Journal topic
Earth Syst. Dynam., 11, 77–96, 2020
https://doi.org/10.5194/esd-11-77-2020
Earth Syst. Dynam., 11, 77–96, 2020
https://doi.org/10.5194/esd-11-77-2020

Research article 10 Feb 2020

Research article | 10 Feb 2020

Synthesis and evaluation of historical meridional heat transport from midlatitudes towards the Arctic

Synthesis and evaluation of historical meridional heat transport from midlatitudes towards the Arctic
Yang Liu1,2, Jisk Attema1, Ben Moat3, and Wilco Hazeleger1,2,4 Yang Liu et al.
• 1Netherlands eScience Center, 1098 XG, Amsterdam, the Netherlands
• 2Wageningen University, 6708 PB, Wageningen, the Netherlands
• 3National Oceanography Center, SO14 3ZH, Southampton, UK
• 4Faculty of Geoscience, Utrecht University, 3512 JE, Utrecht, the Netherlands

Correspondence: Yang Liu (y.liu@esciencecenter.nl)

Abstract

Meridional energy transport (MET), both in the atmosphere (AMET) and ocean (OMET), has significant impact on the climate in the Arctic. In this study, we quantify AMET and OMET at subpolar latitudes from six reanalysis data sets. We investigate the differences between the data sets and we check the coherence between MET and the Arctic climate variability at interannual timescales. The results indicate that, although the mean transport in all data sets agrees well, the spatial distributions and temporal variations of AMET and OMET differ substantially among the reanalysis data sets. For the ocean, only after 2007, the low-frequency signals in all reanalysis products agree well. A further comparison with observed heat transport at 26.5 N and the subpolar Atlantic, and a high-resolution ocean model hindcast confirms that the OMET estimated from the reanalysis data sets are consistent with the observations. For the atmosphere, the differences between ERA-Interim and the Japanese 55-year Reanalysis (JRA-55) are small, while the Modern-Era Retrospective analysis for Research and Applications version 2 (MERRA-2) differs from them. An extended analysis of linkages between Arctic climate variability and AMET shows that atmospheric reanalyses differ substantially from each other. Among the chosen atmospheric products, ERA-Interim and JRA-55 results are most consistent with those from coupled climate models. For the ocean, the Ocean Reanalysis System 4 (ORAS4) and Simple Ocean Data Assimilation version 3 (SODA3) agree well on the relation between OMET and sea ice concentration (SIC), while the GLobal Ocean reanalyses and Simulations version 3 (GLORYS2V3) deviates from those data sets. The regressions of multiple fields in the Arctic on both AMET and OMET suggest that the Arctic climate is sensitive to changes of meridional energy transport at subpolar latitudes in winter. Given the good agreement on the diagnostics among assessed reanalysis products, our study suggests that the reanalysis products are useful for the evaluation of energy transport. However, assessments of products with the AMET and OMET estimated from reanalysis data sets beyond interannual timescales should be conducted with great care and the robustness of results should be evaluated through intercomparison, especially when studying variability and interactions between the Arctic and midlatitudes.

1 Introduction

Poleward meridional energy transport, both in the atmosphere (AMET) and ocean (OMET), is one of the most fundamental aspects of the climate system. It is closely linked to the changes of weather and climate at different latitudes. The quantifications of AMET and OMET have been studied extensively. In the 1980s, many efforts were made to reproduce the AMET and OMET with very limited observational data available . After entering the satellite era, much progress has been made in particular during the recent two data-rich decades. Using the radiation at the top of the atmosphere from satellite data and the reanalysis data, a complete picture of AMET and OMET is given by . Following their work, rapid progress was made using similar methodologies and new data sets of observations . Nevertheless, these estimations still suffered from problems like mass imbalance, unrealistic moisture budget, coarse resolution and sparseness of observations . Fortunately, recent improvements in numerical weather prediction and ocean models, and increased data coverage of observations provide a basis to improve the estimation of AMET and OMET. As a result of an increase of available reanalysis products, an increase in resolution and length of the covered time span and an increase of components of the Earth system that are included in the products , it is very promising to have better quantification of AMET and OMET using the latest reanalysis data sets. In this study, we will provide further insights into MET from midlatitudes towards the Arctic, with the state-of-the-art reanalysis products.

To support the examination of MET from midlatitudes towards the Arctic, it is worth investigating the AMET and OMET in relation to climate variability at different timescales in the Arctic region. In recent decades, the Arctic has been warming twice as fast as the global average . This phenomenon is known as Arctic amplification (AA) and it has an impact far beyond the Arctic . In order to understand the warming, the processes behind the AA and its wider consequences, and to make reliable predictions of the Arctic climate, it is crucial to understand Arctic climate variability. Among all factors responsible for the variability in the processes described above, meridional energy transport, from midlatitudes toward the Arctic, plays a significant role . There is a large volume of published studies describing the impacts of AMET and OMET on the variation of sea ice and the warming in the Arctic. Using reanalysis data, showed that poleward AMET is linked with the evolution of temperature in the free troposphere at decadal timescales. By separating the planetary and synoptic-scale waves, showed that latent heat transport, as a component of AMET, influences the Arctic warming with reanalysis data. studied moisture transport with reanalysis data and observations, and showed that the moisture sources in the Arctic region are linked with interannual fluctuations of Arctic sea ice. analyzed the linkages between OMET, ocean heat content (OHC) and AA through climate model simulations within the Coupled Model Intercomparison Project phase 5 (CMIP5). They reported an enhancement of OMET as a result of heat loss in the subpolar ocean and the contribution of OMET to the AA through increasing OHC in the Arctic Ocean. Also by analyzing CMIP5 simulations, showed a large impact of heat transport in the Barents Sea on sea ice loss. However, ocean reanalyses do not show a clear sign of AA in the Arctic OHC increases . Consequently, knowledge on poleward AMET and OMET at subpolar and polar latitudes will aid in the understanding of AA.

Global climate models show compensations between variations in atmospheric and oceanic heat transport at subpolar latitudes and midlatitudes . This is indicative of positive feedbacks between the ocean and atmosphere, and it has been associated with variations in sea ice by some studies . These studies all point to connection between energy transport and variations of the Arctic climate. However, these results are mostly based on numerical model simulations and they tend to differ among these models. In contrast to numerical modeling studies, here we intend to examine AMET and OMET variability and their relation with the Arctic using reanalysis data sets, which are regarded as the best estimates of the historical variability.

In this paper, we quantify AMET and OMET using multiple state-of-the-art reanalysis products. These are representations of the historical state of the atmosphere and ocean optimally combining available observations and numerical simulations using data assimilation techniques. Emphasis is placed on the variation of AMET and OMET from midlatitudes to the Arctic at interannual timescales (∼5 years). Different from earlier studies, we include multiple reanalysis data sets for intercomparison. Independent observations in the Atlantic from the Rapid Climate Change-Meridional Overturning Circulation and Heatflux array (RAPID array) and the Overturning in the Subpolar North Atlantic Program (OSNAP) are included in the comparison. The RAPID array is a trans-basin observing array along 26.5 N in the Atlantic . It has been in operation since 2004 and provides the volume and heat transport in the Atlantic basin. OSNAP is an ocean observation program designed to provide a continuous record of the trans-basin fluxes of heat, mass and freshwater in the subpolar North Atlantic . Moreover, a state-of-the-art NEMO-LIM2 1∕12 ocean circulation/sea ice model simulation forced by the Drakkar surface forcing data set version 5.2 is also employed in the comparison. Based on the intercomparison of reanalysis data, especially with the independent observation data, we will be able to identify the sources of uncertainty. To support our comparison of AMET and OMET, we also investigate the interactions between oceanic and atmospheric variations and remote responses. The correlations between the variability of AMET and OMET, and the changes in the Arctic climate are compared to literature. This is motivated by previous studies that explain those connections with only numerical models or a single reanalysis data set .

The paper is organized as follows: Sect. 2 presents the data and our methodology. Results and analysis are given in Sect. 3. It includes AMET and OMET calculated from reanalysis data and an intercomparison of them. The correlation between the variability of AMET and OMET, and the Arctic climate is elaborated upon in detail. Finally, remarks are given in Sect. 4 and conclusions are provided in Sect. 5.

2 Data and methodology

The reanalysis data sets used in this study are introduced in this section. Moreover, the methodology for the quantification of AMET and OMET is also included in this section. The statistical tests performed in this study are elucidated in detail.

2.1 Reanalyses

In order to make use of observations and advanced numerical models, six state-of-the-art reanalysis data sets are used in this study. The chosen reanalysis products have a high temporal and spatial resolution; thus, they are suitable for the computation of energy transport (see Sect. 2.3). We chose three atmosphere reanalysis data sets: ERA-Interim, the Modern-Era Retrospective analysis for Research and Applications version 2 (MERRA-2) and the Japanese 55-year Reanalysis (JRA-55) (references below), and three ocean reanalysis data sets: the Ocean Reanalysis System 4 (ORAS4), GLobal Ocean reanalyses and Simulations version 3 (GLORYS2V3) and Simple Ocean Data Assimilation version 3 (SODA3) (references below). To avoid interpolation errors and imbalances in the mass budget introduced by regridding, the calculations are based on data from the original model grid. Note that the latest atmospheric reanalysis (ERA5) from the European Centre for Medium Range Weather Forecasts (ECMWF) is not included here since the model-level data have not been opened to the public yet (ECMWF2017). In addition, the computation is too expensive to achieve a longer time series for the study of the interannual variability of AMET using ERA5. As a synthesis, Table 1 shows the basic specifications of the reanalysis products contained in this study.

Table 1Basic specification of reanalyses products included in this study.

2.1.1 ERA-Interim

ERA-Interim is a global reanalysis data set produced by ECMWF , which has covered the data-rich period since 1979. It employs cycle 31r2 of ECMWF's Integrated Forecast System (IFS) and generates atmospheric state estimates using a 4D-Var data assimilation with a T255 (∼79 km) horizontal resolution on 60 vertical levels . Compared with its predecessor, ERA-40 , ERA-Interim is superior in quality in terms of the atmospheric properties like mass, moisture and energy . The improvement in observations and the ability of 4D-Var contributes a lot to the quality of the divergent wind , which is significant for the mass budget and hence the energy budget. We use the data that are provided on a 256×512 Gaussian grid, with a 0.75× 0.75 horizontal resolution and 60 vertical hybrid model levels. We take 6-hourly data with a range from 1979 to 2016.

2.1.2 MERRA-2

MERRA-2 is the successor of MERRA from the Global Modeling and Assimilation Office (GMAO) of the National Aeronautics and Space Administration (NASA). It assimilates observational data with the Goddard Earth Observing System (GEOS) model and analysis scheme . The atmospheric state estimates are produced by a 3D-Var incremental analysis update (IAU) assimilation scheme and have coverage from 1980 to the present. Unlike most of the reanalysis products, the GEOS atmospheric model includes a finite-volume dynamical core that uses a cubed-sphere horizontal discretization . The model grid has a resolution of 0.5× 0.625 with 72 hybrid levels. For this study, we use the 3-hourly assimilation data on the native model grid from 1980 to 2016.

2.1.3 JRA-55

Extending back to 1958, JRA-55 is the second reanalysis product made by the Japan Meteorological Agency (JMA) . JRA-55 applies 4D-Var assimilation and it is generated on TL319 horizontal resolution with 60 hybrid levels. Before entering the satellite era in 1979, the assimilated upper air observations mainly come from radiosonde data. In this project, we take 6-hourly data from 1979 to 2015 on the original model grid, which has a horizontal resolution of 0.5625× 0.5625 with 60 hybrid model levels.

2.1.4 ORAS4

Serving as the historical reconstruction of the ocean's climate, ORAS4 is the replacement of its predecessor used by the ECMWF, the reanalyses system ORAS3 . It implements the Nucleus for European Modelling of the Ocean (NEMO) as the ocean model and uses NEMOVAR as the data assimilation system . The model is forced by atmosphere-derived daily surface fluxes, from ERA-40 from 1957 to 1989 and ERA-Interim from 1989 to 2010. Since 2010, the forcing has changed to operational forcing . ORAS4 produces analyses with a 3D-Var first guess at appropriate time (FGAT) assimilation scheme and spans from 1958 to the present. ORAS4 runs on the ORCA1 grid, which is associated with a horizontal resolution of 1 in the extratropics and a refined meridional resolution up to 0.3 in the tropics. It has 42 vertical levels, 18 of which are located in the upper 200 m. Here, we skip the first two decades and use the monthly data from 1979 to 2014 to avoid the uncertainties reported by . We use the monthly mean fields on the native model grid.

2.1.5 GLORYS2V3

GLORYS2V3 is a global ocean and sea ice eddy-permitting reanalysis system that yielded from the collaboration between the Mercator Ocean, the Drakkar consortium and Coriolis data center . It spans the altimeter and Argo eras, from 1993 to the present. The NEMO ocean model is implemented on the ORCA025 grid (approximately 0.25× 0.25 with 75 vertical levels). The model is forced by a combination of ERA-Interim fluxes (e.g., shortwave radiation) and turbulent fluxes obtained with bulk formulae using ERA-Interim near-surface parameters. The data are generated by a 3D-Var assimilation scheme with temperature and salinity profiles assimilated from the CORA3.3 database . In this study, monthly data from 1993 to 2014 on the original ORCA025 grid are used.

2.1.6 SODA3

SODA3 is the latest version of Simple Ocean Data Assimilation (SODA) ocean reanalyses conducted mainly at the University of Maryland . SODA3 is built on the Modular Ocean Model v5 (MOM5) ocean component of the Geophysical Fluid Dynamics Laboratory CM2.5 coupled model with a grid configuration of approximately 0.25 (latitude) × 0.25 (longitude) × 50-level resolution . To be consistent with the other two reanalysis data sets assessed in this study, SODA 3.4.1 is chosen since it applies surface forcing from ERA-Interim. For this specific version, the 5 d data are available from 1980 to 2015. Reanalysis data from this period on the original MOM5 grid are used in this case.

2.2 Oceanic observations and OGCM hindcast

For independent examination of the OMET calculated from reanalysis data sets, observations of the meridional transport of mass and heat throughout the Atlantic basin are used here. We use data from the RAPID-MOCHA-WBTS program and the OSNAP program . The RAPID-MOCHA-WBTS program, which is known as the RAPID array, employs a trans-basin observing array along 26.5 N and has been in operation since 2004. The OMET from the RAPID array available to this study is from April 2004 to March 2016. The OSNAP program has an observing system that comprises an integrated coast-to-coast array extending from the southeastern Labrador Shelf to the southwestern tip of Greenland and from the southeastern tip of Greenland to the Scottish shelf. So far, it provides OMET data from the full installation of the array in 2014 to the first complete data recovery in 2016 (21 months in total). Although it is too short to provide a good estimate of the interannual variability of OMET, we still include it as it is a unique observation system for OMET in the subpolar Atlantic.

Apart from the RAPID array and OSNAP observational data, a NEMO ORCA hindcast is also included here to provide more insights, since two of the chosen reanalysis products are also built on the NEMO ocean circulation model . This forced model simulation implements the NEMO ORCA global ocean circulation model version 3.6 (Madec2008). It is configured with the ORCA0083 grid, which has a nominal resolution of 1∕12 on 75 vertical levels. Climatological initial conditions for temperature and salinity were taken in January from PHC2.1 at high latitudes , MEDATLAS in the Mediterranean and the rest from . It is forced by the surface fields produced by the Drakkar project, which supplies surface air temperature, winds, humidity, surface radiative heat fluxes and precipitation, and a formulation that parameterizes the turbulent surface heat fluxes and is provided for the period from 1958 to 2012 (data set version 5.2) . More information about this hindcast is given by . We take monthly mean data from the hindcast, which spans from 1979 to 2012. For clarity, this hindcast will be referred to as the oceanic general circulation model (OGCM) simulation in this paper.

2.3 Computation of meridional energy transport

The methods for quantification of AMET and OMET with atmospheric and oceanic reanalyses are included in this section, respectively.

2.3.1 Energy budget in the atmosphere

The total energy per unit mass of air has four major components: internal energy (I), latent heat (H), geopotential energy (ϕ) and kinetic energy (k). They are defined as

$\begin{array}{}\text{(1)}& \begin{array}{rl}& I={c}_{\mathrm{v}}T\\ & H={L}_{\mathrm{v}}q\\ & \mathrm{\Phi }=gz\\ & k=\frac{\mathrm{1}}{\mathrm{2}}v\cdot v,\end{array}\end{array}$

with cv the specific heat capacity of dry air for constant volume (J kg−1 K−1), T the absolute temperature (K), Lv the specific heat of condensation (J kg−1), q the specific humidity (kg kg−1), g the gravitational acceleration (kg m−1 s−2), z the altitude (m) and v the zonal/meridional wind velocity (m s−1). The northward propagation is positive. In addition, these four quantities can be divided into three groups: the dry static energy I+ϕ, the moist static energy $I+\mathit{\varphi }+H$ and the kinetic energy k. A constant value of Lv=2500 kJ kg−1 was used to compute the AMET with the atmosphere reanalysis data sets. In addition, recently improved formulations of energy budget equations proposed by and are addressed here. We use an updated formulation of AMET as a combination of the divergence of dry-air enthalpy, latent heat, geopotential and kinetic energy transport, which is suggested by . Note that in this case the enthalpy transport associated with vapor fluxes is neglected.

In pressure coordinates, the total energy transport at a given latitude Φi can be expressed as

$\begin{array}{}\text{(2)}& E=\underset{\mathrm{\Phi }={\mathrm{\Phi }}_{i}}{\oint }\underset{{p}_{\mathrm{s}}}{\overset{{p}_{\mathrm{t}}}{\int }}\left[\left(\mathrm{1}-q\right){c}_{\mathrm{p}}T+{L}_{\mathrm{v}}q+gz+\frac{\mathrm{1}}{\mathrm{2}}v\cdot v\right]v\frac{\mathrm{d}p}{g}\mathrm{d}x,\end{array}$

with cp the specific heat capacity of dry air at constant pressure, pt the pressure level at the top of the atmosphere (Pa) and ps the pressure at the surface (Pa). A constant value of cp=1004.64 J kg−1 K−1 was used. Since we work on the native hybrid model coordinate with each atmosphere reanalysis product, the equation can be adjusted as follows (see ):

$\begin{array}{}\text{(3)}& E=\underset{\mathrm{\Phi }={\mathrm{\Phi }}_{i}}{\oint }\frac{\mathrm{1}}{g}\underset{\mathrm{0}}{\overset{\mathrm{1}}{\int }}\left[\left(\mathrm{1}-q\right){c}_{\mathrm{p}}T+{L}_{\mathrm{v}}q+gz+\frac{\mathrm{1}}{\mathrm{2}}v\cdot v\right]v\frac{\partial p}{\partial \mathit{\eta }}\mathrm{d}\mathit{\eta }\mathrm{d}x,\end{array}$

where η indicates the number of the hybrid level.

Unfortunately, a direct estimation of AMET based on the equations above cannot provide meaningful energy transport obtained from reanalysis data. It has been widely reported that reanalysis products suffer from mass inconsistency . Spurious sinks and sources mainly come from low spatial and temporal resolution, interpolation and regridding, and data assimilation. The interpolation from the original model level to pressure level can introduce considerable errors to the mass budget . Therefore, we prevent interpolations onto the pressure levels and use data on the native model levels with a high temporal resolution. provided a method to correct the mass budget through the use of the continuity equation. The method assumes that the mass imbalance mainly comes from the divergent wind fields and corrects the overall mass budget by adjusting the barotropic wind. The conservation of mass for a unit column of air can be represented as

$\begin{array}{}\text{(4)}& \frac{\partial {p}_{\mathrm{s}}}{\partial t}+\mathrm{\nabla }\cdot \underset{{p}_{\mathrm{s}}}{\overset{{p}_{\mathrm{t}}}{\int }}v\mathrm{d}p=g\left(E-P\right),\end{array}$

where E stands for evaporation and P denotes precipitation. It has been noted that big uncertainties reside in the evaporation and precipitation of global reanalyses . Hence, we use the moisture budget to derive the net moisture change in the air column, according to

$\begin{array}{}\text{(5)}& E-P=\frac{\partial }{\partial t}\left(\underset{{p}_{\mathrm{s}}}{\overset{{p}_{\mathrm{t}}}{\int }}q\frac{\mathrm{d}p}{g}\right)+\mathrm{\nabla }\cdot \underset{{p}_{\mathrm{s}}}{\overset{{p}_{\mathrm{t}}}{\int }}\left(v\cdot q\right)\frac{\mathrm{d}p}{g}.\end{array}$

The related fields for the mass budget correction are surface pressure (ps), meridional and zonal winds (uv) and specific humidity (q). After determining the mass budget imbalance, we correct the barotropic wind fields (ucvc), with uc and vc indicating the correction terms for zonal and meridional wind components as a result of the barotropic mass budget correction, and then calculate AMET . Note that all the computations regarding barotropic mass budget correction were performed in the spectral domain via spherical harmonics. Figure 1 shows the mean AMET and each component in each month at 60 N estimated from ERA-Interim.

Figure 1Estimation of mean AMET and each component in each month at 60 N with ERA-Interim from 1979 to 2017.

It is worth mentioning that MERRA-2 is very different from ERA-Interim and JRA-55, in terms of the discretization method and grid incorporated by the dynamical core. The dynamical core for MERRA-2 is the GEOS-5 model and it computes all fields on a cubed-sphere grid with a resolution of 50×50 km , while in ERA-Interim and JRA-55 the computations were performed in the spectral domain. However, the data collections are saved only on the latitude–longitude grid after interpolation. Thus, the data cannot be transferred back to the cubed-sphere grid without loss of information. Moreover, the vector field computations on the cubed-sphere grid are not divergence-free due to the implementation of finite volume discretization methods . Consequently, we transferred MERRA-2 fields to the spectral domain and performed vector field computations via spherical harmonics to minimize the numerical errors, the same treatment as ERA-Interim and JRA-55.

2.3.2 Energy budget in the ocean

Unlike the atmosphere, energy transport in the ocean can be well represented by the internal energy itself. Consequently, the total energy transport in the ocean at a given latitude ϕi can be expressed in terms of the temperature transport :

$\begin{array}{}\text{(6)}& E=\underset{\mathrm{\Phi }={\mathrm{\Phi }}_{i}}{\oint }\underset{{z}_{\mathrm{b}}}{\overset{{z}_{\mathrm{0}}}{\int }}{\mathit{\rho }}_{\mathrm{0}}{c}_{{\mathrm{p}}_{\mathrm{0}}}\mathit{\theta }\cdot v\mathrm{d}z\mathrm{d}\mathit{\varphi },\end{array}$

where ρ0 is the seawater density (kg m−3), ${c}_{{\mathrm{p}}_{\mathrm{0}}}$ is the specific heat capacity of seawater (J kg−1C−1), θ is the potential temperature (C), v is the meridional current velocity (m s−1), and z0 and zb are sea surface and the depth to the bottom (m), respectively. A constant value of ${c}_{{\mathrm{p}}_{\mathrm{0}}}=\mathrm{3987}$ J kg−1C−1 was used in all the calculations of OMET. OHC (with unit J) is another variable that plays a role in the ocean heat budget. The total OHC between certain latitudes can be calculated by

$\begin{array}{}\text{(7)}& \mathrm{OHC}=\underset{{\mathrm{\Phi }}_{i}}{\overset{{\mathrm{\Phi }}_{\mathrm{0}}}{\int }}\underset{{z}_{\mathrm{b}}}{\overset{{z}_{\mathrm{0}}}{\int }}{\mathit{\rho }}_{\mathrm{0}}{c}_{{\mathrm{p}}_{\mathrm{0}}}\mathit{\theta }\mathrm{d}z\mathrm{d}\mathit{\varphi }.\end{array}$

Our computation of OMET suffers from a small mass imbalance (e.g., mass imbalance coming from the difference between precipitation and evaporation; ). In the ocean, with its strong boundary circulations, even the smallest imbalance can lead to large errors in the heat flux. However, the barotropic correction method adopted by the atmosphere is not feasible here due to the mass imbalance coming from the residual between precipitation and evaporation, and some budget terms that are hard to diagnose. In oceanographic literature, it is common to use a reference temperature when calculating OMET in both observations and model diagnostics . Here, we also take a reference temperature: θr (C). Note that the influence of taking a reference temperature on zonally integrated transport is smaller than that on a single strait . Then, the quantification of OMET becomes

$\begin{array}{}\text{(8)}& E=\underset{\mathrm{\Phi }={\mathrm{\Phi }}_{i}}{\oint }\underset{{z}_{\mathrm{b}}}{\overset{{z}_{\mathrm{0}}}{\int }}{\mathit{\rho }}_{\mathrm{0}}{c}_{{\mathrm{p}}_{\mathrm{0}}}\left(\mathit{\theta }-{\mathit{\theta }}_{\mathrm{r}}\right)\cdot v\mathrm{d}z\mathrm{d}\mathit{\varphi }.\end{array}$

Here, we take θr equal to 0 C. Finally, operations in the “zonal” direction are different from their conventional meaning. As the three ocean reanalysis products used here are all built on a curvilinear grid, the zonal direction on the native model grid is curvilinear as well. Similar to the considerations made in Sect. 2.1, regridding from the native curvilinear grid to a uniform geographical grid will introduce large errors. So, we worked on the original multi-pole grid and followed a zig-zag setup when taking zonal integrals. The method is illustrated by in their Fig. 2. After applying this method, the resulting OMET values are comparable to those in earlier publications . Note that we only have access to sub-monthly data for SODA3. The computation of OMET using monthly data in GLORYS2V3 could miss part of heat transport by eddies, while ORAS4 does not include the heat transport from the eddy parameterization scheme , as the related eddy-induced velocity field was not archived.

2.4 Statistical analysis

In order to understand the connection between MET and changes in the Arctic, and to compare to the results from numerical climate models or a single reanalysis data set , in the following section, we performed linear regressions on multiple fields with AMET and OMET. To test the significance of the regressions, we use Student's t test. The autocorrelations are taken into account. Note that all the reanalysis data sets included in this study have relatively short time series (no more than 456 months; see Table 1).

3 Results

Unless specifically noted, the results shown in this section are all based on monthly mean fields with a low-pass filter of 5 years, which will be referred to as interannual timescales for the rest of the paper.

3.1 Overview of AMET and OMET

Globally, MET is driven by the unequal distribution of net solar radiation and thermal radiation. There is transport from regions with positive net top-of-the-atmosphere (TOA) radiation to regions with negative net TOA radiation. Figure 2 shows the mean AMET and OMET over the entire time series of every product at each latitude in the Northern Hemisphere. For the atmosphere, all three data sets agree very well. The results differ a bit in amplitude but capture similar variations at each latitude. The peak of AMET is around 41 N, after which it starts to decrease towards the North Pole. In ERA-Interim and JRA-55, AMET peaks at 4.45 PW at 41 N, while in MERRA-2 AMET peaks at 4.5 PW at 41.5 N. These findings are consistent with previous work (e.g., Trenberth and Caron2001; Fasullo and Trenberth2008; Mayer and Haimberger2012, and many others).

Figure 2Mean AMET and OMET over the entire time span of each product as a function of latitude in the Northern Hemisphere. AMET is illustrated with solid lines and OMET with dashed lines. The shades represent the full range of MET across the entire time series at each latitude. The time span of each product used in this study is given in Table 1.

Apart from the climatology of MET, we are particularly interested in the variations across different timescales from midlatitudes towards the Arctic. The time series of AMET, integrated zonally over 60 N, are shown in Fig. 3a. The seasonal cycle is dominant in each component, as expected, and the phase is very similar, but differences in the amplitudes are noted. The mean AMET provided by the chosen three atmospheric reanalysis data sets agrees well. However, their variations differ from each other. In ERA-Interim, the standard deviation (SD) of AMET is 0.92 PW, while MERRA-2 has a relatively large SD of 0.97 PW, and in JRA-55 the SD is 0.91 PW. Hence, it can be concluded that the seasonal cycles of AMET presented by the chosen atmospheric reanalysis data sets are similar. After removing the seasonal cycles and applying a 5-year low-pass filter, we obtain the low-frequency signals of AMET anomalies at interannual timescales (see Fig. 3b). ERA-Interim and JRA-55 agree well, and the correlation coefficient between them is 0.82. MERRA-2 provides a different result, and the correlation coefficient between ERA-Interim and MERRA-2 is −0.53. The SD of AMET anomaly in ERA-Interim is 0.02 PW, while in MERRA-2 the SD is 0.04 PW and in JRA-55 the SD is 0.03 PW. This implies that the variations of AMET anomalies at large timescales are similar in ERA-Interim and JRA-55 but not in MERRA-2. We further assess the sources of the difference in the next section.

Figure 3Time series of zonal integral of AMET at 60 N without/with a low-pass filter. (a) The original time series and (b) the ones with a low-pass filter include signals from ERA-Interim (blue), MERRA-2 (red) and JRA-55 (green). For the low-pass-filtered ones, we take a running mean of 5 years. The shades represent the confidence intervals with 1 standard deviation. σ is the standard deviation and μ is the mean of the entire time series.

For the ocean, all the reanalysis data sets agree well at almost all the latitudes, except for the OMET between 30 and 40 N, where the Gulf Stream resides (Fig. 2). One possible explanation is that GLORYS2V3 and SODA3 both have been generated with eddy-permitting models, while ORAS4 was not. In ORAS4, an eddy parameterization scheme from is implemented. The implementation of this eddy parameterization scheme can lead to a big difference in heat transport, compared to eddy-permitting models . However, in this case, the computation of OMET with ORAS4 does not include the contribution from eddy-induced velocity as the fields related to the use of eddy advection schemes were not archived. The eddy-permitting reanalysis data sets with high resolution, like GLORYS2V3 and SODA3, are capable of addressing the large-scale geostrophic turbulence. It has been shown that their eddy-permitting capacity can account for the large-scale eddy variability and represent the eddy energy associated with both the Gulf Stream and the Kuroshio pathways well . Consequently, at the latitude of the Gulf Stream (between 30 and 40 N), a strong spatial variability, which might represent more realistic patterns of the large-scale eddy variability, is apparent in all data sets but ORAS4.

Similarly, we show the zonal integral of the OMET at 60 N in Fig. 4. Differences in amplitudes and trends can be observed in the unfiltered time series. The mean and SD of all the OMET time series are similar (see Fig. 4a). The mean of OMET in ORAS4 is 0.47 PW, in GLORYS2V3 it is 0.44 PW, and in SODA3 it is 0.46 PW. The OGCM hindcast gives a similar result, which is also 0.47 PW. The SD of OMET in ORAS4 and the OGCM hindcast is 0.06 PW, while in GLORYS2V3 and SODA3 the SD is 0.07 PW. The OMET anomalies with a 5-year low-pass filter are shown in Fig. 4b. OMET anomalies in ORAS4 resemble that in SODA3, especially after 1998, while OMET anomalies in GLORYS2V3 are very different from that in ORAS4 and SODA3 from 1998 to 2006. The differences reveal that the first 10 years in GLORYS2V3 are quite suspicious because of its large deviation from the other products. Such large differences should be noticeable in the heat content changes or surface fluxes. We find that OHC anomalies in GLORYS2V3 are indeed very different from ORAS4 and SODA3 during this period (see Fig. 8). Nevertheless, after 2007, all the oceanic reanalyses agree well, and the OGCM hindcast deviates from the reanalyses. It is noteworthy that the observations improve considerably around that period due to an increasing number of Argo floats in use . The reanalysis products used here are greatly influenced by the number of available in situ observations. We further assess the sources of differences in the next section.

Figure 4Time series of zonal integral of OMET at 60 N without/with a low-pass filter. (a) The original time series and (b) the ones with a low-pass filter include signals from ORAS4 (blue), GLORYS2v3 (red), SODA3 (green) and the OGCM hindcast (yellow). For the low-pass-filtered ones, we take a running mean of 5 years. The shades represent the confidence intervals with 1 standard deviation. σ is the standard deviation and μ is the mean of the entire time series.

3.2 Sources of disparity

In order to further understand the difference between the AMET estimated from each atmosphere reanalysis product, we compare each component of AMET separately. We investigate the difference between each component of AMET at 60 N estimated from ERA-Interim against those from MERRA-2 and JRA-55. It is noticed that the differences mainly originate from meridional temperature transport (vcpT) and geopotential energy transport (vgz). We find that the correlation between the difference in total energy transport and the difference in meridional temperature transport between ERA-Interim and MERRA-2 is 0.55, while between ERA-Interim and JRA-55 it is 0.21. In addition, the correlation between the difference in total energy transport and the difference in geopotential energy transport (vgz) between ERA-Interim and MERRA-2 is 0.56, while between ERA-Interim and JRA-55 it is 0.60. For the other components, the correlations between them and the total difference are small. The results are all obtained with a confidence interval of 95 %. Large differences in temperature transport among reanalysis products are found at almost all latitudes (not shown). Such differences are consistent with the fact that the temperature transport and geopotential energy transport have a large contribution to the total AMET (see Fig. 1). Note that the differences in each AMET component are of the same order of magnitude as AMET. Besides, the mean and anomalous latent heat transport agree well between the chosen atmospheric products (not shown). A similar result was found by in their study using more reanalysis data sets.

In order to know the relative contribution of each field to the difference of the mean total AMET among the chosen reanalyses, a direct comparison of the vertical profile of temperature and meridional velocity fields between ERA-Interim and MERRA-2 is presented in Fig. 5. We compare the monthly mean temperature and velocity fields of ERA-Interim and MERRA-2 from 1994 to 1998, in which the biggest difference was observed (Fig. 3, taking into account the running mean of 5 years). To accommodate a point-wise comparison, the fields from MERRA-2 are interpolated onto the vertical grid of ERA-Interim. It shows that these two reanalysis products differ substantially regarding each variable field (Fig. 5a and b). Big differences in temperature reside mostly at the tropopause. Large differences in meridional wind components are distributed over the entire vertical column of the tropopause. Such differences in both fields are expected to be responsible for the difference in mean temperature transport (vcpT). Large differences are found in geopotential height fields, too (not shown). It should be noted that this comparison is carried out on pressure levels, and mass conservation is not ensured. Therefore, it can only provide insight qualitatively, and a quantitative contribution of the difference in every single field to the mean temperature transport cannot be identified here.

Figure 5Difference in temperature, meridional wind velocity and temperature transport between MERRA-2 and ERA-Interim at 60 N. The vertical profiles of (a) temperature difference and (b) meridional wind velocity difference are calculated from the climatology of each field from 1994 to 1998, respectively.

Differences between every two chosen atmospheric products are found at nearly each pressure level. This analysis is not sufficient to explain conclusively where the uncertainty mainly comes from in terms of the dynamics and physics in the atmosphere model and data assimilation system. We do find that uncertainties, as indicated by the spread between the data sets, in both the temperature and meridional velocity fields, are too large to constrain the AMET. Note that the difference in horizontal advection schemes can also influence the results. The chosen atmospheric reanalyses systems use semi-Lagrangian advection schemes, but this is not the case for MERRA-2. Hence, studies on low-frequency variability of energy transport and associated variables should be interpreted with care as the reanalysis products differ substantially, and we cannot judge a priori how close they are to actual energy transport since independent direct observations are not available.

For the ocean, fortunately observations of OMET in the Atlantic Ocean are available. First, OMET estimated from ORAS4, GLORYS2V3, SODA3 and the OGCM hindcast is evaluated against OMET measured at 26.5 N. The intercomparison shows that the reanalysis products capture roughly the mean amplitude of the OMET (Fig. 6). Some large events are captured as well, such as the strong weakening in 2009. Statistically, the mean OMET provided by the RAPID array is 1.21±0.27 PW. It is higher than the chosen products here. The mean OMET in ORAS4 is 0.66±0.27 PW, in GLORYS2V3 it is 0.89±0.52 PW, in SODA3 it is 0.81±0.52 PW, and in OGCM hindcast it is 1.05±0.21 PW. This means that all chosen products underestimate the mean OMET at 26.5 N in the Atlantic basin. Of all products, ORAS4 has the largest bias. The SD of OMET given by ORAS4 is the same as that from the RAPID array, while in GLORYS2V3 and SODA3 we find a higher SD of OMET. The OGCM hindcast has a relatively small OMET SD, which is 0.21 PW. In terms of the correlation and standard deviation, ORAS4 and the OGCM hindcast agree well with observations. It is noteworthy that the OGCM does not assimilate ocean data. The simulation is only constrained by the surface fluxes, and this suggests that the surface forcing is a very important driver of OMET variability. To conclude, the heat transport at 26.5 N is too low in these products, but ORAS4 and OGCM hindcasts appear to have reasonable variability.

Figure 6OMET estimated from ORAS4 (blue), GLORYS2V3 (red), SODA3 (green) and the OGCM hindcast (orange) compared to the RAPID array observation (gray) at 26.5 N across the Atlantic basin. The time series of OMET is presented in panel (a). The statistical properties are shown in (b) the Taylor diagram, including bias, correlation (blue), standard deviation (black) and root mean square deviation (green). σ is the standard deviation and μ is the mean of the entire time series.

Moreover, the comparison of time series in the chosen reanalyses and OSNAP observations is given in Fig. 7. Due to the limited length of OMET time series, only ORAS4 and SODA3 are included in the comparison. It can be noticed that the OMET given by ORAS4 is comparable to that in OSNAP in terms of the amplitude and variability. For most of the time within the observation period, OMET in ORAS4 falls into the range of the OSNAP observation including the uncertainty margins. The mean of OMET in ORAS4 is 0.39±0.11 PW, which is quite similar to the mean OMET (0.45±0.07 PW) of OSNAP. However, OMET in SODA3 has a larger mean and standard deviation than that in OSNAP and thus deviates from the observations.

Figure 7OMET estimated from ORAS4 (blue), SODA3 (green) and compared to the OSNAP observation (gray) at subpolar Atlantic basin. The range of uncertainty from OSNAP observation is marked by the red shade. σ is the standard deviation and μ is the mean of the entire time series.

Figure 8Time series of (a) OHC and (b) OHC anomalies with a low-pass filter at the polar cap. The OHC is integrated from surface to the bottom between 60 and 90 N. It is estimated from ORAS4 (blue), GLORYS2V3 (red), SODA3 (green) and the OGCM hindcast (yellow). The shades represent the confidence intervals with 1 standard deviation. σ is the standard deviation and μ is the mean of the entire time series.

Just as in the atmosphere, we would like to study the temperature and meridional current velocity contributions to the ocean heat transport to identify the sources of the difference between products. However, due to the nature of the curvilinear grid, the comparison of local fields after interpolation is not trustworthy. To get further insight, we calculate the OHC, since the convergence of the heat transport is likely related to OHC change. A full budget analysis was not feasible as most data sets did not include the surface fluxes. Figure 8 illustrates the OHC (Fig. 8a) and OHC anomalies (Fig. 8b) quantified from ORAS4, GLORYS2V3, SODA3 and the OGCM hindcast. It depicts the OHC integrated in the polar cap (from 60 to 90 N) over all depths. The mean OHC in ORAS4 is $\mathrm{4.48}±\mathrm{0.78}×{\mathrm{10}}^{\mathrm{22}}$ J, in GLORYS2V3 it is $\mathrm{4.23}±\mathrm{0.59}×{\mathrm{10}}^{\mathrm{22}}$ J, and in SODA3 it is $\mathrm{3.79}±\mathrm{0.93}×{\mathrm{10}}^{\mathrm{22}}$ J, while the OGCM hindcast shows a much larger mean OHC of $\mathrm{7.85}±\mathrm{0.58}×{\mathrm{10}}^{\mathrm{22}}$ J. Actually, we found that the OHC between 60 and 70 N in the OGCM hindcast agrees well with the reanalyses (not shown). Thus, the difference seems to be associated with changes to the sea ice distribution. Given the limited observations in the Arctic to constrain the reanalyses and different assumptions about the Arctic sea ice due to the differences in spatial resolutions, it is more complex than just concluding that the reanalyses are better. The variations of OHC are similar between chosen products. Regarding the OHC anomalies in Fig. 8b, a positive trend of OHC anomalies in the polar cap is captured by each product. However, the variability is different, and these are reflected in the standard deviation of OHC anomalies time series. Increases in surface temperature and OHC are often taken as a sign of AA in many papers (e.g., Serreze and Barry2011). Qualitatively, the trends of OHC in the chosen reanalyses at the polar cap could be taken as a sign of the AA, but it might be just Arctic warming and not necessarily a higher warming rate than the global mean temperature change. A quantitative evaluation of the AA is not possible due to large differences between products. To conclude, there are large differences in OHC between chosen products, while their variations agree relatively well. Since OHC is a function of temperature fields only, this can imply that temperature profiles are different among the chosen ocean reanalysis data sets. The differences of OHC between chosen products are partially consistent with the differences that we found for OMET. However, the OHC anomalies agree better among reanalysis products than the absolute OHC, which indicates that the trend of OHC is captured in a similar way among all the ocean reanalysis products.

3.3 MET and the Arctic

In previous sections, it is found that MET values in different reanalysis products at subpolar and subtropical latitudes differ substantially from each other. In order to further evaluate AMET and OMET given by different reanalyses and to provide more insight, we investigate the links between MET and remote regions. We focus on the Arctic because previous studies indicate a strong role for subpolar MET in low-frequency variability in the Arctic region. Given the complexity of the interaction between MET and the Arctic, and the short time series available, determining cause–effect relations is out of the scope of this paper. We aim to compare the relation between MET and the Arctic within each reanalysis product to investigate the physical plausibility and compare it with previous studies that use data from one reanalysis product or from coupled climate models .

Many of these studies perform linear regressions between a time series of MET and grid-point values of other physical variables. Here, we follow the same procedure and perform linear regressions of sea level pressure (SLP), 2 m temperature (T2M) and sea ice concentration (SIC) anomalies on AMET and OMET anomalies at 60 N for the chosen products. We show linear regressions in summer and winter separately in order to account for the seasonal variability of the relationships. It should also be noted that there are strong trends in OMET, T2M and SIC. We removed them by applying a polynomial fit to the time series on each grid point. We find that the second-order polynomial fit is able to capture the trend without losing variations at interannual timescales. Hereafter, we only address detrended OMET, T2M and SIC. For the sake of consistency, the regressions are carried out on the surface fields included in each respective reanalysis product. For instance, the regression of SLP on AMET estimated from ERA-Interim involves SLP fields from ERA-Interim itself. For the ocean reanalyses, as they all apply forcing derived from ERA-Interim, the regressions are performed on the fields from ERA-Interim. Note that there is a known issue with the quality of the sea ice field close to the North Pole in ERA-Interim, which can be inferred from an evaluation of reanalysis data sets concerning near-surface fields in . Following the regressions performed by and , we repeated the same procedure here with AMET at interannual scales (∼5 years).

First, we investigate the links between MET and the Arctic in winter. The regressions of anomalies of multiple fields on AMET anomalies at 60 N in each atmospheric product in winter are shown in Fig. 9. The regression coefficients reach their maximum when the regressions are instantaneous with given fields. In ERA-Interim and JRA-55, AMET is correlated with SLP over the Greenland, the North Atlantic, the Barents Sea, the Kara Sea and the northern part of the Eurasian continent. It suggests that an increase in subpolar AMET is linked to a northward advection over the Greenland which could bring relatively warm and humid air into the Arctic. Such patterns are consistent with the relatively warm air over the Greenland and part of the central Arctic close to the Eurasian side shown in Fig. 9d and f. Using ERA-40, found a similar correlation between AMET and surface air temperature (SAT) in the Greenland Sea and Barents Sea as Fig. 9d and f, without time lag. This is also consistent with a model study by . The decrease of sea ice concentration with increasing AMET in Baffin Bay and the northern part of the Barents Sea given in Fig. 9g and i is consistent with the relations between AMET and T2M. A further eddy decomposition of AMET following the method from indicates that heat transported by standing eddies has the biggest contribution to the total AMET (not shown), which is consistent with . These patterns are found only in ERA-Interim and JRA-55 but not in MERRA-2. Such different patterns in MERRA-2 likely stem from its shift in AMET around 2000. Hence, there is also large uncertainty in the assertion that heat and humidity transport by stationary eddies contributes to the changes in the subpolar and Arctic regions at interannual timescales.

Figure 9Regressions of sea level pressure, 2 m temperature and sea ice concentration anomalies on AMET anomalies at 60 N in winter (DJF) at interannual timescales with no time lag. The monthly mean fields are used here after taking a running mean of 5 years. Both the 2 m temperature and sea ice concentration are detrended. From left to right, they are the regressions on AMET of (a, d, g) ERA-Interim, (b, e, h) MERRA-2 and (c, f, i) JRA-55. The stippling indicates a significance level of 95 %.

Moreover, similar to and , we investigate the links between the variability of OMET and variations of multiple fields at interannual timescales. The regressions of anomalies of multiple fields on detrended OMET anomalies at 60 N in winter are shown in Fig. 10, with OMET leading by 1 month. It is noteworthy that it takes around 1 to 2 years for the OMET anomalies to propagate from the North Atlantic to the Barents Sea . However, the regression coefficients are maximal when the OMET leads by 1 month, which could be attributed to the implementation of the low-pass filter. In ORAS4 and SODA3, increasing OMET can lead to a decrease in SLP in the Arctic, while in ORAS4 this polar low is much stronger. This seems to indicate that an increase in OMET is related to sea ice melt and increase in T2M around the Nordic Seas. There is an Arctic Oscillation (AO)-/North Atlantic Oscillation (NAO)-like SLP anomaly with the associated large-scale temperature pattern. However, GLORYS2V3 tells an entirely different story. This is mainly due to the difference between OMET in this data set compared to the other ocean data sets during the 1990s, as shown in Fig. 4.

Figure 10Regressions of sea level pressure, 2 m temperature and sea ice concentration anomalies on OMET anomalies at 60 N in winter (DJF) at interannual timescales. OMET leads the fields by 1 month. The 2 m temperature, sea ice concentration and OMET are detrended. From left to right, they are the regressions on OMET of (a, d, g) ORAS4, (b, e, h) GLORYS2V3 and (c, f, i) SODA3. The stippling indicates a significance level of 95 %.

In general, the decrease of OMET leads to an increase in the growth rate of SIC, which is consistent with studies performed with global climate models at decadal to interdecadal timescales . Studies with observations of sea ice in the Barents Sea and OMET across the Barents Sea Opening (BSO) also confirm the strong correlation between the OMET and sea ice variation over the Barents Sea . However, note that some discussed regions are below the significance of 95 %.

In summer, the situation becomes more intricate and unclear. The same regressions of anomalies of multiple fields on AMET and OMET anomalies at 60 N in each reanalysis product in summer are included in the Supplement. It is noted that the consistency of associations between AMET, OMET and multiple fields is better in winter than that in summer within the chosen products. Atmospheric dynamical processes are more dominant in winter, which is also reflected in large-scale patterns of variability such as the AO and NAO which are more pronounced in winter than in summer . Therefore, the regressions of SLP, T2M and SIC on AMET in winter are easier to understand than those in summer.

In this section, we compared the reanalysis data with findings from previous studies. We found that ERA-Interim and JRA-55 are most consistent with the results given by coupled numerical models in winter, while MERRA-2 does not corroborate model studies. For the ocean, results from ORAS4 and SODA3 are more consistent with literature in winter. However, given the low statistical significance and the difference among chosen products, it is still hard to determine which atmospheric product provides more convincing plausible interannual variations in AMET.

4 Discussion

In this study, we found substantial differences between reanalysis products with respect to MET. In order to improve the accuracy of the variability of AMET and OMET estimated from reanalyses, one needs more observations to constrain the models. Vertical profiles differ substantially between products, and surface and top-of-the-atmosphere radiation budget are too uncertain to constrain variability in the different products. Note that reanalyses do not assimilate direct observation of the TOA and surface energy budgets. Climate models already provide information on the interaction between atmosphere and ocean and connections provided by the energy transport from midlatitudes to high latitudes . This can potentially sketch the mechanism of the interaction between energy transport and the Arctic climate change. Moreover, some studies point out that the latent heat is more influential on the Arctic sea ice rather than the dry static energy . With improved reanalysis products and independent observations, such as ocean mooring arrays and atmospheric in situ and satellite observations, to validate the reanalyses, the validity of these mechanisms can be further studied.

The regression of SIC on OMET suggests that sea ice variations are sensitive to changes of meridional energy transport at subpolar latitudes, which is noticed by other studies on SIC and MET as well . ORAS4 and SODA3 show a large anticorrelation between SIC and OMET in winter around the Greenland Sea and the Barents Sea. However, GLORYS2V3 does not show this relation. The differences in OMET are reflected in the regressions on sea ice. The strong connection between OMET from mid-to-high latitudes and the Arctic sea ice indicates an indirect link between midlatitudes and the Arctic. Many studies that explored these remote links found large-scale “horseshoe” and dipole patterns over the Atlantic . However, the physical mechanism remains disputable. propose that the multiple linkages between the Arctic and midlatitudes are based on the amplification of existing jet stream wave patterns, which might also be driven by tropical and midlatitude sea surface temperature (SST) anomalies . lists possible pathways for the teleconnection between the Arctic and midlatitudes, including changes in storm tracks, the jet stream, and planetary waves and their associated energy propagation. However, due to the shortness of time series, a small signal-to-noise ratio, uncertain external forcing and the internal atmospheric variability , this question has no easy answer.

Previous studies have shown that the variations of total OMET are very sensitive to the changes of its overturning component (e.g., McCarthy et al.2015; Lozier et al.2019). Hence, the Atlantic meridional overturning circulation (AMOC) may serve as an indicator of the changes of OMET. In our case, a quantitative estimation of the difference in the AMOC among the chosen data sets is beyond the scope of this paper. However, the downward trend of AMOC, which has been reported by several studies , is consistent the downward trend observed in OMET at 60 N in our chosen oceanic reanalyses (see Fig. 4). After analyzing six oceanic reanalysis data sets, find the reanalysis products are not consistent in their year-to-year AMOC variations. The discrepancy between AMOC represented by each reanalysis product may explain the differences in OMET in each reanalysis data set.

5 Conclusions

This study aimed to quantify and intercompare AMET and OMET variability from three atmospheric and three oceanic reanalysis data sets at subpolar latitudes. It also serves to illustrate the relation between AMET and OMET with high-latitude climate characteristics. The study is motivated by previous studies with coupled models that show a strong relation between meridional energy transport and sea ice. It is also motivated by previous studies with reanalysis data, where generally only one reanalysis data set is considered and which include mostly only oceanic or atmospheric analysis.

All selected data sets agree on the mean AMET and OMET in the Northern Hemisphere. The results are consistent with those achieved over the previous 20 years . However, when it comes to anomalies at interannual timescales, they differ from each other both spatially and temporally. The variations between ERA-Interim and JRA-55 are small, while MERRA-2 is very different from them. Although there is an overlap of observational data assimilated by different reanalysis products, large deviations still exist in many fields, especially for the vertical profiles of temperature and velocity in atmospheric reanalyses, which were also reported by some reanalysis quality reports . A further investigation of the relations between multiple fields in the Arctic and meridional energy transport shows that the Arctic climate is sensitive to the variations of AMET and OMET in winter. The patterns in ERA-Interim and JRA-55 are more consistent in winter. For the ocean, ORAS4 and SODA3 provide similar patterns in winter. Based on our results, it seems that the interannual variability of AMET and OMET cannot be constrained by the available observations. The existence of sources and sinks in reanalysis data sets introduces large uncertainties in the computation of energy transport . Although the reanalysis data sets are not specifically designed for the studies on energy transport, given the good agreement on mean AMET and OMET and their annual cycles among assessed reanalysis products, we still recommend to use these reanalysis products for the energy transport diagnostics. However, much care should be taken when adopting reanalyses for the examination of energy transport at relatively long timescales. The robustness of those results based on the AMET and OMET estimated from reanalyses should be further assessed.

Code and data availability
Code and data availability.

The reanalysis products used in this study are open to the public and they are available online. The computation and post-processing were carried out with the Python package META (https://doi.org/10.5281/zenodo.3609505; ).

Supplement
Supplement.

Author contributions
Author contributions.

YL, JA and WH designed this study, performed computations using reanalyses and analyzed the results. BM performed OGCM simulation and contributed to the analysis.

Competing interests
Competing interests.

The authors declare that they have no conflict of interest.

Acknowledgements
Acknowledgements.

The research was supported by the Netherlands eScience Center, Wageningen University, the National Oceanography Center in the UK and Blue Action project (European Union's Horizon 2020 research and innovation programme, grant no. 727852). The high-resolution NEMO ORCA hindcast was completed in the North Atlantic Climate System: Integrated Study (ACSIS) project (grant no. NE/N018044/1). The authors are grateful for the high performance computational infrastructure (HPC cloud and Cartesius) provided by SURFsara in the Netherlands. We would like to express our gratitude to all the researchers working on the reanalysis data sets and making the data open to the public. We also want to thank the OSNAP (Overturning in the Subpolar North Atlantic Program; https://doi.org/10.7924/r4z60gf0f) project and the RAPID-AMOC program (https://doi.org/10/bkzc) for making the observation data in the North Atlantic freely available. We also acknowledge the editor, Gerrit Lohmann, and our two anonymous reviewers for their help in improving the manuscript.

Financial support
Financial support.

This research has been supported by the Blue Action project (European Union's Horizon 2020 research and innovation programme, grant no. 727852).

Review statement
Review statement.

This paper was edited by Gerrit Lohmann and reviewed by two anonymous referees.

References

Årthun, M., Eldevik, T., Smedsrud, L., Skagseth, Ø., and Ingvaldsen, R.: Quantifying the influence of Atlantic heat on Barents Sea ice variability and retreat, J. Climate, 25, 4736–4743, 2012. a, b

Balmaseda, M. A., Mogensen, K., and Weaver, A. T.: Evaluation of the ECMWF ocean reanalysis system ORAS4, Q. J. Roy. Meteorol. Soc., 139, 1132–1161, 2013. a, b, c, d

Barnes, E. A. and Screen, J. A.: The impact of Arctic warming on the midlatitude jet-stream: Can it? Has it? Will it?, Wiley Interdisciplin. Rev.: Clim. Change, 6, 277–286, 2015. a

Berrisford, P., Dee, D., Fielding, K., Fuentes, M., Kallberg, P., Kobayashi, S., and Uppala, S.: The ERA-interim archive, ERA report series, ECMWF, Reading, 1–16, 2009. a

Berrisford, P., Kållberg, P., Kobayashi, S., Dee, D., Uppala, S., Simmons, A., Poli, P., and Sato, H.: Atmospheric conservation properties in ERA-Interim, Q. J. Ro. Meteorol. Soc., 137, 1381–1399, 2011. a, b, c

Brodeau, L., Barnier, B., Treguier, A.-M., Penduff, T., and Gulev, S.: An ERA40-based atmospheric forcing for global ocean circulation models, Ocean Model., 31, 88–104, 2010. a

Bryan, K.: Measurements of meridional heat transport by ocean currents, J. Geophys. Res., 67, 3403–3414, 1962. a

Carton, J. A., Chepurin, G. A., and Chen, L.: SODA3: a new ocean climate reanalysis, J. Climate, 31, 6967–6983, https://doi.org/10.1175/JCLI-D-18-0149.1, 2018. a, b, c

Chiodo, G. and Haimberger, L.: Interannual changes in mass consistent energy budgets from ERA-Interim and satellite data, J. Geophys. Res.-Atmos., 115, D02112, https://doi.org/10.1029/2009JD012049, 2010. a

Cohen, J., Screen, J. A., Furtado, J. C., Barlow, M., Whittleston, D., Coumou, D., Francis, J., Dethloff, K., Entekhabi, D., Overland, J., and Jones, J.: Recent Arctic amplification and extreme mid-latitude weather, Nat. Geosci., 7, 627–637, 2014. a

Comiso, J. C. and Hall, D. K.: Climate trends in the Arctic as observed from space, Wiley Interdisciplin. Rev.: Clim. Change, 5, 389–409, 2014. a

Curry, J. A., Schramm, J. L., and Ebert, E. E.: Sea ice-albedo climate feedback mechanism, J. Climate, 8, 240–247, 1995. a

Czaja, A. and Frankignoul, C.: Observed impact of Atlantic SST anomalies on the North Atlantic Oscillation, J. Climate, 15, 606–623, 2002. a

Dee, D. P., Uppala, S. M., Simmons, A. J., Berrisford, P., Poli, P., Kobayashi, S., Andrae, U., Balmaseda, M. A., Balsamo, G., Bauer, D. P., Bechtold, P., Beljaars, A. C. M., van de Berg, L., Bidlot, J., Bormann, N., Delsol, C., Dragani, R., Fuentes, M., Geer, A. J., Haimberger, L., Healy, S. B., Hersbach, H., Hólm, E. V., Isaksen, L., Kållberg, P., Köhler, M., Matricardi, M., McNally, A. P., Monge-Sanz, B. M., Morcrette, J.-J., Park, B.-K., Peubey, C., de Rosnay, P., Tavolato, C., Thépaut, J.-N., and Vitart, F.: The ERA-Interim reanalysis: Configuration and performance of the data assimilation system, Q. J. Roy. Meteorol. Soc., 137, 553–597, 2011. a, b

Delworth, T. L., Rosati, A., Anderson, W., Adcroft, A. J., Balaji, V., Benson, R., Dixon, K., Griffies, S. M., Lee, H. C., Pacanowski, R. C., Vecchi, G. A., Wittenberg, A. T., Zeng, F., and Zhang, R.: Simulated climate and climate change in the GFDL CM2.5 high-resolution coupled climate model, J. Climate, 25, 2755–2781, 2012. a

Delworth, T. L., Zeng, F., Zhang, L., Zhang, R., Vecchi, G. A., and Yang, X.: The central role of ocean dynamics in connecting the North Atlantic Oscillation to the extratropical component of the Atlantic Multidecadal Oscillation, J. Climate, 30, 3789–3805, 2017. a

Dufour, A., Zolina, O., and Gulev, S. K.: Atmospheric moisture transport to the Arctic: Assessment of reanalyses and analysis of transport components, J. Climate, 29, 5061–5081, 2016. a

Dussin, R., Barnier, B., Brodeau, L., and Molines, J.: The making of the Drakkar forcing set DFS5, DRAKKAR/MyOcean Rep., Grenoble, France, 01–04, 2016. a

ECMWF: ERA5: Fifth generation of ECMWF atmospheric reanalyses of the global climate, Copernicus Climate Change Service Climate Data Store (CDS), 2017. a

Fasullo, J. T. and Trenberth, K. E.: The annual cycle of the energy budget. Part II: Meridional structures and poleward transports, J. Climate, 21, 2313–2325, 2008. a, b, c

Ferry, N., Parent, L., Garric, G., Barnier, B., Jourdain, N. C., and the Mercator Ocean Team: Mercator global Eddy permitting ocean reanalysis GLORYS1V1: Description and results, Mercator-Ocean Quart. Newslett., 36, 15–27, 2010. a

Ferry, N., Barnier, B., Garric, G., Haines, K., Masina, S., Parent, L., Storto, A., Valdivieso, M., Guinehut, S., and Mulet, S.: NEMO: the modeling engine of global ocean reanalyses, Mercator-Ocean Quart. Newslett., 46, 46–59, 2012a. a

Ferry, N., Parent, L., Garric, G., Bricaud, C., Testut, C. E., Le Galloudec, O., Lellouche, J. M., Drevillon, M., Greiner, E., Barnier, B., Molines, J. M., Jourdain, N., Guinehut, S., Cabanes, C., and Zawadzki, L.: GLORYS2V1 global ocean reanalysis of the altimetric era (1992–2009) at meso scale, Mercator Ocean-Quart. Newslett., 44, 28–39, 2012b. a, b, c

Francis, J. A., Vavrus, S. J., and Cohen, J.: Amplified Arctic warming and mid-latitude weather: new perspectives on emerging connections, Wiley Interdisciplin. Rev.: Clim. Change, 8, e474, https://doi.org/10.1002/wcc.474, 2017. a

Ganachaud, A. and Wunsch, C.: Improved estimates of global ocean circulation, heat transport and mixing from hydrographic data, Nature, 408, 453–457, 2000. a

Ganachaud, A. and Wunsch, C.: Large-scale ocean heat and freshwater transports during the World Ocean Circulation Experiment, J. Climate, 16, 696–705, 2003. a

Gastineau, G. and Frankignoul, C.: Influence of the North Atlantic SST variability on the atmospheric circulation during the twentieth century, J. Climate, 28, 1396–1416, 2015. a

Gelaro, R., McCarty, W., Suárez, M. J., Todling, R., Molod, A., Takacs, L., Randles, C. A., Darmenov, A., Bosilovich, M. G., Reichle, R., Wargan, K., Coy, L., Cullather, R., Draper, C., Akella, S., Buchard, V., Conaty, A., da Silva, A. M., Gu, W., Kim, G.-K., Koster, R., Lucchesi, R., Merkova, D., Nielsen, J. E., Partyka, G., Pawson, S., Putman, W., Rieneckera, M., Schuberta, S. D., Sienkiewicza, M., and Zhao, B.: The modern-era retrospective analysis for research and applications, version 2 (MERRA-2), J. Climate, 30, 5419–5454, 2017. a, b, c, d, e

Gent, P. R. and Mcwilliams, J. C.: Isopycnal mixing in ocean circulation models, J. Phys. Oceanogr., 20, 150–155, 1990. a, b

Gimeno-Sotelo, L., Nieto, R., Vázquez, M., and Gimeno, L.: The role of moisture transport for precipitation in the inter-annual and inter-daily fluctuations of the Arctic sea ice extension, Earth Syst. Dynam., 10, 121–133, https://doi.org/10.5194/esd-10-121-2019, 2019. a

Goosse, H., Kay, J. E., Armour, K. C., Bodas-Salcedo, A., Chepfer, H., Docquier, D., Jonko, A., Kushner, P. J., Lecomte, O., Massonnet, F., Park, H. S., Pithan, F., Svensson, G., and Vancoppenolle, M. : Quantifying climate feedbacks in polar regions, Nat. Commun., 9, 1919, https://doi.org/10.1038/s41467-018-04173-0, 2018. a

Graversen, R. G.: Do changes in the midlatitude circulation have any impact on the Arctic surface air temperature trend?, J. climate, 19, 5422–5438, 2006. a, b, c, d, e, f, g

Graversen, R. G. and Burtu, M.: Arctic amplification enhanced by latent energy transport of atmospheric planetary waves, Q. J. Roy. Meteorol. Soc., 142, 2046–2054, 2016. a, b, c

Graversen, R. G., Källén, E., Tjernström, M., and Körnich, H.: Atmospheric mass-transport inconsistencies in the ERA-40 reanalysis, Q. J. Roy. Meteorol. Soc., 133, 673–680, 2007. a

Graversen, R. G., Mauritsen, T., Tjernström, M., Källén, E., and Svensson, G.: Vertical structure of recent Arctic warming, Nature, 451, 53–56, 2008. a, b, c, d

Hall, M. M. and Bryden, H. L.: Direct estimates and mechanisms of ocean heat transport, Deep-Sea Res. Pt. A, 29, 339–359, 1982. a, b

Harada, Y., Kamahori, H., Kobayashi, C., Endo, H., Kobayashi, S., Ota, Y., Onoda, H., Onogi, K., Miyaoka, K., and Takahashi, K.: The JRA-55 Reanalysis: Representation of atmospheric circulation and climate variability, J. Meteorol. Soc. Jpn. Ser. II, 94, 269–302, 2016. a, b

Johns, W. E., Baringer, M. O., Beal, L. M., Cunningham, S. A., Kanzow, T., Bryden, H. L., Hirschi, J. J. M., Marotzke, J., Meinen, C. S., Shaw, B., and Curry, R.: Continuous, array-based estimates of Atlantic Ocean heat transport at 26.5 N, J. Climate, 24, 2429–2449, 2011. a, b

Jourdan, D., Balopoulos, E., Garcia-Fernandez, M.-J., and Maillard, C.: Objective analysis of temperature and salinity historical data set over the Mediterranean Basin, in: IEEE OCEANS'98 Conference Proceedings, vol. 1, 28 September–1 October 1998, Nice, France, 82–87, 1998. a

Jungclaus, J. H. and Koenigk, T.: Low-frequency variability of the arctic climate: the role of oceanic and atmospheric heat transport variations, Clim. Dynam., 34, 265–279, 2010. a, b, c, d, e, f, g, h, i, j

Kapsch, M.-L., Graversen, R. G., and Tjernström, M.: Springtime atmospheric energy transport and the control of Arctic summer sea-ice extent, Nat. Clim. Change, 3, 744–748, 2013. a, b, c, d, e

Karspeck, A. R., Stammer, D., Köhl, A., Danabasoglu, G., Balmaseda, M., Smith, D. M., Fujii, Y., Zhang, S., Giese, B., Tsujino, H., and Rosati, A.: Comparison of the Atlantic meridional overturning circulation between 1960 and 2007 in six ocean reanalysis products, Clim. Dynam., 49, 957–982, 2017. a

Kobayashi, S., Ota, Y., Harada, Y., Ebita, A., Moriya, M., Onoda, H., Onogi, K., Kamahori, H., Kobayashi, C., Endo, H., Miyaoka, K., and Takahashi, K.: The JRA-55 reanalysis: General specifications and basic characteristics, J. Meteorol. Soc. Jpn. Ser. II, 93, 5–48, 2015. a

Levitus, S., Boyer, T., Conkright, M., O'brien, T., Antonov, J., Stephens, C., Stathoplos, L., Johnson, D., and Gelfeld, R.: NOAA Atlas NESDIS 18, World Ocean Database 1998: vol. 1: Introduction, US Government Printing Office, Washington, D.C., 346 pp., 1998. a

Lian, M. and Cess, R.: Energy balance climate models: A reappraisal of ice-albedo feedback, J. Atmos. Sci., 34, 1058–1062, 1977. a

Lindsay, R., Wensnahan, M., Schweiger, A., and Zhang, J.: Evaluation of seven different atmospheric reanalysis products in the Arctic, J. Climate, 27, 2588–2606, 2014. a

Liu, Y.: Meridional Energy Transport Analyzer (META), https://doi.org/10.5281/zenodo.3609505, 2020. a

Lozier, M. S., Li, F., Bacon, S., Bahr, F., Bower, A. S., Cunningham, S. A., De Jong, M. F., De Steur, L., Deyoung, B., Fischer, J., Gary, S. F., Greenan, B. J. W., Holliday, N. P., Houk, A., Houpert, L., Inall, M. E., Johns, W. E., Johnson, H. L., Johnson, C., Karstensen, J., Koman, G., Le Bras, I. A., Lin, X., Mackay, N., Marshall, D. P., Mercier. H., Oltmanns, M., Pickart, R. S., Ramsey, A. L., Rayner, D., Straneo, F., Thierry, V., Torres, D. J., Williams, R. G., Wilson, C., Yang, J., Yashayaev, I., and Zhao, J.: A sea change in our view of overturning in the subpolar North Atlantic, Science, 363, 516–521, 2019. a, b, c

Madec, G.: NEMO reference manual, ocean dynamic component: NEMO-OPA, Note du Pôle modélisation, Inst. Pierre Simon Laplace, France, 2008. a, b

Marzocchi, A., Hirschi, J. J.-M., Holliday, N. P., Cunningham, S. A., Blaker, A. T., and Coward, A. C.: The North Atlantic subpolar circulation in an eddy-resolving global ocean model, J. Mar. Syst., 142, 126–143, 2015. a

Masina, S., Storto, A., Ferry, N., Valdivieso, M., Haines, K., Balmaseda, M., Zuo, H., Drevillon, M., and Parent, L.: An ensemble of eddy-permitting global ocean reanalyses from the MyOcean project, Clim. Dynam., 49, 813–841, 2017. a

Mayer, M. and Haimberger, L.: Poleward atmospheric energy transports and their variability as evaluated from ECMWF reanalysis data, J. Climate, 25, 734–752, 2012. a, b, c

Mayer, M., Haimberger, L., Pietschnig, M., and Storto, A.: Facets of Arctic energy accumulation based on observations and reanalyses 2000–2015, Geophys. Res. Lett., 43, 10–420, 2016. a

Mayer, M., Haimberger, L., Edwards, J. M., and Hyder, P.: Toward consistent diagnostics of the coupled atmosphere and ocean energy budgets, J. Climate, 30, 9225–9246, 2017. a, b, c, d

Mayer, M., Tietsche, S., Haimberger, L., Tsubouchi, T., Mayer, J., and Zuo, H.: An improved estimate of the coupled Arctic energy budget, J. Climate, 32, 7915–7934, 2019. a

McCarthy, G., Smeed, D., Johns, W., Frajka-Williams, E., Moat, B., Rayner, D., Baringer, M., Meinen, C., Collins, J., and Bryden, H.: Measuring the Atlantic meridional overturning circulation at 26 N, Prog. Oceanogr., 130, 91–111, 2015. a, b, c, d

Miller, G. H., Alley, R. B., Brigham-Grette, J., Fitzpatrick, J. J., Polyak, L., Serreze, M. C., and White, J. W.: Arctic amplification: can the past constrain the future?, Quaternary Sci. Rev., 29, 1779–1790, 2010. a

Moat, B. I., Josey, S. A., Sinha, B., Blaker, A. T., Smeed, D. A., McCarthy, G. D., Johns, W. E., Hirschi, J. M., Frajka‐Williams, E., Rayner, D., Duchez, A., and Coward, A. C.: Major variations in subtropical North Atlantic heat transport at short (5 day) timescales and their causes, J. Geophys. Res.-Oceans, 121, 3237–3249, 2016. a, b, c

Mogensen, K., Balmaseda, M. A., and Weaver, A.: The NEMOVAR ocean data assimilation system as implemented in the ECMWF ocean analysis for System 4, European Centre for Medium-Range Weather Forecasts, Toulouse, France, 2012. a

Molod, A., Takacs, L., Suarez, M., and Bacmeister, J.: Development of the GEOS-5 atmospheric general circulation model: evolution from MERRA to MERRA2, Geosci. Model Dev., 8, 1339–1356, https://doi.org/10.5194/gmd-8-1339-2015, 2015. a

Nummelin, A., Li, C., and Hezel, P. J.: Connecting ocean heat transport changes from the midlatitudes to the Arctic Ocean, Geophys. Res. Lett., 44, 1899–1908, 2017. a

Oltmanns, M., Karstensen, J., and Fischer, J.: Increased risk of a shutdown of ocean convection posed by warm North Atlantic summers, Nat. Clim. Change, 8, 300–304, 2018. a

Onarheim, I. H., Eldevik, T., Årthun, M., Ingvaldsen, R. B., and Smedsrud, L. H.: Skillful prediction of Barents Sea ice cover, Geophys. Res. Lett., 42, 5364–5371, 2015. a

Oort, A. H. and Vonder Haar, T. H.: On the observed annual cycle in the ocean-atmosphere heat balance over the Northern Hemisphere, J. Phys. Oceanogr., 6, 781–800, 1976. a

Outten, S., Esau, I., and Otterå, O. H.: Bjerknes Compensation in the CMIP5 Climate Models, J. Climate, 31, 8745–8760, 2018. a, b

Overland, J., Francis, J. A., Hall, R., Hanna, E., Kim, S.-J., and Vihma, T.: The melting Arctic and midlatitude weather patterns: Are they connected?, J. Climate, 28, 7917–7932, 2015. a

Overland, J. E.: A difficult Arctic science issue: Midlatitude weather linkages, Polar Science, 10, 210–216, 2016. a, b

Peixoto, J. P. and Oort, A. H.: Physics of climate, American Institute of Physics, USA, 520 pp., ISBN 0883187124, 9780883187128, 1992. a

Putman, W. M. and Lin, S. J.: Finite-volume transport on various cubed-sphere grids, J. Comput. Phys., 227, 55–78, 2007. a

Riser, S. C., Freeland, H. J., Roemmich, D., Wijffels, S., Troisi, A., Belbéoch, M., Gilbert, D., Xu, J., Pouliquen, S., Thresher, A., Traon, P. L., Maze, G., Klein, B., Ravichandran, M., Grant, F., Poulain, P., Suga, T., Lim, B., Sterl, A., Sutton, P., Mork, K., Vélez-Belchí, P. J., Ansorge, I., King, B., Turton, J., Baringer, M., and Jayne, S. R.: Fifteen years of ocean observations with the global Argo array, Nat. Clim. Change, 6, 145–153, 2016. a

Sandø, A., Gao, Y., and Langehaug, H.: Poleward ocean heat transports, sea ice processes, and Arctic sea ice variability in NorESM1-M simulations, J. Geophys. Res.-Oceans, 119, 2095–2108, 2014. a

Schauer, U. and Beszczynska-Möller, A.: Problems with estimation and interpretation of oceanic heat transport – conceptual remarks for the case of Fram Strait in the Arctic Ocean, Ocean Sci., 5, 487–494, https://doi.org/10.5194/os-5-487-2009, 2009. a

Screen, J. A. and Francis, J. A.: Contribution of sea-ice loss to Arctic amplification is regulated by Pacific Ocean decadal variability, Nat. Clim. Change, 6, 856–860, 2016. a

Serreze, M. C. and Barry, R. G.: Processes and impacts of Arctic amplification: A research synthesis, Global Planet. Change, 77, 85–96, 2011. a, b

Shaffrey, L. and Sutton, R.: Bjerknes compensation and the decadal variability of the energy transports in a coupled climate model, J. Climate, 19, 1167–1181, 2006. a

Simmons, A., Poli, P., Dee, D., Berrisford, P., Hersbach, H., Kobayashi, S., and Peubey, C.: Estimating low-frequency variability and trends in atmospheric temperature using ERA-Interim, Q. J. Roy. Meteorol. Soc., 140, 329–353, 2014. a

Simmons, A., Berrisford, P., Dee, D., Hersbach, H., Hirahara, S., and Thépaut, J.-N.: A reassessment of temperature variations and trends from global reanalyses and monthly surface climatological datasets, Q. J. Roy. Meteorol. Soc., 143, 101–119, 2017. a

Smeed, D. A., McCarthy, G. D., Cunningham, S. A., Frajka-Williams, E., Rayner, D., Johns, W. E., Meinen, C. S., Baringer, M. O., Moat, B. I., Duchez, A., and Bryden, H. L.: Observed decline of the Atlantic meridional overturning circulation 2004–2012, Ocean Sci., 10, 29–38, https://doi.org/10.5194/os-10-29-2014, 2014. a

Steele, M., Morley, R., and Ermold, W.: PHC: A global ocean hydrography with a high-quality Arctic Ocean, J. Climate, 14, 2079–2087, 2001. a

Stepanov, V. N. and Haines, K.: Mechanisms of Atlantic Meridional Overturning Circulation variability simulated by the NEMO model, Ocean Sci., 10, 645–656, https://doi.org/10.5194/os-10-645-2014, 2014. a

Susan Lozier, M., Bacon, S., Bower, A. S., Cunningham, S. A., Femke de Jong, M., De Steur, L., deYoung, B., Fischer, J., Gary, S. F., Greenan, B. J., Heimbach, P., Holliday, N. P., Houpert, L., Inall, M. E., Johns, W. E., Johnson, H. L., Karstensen, J., Li, F., Lin, X., Mackay, N., Marshall, D. P., Mercier, H., Myers, P. G., Pickart, R. S., Pillar, H. R., Straneo, F., Thierry, V., Weller, R. A., Williams, R. G., Wilson, C., Yang, J., Zhao, J., and Zika, Z. D.: Overturning in the Subpolar North Atlantic Program: A new international ocean observing system, B. Am. Meteorol. Soc., 98, 737–752, 2017. a, b

Svendsen, L., Keenlyside, N., Bethke, I., Gao, Y., and Omrani, N.-E.: Pacific contribution to the early twentieth-century warming in the Arctic, Nat. Clim. Change, 8, 793–797, 2018. a

Trenberth, K. E.: Climate diagnostics from global analyses: Conservation of mass in ECMWF analyses, J. Climate, 4, 707–722, 1991. a, b, c, d, e

Trenberth, K. E. and Caron, J. M.: Estimates of meridional atmosphere and ocean heat transports, J. Climate, 14, 3433–3443, 2001. a, b, c, d

Trenberth, K. E. and Fasullo, J. T.: An observational estimate of inferred ocean energy divergence, J. Phys. Oceanogr., 38, 984–999, 2008. a

Trenberth, K. E. and Fasullo, J. T.: Applications of an Updated Atmospheric Energetics Formulation, J. Climate, 31, 6263–6279, 2018. a

Trenberth, K. E. and Solomon, A.: The global heat balance: Heat transports in the atmosphere and ocean, Clim. Dynam., 10, 107–134, 1994. a, b

Trenberth, K. E., Stepaniak, D. P., and Caron, J. M.: Accuracy of atmospheric energy budgets from analyses, J. Climate, 15, 3343–3360, 2002. a, b

Uotila, P., Goosse, H., Haines, K., Chevallier, M., Barthélemy, A., Bricaud, C., Carton, J., Fučkar, N., Garric, G., Iovino, D., Kauker, F., Korhonen, M., Lien, V. S., Marnela, M., Massonnet, F., Mignac, D., Peterson, K. A., Sadikni, R., Shi, L., Tietsche, S., Toyoda, T., Xie, J., and Zhang, J.: An assessment of ten ocean reanalyses in the polar regions, Clim. Dynam., 52, 1613–1650, 2018. a

Uppala, S. M., Kållberg, P., Simmons, A., Andrae, U., Bechtold, V. D. C., Fiorino, M., Gibson, J., Haseler, J., Hernandez, A., Kelly, G., Li, X., Onogi, K., Saarinen, S., Sokka, N., Allan, R. P., Andersson, E., Arpe, K., Balmaseda, M. A., Beljaars, A. C. M., Van De Berg, L., Bidlot, J., Bormann, N., Caires, S., Chevallier, F., Dethof, A., Dragosavac, M., Fisher, M., Fuentes, M., Hagemann, S., Hólm, E., Hoskins, B. J., Isaksen, L., Janssen, P. A. E. M., Jenne, R., Mcnally, A. P., Mahfouf, J. F., Morcrette, J. J., Rayner, N. A., Saunders, R. W., Simon, P., Sterl, A., Trenberth, K. E., Untch, A., Vasiljevic, D., Viterbo, P., and Woolen, J.: The ERA-40 re-analysis, Q. J. Roy. Meteorol. Soc., 131, 2961–3012, 2005. a

van der Linden, E. C., Bintanja, R., Hazeleger, W., and Graversen, R. G.: Low-frequency variability of surface air temperature over the Barents Sea: causes and mechanisms, Clim. Dynam., 47, 1247–1262, 2016. a, b, c

Van der Swaluw, E., Drijfhout, S., and Hazeleger, W.: Bjerknes compensation at high northern latitudes: The ocean forcing the atmosphere, J. Climate, 20, 6023–6032, 2007. a, b, c, d, e, f, g, h, i

Vonder Haar, T. H. and Oort, A. H.: New estimate of annual poleward energy transport by Northern Hemisphere oceans, J. Phys. Oceanogr., 3, 169–172, 1973. a

von Schuckmann, K., Le Traon, P.-Y., Smith, N., Pascual, A., Brasseur, P., Fennel, K., Djavidnia, S., Aaboe, S., Fanjul, E. A., Autret, E., Axell, L., Aznar, R., Benincasa, M., Bentamy, A., Boberg, F., Bourdallé-Badie, R., Nardelli, B. B., Brando, V. E., Bricaud, C., Breivik, L., Brewin, R. J. W., Capet, A., Ceschin, A., Ciliberti, S., Cossarini, G., de Alfonso, M., Collar, A. P., de Kloe, J., Deshayes, J., Desportes, C., Drévillon, M., Drillet, Y., Droghei, R., Dubois, C., Embury, O., Etienne, H., Fratianni, C., Lafuente, J. G., Sotillo, M. G., Garric, G., Gasparin, F., Gerin, F., Good, S., Gourrion, J., Grégoire, M., Greiner, E., Guinehut, S., Gutknecht, E., Hernandez, F., Hernandez, O., Høyer, J., Jackson, L., Jandt, S., Josey, S., Juza, M., Kennedy, J., Kokkini, Z., Korres, G., Kõuts, M., Lagemaa, P., Lavergne, T., Cann, B. I., Legeais, J.-F., Lemieux-Dudon, B., Levier, B., Lien, V., Maljutenko, I., Manzano, F., Marcos, M., Marinova, V., Masina, S., Mauri, E., Mayer, M., Melet, A., Mélin, F., Meyssignac, B., Monier, M., Müller, M., Mulet, S., Naranjo, C., Notarstefano, G., Paulmier, A., Gomez, B. P., Gonzalez, I. P., Peneva, E., Perruche, C., Peterson, K. A., Pinardi, N., Pisano, A., Pardo, S., Poulain, P.-M., Raj, R. P., Raudsepp, U., Ravdas, M., Reid, R., Rio, M.-H., Salon, S., Samuelsen, A., Sammartino, M., Sammartino, S., Sandø, A. B., Santoleri, R., Sathyendranath, S., She, J., Simoncelli, S., Solidoro, C., Stoffelen, A., Storto, A., Szerkely, T., Tamm, S., Tietsche, S., Tinker, J., Tintore, J., Trindade, A., van Zanten, D., Vandenbulcke, L., Verhoef, A., Verbrugge, N., Viktorsson, L., von Schuckmann, K., Wakelin, S. L., Zacharioudaki, A., and Zuo, H.: Copernicus marine service ocean state report, J. Operat. Oceanogr., 11, S1–S142, 2018. a

Wunsch, C.: The total meridional heat flux and its oceanic and atmospheric partition, J. Climate, 18, 4374–4380, 2005. a, b

Yang, X.-Y., Fyfe, J. C., and Flato, G. M.: The role of poleward energy transport in Arctic temperature evolution, Geophys. Res. Lett., 37, L14803, https://doi.org/10.1029/2010GL043934, 2010. a

Zhang, R.: Mechanisms for low-frequency variability of summer Arctic sea ice extent, P. Natl. Acad. Sci. USA, 112, 4570–4575, https://doi.org/10.1073/pnas.1422296112, 2015. a

Zheng, Y. and Giese, B. S.: Ocean heat transport in simple ocean data assimilation: Structure and mechanisms, J. Geophys. Res.-Oceans, 114, C11009, https://doi.org/10.1029/2008JC005190, 2009. a, b