The energy balance over land and oceans: an assessment based on direct observations and CMIP5 climate models
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- Wild, M., Folini, D., Hakuba, M.Z. et al. Clim Dyn (2015) 44: 3393. doi:10.1007/s00382-014-2430-z
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The energy budgets over land and oceans are still afflicted with considerable uncertainties, despite their key importance for terrestrial and maritime climates. We evaluate these budgets as represented in 43 CMIP5 climate models with direct observations from both surface and space and identify substantial biases, particularly in the surface fluxes of downward solar and thermal radiation. These flux biases in the various models are then linearly related to their respective land and ocean means to infer best estimates for present day downward solar and thermal radiation over land and oceans. Over land, where most direct observations are available to constrain the surface fluxes, we obtain 184 and 306 Wm−2 for solar and thermal downward radiation, respectively. Over oceans, with weaker observational constraints, corresponding estimates are around 185 and 356 Wm−2. Considering additionally surface albedo and emissivity, we infer a surface absorbed solar and net thermal radiation of 136 and −66 Wm−2 over land, and 170 and −53 Wm−2 over oceans, respectively. The surface net radiation is thus estimated at 70 Wm−2 over land and 117 Wm−2 over oceans, which may impose additional constraints on the poorly known sensible/latent heat flux magnitudes, estimated here near 32/38 Wm−2 over land, and 16/100 Wm−2 over oceans. Estimated uncertainties are on the order of 10 and 5 Wm−2 for most surface and TOA fluxes, respectively. By combining these surface budgets with satellite-determined TOA budgets we quantify the atmospheric energy budgets as residuals (including ocean to land transports), and revisit the global mean energy balance.
KeywordsGlobal energy balanceRadiation budgetGlobal climate modelsSurface and satellite observationsCMIP5
The energy balance of the Earth is a fundamental determinant of the climatic conditions on our planet. Thanks to impressive progress in space-based observation systems in the past decade, we now know the exchanges of radiative energy flows between our planet and surrounding space with unprecedented accuracy. This has enabled detailed assessments of the radiation budgets at the top of atmosphere (TOA) in climate models (e.g., Potter and Cess 2004; Trenberth and Fasullo 2010; Wang and Su 2013; Dolinar et al. 2014). However, the distribution of the radiative energy within the climate system has not been established with the same accuracy, since it cannot be directly measured from satellites. Accordingly, estimates on the magnitude of the energy balance components at the surface and within the atmosphere as presented in the literature largely vary even on a global annual mean basis (e.g., Budyko 1956; Hartmann et al. 1986; Ramanathan 1987; Ohmura and Gilgen 1993; Kiehl and Trenberth 1997; Wild et al. 1998; Hatzianastassiou et al. 2005; Trenberth et al. 2009; Stephens et al. 2012; Stevens and Schwartz 2012; Wild et al. 2013a; Trenberth and Fasullo 2012). Also the surface radiation budgets as represented in climate models thus traditionally largely differ (e.g., Wild et al. 1995b, 2013a; Wild 2008; Stephens et al. 2012; Li et al. 2013).
As in Wild et al. (2013a), the approach taken here relies on a combination of direct observations and modeling results performed within the Coupled Model Intercomparison Project Phase 5 (CMIP5) for the latest 5th IPCC assessment report (IPCC-AR5). This goes along with a validation of the land and ocean energy budgets of the comprehensive set of climate models that is now available in the CMIP5 archive. Compared to Wild et al. (2013a) more than twice the number of climate models were available in the CMIP5 archive for the present study.
Emphasis in the present study is placed on the land surface energy balance, which is best constrained by direct surface observations, since the vast majority of direct flux measurements are taken over land surfaces. In addition and for completeness, an attempt is made to derive estimates for the energy balance components averaged over oceans, which are consistent with the land mean energy balance derived here and the global mean energy balance derived in Wild et al. (2013a), as well as with the limited information from direct observations taken in maritime environments. We further discuss our estimates in light of other recent land and ocean-separated estimates relying on independent approaches based on reanalyses and satellite products, to assess the consistency and robustness of these recent independent estimates. Finally, we recompose the global mean energy balance by combining the land and ocean mean energy balances derived here, to check its consistency with our previously published global estimates (Wild et al. 2013a, b).
Section 2 describes the observational data and climate models used in this study. Section 3 discusses the energy balance over land as simulated in the CMIP5 models, and infers best estimates for its components. Section 4 focuses on the energy balance over oceans. Section 5 reassembles the global mean energy balance from the land and ocean mean energy balances. Section 6 summarizes the main findings of this study.
2 Observational data and models
As in Wild et al. (2013a), the observational reference values for the radiative fluxes at the TOA are taken from the spaceborne Clouds and the Earth’s Radiant Energy System (CERES, Wielicki et al. 1996), but now separated into fluxes over land and oceans. CERES measures filtered radiances in the solar (between 0.3 and 5 μm), total (0.3 and 200 μm), and window (8 and 12 μm) regions on board of the NASA satellites Terra and Aqua, with thermal radiances determined as differences between total and solar channel radiances. The uncertainty in the solar reflected TOA fluxes from CERES due to uncertainty in absolute calibration is ~2 % (2 − σ), or equivalently 2 Wm−2. The uncertainty of the outgoing thermal flux at the TOA as measured by CERES due to calibration is ~3.7 W m−2 (2 − σ) (Loeb et al. 2009). In the CERES energy balanced and filled (EBAF) dataset, solar and thermal TOA fluxes are adjusted within their range of uncertainty to be consistent with independent estimates of the global heating rate based upon in situ ocean observations, and are made available on a 1° grid (Loeb et al. 2009). We calculated global land and ocean averages of the TOA radiative flux components from CERES EBAF for the periods 2001–2005 and 2001–2010, based on version EBAF 2.7 (Loeb et al. 2012), using a 10′ land-sea mask provided by CERES. We include in the global land budget Greenland and Antarctica as well as the ice shelves, whereas sea ice and inland seas are considered in the ocean budgets. This applies for all variables and results discussed in this study.
The land and ocean mean TOA reference fluxes determined this way for the period 2001–2005 are found to be within a few tenths of a W/m−2 as compared to the same quantities averaged over the period 2000–2010, the entire period now available from CERES EBAF (c.f. also Trenberth et al. 2014). Thus the exact length of the CERES EBAF record is not very critical for the present purpose of determining climatological land and ocean mean budgets. In sensitivity tests with different available land sea masks, we noted that differences up to 1 Wm−2 in the land and ocean averaged TOA insolation can emerge depending on whether floating ice shelve areas (predominantly in Antarctica) are considered as land or ocean. We define them here as land areas. Differences in the definition of fractional land/sea boxes along coastlines were found to cause differences of no more than a few tenth of a W/m−2 at the maximum in the land and ocean mean TOA insolation, whereas adding or dismissing interior lakes in the land-sea mask has a negligible impact on this quantity.
Observational constraints for surface fluxes primarily stem from two databases for worldwide measurements of radiative fluxes at the Earth surface, the global energy balance archive (GEBA, Gilgen et al. 1998; Ohmura et al. 1989) and the database of the Baseline Surface Radiation Network (BSRN, Ohmura et al. 1998; König-Langlo et al. 2013). GEBA, maintained at ETH Zurich, is a database for the worldwide measured energy fluxes at the Earth’s surface and currently contains 2500 stations with 450‘000 monthly mean values of various surface energy balance components. By far the most widely measured quantity is the solar radiation incident at the Earth’s surface, with many of the records extending back to the 1950s, 1960s or 1970s. This quantity is also known as global radiation, and is referred to here as downward solar radiation. Gilgen et al. (1998) estimated the relative random error (root mean square error/mean) of the downward solar radiation values at 5 % for the monthly means and 2 % for yearly means.
BSRN became operational in the early 1990s and provides radiation measurements with the highest available accuracy and high temporal resolution of 1 min at a limited number of sites in various climate zones. To date 54 anchor sites exposed to different climate regimes report their data to the BSRN Archive at the Alfred Wegener Institute (AWI) (http://www.bsrn.awi.de/). The accuracy of the BSRN solar and thermal radiation measurements used in this study is discussed in detail in Wild et al. (2013a).
At oceans surfaces, downward solar and thermal radiation is increasingly recorded from measurements on buoys with sensors that compose the Improved Meteorological (IMET) system (Colbo and Weller 2009). The quality of these unmanned sites is, however, not at the level of the BSRN measurements. Records are typically still fairly short, covering a few years only. For downward solar radiation, 48 buoys provide data that enable the determination of at least one monthly mean for each month of the year, thus allowing for the calculation of annual means from complete annual cycles and excluding the risk of spurious biases due to incomplete seasonal cycles. Out of these 48 buoys, 17 buoys stem from the Prediction and Research Moored Array in the Tropical Atlantic (PIRATA) (Bourles et al. 2008), 18 buoys from the Tropical Atmosphere Ocean/Triangle Trans-Ocean Buoy Network (TAO/TRITON) in the Tropical Pacific (McPhaden et al. 1998), 10 buoys from the Research Moored Array for African–Asian–Australian Monsoon Analysis and Prediction (RAMA) in the Indian Ocean (McPhaden et al. 2009), and three buoys from the Woods Hole Oceanographic Institution, located in the Northwest Tropical Atlantic (15°N, 51°W), East Tropical Pacific (20°S, 85°W, off northern Chile) and north of Hawaii, respectively (Colbo and Weller 2009). We further excluded 5 buoys from the PIRATA network, whose measurements were shown to be biased low due to the contamination of the domes of the radiometers with dust (Foltz et al. 2013), leaving a total of 43 buoy sites for the analysis of solar radiation. From the 53 buoys measuring the downward thermal radiation at the above networks, only 17 buoys fulfill the criterion of providing a complete annual cycle. These stem from PIRATA (2 buoys), RAMA (2 buoys), TAO/TRITON (9 buoys), and Woods Hole (3 buoys). The uncertainty of these buoy measurements is estimated at 5–6 Wm−2 for annual mean downward solar and 4 Wm−2 for annual mean thermal radiation (Colbo and Weller 2009).
Brief listing of the 43 models used in this study, together with their abbreviations, host institutions and horizontal resolution
Commonwealth Scientific and Industrial Research Organization (CSIRO) and Bureau of Meteorology (BOM), Australia
1.88° × 1.24°
1.88° × 1.24°
Beijing Climate Center, China Meteorological Administration
2.81° × 2.81°
1.13° × 1.13°
College of Global Change and Earth System Science, Beijing Normal University
2.81° × 2.81°
Canadian Centre for Climate Modelling and Analysis
2.81° × 2.81°
National Center for Atmospheric Research
1.25° × 0.94°
Community Earth System Model Contributors
1.25° × 0.94°
1.25° × 0.94°
2.50° × 1.88°
1.25° × 0.94°
2.50° × 1.88°
Centro Euro-Mediterraneo per I Cambiamenti Climatici
3.75° × 3.75°
0.75° × 0.75°
1.88° × 1.88°
Centre National de Recherches Meteorologiques/Centre Europeen de Recherche et Formation Avancees en Calcul Scientifique
1.41° × 1.41°
Commonwealth Scientific and Industrial Research Organization in collaboration with Queensland Climate Change Centre of Excellence
1.88° × 1.88°
LASG, Institute of Atmospheric Physics, Chinese Academy of Sciences and CESS,Tsinghua University
2.81° × 3.00°
NOAA Geophysical Fluid Dynamics Laboratory
2.50° × 2.00°
2.50° × 2.00°
2.50° × 2.00°
NASA Goddard Institute for Space Studies
2.50° × 2.00°
2.50° × 2.00°
2.50° × 2.00°
Met Office Hadley Centre
3.75° × 3.47°
1.88° × 1.24°
1.88° × 1.24°
Institute for Numerical Mathematics
2.00° × 1.50°
Institut Pierre-Simon Laplace
3.75° × 1.88°
2.50° × 1.26°
3.75° × 1.88°
Japan Agency for Marine-Earth Science and Technology, Atmosphere and Ocean Research Institute (The University of Tokyo), and National Institute for Environmental Studies
2.81° × 2.81°
2.81° × 2.81°
Atmosphere and Ocean Research Institute (The University of Tokyo), National Institute for Environmental Studies, and Japan Agency for Marine-Earth Science and Technology
0.56° × 0.56°
1.41° × 1.41°
Max Planck Institute for Meteorology
1.88° × 1.88°
1.88° × 1.88°
1.88° × 1.88°
Meteorological Research Institute
1.13° × 1.13°
1.13° × 1.13°
Norwegian Climate Centre
2.50° × 1.88°
2.50° × 1.88°
The GCM radiation budgets representing the conditions at the beginning of the twenty-first century are determined as averages over the five-year period 2000–2004, which state the final five complete years of the historical experiments available from all investigated models. The slight shift in period by 1 year compared to the CERES radiation budgets (2001–2005, see above) is irrelevant for the comparisons since the GCMs are not deterministic by nature, and both ocean and land mean budgets are insensitive to the exact choice of the period as outlined above. Specifically, a shift in the CMIP5 radiation budget climatologies by 1 year typically introduces differences in the tenth of a Wm−2 range only, thus negligible for the accuracy level considered in this study. Similar to the CERES EBAF land and ocean mean budgets, the CMIP5 budgets are calculated using the land-sea masks of the individual GCMs and the Climate Data Operators (CDO) software package (https://code.zmaw.de/projects/cdo).
3 Energy balance over land
3.1 Assessment of land radiation budgets in CMIP5 models
3.1.1 Solar radiation
Simulated energy balance components averaged over land, oceans and the entire globe from 43 CMIP5/IPCC AR5 models at the TOA, atmosphere, and surface
Estimates for land, ocean, and global mean energy balance components in the present and other recent studies
Trenberth et al. (2009)
Root mean square (RMS) and average differences between climatological annual mean downward solar and thermal surface fluxes as calculated in the various CMIP5 models and as observed at GEBA/BSRN sites. Units Wm−2
Downward solar 760 GEBA sites
Downward solar 38 BSRN sites
Downward thermal 41 BSRN sites
Mean of all models
Median of all models
The overestimation of solar radiation incident at the Earth’s surface is a long-standing issue in climate modeling, and is still present in many of the CMIP5 models (see e.g. Wild 2008 for a review and discussion of possible causes).
3.1.2 Thermal radiation
3.2 Best estimates for the downward solar and thermal radiation at land surfaces
Similar to the global mean estimates in Wild et al. (2013a), we also tested the robustness of this land mean estimate, by repeating the analyses using the 38 worldwide distributed BSRN sites instead of the 760 GEBA sites as observational references (Fig. 13). The correlation between the model biases, now determined at the 38 BSRN sites (as given in Fig. 8), and their respective land mean values of downward solar radiation (as given in Fig. 6, upper panel) is again high, at 0.9. The slope of the corresponding linear regression in Fig. 13 deviates slightly more from one than the respective slope when using the 760 GEBA sites, indicative of the lower spatial sampling with the BSRN sites. Still, the best estimate deduced from the linear regression in Fig. 13 using the 38 BSRN sites as reference is very similar to the one obtained with the GEBA sites as references in Fig. 12. With the BSRN sites as reference, the best estimate for the land mean downward solar radiation amounts to 184.0 (±1.6) Wm−2 (2σ uncertainty given in the parentheses), closely matching the 183.7 (±1.8) Wm−2 inferred above based on the GEBA sites. The close agreement, despite entirely different and independent surface reference networks, suggests that the best estimate inferred in this way is fairly robust.
As a conservative uncertainty range for this estimate, we expand the 2σ regression uncertainty range to cover all land mean values calculated by those GCMs which show only marginal biases compared to the surface stations, in line with the conceptual approach applied here that infers land mean estimates from GCMs which show no biases. Land mean estimates from models with no obvious biases against the surface sites strictly cannot be disqualified as being biased in this approach. Thus, in Figs. 12 and 13 we note also land mean downward solar radiation values of 182 and 187 Wm−2 (rounded) which stem from GCMs with marginal biases (defined here as smaller than 1 Wm−2) and thus should be included in the uncertainty range. With this definition, the uncertainty range for the land mean downward solar radiation, encompassing all GCM land mean values as defined above, extends from 182 to 187 Wm−2.
Interestingly, the above estimate for the land mean downward solar radiation around 184 Wm−2 is also nearly identical to the land mean estimate given in Trenberth et al. (2009) of 184.7 Wm−2 derived independently using the International Satellite Cloud Climatology Project (ISCCP FD) surface flux dataset with an adjustment for underestimated water vapor absorption (Kim and Ramanathan 2008), thereby not taking into account in any way the surface observations (Table 3). From the satellite-based surface flux dataset “Surface EBAF Ed2.7” (Kato et al. 2013) we calculated a slightly higher land mean surface downward solar radiation of 186.5 Wm−2 (Table 3), which is within the uncertainty range derived above. This product determines surface irradiances using observational constraints given by the TOA irradiances from CERES, and again, is independently derived from the approach taken here. Compared to Kato et al. (2011), a better treatment of the diurnal cycle in adjusting surface shortwave irradiance significantly reduced the downward solar radiation in this product (Kato et al. 2013; Rutan et al. 2014), which improves the agreement with the present study and Trenberth et al. (2009). ERA-Interim, yet another independent approach based on reanalysis, determines a slightly higher land mean downward solar radiation, at 187.2 Wm−2 (Table 3; Berrisford et al. 2011). The similar estimates obtained by these independent approaches, covering a range of only 3 Wm−2, gives additional confidence that we have now a better handle on the magnitude of the land mean downward solar radiation.
It is further interesting to note that the estimate for land mean downward solar radiation derived here matches its global mean estimate of 184.6 Wm−2 derived in Wild et al. (2013a) to within 1 Wm−2. The close agreement between global and land mean downward solar radiation does not only emerge from the present analysis, but we note this concurrence also in other estimates of the global and land mean energy balance. From Trenberth et al. (2009) we take that their estimates for the global and land mean downward solar radiation, at 184.3 and 184.7 Wm−2, respectively, differ by only 0.4 Wm−2. From the same study we take that also the ISCCP-FD satellite derived land mean surface downward solar radiation differs only by 0.6 Wm−2 from its global mean value. Further, the above-mentioned land mean estimate of 186.5 Wm−2, which we determined from the Surface EBAF Ed2.7 (Kato et al. 2013) differs by only 0.1 Wm−2 from the respective global mean estimate. In terms of reanalyses, we find in Berrisford et al. (2011) that also the ERA-Interim and the ERA-40 show differences of only 0.9 and 1.1 Wm−2 between their global and land mean estimates, respectively. The close similarity between the global and land mean estimates across various independent observation-based estimates gives some trust in the robustness of this finding. It also has implications for the ocean budget discussed in Sect. 4, as the above notion implies a close agreement between land and ocean mean surface downward solar radiation. In the CMIP5 climate models, global and land mean downward solar radiation differ in the multimodel mean by 2.8 Wm−2 (Table 2).
We enlarge also the 2σ regression uncertainty range for this land mean downward thermal radiation estimate, to accept all land mean values from GCMs with marginal (<1 Wm−2) biases. In Fig. 14 land mean values ranging from 302 to 309 Wm−2 fulfill this criterion and form a conservative uncertainty range for this estimate.
The estimate of ERA-Interim is, at 304 Wm−2 (Table 3), very close to the estimate derived here. ERA-Interim includes the Rapid Radiation Transfer Model (RRTM, Mlawer et al. 1997), which was shown to substantially improve the downward thermal fluxes at the surface when included in a climate model (Wild and Roeckner 2006). In addition, reanalyses take into account the possibly best available estimates of atmospheric temperature and humidity profiles at high temporal frequency in their radiative transfer calculations, which further contributes to an accurate determination of the downward thermal radiation. It is interesting to note that also the estimate of Trenberth et al. (2009) (303.6 Wm−2, Table 3), who did not directly determine the magnitude of the downward thermal radiation, but inferred it as a residual of the other surface energy balance components, is close to our best estimate derived here.
3.3 Discussion of the energy balance over land
Figure 2 (upper panel) depicts a schematic representation of the land mean energy balance, which includes the estimates of land-mean downward solar and thermal radiation derived above along with best estimates for the other land energy balance components as discussed in the following.
3.3.1 Radiative components
The most accurate information currently available on the radiative energy exchanges at the TOA over land is compiled in the CERES EBAF Ed2.7 dataset. From this dataset we estimate the TOA land mean downward, upward and net solar radiation at 324.7, −111.4 and 213.3 Wm−2, respectively, and the thermal outgoing radiation at −232.4 Wm−2 (Table 3). All these estimates are averages over the period 2001–2005, with no significant change when averaged over the entire available period 2001–2010. They are displayed in Fig. 2 (upper panel), rounded to integers. Uncertainty ranges for land mean TOA fluxes correspond to those discussed in Wild et al. (2013a) for the global mean fluxes. Note that, in contrast to the global energy balance under equilibrium conditions, in the land energy balance the outgoing thermal radiation is not required to match the absorbed solar radiation at the TOA. Radiative imbalances can be induced by advective exchanges of latent and sensible energy in the atmosphere between the land and ocean domains. According to Table 3 and Fig. 2 (upper panel), the outgoing thermal radiation at the TOA over land is 19 Wm−2 larger than the absorbed solar radiation. This imbalance implies a corresponding net atmospheric energy transport of sensible and latent heat from the ocean to the land surfaces which compensates the net radiative energy loss through the TOA over land surfaces. Comprehensive analyses of the energy transport from ocean to land have been performed by Fasullo and Trenberth (2008a, b) and Trenberth and Fasullo (2013), who identified a strong annual cycle in this quantity, with large energy transport in the northern winter onto land, and small net transport from land to ocean in northern summer. Trenberth and Fasullo (2013) further estimated that latent energy is the dominant component of the annual mean energy transport from ocean to land, i.e. the moisture convergence over land. The required transport of 19 Wm−2 to compensate for the excess thermal emission compared to solar absorption over land according to CERES EBAF is illustrated in Fig. 2 (upper panel), and corresponds, when multiplied with the total land surface area of 149 × 1012 m−2, to a total annual energy transport of 2.8 × 1015 W (2.8 PW), as also determined by Trenberth and Fasullo (2013). This is somewhat higher than the corresponding transport in the ERA Interim reanalysis of 2.5 PW established by Trenberth and Fasullo (2013). Trenberth and Fasullo (2013) inferred the ocean to land energy transport also from a number of other reanalyses and show that they differ in a range close to 1 PW. We use this range to infer a corresponding uncertainty range of 7 Wm−2 for the transport in Fig. 2 (upper panel). The convergence of latent energy over land corresponds to the latent heat release of the excess precipitation formation compared to evaporation over land, which is transported in form of runoff back to the oceans (Trenberth and Fasullo 2013 and references therein). Thus, a net atmospheric transport of energy from oceans to land can be expected from hydrological considerations. The TOA land mean imbalance in the CMIP5 multimodel mean (19.8 Wm−2) differs by less than 1 W from CERES EBAF (Table 2), suggesting that the models overall adequately reproduce the net energy transport from oceans to land on an annual mean basis.
For the solar radiation incident at the land surface in Fig. 2 (upper panel), we take the best estimate of 184 Wm−2 with uncertainty range as defined and derived in Sect. 3.2. As pointed out in Sect. 3.2 the close agreement of recent estimates based on entirely independent approaches enhances our confidence in this estimate. The magnitude of the downward solar radiation traditionally has been a major source of uncertainty, and still shows the largest discrepancies of all energy balance components in the latest (CMIP5) climate model generation (Table 2; Fig. 6, upper panel, Sect. 3.1).
To obtain an estimate for the land mean absorbed solar radiation at the surface, we need in addition information on the (radiation weighted) land surface albedo. The satellite-derived radiation weighted land mean albedo taken from MODIS (Moderate-resolution Imaging Spectroradiometer) amounts to 0.24 (Zhang et al. 2010). The various validation exercises of this albedo product in the literature indicate that the MODIS albedo might be overall slightly too low on the order of 0.02 (see Discussion in Hakuba et al. (2014) and references therein). From the surface solar upward and downward fluxes in Table 2 we infer that the CMIP5 models calculate a multimodel mean radiation weighted land albedo of 0.264. Similarly, from the surface CERES EBAF Ed2.7 product we obtain a land mean albedo estimate of 0.255 (Table 3). From Berrisford et al. (2011) we deduce an albedo of 0.253 and 0.246 for the ERA-Interim and ERA-40 reanalyses, respectively. For the determination of the surface reflected and absorbed solar radiation in Fig. 2 (upper panel), we use a radiation weighted land mean albedo of 0.26 close to the surface CERES EBAF Ed2.7 product, which is near to the median of the different estimates, and currently considered best suited for large scale surface albedo estimates (Crystal Schaaf, personal communication 2014). This gives a (rounded) land mean surface reflected and absorbed solar radiation of 48 and 136 Wm−2, respectively (Fig. 2 upper panel). Uncertainties introduced by the surface albedo estimates, however, remain. Deducing a range of potentially realistic radiation weighted land mean albedo values between 0.24 and 0.27 from the above discussion results in an uncertainty range of 44–50 Wm−2 for the surface reflected solar radiation, and enlarges the uncertainty range of the absorbed compared to the downward surface solar radiation accordingly (Fig. 2, upper panel).
With an absorbed land-mean solar radiation of 136 Wm−2 at the surface and 213 Wm−2 in the total system (TOA solar net), this leaves 77 Wm−2 of solar radiation absorbed within the atmosphere over land surfaces (Table 3; Fig. 2, upper panel). The CMIP5 multi-model mean is, at 70.3 Wm−2, more than 6 Wm−2 lower than the best estimate inferred here. This suggests that in the majority of the models, the atmosphere over land surfaces is not absorptive enough for solar radiation, a feature common to several generations of GCMs.
For the land mean downward thermal radiation in Fig. 2 (upper panel), we use the value of 306 Wm−2 and the uncertainty range as discussed in Sect. 3.2. The predominant part of the downward thermal radiation is absorbed at the surface. However, since the Earth surface is not a perfect blackbody, with a surface absorptivity/emissivity ε somewhat lower than 1, a small part of the downward thermal radiation is reflected upward, namely (1 − ε) times the downward thermal flux. The Earth surface emits radiation according to the Stefan–Boltzman law at εσTskin4, with Tskin representing the surface skin temperature, and σ the Stefan–Boltzman constant (5.67 × 10−8 Wm−2K−4). The total upward thermal flux as shown in Figs. 1 and 2 consists thus of the above-mentioned surface emission plus a small contribution from the reflected part of the downward thermal flux. The upward thermal flux is not overly sensitive to the exact specification of the surface emissivity ε, since compensational changes between reflected downward and surface emitted radiation apply in the upward thermal flux when ε is changed, leading to an only small sensitivity of 0.5 Wm−2 per percent emissivity change (e.g., Kato et al. 2013). Kato et al. (2013) estimated the uncertainty in land surface ε at 3 % based on different datasets, introducing thus an uncertainty of 1.5 Wm−2 in the upward thermal radiation due to the specification of ε alone. For the determination of the land mean surface upward thermal radiation, we consider reanalyses as a useful source. Reanalyses assimilate the observed state of the atmosphere several times per day and determine the fluxes with high temporal frequency to capture also the full diurnal cycle (atmospheric time step of 30 min in the case of ERA-Interim). The assimilation of screen-level temperature observations in the reanalyses further helps to reduce long-term biases in their simulated surface skin temperatures used in the determination of the surface upward thermal radiation (Simmons et al. 2004), although screen and skin temperatures can greatly differ during the course of a day (e.g., Jin and Dickinson 2010). In Berrisford et al. (2011) we note that four different reanalysis products vary in a range of no more than 3 Wm−2 with respect to the land mean surface upward thermal radiation. Specifically, Berrisford et al. (2011) give land mean values for ERA-Interim of 370.6 Wm−2 covering the period 1989–2008, and 371.0 Wm−2 for ERA-40 over the period 1989–2001. Considering an increase of 0.17 Wm−2/year in the land mean surface upward thermal radiation due to global warming (Wild et al. 2008), we apply an upward correction of 1 Wm−2 for the slight shift in the period means between the published ERA values and the early 2000s considered here as reference period. This results in a best estimate of 372 Wm−2 for the land mean surface upward thermal radiation. This value is in between the estimates of 374.4 Wm−2 determined from the surface EBAF Ed2.7 product (Table 3) and the CMIP5 multimodel mean estimate of 370.3 Wm−2 (Table 2), which also define the uncertainty range we attach to this flux in Fig. 2 (upper panel). The land surface temperatures simulated by the CMIP5 models show overall a slight cold bias in the annual mean (Mueller and Seneviratne 2014) which fits to the somewhat lower surface upward thermal radiation in the CMIP5 multimodel mean compared to the above estimates.
3.3.2 Nonradiative components
Most of the radiative energy available at the land surface (70 Wm−2 as estimated above) is used for the terrestrial fluxes of sensible and latent heat. Compared to these fluxes, the additional non-radiative energy balance components, namely ground heat flux and melt, are small (below 1 %) over land on a multiyear average basis (Ohmura 2004). They can be neglected here. The partitioning of the surface net radiation into sensible and latent heat flux over land, largely controlled by the availability of soil water and vegetation characteristics, is afflicted with considerable uncertainties, since very limited reliable observational constraints from surface or spaceborne measurements are available for these fluxes. Accordingly, also the CMIP5 models vary greatly in their calculation of the land mean latent and sensible heat fluxes (Fig. 15, middle and lower panel; Table 2).
Jimenez et al. (2011) estimated the land mean latent heat flux at 45 Wm−2, based on an all-product land mean average of 12 latent heat flux products, including satellite‐based products and estimates from offline land surface models in addition to reanalyses. The spread amongst these estimates amounts to 20 Wm−2. However, their analysis covered only 70 % of the land surfaces, neglecting particularly areas over Greenland and Northern Africa with low latent heat fluxes. Similarly, Mueller et al. (2011) noted in their investigation of a variety of observation-based evaporation datasets as well as climate models from the former CMIP3 model intercomparison project that the land mean latent heat fluxes are scattered around 46 Wm−2 in the various products with a standard deviation of ±5 Wm−2, excluding also Greenland and the Sahara, where latent heat fluxes are generally low. More recently, Mueller et al. (2013) merged 40 datasets of estimated land surface evapotranspiration into different categories (diagnostic datasets, land surface models and reanalyses) and found the merged land mean estimates to vary between 423 mm/year (merged land surface model datasets, corresponding to a latent heat flux of 34 Wm−2) and 563 mm/year (merged reanalysis datasets, corresponding to a latent heat flux of 45 Wm−2). The merging of all available datasets into the LandFlux-EVAL synthesis product gave a land mean evapotranspiration of 493 mm/year, corresponding to a latent heat flux of 40 Wm−2 (Mueller et al. 2013), with a standard deviation of 12 Wm−2. This synthesis product does not include Antarctica. A best estimate of the land mean latent heat flux as defined in the present study (including Antarctica) based on the synthesis product should be therefore slightly below 40 Wm−2. A recent unpublished space-based estimate from the GEWEX LandFlux project uses four different retrieval algorithms for the period 1984–2006 and provides a multimodel mean and standard deviation estimate of 488.4 ± 38.3 mm/year (38.0 ± 3 Wm−2). We adopt this value of 38.0 Wm−2 in Fig. 2 (upper panel), also in line with the LandFlux-EVAL synthesis product estimate as discussed above. This is also close to the land mean latent heat flux estimate given by Trenberth et al. (2009) of 38.5 Wm−2 and near the 40 Wm−2 inferred from the water budget estimates in Trenberth et al. (2007, 2011). The ERA-Interim land mean latent heat flux is somewhat higher, at 44 Wm−2 (Table 3). Berrisford et al. (2011) note, however, that the latent heat flux in ERA-Interim may be overestimated by 9 %, which also favors a land mean latent heat flux in the vicinity of 40 Wm−2. Other reanalyses vary in a range from 38 up to 54 Wm−2 as can be deduced from the water budget analyses of Trenberth et al. (2011). Similarly to ERA-Interim, some of the CMIP5 models tend to overestimate the latent heat fluxes over terrestrial surfaces in the annual mean as evidenced by Mueller and Seneviratne (2014), related to excessive precipitation in these models. The uncertainty range given in Fig. 2 (upper panel) acknowledges the spread between the merged land surface model estimates (low end) and the merged reanalysis datasets (high end) given in Mueller et al. (2013). This range encompasses also most estimates of the CMIP5 models in Fig. 15 (middle panel).
With a land mean surface net radiation of 70 Wm−2 and latent heat flux slightly below 40 Wm−2, this leaves slightly more than 30 Wm−2 for the land mean sensible heat flux as a residual of the land surface energy balance. The estimated residual of 32 Wm−2 for the land mean sensible heat flux in Fig. 2 (upper panel) is close to the multimodel mean CMIP5 estimate of 31.3 Wm−2 (Table 2) which may be slightly biased low doe to excessive precipitation as pointed out above. The land mean sensible heat flux of 32 Wm−2 is higher than the ERA-Interim value of 28.2 Wm−2 (Table 3), but soil moisture is overestimated in ERA-Interim, particularly for dry land, as pointed out in Trenberth and Fasullo (2013) and Albergel et al. (2012), which may cause a low bias in the reanalysis sensible heat flux. The uncertainty in this component is, however, still particularly large, and the CMIP5 model estimates for the land mean sensible heat fluxes show larger ranges and standard deviations than for the corresponding latent heat fluxes, despite their lower absolute magnitudes (Table 2; Fig. 15). This justifies the above determination of the sensible heat flux as a residual in the surface energy balance. Excluding outliers outside two standard deviations, most land mean sensible heat fluxes simulated by the CMIP5 models lie between 25 and 36 Wm−2, which constitutes the uncertainty range attached to the land mean sensible heat flux in Fig. 2 (upper panel). This range encompasses also the various reanalysis estimates, which show a tendency to cluster towards the lower end of the range (Trenberth et al. 2009; Berrisford et al. 2011).
The reduction in the uncertainties related to the partitioning of the surface net radiation into sensible and latent heat over land surfaces remains a major challenge in global energy balance studies.
4 Energy balance over oceans
4.1 Assessment of ocean radiation budgets in CMIP5 models
4.1.1 Solar radiation
At the TOA, the net solar flux averaged over oceans in the CMIP5 multimodel mean (250.8 Wm−2) is again close to the CERES EBAF TOA reference which we determined at 251.7 Wm−2. As over land, no obvious bias in the simulated net solar flux at the TOA can be noted overall over oceans.
From GEBA, we used 20 sites with extended records in maritime environments. These sites include locations on various islands as shown in Fig. 3. Compared to these sites, the multimodel mean is higher by 4.2 Wm−2 on average.
4.1.2 Thermal radiation
From CERES EBAF, we determined an outgoing thermal radiation averaged over oceans at the TOA of 242.9 Wm−2 for the usual period 2001–2005. The associated multimodel mean of the CMIP5 models is 240.9 Wm−2 (Table 2), thus within 2 Wm−2 of the CERES EBAF estimate. At the ocean surface, the flux that can be compared with direct observations is again the downward thermal radiation, shown for the CMIP5 models in Fig. 17 (lower panel). We compared also these fluxes with the 6 BSRN sites considered as representing maritime conditions (Fig. 18b). The overall multimodel mean bias averaged over the 6 sites is marginal, at −0.3 Wm−2. The fluxes at 3 sites are underestimated by the multimodel mean (Bermuda −2.0 Wm−2, Cocos Island −3.1 Wm−2, Nauru −3.6 Wm−2), two sites show biases of less than 1 Wm−2 (Kwajalein 0.5 Wm−2, Manus 0.7 Wm−2), while one site (Chesapeake Lighthouse) shows an overestimation of 6.9 Wm−2. The comparison with the 17 buoy sites with useful thermal measurements (Sect. 2) gave an overall 3.0 Wm−2 lower value for the multimodel mean compared to observations. It has been argued that the lack of shading on the buoy measurements may cause an overestimation of the downward thermal measurements of a similar amount (Wang and Dickinson 2013 and references therein). This would reduce the overall bias similar to the one seen when compared to the BSRN sites. Thus, based on the limited observational evidence from BSRN and buoys, there seems no indication for a large bias of the model-calculated downward thermal fluxes over oceans, if anything, then a small underestimation. Regionally, the simulated multimodel mean fluxes show an almost zero bias at the TAO/TRITON buoys in the Tropical Pacific (Fig. 19b), as already noted with the simulated solar fluxes in this region (Fig. 19a). The simulated downward thermal fluxes overall are lower than the buoy observations in the Eastern Tropical Atlantic (PIRATA), at the RAMA buoys in the Indian Ocean, and at the 3 Woodshole buoys (Fig. 19b).
4.2 Best estimates for the downward solar and thermal radiation at the ocean surface
When the 43 buoy sites instead of the 26 BSRN/FGEBA sites are used as reference, the correlation between the model biases and their ocean means is much weaker (correlation coefficient 0.48), and the regression approach may not be applicable. This indicates, that model differences in downward surface solar radiation over the inner tropical oceans where the buoys are located are not very indicative of their respective ocean mean differences.
Alternatively, a best estimate may be obtained by applying a simple bias correction to the model-calculated ocean mean downward surface solar radiation, by correcting this value with the model bias as obtained when compared to observations. Specifically, taking the multimodel ocean mean downward surface solar radiation of 188.3 Wm−2 (c.f. Table 2), and correcting it with a multimodel mean bias of −3.0 Wm−2 (as obtained when compared to the 69 maritime sites, c.f. Sect. 4.1.1), this results in a best estimate of 185.3 Wm−2.
A best estimate near 185 Wm−2 for the ocean mean downward surface solar radiation seems therefore in least conflict with the limited observational references according to the above analyses. This estimate comes surprisingly close to the estimates given by Trenberth et al. (2009) of 184.4 Wm−2 and the estimate from the surface CERES EBAF dataset which we determined at 186.6 Wm−2 over ocean surfaces. The ocean mean downward surface solar radiation determined by the ERA-Interim reanalysis is 188.4 Wm−2 (Table 3). It is noteworthy that these recent estimates of ocean mean surface downward solar radiation are thus remarkably consistent despite being completely independently derived, and differ by no more than 4 Wm−2. Arguably all these different approaches have their own set of limitations and critically seen may provide no more than indications on the magnitude of this flux over oceans. Yet the sum of these independent lines of evidence and their close agreement overall increases our confidence in the derived flux magnitude.
As noted already in Sect. 3.2, a feature common to many estimates is the close agreement of the land mean, global mean, and thus also ocean mean downward surface solar radiation. The absolute difference between land and ocean mean downward solar radiation amounts to 0.1 Wm−2 in CERES EBAF and 0.3 Wm−2 in Trenberth et al. (2009) (Table 3). The ocean mean values in ERA-Interim and ERA-40 are only slightly higher than their land mean values by 1.2 and 1.5 Wm−2, respectively (Table 3, Berrisford et al. 2011). This applies also for the present study, where our best estimate over land (184 Wm−2, Sect. 3.2) also closely matches our above estimates over oceans. Given the confidence we have in the estimated land mean downward solar radiation with strong observational constraints (c.f. Sect. 3.2), and taking into account the seemingly robust indications for a flux of similar magnitude over oceans, this further adds plausibility to an ocean mean downward solar radiation near 185 Wm−2. A best estimate near 185 Wm−2 for the downward surface solar radiation over oceans is thus in line with several independent estimates and consistent with both the limited number of available direct observations in maritime environments as well as the criterion of closely matching the land mean value.
When the reference dataset is reduced to consider only the biases against the maritime BSRN stations in the regression analysis, the correlation is somewhat lower (0.63), but the best estimate in downward thermal radiation remains, at 355.6 Wm−2, very similar (not shown).
These best estimates fit also well to the notion in Sect. 4.1.2, that the CMIP5 models over oceans only marginally underestimate the downward thermal radiation when compared to the direct observations. The CMIP5 multimodel ocean mean downward thermal radiation amounts to 355.6 Wm−2 (Table 2). A best estimate near 356 Wm−2 for the downward thermal radiation seems therefore most consistent with the limited observations. Ma et al. (2014) applied also the regression approach of Wild et al. (2013a) and obtained a similar estimate of 354.8 Wm−2. The ERA-Interim determines an ocean mean downward thermal radiation of 356.2 Wm−2, thus matching the above estimates (Table 3). As noted in Sect. 3.2, the ERA estimate profits from both an accurate radiation scheme and an optimal meteorological input to this scheme. This gives additional support for a best estimate near 356 Wm−2 for the downward thermal radiation over oceans as inferred above. The surface CERES EBAF dataset determines the downward surface thermal radiation somewhat higher at 358.9 Wm−2. As with the ocean mean downward solar radiation, it is again remarkable that the completely independently derived estimates for the ocean mean downward solar radiation discussed above (i.e. satellite-derived estimates (CERES EBAF), reanalysis estimates (ERA-Interim) and bias-corrected GCM estimates) vary by no more than 3 Wm−2 (Table 3). This increases confidence that we now have a fairly good handle also on the magnitude of the ocean-mean downward thermal radiation.
The downward thermal radiation over oceans indirectly determined by Trenberth et al. (2009) as a residual of the other energy balance components, is, at 343 Wm−2, more than 10 Wm−2 lower than the above estimates that take into account observations in different ways (Table 3). This points to remaining uncertainties, particularly in the estimates of the non-radiative components of the surface energy budget over oceans.
4.3 Discussion of the maritime energy balance
A schematic representation of the ocean-mean energy balance is shown in Fig. 2 (lower panel), which combines the above estimates of ocean-mean downward solar and thermal radiation with best estimates for the other ocean energy balance components as discussed below.
4.3.1 Radiative components
The best estimates for the TOA fluxes averaged over oceans inferred from CERES EBAF for the TOA solar incoming, reflected, and absorbed radiation amount to 346.6, −94.9 and 251.7 Wm−2 respectively, and for the outgoing thermal radiation to −242.9 Wm−2 (Table 3). They are displayed as rounded values in Fig. 2 (lower panel). Thus, 72.5 % of the corresponding TOA solar irradiance is absorbed in the ocean domain of the climate system, compared to a 65.7 % in the land domain (Fig. 2, upper panel), as might be expected from the higher surface albedo over land. Uncertainty ranges of these TOA fluxes are again as discussed in Wild et al. (2013a). The total solar absorption in the ocean domain is now larger than the thermal emission at the TOA, which compensates for the energy loss due to the net atmospheric energy transport away from the ocean domain onto land (c.f. Discussion in Sect. 3.3.1). Quantitatively, the excess absorption compared to thermal emission averaged over oceans amounts to 8.8 Wm−2 (Table 2). Since close to 1 Wm−2 is taken up by the oceans, 7.9 Wm−2 remain to be exported from ocean to land, as indicated in Fig. 2 (lower panel). Note that the actual value associated with the arrow of the transport term from ocean to land (8 Wm−2) as well as its uncertainty range in the ocean energy balance diagram (Fig. 2, lower panel) are less than half of the corresponding value in the land energy balance diagram (Fig. 2 upper panel), due to the larger ocean domain. Multiplied by the global ocean area of 361 × 1012 m−2, this corresponds to the same 2.8 PW of ocean land transport as discussed in Sect. 3.3.1.
While the TOA fluxes are equally well known over both land and oceans from satellites, surface fluxes over oceans are less well constrained than over land, since direct observations at the ocean surface are much more scarce. For the downward ocean mean solar and thermal fluxes we use in Fig. 2 (lower panel) the estimates of 185 and 356 Wm−2, derived together with their uncertainty ranges in Sect. 4.2. As outlined there, these estimates, inferred from GCMs and their biases with respect to direct observations, are remarkably close (within 4 Wm−2) to reanalysis (ERA-Interim) estimates and the CERES satellite derived products. This increases our confidence in the magnitude of the ocean mean surface downward solar and thermal fluxes, despite the limited availability of direct observations. As also noted above and evident from Fig. 2, the surface downward solar fluxes averaged over land and oceans are nearly identical, which seems a robust feature in various estimates (see Sect. 4.2). This is the case despite an insolation at the TOA which is higher by 22 Wm−2 over ocean than over land, indicative of a stronger attenuation of the solar beam over oceans than over land, in line with higher water vapor content and cloudiness in the ocean domain, leading to stronger atmospheric reflection.
To determine the solar radiation absorbed by the oceans we need, in addition to the surface downward solar fluxes, also information on the albedo of the ocean surfaces. The surface CERES EBAF dataset incorporates a radiation weighted ocean mean albedo of 0.078, as can be deduced from Table 3. The albedo in this dataset is inferred from a coupled atmosphere/ocean radiative transfer model that has been extensively validated with BSRN data (Jin et al. 2002). From Berrisford et al. (2011) we deduce a radiation weighted ocean mean surface albedo used in ERA-Interim and ERA-40 of 0.075 and 0.077 respectively, while the average over the 43 CMIP5 models gives an ocean mean albedo of 0.074 (with a standard deviation of 0.01), as can be inferred from Table 2. From Trenberth et al. (2009) we take a value of 0.09 for their estimate of ocean mean albedo, as well as a value of 0.86 from the satellite derived ISCCP FD satellite-derived product. Assuming an ocean mean surface albedo of 0.08 (closely following the CERES EBAF value as over land) and our best estimate near 185 Wm−2 for downward solar radiation, this implies a reflected solar radiation over oceans of around 15 Wm−2, and an ocean mean absorbed surface solar radiation around 170 Wm−2. As over land, an accurate determination of surface albedo remains a challenge and introduces additional uncertainties in the absorbed and reflected solar fluxes at ocean surfaces. The estimates of solar radiation reflected at ocean surfaces in the recent literature span a range from 13 to 18 Wm−2 (Table 3; Berrisford et al. 2011; Trenberth et al. 2009) which confine the associated uncertainty range applied in Fig. 2 (lower panel).
The TOA and surface absorption of 252 and 170 Wm−2 imply an average absorption of solar radiation in the atmosphere above oceans of 82 Wm−2. This is 5 Wm−2 more than in the CMIP5 multimodel mean. Thus we quantitatively find a similar underestimation of atmospheric absorption over land and oceans in the CMIP5 models (cf. Sect. 3.3.1). Percent wise, Fig. 2 (lower panel) and Table 3 suggest that 23.6 % of the incoming solar radiation at the TOA over oceans is absorbed within the atmosphere, while 49.0 % is absorbed at ocean surfaces. Over land 23.7 % of the TOA insolation is absorbed in the atmosphere, while 41.9 % is absorbed at land surfaces. Thus, the fraction of incoming solar radiation absorbed in the atmosphere is very similar over both land and oceans in Fig. 2. This is not in conflict with the abovementioned higher attenuation over oceans which is primarily caused by a higher atmospheric reflection from the increased cloudiness. On a more regional scale over Europe, Hakuba et al. (2014) estimated the atmospheric absorption at 23.1 % based on a dense network of surface observations collocated with CERES EBAF TOA fluxes, which is remarkably close to the large-scale estimates obtained here. They further noted the fraction of atmospheric absorption, near 23 %, to be a very robust estimate largely unaffected by variations in latitude and season.
4.3.2 Non-radiative components
As over land, there are very limited direct observational constraints for the sensible and latent heat fluxes over oceans. Accordingly, also the CMIP5 models show a substantial spread in their ocean mean surface sensible and latent heat fluxes (Fig. 23). However, in contrast to the land mean estimates in Sect. 3.3.2, the simulated ocean mean latent heat fluxes show now both larger ranges and standard deviations than the corresponding sensible heat fluxes, as can be expected from their larger absolute values. We therefore determine here the latent heat flux as a residual of the ocean surface energy balance.
The CMIP5 model-calculated ocean mean sensible heat flux values cover a range from 11 to 17 Wm−2, when outliers exceeding 2 times the standard deviation are neglected (Fig. 23 lower panel). Reanalysis products give for the same quantity a very similar range of 11–16 Wm−2 (Trenberth et al. 2009; Berrisford et al. 2011). However, Clayson et al. (2014) recently estimated a higher ocean sensible heat flux of 17.8 Wm−2 over the 10 years period 1998–2007, based on the Seaflux dataset, which relies almost exclusively on satellite observations. This suggests that values towards the upper end of the model and reanalysis estimates may be more realistic than towards the lower end. Therefore we use a value of 16 Wm−2, corresponding to the highest reanalysis estimate, for the ocean mean sensible heat flux in Fig. 2 (lower panel). At the same time we acknowledge the mostly lower reanalyses and CMIP5 values and the slightly higher Seaflux value by adjusting the associated uncertainty range in Fig. 2 (lower panel) so that it covers the different reanalysis estimates as well as the Seaflux estimate, in absence of more specific uncertainty information and direct observational constraints. We thereby also acknowledge that to date, the uncertainties in this flux component remain substantial, particularly in relative terms, with the different estimates covering a range of almost half the absolute flux magnitude.
With a surface net radiation of 117 Wm−2 over oceans, a sensible heat flux near 16 Wm−2, and a subsurface ocean heat flux of the order of 1 Wm−2 due to the current imbalance of the climate system (e.g., Hansen et al. 2011), this leaves around 100 Wm−2 as a residual for the latent heat flux over oceans. This value comes very close to the ERA-40 and ERA-Interim ocean mean latent heat flux values of 99.0 and 99.3 Wm−2, respectively (Berrisford et al. 2011), and is also not too far from the estimate given in Trenberth et al. (2009) of 97.1 Wm−2. The value adopted here is, however, substantially higher than the value of 90.3 Wm−2 estimated in Seaflux (Clayson et al. 2014). The Seaflux value is the lowest recently published latent heat flux estimate over oceans and therefore also confines the uncertainty range at the low end in Fig. 2 (lower panel). Estimates of ocean mean latent heat fluxes from eight different reanalyses cover a wide range from 90 to 109 Wm−2 as can be deduced from the water budget estimates given in Trenberth et al. (2011). Our best estimate for the ocean mean latent heat flux near 100 Wm−2 is still considerably lower than the multimodel mean of the CMIP5 models of 104.8 Wm−2 (Table 2; Fig. 23). The higher value of the CMIP5 multimodel mean is a consequence of a higher surface net radiation over oceans due to a higher (and likely overestimated) surface solar radiation (cf. Sect. 4.1.1), as well as a somewhat lower sensible heat flux than estimated here. Estimates of ocean mean latent heat flux exceeding the multimodel mean value are therefore considered unrealistic, as it would require either an unrealistically high surface net radiation, or an unrealistically low sensible heat flux. We therefore use the CMIP5 multimodel mean value of 105 Wm−2 to confine the uncertainty range of the ocean mean latent heat flux at the upper end, in absence of other more stringent observational constraints.
In summary, the energy balance over oceans as schematically displayed in Fig. 2 (lower panel) is derived in a framework that is consistent with the land energy balance in Fig. 2 (upper panel), and does not violate the limited observational constraints. Uncertainties remain, as over land, particularly also in the partitioning of the available radiative energy at the ocean surface between the sensible and latent heat flux components.
5 Revisiting the global mean energy balance
To check the consistency of the land and ocean mean energy balance diagrams derived here with the global mean energy balance diagrams we published earlier in Wild et al. (2013a, b) and IPCC-AR5 we finally combine the ocean and land mean energy budget estimates in Fig. 2 into a global mean budget. The numbers displayed in Fig. 1 and Table 3 are thus derived by adding the land mean numbers in Fig. 2 (upper panel) multiplied by the global land fraction of 0.292, with the ocean mean numbers in Fig. 2 (lower panel) multiplied by the global land fraction of 0.708. The global mean radiative components obtained this way in Fig. 1 and Table 3 are nearly identical to the estimates in Wild et al. (2013a, b). Uncertainty ranges in Fig. 1 correspond to those in Wild et al. (2013b). Compared to Wild et al. (2013b) we obtain a global mean latent heat flux which, at 82 Wm−2, is lower by 2 Wm−2, due to emerging lower estimates of the land evaporation (c.f. Sect. 3.3.2), at the expense of a slightly higher global mean sensible heat flux required to close the surface energy balance. This lower global mean latent heat flux is more compatible with global precipitation estimates which may be used to constrain the magnitude of the global mean evaporation and their energy equivalent, the global mean latent heat flux. At 82 Wm−2, the estimated global mean latent heat flux is close to the estimate of Trenberth et al. (2009) at 80 Wm−2. The 82 Wm−2 are still somewhat higher than the energy equivalent of the precipitation estimates given in given in the Global Precipitation Climatology Project (GPCP, Adler et al. 2012) of 76 Wm−2, yet within their uncertainty range, and clearly below the 85 Wm−2 considered by Trenberth and Fasullo (2012) as upper limit of current uncertainties in precipitation retrieval. We adopt the 85 Wm−2 as upper bound of the uncertainty range specified for the latent heat flux in Fig. 1, and 70 Wm−2 as lower bound, corresponding to the lower limit given in GPCP. This range has been exceeded by Stephens et al. (2012) who determined the global mean latent heat at 88 Wm−2 (with a considerable uncertainty range of ±10 Wm−2). The higher latent heat flux in Stephens et al. (2012) is a consequence of their use of higher solar and thermal downward radiation fluxes from satellite products than estimated here.
The apparent discrepancy between the global mean latent heat flux estimate as inferred from global precipitation observations on the one hand, and as inferred from the available surface radiative energy as given by some of the satellite products on the other hand, has lead to controversial discussions on potential inconsistencies between the global energy and water cycles (e.g., Wild 2012). The estimates presented in Fig. 1 may be able to reconcile the observational constraints imposed on the global latent heat flux and associated intensity of the global water cycle from both the precipitation and surface radiation observation perspective.
In this study we assessed the energy budgets separated over land and oceans in state-of-the-art climate models (CMIP5) considered in the latest IPCC report (AR5), using to the extent possible direct observations from both surface and space. Based on these analyses and a literature review we made an attempt to establish reference estimates for the magnitude of the components of the Earth’s energy balance separately averaged over land and oceans, along with a validation of these components in the CMIP5 models. This study is thus an extension of the study of Wild et al. (2013a) who focused on the global mean energy balance.
The magnitudes of TOA fluxes over land and oceans can now well be determined from the CERES satellite observations. The CMIP5 multimodel mean solar and thermal fluxes closely match these observations when averaged over land and oceans. More substantial biases remain in individual models. Compared to the TOA fluxes, the magnitudes of the surface fluxes are much less well established, as they are not directly measurable by satellites. Historically, this has lead to an unsatisfactory large spread in the surface flux estimates already on global or land/ocean averaged-scales, and has prevented the establishment of firm agreed-upon reference values for the magnitudes of the ocean and land surface energy balance components. This is still evident in the significant spread in the land and ocean surface budgets of the CMIP5 models. Compared to direct surface observations, the majority of these models tend to overestimate the downward solar radiation over land and oceans, and underestimate the downward thermal radiation particularly over land.
We used the information contained in the direct surface observations to constrain the model-calculated surface radiative fluxes and to derive reference estimates for surface radiation over land and oceans. We infered these estimates by relating the surface radiation biases in the various CMIP5 models to their respective land and ocean mean values through orthogonal linear regressions, and evaluating the regression function at the zero bias intersect. The estimates determined this way are remarkably consistent with other recent estimates based on reanalysis and satellite-products, which were completely independently derived. This is particularly true for the land mean budget where we can rely on a comprehensive database of radiation measurements, but also to some extent over oceans with weaker observational constraints, where our downward solar and thermal radiation estimates are within 4 Wm−2 of the independently derived reanalysis and satellite estimates. While the different approaches undeniably have their individual limitations, the agreement of their independently derived estimates is remarkable, even over oceans with limited observational constraints.
This suggests that we are approaching a stage where we are not only confident in the magnitudes of the radiation budgets at the TOA, but increasingly also at the surface, when considered on a global or land/ocean mean basis. Remaining challenges include the accurate determination of large-scale surface albedo estimates, and the adequate representation of the surface skin temperatures in the estimation of the surface upward thermal radiation. Considerable uncertainties remain also in the magnitudes of the non-radiative fluxes of sensible and latent heat and their partitioning over both land and oceans. The more reliable estimates of the land and ocean surface radiation balance may be able to impose additional constraints on the non-radiative components of the surface energy balance, and thereby for example also on the intensity of the water cycles over land and oceans. Future steps will require a further regionalization of observationally-constrained energy budgets beyond global, land, and ocean means. An attempt is currently underway to constrain the solar radiation budgets over Europe, making full use of both surface and spaceborne observations (Hakuba et al. 2014).
This study got support from the Swiss National Science Foundation Grant No. 135395 “Towards an improved understanding of the global energy balance: absorption of solar radiation” and from the National Centre for Competence in Climate Research (NCCR Climate) of the Swiss National Science Foundation as part of the NCCR Project HyClim. We highly appreciate the valuable review comments of Dr. Kevin Trenberth on this manuscript. We are grateful to Prof. Atsumu Ohmura for numerous discussions and for his leadership in the establishment of GEBA and BSRN. We would like to thank Dr. Guido Mueller for processing the BSRN data, Dr. Urs Beyerle and Prof. Reto Knutti for their efforts to download the immense CMIP5 dataset and Dr. Gabriela Schaepmann-Strub for advice on the albedo issues. We highly acknowledge Barbara Schär for the design of the global energy balance figures, and an anonymous reviewer for useful comments. We acknowledge the international modeling groups for providing their data for analysis, the Program for Climate Model Diagnosis and Intercomparison (PCMDI) for collecting and archiving the model data, the JSC/CLIVAR Working Group on Coupled Modeling (WGCM) and their Coupled Model Intercomparison Project (CMIP) and Climate Simulation Panel for organizing the model data analysis activity, and the IPCC WG1 TSU for technical support. The IPCC Data Archive at Lawrence Livermore National Laboratory is supported by the Office of Science, U.S. Department of Energy.
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