and WSC anomalies are mainly positive, with respective maxima in 2015 (Fig. 5a), while there were negative between 2002 and 2014 (P2). This is associated with a change in the hydrographic properties and stratification of the upper water column: during P1 and P3 (P2), the upper layer is cold (warm) and the stratification is low (high), and the oxygen concentration in the LSW is high (low).

The variability of the circulation of the subpolar gyre as well as the WSC are also well correlated with the temperature and depth of the mixed layer (i.e. convection depth, (Fig. 5b)). During the period 2015–2017 the Mixed Layer Depth (MLD) reached its maximum depth (between 1000 and 2000 m) and minimum temperature (MLT < 4.5 C)), which evidences the occurrence of strong winter convection in the Irminger Sea (Fig. 5b). During this period, the winter MLD is deep enough to reach and ventilate the LSW layer and increase the local injection of oxygen (Fig. 2). In turn, in 2018, the last year of P3, we observe a weak convection and warmer mixed layer, which is in agreement with weak North Atlantic Oscillation (NAO), SLA and WSC anomalies. Shallower and warmer MLD associated to negative NAO and WSC anomalies were also observed during the 2002–2014 period. This shift in the atmospheric forcing during P2 is in agreement with the slowdown of the subpolar gyre in the Irminger basin (Fig. 5c), with the presence of a warmer and more stratified surface layer, and with shallower convection.

Due to the lack of Argo data before 2002, we cannot compute the seasonal mixed layer depth and properties before this year. However, the variability of the NAO can be linked to the observed characteristics of the LSW in the 90s. As during the 2015–2018 and 1990–1997 periods, the NAO and WSC anomalies are positive and relatively strong.

## Discussion and conclusion

In this study, an oxygen dataset covering almost three decades between 1991 and 2018 has revealed strong interannual to decadal variability in the oxygen concentration within the LSW layer. High oxygen concentration (≈300 μmol  kg−1) is observed in the LSW between 1991 and 1997 (P1). After a 5-year data gap, from 2002 to 2014 (P2), LSW became lighter, warmer and less oxygenated (≈280 μmol kg−1), but from 2015 to 2018 (P3) the characteristics of LSW recovered to those observed in the 90s decade. Interestingly, the available record appears to resolve one cycle of the subpolar gyre in Irminger Sea in which the oxygen and hydrographic conditions of the 90s are mostly recovered at the end of the period.

The analyses carried out here shed new light on the relative contribution of the changes in solubility and the processes related to changes in AOU to the observed variability of the oxygen concentration in the LSW layer. We found that the variations in $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$ account only for 17% of the total oxygen variability over the 28-years period, while most of it was related with changes in AOU (73%). However, the relative contribution of both terms, as well as the processes explaining the changes in AOU, vary over interannual to decadal scales depending on the dynamical features in the Irminger Sea. During the periods of intense convection in the 90’s (P1), when the subpolar gyre was cold and the mixed layer was deep, the oxygen concentration is close to 93% of $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$. This percentage has been reported as the average value of the maximum oxygen saturation that can be reached in the mixed layer under deep convection episodes in the Labrador Sea12,13,15. Thus, the smaller AOU estimated during this period can be attributed to strong ventilation and oxygen uptake.

During the 2002–2014 period, when $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$ was lower, convection was generally weak, and the observed undersaturation cannot be mainly attributed to vertical mixing13. Thus, the higher AOU within the LSW layer likely resulted from a combination between (little) vertical mixing, biological consumption, and, mainly, changes in lateral advection that may have increased the water age. Nevertheless, during this period, the AOU exhibits important interannual variability. Peaks of low AOU coincide with high oxygen concentration that can be explained by larger deep convection events that took place during the warm phase of the subpolar gyre11,15,18.

In contrast, during the P3 period (2015–2018), AOU progressively diminishes, and the observed oxygen concentration only approaches 93% of $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$ in 2017–2018. The relatively high values of AOU during the deepest convection years (2015 and 2016) could be attributed to the continuous entrainment of undersaturated waters from the less oxygenated and deeper LSW as the mixed layer deepens until its deepest level in 2016. After 2016, the convection get shallower, so the entrained waters that have been ventilated the previous winter are more oxygenated, and the mixed layer waters re-saturate quicker13. Thus, AOU progressively decreases, and the oxygen concentration approaches again the 93% of $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$.

To the best of our knowledge, our results allowed us, for the first time, to attribute the observed change in oxygen concentration of the LSW layer in the Irminger Sea to different processes that took place in the North Atlantic. These processes are tied to the natural interannual-to-multidecadal variability of the subpolar gyre that has been reported in previous studies. Indeed, the atmospheric forcing and the oxygen content are connected in different ways: (i) positive NAO index implies increased heat loss, stronger winds, stronger WSC, and enhanced winter convection in the Irminger Sea18, (ii) stronger WSC contributes to an intensification of the subpolar gyre, and (iii) the previous points (i) and (ii) are associated with less stratified and cooler surface waters23. Under these conditions, from 2015 and during successive winters until 2018, strong convection events associated with cold and deep mixed layers explained the deeper ventilation, a progressive reduction in the water age (AOU), thus an increase of the oxygen concentration in the LSW.

During the 90s, winter MLD data are not available, but the intensity of the NAO and the WSC, as well as the thick and deep characteristics of the LSW, are similar to those between 2015 and 2018. Therefore, we hypothesize that similar processes are responsible for the high oxygen concentration of the LSW in both periods. In between, negative NAO and WSC have favored weaker, warmer and more stratified gyre, thus shallower ventilation and lower oxygen concentration.

During the beginning and the end of the time series (P1 and P3), part of the newly ventilated LSW formed in the Labrador Sea could be advected into the Irminger Sea, partly contributing to its high oxygen concentration. However, during deep convection events, the remote LSW is likely re-ventilated and re-saturated, which complicates the quantitative assessment of the role of advection in the observed oxygen variability in the Irminger sea. More resolved current data or model study would be necessary to separate the local and advected LSW and understand the effects on oxygen variability. In this context, one blind spot of our study is the role of biological consumption in the ventilated region. The role of biological activity on the North Atlantic subpolar gyre is complex and not fully understood, especially during winter27. In this highly dynamic region, where the physical drivers of the ventilation are dominant, we have not disentangled the contribution of biological consumption that modulates the AOU over the studied period. This question could be addressed with sustained observation of full BGC parameters in the context of Biogeochemical Argo mission28. Although this study demonstrates the value of combining the sustained Argo and hydrological oxygen sampling in the North Atlantic, longer OneArgo sampling, especially for full BGC parameters, combined with improved model studies could help address those questions. Last, it would be interesting to study the oxygen variability in the deeper water masses, i.e., in the Iceland Scotland Overflow Water (ISOW) and Denmark Straight Overflow Water (DSOW), and in relation with the LSW oxygen variability. Note that Argo profiles only reach 2000 m depth and, therefore, do not resolve the full water column, notably the ISOW (classically defined between the 27.8 and 27.85 kg m−3 and found below 2000 m29), and the DSOW (potential density higher than 27.88 kg m−330). Therefore, more deep Argo floats with oxygen sensor would be necessary to fully resolve the ISOW and DSOW layers.

Over the time period 1991–2018, we did not observe any significant linear trend of the oxygen content either within the LSW, or over the entire water column. The natural oxygen variability in the LSW linked to that of the subpolar gyre, together with the relative short record that we have available (28 years) makes it difficult to determine whether anthropogenic-induced changes in the oxygenation of the LSW have occurred31. The North Atlantic is one of the regions of the world where no significant warming32,33,34 or deoxygenation trends1,4 are observed, and it is rather dominated by the natural decadal variability. However, in a warming ocean, the surface heating, glacier melt, and increased precipitation at high latitudes will likely increase the ocean stratification4,35,36. This is thought to lead to a reduced ventilation of the interior ocean and the AMOC strength37. In the North Atlantic Ocean, the role of these long-term players on the ocean oxygen ventilation are still to be elucidated.

## Methods

### Argo data and products

The data from the observational Argo array38,39 were downloaded from the ftp server of the French Global Data Assembly Center Coriolis40. We selected the profiles containing oxygen, temperature, and practical salinity data available in delayed mode and we used only those with Quality Control (QC) flag set to 1 and 2 (i.e., ’good’ and ’probably good’ data, see reference Table 2 in the Argo report41. Argo floats typically sample down to 2000 m. We have then extracted the profiles located in the core of the Irminger Sea region, which was defined by the area within the bathymetric contour of 2700 m (Fig. 1). Within the core of the Irminger Sea, a collection of 581 profiles from 27 Argo floats was obtained between 2010 and 2018. All the properties, i.e., potential temperature (θ), practical salinity, dissolved oxygen, and potential density anomaly (σ0) were monthly averaged within this area. We ensured that neither temporal and spatial biases were found in the yearly nor in the monthly distribution of the profiles (Figs. S1 and S2). The spatial variability of the LSW oxygen concentration within this Irminger Sea region is accounted for in our computations of the uncertainty of the Irminger basin averages of hydrological and oxygen parameters.

In addition, we used two Argo-based products: the ANDRO product42 and the In Situ Analysis System (ISAS) product43. ANDRO is a quality-controlled subsurface displacement dataset for the global ocean from all Argo floats from January 2010 (with more than 1.2 million deep displacements). Every cycle, the Argo floats dive to the parking depth, typically 1000  m, where they drift during about 9-days before descending to 2000 m and then rising to the sea surface while performing all the measurements. The deep displacement of Argo floats at this parking depth is used to map the ocean circulation at 1000 m depth and its variability. We then computed the relative vorticity from the meridional and zonal velocity ($$\zeta =\frac{dv}{dx}-\frac{du}{dy}$$), and averaged it over consecutive and overlapping 4-year periods. Last, the anomaly of the relative vorticity is computed by removing the mean value.

ISAS is a 3D gridded product derived from monthly optimal interpolation of temperature and salinity data from 2002 to 202043. ISAS was used to compute the mixed layer depth (MLD) and temperature (MLT) between 2010 and 2018 as well as for obtaining the mean oxygen concentration at 1000  m shown in Fig. 1.

MLD was computed by using a criterion based on a density difference between the surface and the base of the mixed layer44 of Δσ0 = 0.03 kg m−3. The criteria to compute the MLD on individual in situ profiles in the North Atlantic subpolar gyre15 is usually Δσ0 = 0.01 kg m−3. However, ISAS is a gridded product that tends to smooth the profiles. Thus, using ISAS with a smaller density criterion may underestimate the depth of the mixed layer. MLT was averaged over the winter each year (January to March). Then winter MLT and MLD were spatially averaged in the defined area within the core of the Irminger Sea (Fig. 1).

### Hydrographic sections

Along with Argo data, we obtained potential temperature, practical salinity and dissolved oxygen data from 15 ship-based hydrographic sections in the Irminger Sea: nine OVIDE (Observatoire de la variabilité interannuelle et décennale en Atlantique Nord45) sections that were performed every two years from 2002 to 2018, four AR07E (Atlantic Repeat Hydrography Line 7 East) sections (two in 1991, one in 1992, and one in 1997), and two A01E (Atlantic Repeat Hydrography Line 1) sections (1991 and 1994). These cruises were conducted at approximately the same time of the year (from June to September, except for two: the AR07E section in 1991 which was conducted in April, and the A01E section in 1994, in November). All the OVIDE, AR07E, and A01E cruises were performed along the same section between 45 W and 30 W in the Irminger Sea (Fig. 1). We thus interpolated all these sections along a regular longitudinal axis. For the OVIDE data, the accuracy of the temperature, salinity, pressure and oxygen measurements46,47 are better than 0.002 C, 0.002, 1 dbar and 3 μmol kg−1, respectively.

The combined use of the hydrographic cruises and Argo data allowed us to extend the Argo time series back in time and in depth until 3000 m, and it reinforces the robustness of our results. Furthermore, thanks to high temporal resolution of Argo data, we have corroborated that the oxygen concentration along the hydrographic sections is representative of the decadal variability of oxygen concentration and was not biased by the seasonal cycle (cruises take place generally during summer) or interannual events within the Irminger Sea region. When averaging the Argo oxygen profiles within the Irminger Sea and over the period when the hydrographic sections are performed, the data agree within 5 μmol kg−1, which lays within the hydrographic and Argo data uncertainties48. All available profiles were interpolated onto a regular depth axis going from the surface down to 2000 m for the Argo data and down to 3000 m for the hydrographic data, with a 5 m resolution.

### Wind data and NAO index

Wind speed and wind-stress were obtained from the NCEP reanalysis49. The fields were available every 6 h from 1990 to 2018 at a horizontal resolution of 2 in longitude and latitude. The Wind Stress Curl (WSC) was computed using the meridional and zonal wind stress component and 6-hourly outputs of the surface wind stress have been used for the computation (WSC $$=\frac{d{\tau }_{y}}{dx}-\frac{d{\tau }_{x}}{dy}$$ in N m−3). In addition, we obtained the NAO index from the UCAR Climate Data Guide website50. The NAO index is based on the surface sea-level pressure difference between the Subtropical High (Azores) and the Subpolar Low (Iceland). The NAO is the dominant mode of atmospheric variability in the North Atlantic ocean, a positive NAO index is expected to favor the occurrence of deep convection in the North Atlantic subpolar gyre because of stronger wind and colder waters than during negative phase of NAO26. Data were available from 1990 to 2018. The winter WSC anomalies were computed relative to the mean value of the 1990–2018 period and averaging the values from January to March. The winter anomalies of the NAO were computed by removing its seasonal cycle and then averaging the values from January to March.

### Sea level anomalies

To estimate the strength of the subpolar gyre and in addition to the ANDRO dataset that provided the velocity field at 1000 m depth, we used the detrended annual-mean sea-level anomaly (SLA) within the subpolar gyre obtained from Satellite Altimetry (Aviso multi-sensor altimetry data23).

### Oxygen solubility and AOU computation

To get more insight on the processes behind the oxygen variability, we computed the oxygen concentration at 100% saturation ($${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$) and the Apparent Oxygen Utilization ($${{{{{{{\rm{AOU}}}}}}}}={{{{{{{{\rm{O}}}}}}}}}_{2}^{sat}-{{{{{{{{\rm{O}}}}}}}}}_{2}$$). $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$, represents the oxygen concentration that a water mass with given temperature and salinity can reach when in equilibrium with the atmosphere. It is computed following Weiss (1970)’s formulation of oxygen solubility and depends mainly on temperature and only slightly on salinity. Previous studies have estimated the oxygen undersaturation in the mixed layer during deep convection periods in the North Atlantic (Irminger and Labrador seas) to vary between 3% and 10%, with an average estimated value of around 7%12,13,15,16. Therefore, to help in the interpretation of the drivers of oxygen variability we have computed the 93% of $${{{{{{{{\rm{O}}}}}}}}}_{2}^{{{{{{{{\rm{sat}}}}}}}}}$$ for comparative purposes (Fig. 2).

AOU can be considered as a proxy of the water-mass age and it represents the combined effect of oxygen consumption from the remineralization of organic matter, and vertical and horizontal mixing between waters with different oxygen concentration6. High AOU values are usually found in waters with remote origin that have undergone mixing with lower oxygenated water and/or biological consumption along their path to the sampling location. Low AOU values are found in waters that are newly ventilated without much mixing or biological history. Therefore, AOU can provide complementary information on the role of the circulation and its changes on the oxygen content that cannot be revealed from measurements of physical properties, such as temperature and salinity51.

### Definition of the LSW

The LSW plays a key role for climate by transferring surface water properties and tracers of atmospheric origin into the ocean interior. Therefore, the LSW layer is the focus of this study. It is formed by intense winter buoyancy loss and mixing during winter convection either locally in the Irminger Sea, or in the Labrador Sea from where it is advected15,17. The LSW is characterized by a weakly stratified core (low potential vorticity52) and high oxygen concentration. It also exhibits a minimum in salinity within the water column.

The LSW is usually defined as the water mass laying between the 27.7 and 27.8 kg m−3 isopycnals17,53. However, it has been shown that the LSW density varies over time10,31 and, therefore, its definition by fixed isopycnals can be misleading. We performed a density layer analysis within the Irminger Sea to define the LSW layer accurately (Fig. 6), and based on previous studies10,31,54. The reader is referred to the aforementioned studies for more details about the methods used to define the LSW layer. In particular in our study, we computed the thickness of potential density σ0 layers from top to bottom, and the LSW layer was defined within the densities that fall within the 73% of the maximum σ0 layer. The maximum isopycnal layer thickness of LSW over the sampling period ranged between 380 and 500 m (Fig. 3).