2.1 Models

For our study, we used the global ocean circulation model NEMO-v3.2 (Nucleus for European Modeling of the Ocean – version 3.2). The NEMO model has three parts: (1) the ocean dynamics and thermodynamics model Océan Parallélisé (OPA) (Madec, 2008), (2) the Louvain-la-Neuve Sea Ice Model (LIM) (Vancoppenolle et al., 2009), and (3) the passive tracer module TOP. This physical model is coupled via TOP to version 1 of PISCES (Pelagic Interactions Scheme for Carbon and Ecosystem Studies) (Aumont and Bopp, 2006). For this study we used NEMO at three resolutions: a laminar 2^∘ configuration (ORCA2) typical of coarse-resolution ocean models (Madec et al., 1998), which does not resolve eddies; an intermediate 0.5^∘ configuration (ORCA05) that just begins to allow eddies to appear spontaneously (Bourgeois et al., 2016); and a higher-resolution, eddy-admitting version, i.e., a 0.25^∘ configuration (ORCA025), which is still not eddy resolving (Barnier et al., 2006). The highest-resolution simulation is referred to as ORCA025-G70 in the DRAKKAR ensemble.

All three configurations have a tripolar, curvilinear horizontal grid. One grid pole (singularity) is located at the geographical South Pole while the conventional North Pole grid singularity over the Arctic Ocean has been replaced by two grid singularities, both displaced over land – one over Canada and the other over Russia (Madec et al., 1998) – thereby saving computational costs and avoiding numerical artifacts. From 90^∘ S to 20^∘ N, the grid is a normal Mercator grid; north of 20^∘ N, it is distorted into ellipses to create the two northern singularities (Barnier et al., 2006; Madec, 2008). The grid size changes depending on resolution and location (Table 1). The mean horizontal grid size in the Arctic Ocean (average length of the four horizontal edges of surface grid cells in the Arctic Ocean) is 121 km in ORCA2, 29 km in ORCA05, and 14 km in ORCA025. The smallest horizontal grid size in the Arctic is 63 km in ORCA2, 9 km in ORCA05, and 3 km in ORCA025.

Table 1Grid size in the Arctic Ocean and volumes by basin as a function of model resolution.

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Vertically, all three model configurations have the same discretization, where the full-depth water column is divided into 46 levels whose thicknesses vary from 6 m (top level) to 249 m (level 45), but the latter can reach up to 498 m, being extended into level 46 as a function of the bathymetry (partial steps). For its bathymetry, the ocean model relies on the 2 min bathymetry file ETOPO2 from the National Geophysical Data Center, which is based on satellite-derived data (Smith and Sandwell, 1997) except for the highest latitudes: the International Bathymetric Chart of the Arctic Ocean (IBCAO) data are used in the Arctic (Jakobsson et al., 2000) and Antarctic Bedrock Mapping (BEDMAP) bathymetric data are used for the Southern Ocean south of 72^∘ S (Lythe and Vaughan, 2001). To interpolate the bathymetry on the model grid, the median of all data points in one model grid cell was computed. NEMO uses the partial-step approach for the model to better match the observed topography. In this approach, the bathymetry of the model is not tied directly to the bottom edge of the deepest ocean grid level, which varies with latitude and longitude; rather, the deepest ocean grid level for each column of grid cells is partially filled in to better match the observed ocean bathymetry (Barnier et al., 2006).

The lateral isopycnal diffusion and viscosity coefficients were chosen depending on the resolution (Table 2). In ORCA2, a Laplacian viscosity operator was used, whereas a bi-Laplacian operator was used in ORCA05 and ORCA025. To simulate the effect of eddies on the mean advective transport in the two coarser-resolution configurations, the eddy parameterization scheme of Gent and Mcwilliams (1990) was applied with eddy diffusion coefficients indicated in Table 2. Vertically, the same eddy viscosity ($\mathrm{1.2}\times {\mathrm{10}}^{-\mathrm{4}}$ m² s⁻¹) and diffusivity coefficients ($\mathrm{1.2}\times {\mathrm{10}}^{-\mathrm{5}}$ m² s⁻¹) were used in all three resolutions.

Table 2Coefficients for lateral diffusivity, lateral viscosity, and eddy-induced velocity for ORCA2, ORCA05, and ORCA025.

^a In ORCA2, a Laplacian viscosity operator was used, whereas a bi-Laplacian operator was used in ORCA05 and ORCA025. ^b Lateral diffusivity and viscosity coefficients decrease towards the poles proportional to the grid size. ^c Reduced to 2100 m² s⁻¹ in the tropics (except along western boundaries).

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The biogeochemical model PISCES (Aumont and Bopp, 2006) includes four plankton functional types: two phytoplankton types (nanophytoplankton and diatoms) and two zooplankton types (micro- and meso-zooplankton). The growth of phytoplankton is limited by the availability of five nutrients: nitrate, ammonium, total dissolved inorganic phosphorus P_T, total dissolved silicon Si_T, and iron. The nanophytoplankton and diatoms are distinguished by their need for all nutrients, with only diatoms requiring silicon. While the Fe : C and Chl : C ratios of both phytoplankton groups as well as the Si : C ratio of diatoms are predicted prognostically by PISCES, the remaining macronutrient ratios are held constant at $\mathrm{C}:\mathrm{N}:\mathrm{P}=\mathrm{122}:\mathrm{16}:\mathrm{1}$ (Takahashi et al., 1985). The same ratio holds for nonliving compartments: dissolved organic matter (DOM) and both small and large sinking particles, which differ in their sinking velocity. In PISCES, nutrients are supplied by three external pathways: atmospheric dust deposition, river delivery, and sediment mobilization of iron. Dust deposition was taken from a simulation by Tegen and Fung (1995). River discharge of C_T and dissolved organic carbon (DOC) is based on the Global Erosion Model (GEM) by Ludwig et al. (1998). Riverine DOC was assumed to be entirely labile, being instantaneously transformed into C_T as soon as it enters the ocean. River delivery of the other four nutrients (Fe, N, P, and Si) was calculated from riverine C_T delivery, assuming constant ratios of $\mathrm{C}:\mathrm{N}:\mathrm{P}:\mathrm{Si}:\mathrm{Fe}=\mathrm{320}:\mathrm{16}:\mathrm{1}:\mathrm{53.3}:\mathrm{3.64}$ $\times {\mathrm{10}}^{-\mathrm{3}}$ (Meybeck, 1982). For sediment mobilization, the dissolved iron input was parameterized as 2 µmol Fe m⁻² d⁻¹ for depths shallower than 386 m and decreases exponentially with depth following Moore et al. (2004).

2.2 Biogeochemical simulations

For initial conditions, we used observational climatologies for (1) temperature and salinity (a combined product from Barnier et al., 2006), (2) dissolved oxygen and nutrients (nitrate, P_T, and Si_T) from the 2001 World Ocean Atlas (Conkright et al., 2002), and (3) preindustrial C_T and A_T from the observation-based Global Data Analysis Product (GLODAP) (Key et al., 2004). As comparable observational climatologies for DOC and iron are lacking, those variables were initialized from the output of a 3000-year spin-up of an ORCA2 simulation including PISCES. Other tracers have short recycling times and were thus initialized with globally uniform constants.

For physical boundary conditions, all simulations were forced with the same DRAKKAR forcing set (DFS) constructed originally by Brodeau et al. (2010) and routinely updated. This historical reanalysis-based forcing data set provides surface air temperature and humidity at 2 m, wind fields at 10 m, shortwave and longwave radiation, and the net surface freshwater flux (evaporation minus precipitation). It covers 55 years, including 1958–2001 from version 4.2 and 2002–2012 from version 4.4.

A 50-year spin-up was first made from rest in the ORCA05 NEMO-PISCES model (coupled circulation–biogeochemistry), after initializing the model variables with the abovementioned fields. The resulting simulated physical and biogeochemical fields were then used to initialize the ORCA05 NEMO-PISCES simulations in 1870, and that model was subsequently integrated over 1870–1957. Since no atmospheric reanalysis is available during that period, we simply looped the DRAKKAR Forcing Set. Then, at the beginning of 1958, the ORCA05 simulated fields were interpolated to the ORCA2 and ORCA025 grids, and simulations were continued in each of the three configurations from 1958 to 2012. We refer to these simulations as B1870-ORCA2, B1870-ORCA05, and B1870-ORCA025 (Table 3), where the first letter refers to the type of simulation (B for biogeochemical), the following four numbers refer to the initialization year, and the remainder refers to the resolution used over 1958–2012.

Table 3Set of simulations.

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The initialization of the ORCA2 and ORCA025 models in 1958 with interpolated fields from ORCA05 introduces an error into the results from B1870-ORCA2 and B1870-ORCA025. To estimate this branching error in the low-resolution model, we also made a simulation using ORCA2 from 1870 to 2012 (referred to as B1870-ORCA2^*) and compared it to B1870-ORCA2 (initialized in 1958 with output from ORCA05). This strategy was not possible for ORCA025 because running ORCA025 with PISCES over 1870–2012 is too costly.

For each member of this “B” class of simulations, we actually made two types of runs: historical and control, both forced with the same reanalysis fields. Those two runs differ only in their atmospheric CO₂ concentrations. The control simulations were forced with the preindustrial CO₂ concentration of 287 ppm in the atmosphere over the entire period from 1870 to 2012. The historical simulations were forced with yearly averaged historical atmospheric CO₂ concentrations reconstructed from ice cores and atmospheric records over 1870 to 2012 starting at the same reference of 287 ppm (Le Quéré et al., 2015). Making both the control and the historical runs for each of the B class of simulations and taking the difference automatically corrects for model drift. That difference is defined as the anthropogenic component.

2.3 C_ant perturbation simulations

Because of computational limitations, it was necessary to start the anthropogenic CO₂ perturbation of our reference ORCA05-PISCES simulation in 1870 as opposed to the traditional earlier reference of 1765 (Sarmiento et al., 1992), a more realistic approximation of the start of the industrial-era CO₂ increase. A similar compromise was adopted for the Coupled Model Intercomparison Project Phase 5 (CMIP5) (Taylor et al., 2012). During the missing 105 years, atmospheric xCO₂ increased from 278 to 287 ppm, a 9 ppm difference that seems small relative to today's total perturbation with atmospheric xCO₂ now above 400 ppm. However, Bronselaer et al. (2017) estimated that global ocean uptake of C_ant in 1995 is actually underestimated by ∼30 % (29 Pg C) for simulations that reference the natural preindustrial state to 1850 rather than 1765. The cause is partly due to ocean carbon uptake during the missing 1765–1850 period, but mostly it is due to the higher preindustrial reference for atmospheric xCO₂ that results in the air–sea flux of C_ant being underestimated throughout the entire simulation. Unfortunately, we cannot use the Bronselaer et al. (2017) results to correct our biogeochemical simulations because they do not include the Arctic Ocean in their global data-based assessment. Furthermore, their reference date in the mid 19th century is 20 years earlier than ours.

Instead, to correct for the late starting date of our biogeochemical simulations, we made additional simulations using the more efficient single-tracer perturbation approach (Sarmiento et al., 1992) rather than the full PISCES biogeochemical model (24 tracers). To account for the missing carbon, we added the difference between two perturbation simulations, denoted as P rather than B, with one starting in 1765 (P1765) and the other starting in 1870 (P1870). For consistency, we applied the same initialization strategy as for the biogeochemical simulations, i.e., using ORCA05 until the end of 1957 with that output serving as the initial fields for subsequent 1958–2012 simulations in all three configurations. The naming convention for the P class of simulations is like that for the B class (indicated by the first letter). The difference is that in each P simulation there is only one tracer and one run for each (no need for a control and a historical run). However, initializing a set of P simulations in 1765 as well as in 1870 implies twice the number of simulations (Table 3). The difference in C_ant between P1765 and P1870 simulations was later added as a late-start correction to the biogeochemical simulations (B1870), for each resolution separately.

The perturbation approach of Sarmiento et al. (1992) avoids the computationally intensive standard CO₂ system calculations by accounting for only the perturbation (C_ant), assuming it is independent of the natural carbon cycle. By focusing only on anthropogenic carbon, this approach exploits a linear relationship between the anthropogenic change in surface-ocean pCO₂ (µatm) and its ratio with the corresponding change in surface-ocean dissolved inorganic carbon (δC_T):

where $\mathit{\delta }p{{\mathrm{CO}}_{\mathrm{2}}}_o$ is the perturbation in surface-ocean pCO₂ and the coefficients z₀ and z₁ are each quadratic functions of surface temperature (^∘C):

In the model, Eq. (1) was rearranged to solve for $\mathit{\delta }p{{\mathrm{CO}}_{\mathrm{2}}}_o$ in terms of δC_T (Sarmiento et al., 1992, Eq. 11), as needed to compute the air–sea flux (Sarmiento et al., 1992, Eq. 2). In the air–sea flux equation, the atmospheric xCO₂ was corrected for humidity and atmospheric pressure to convert to pCO_2atm, which thus varies spatially while atmospheric xCO₂ does not (in the model). The atmospheric xCO₂ history for 1765–1869 is from Meinshausen et al. (2017), while the history for 1870 and beyond is the same as used in the NEMO-PISCES simulations. One set of coefficients was derived for our reference atmospheric xCO₂ in 1765; another set was derived for our reference atmospheric xCO₂ in 1870 (Table 4). The original approach was only updated to use the equilibrium constants recommended for best practices (Dickson et al., 2007) and to cover a perturbation of up to 280 ppm (see Supplement). The relative uncertainty introduced by approximating the perturbation to the ocean CO₂ system equilibria with Eq. (1) remains less than ±0.3 % across the global ocean's observed temperature range when $\mathit{\delta }p{{\mathrm{CO}}_{\mathrm{2}}}^{\mathrm{oc}}<\mathrm{280}$ ppm.

Table 4Fitted parameters in Eqs. (2) and (3) for the perturbation simulations P1765 and P1870.

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The Arctic C_ant inventory in 2012 simulated by the perturbation approach (P1870-ORCA2^*) underestimates that simulated by the full biogeochemical approach (B1870-ORCA2^*) by 3 % (Appendix A). The corresponding underestimation by P1765-ORCA2^* is expected to be similar. The similar bias of P1765-ORCA2^* and P1870-ORCA2^* means that the bias in their difference is probably much less than 3 %. The same holds for P1765-ORCA2 vs. P1870-ORCA2. Thus, using their difference to correct for the late start of B1870-ORCA2 is not only practical but also sufficiently accurate for our purposes. In contrast, not correcting B1870-ORCA2 for its late starting date would lead to a 19 % underestimation of its Arctic C_ant inventory for the full industrial era.

In practice, to make the late-start correction, at each grid cell we added the time-varying difference in C_ant between the two perturbation simulations (P1765−P1870) to the C_ant simulated with B1870 for each resolution separately. From here on, we refer only to these corrected biogeochemical simulations, denoting them as ORCA2, ORCA05, ORCA025, and ORCA2^*.

2.4 CFC-12 simulation

CFC-12 is a purely anthropogenic tracer, a sparingly soluble gas whose concentration began to increase in the atmosphere in the early 1930s and part of which has been transferred to the ocean via air–sea gas exchange. Its uptake and redistribution in the ocean has been simulated following Ocean Carbon-cycle Model Intercomparison Project 2 (OCMIP-2) protocols (Dutay et al., 2002). The CFC-12 flux (F_CFC) at the air–sea interface was calculated as follows:

where k_w is the gas-transfer velocity (piston velocity) in m s⁻¹ (Wanninkhof, 1992), pCFC is the atmospheric partial pressure of CFC-12 from the reconstructed atmospheric history by Bullister (2015), C_s is the sea surface concentration of CFC-12 (mol m⁻³), α_CFC is the solubility of CFC-12 (mol m⁻³ atm⁻¹) from Warner and Weiss (1985), and I is the model's fractional sea-ice cover. Once in the ocean, CFC-12 is an inert tracer that is distributed by advection and diffusion; it has no internal sources and sinks. Many high-precision measurements of CFC-12 are available throughout the ocean, in sharp contrast to C_ant which cannot be measured directly.

As for the other simulations, those for CFC-12 were made using ORCA05 until 1957, at which point those results were interpolated to the ORCA2 and ORCA025 grids. The ORCA05 CFC-12 simulation began in 1932. From 1958 to 2012, CFC-12 was simulated for each resolution separately.

2.5 Arctic Ocean

To assess the anthropogenic carbon budget in the Arctic Ocean, we adopt the regional domain defined by Bates and Mathis (2009) delineated in Fig. 1. That domain's lateral boundaries and the volume of water contained within them vary slightly among the three model versions due to their different resolutions and bathymetries (Table 1). The signature of these different volumes is also apparent in the integrated quantity of anthropogenic carbon that is stored in the Arctic in 1958, although the fields for all three models are based on the same 1957 field from the ORCA05 model (Fig. 2).

Figure 2Arctic Ocean C_ant inventory for ORCA2, ORCA05, ORCA025, and ORCA2^*. The discontinuity for ORCA2 in 1958 is due to its larger total volume of water when integrated across the Arctic domain (Table 1).

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2.6 Transport across boundaries

Transects are defined (Fig. 1) along the four boundaries as consistently as possible for the three resolutions. Water transport across each of the four boundaries is calculated for each model configuration by using monthly average water velocities at each boundary grid cell along a transect multiplied by the corresponding area of the face of the grid cell through which the water flows. For boundaries defined by a row of cells (Fram Strait; Canadian Arctic Archipelago, CAA; and Bering Strait), the transport is calculated across the northern face of each cell. Conversely, for the jagged boundary of the Barents Sea Opening, transport is calculated at the northern and eastern faces of each cell and the two transports are summed. For each transect, transport across all of its cells is summed to obtain the transect's monthly net transport.

For the C_ant transport, we do the same but also multiply the water transport at the boundary between two grid cells with their volume-weighted monthly-average concentration. This multiplication of monthly means introduces an error into the transport calculations owing to neglect of shorter-term variability. To elucidate that error, we sum results from those monthly calculations across all four sections, integrate them over time from 1960 to 2012, and compare that to the net transport of C_ant into the Arctic Ocean implied by the inventory change minus the cumulative air–sea flux over the same time period. The inventory of C_ant is the total mass of C_ant inside the Arctic Ocean at a given time, while the cumulative flux is the time-integrated air–sea flux of anthropogenic CO₂ over the Arctic Ocean since the beginning of the simulation. The difference between these two spatially integrated values is the reference value for the net lateral flux into the Arctic Ocean to which is compared the less exact total lateral flux of anthropogenic carbon computed from monthly mean velocity and concentration fields integrated over time. The relative error for transport of C_ant across all the separate boundaries introduced by the monthly average calculations is 28 % for ORCA2, 7 % for ORCA05, and 3 % for ORCA025. This error applies neither to the C_ant inventory nor to the cumulative C_ant air–sea flux or the lateral C_ant fluxes, which are all calculated online, i.e., during the simulations.

2.7 CFC-12 observational data

Model simulations were evaluated indirectly by comparing simulated to observed CFC-12. We choose CFC-12 to evaluate the model because it is an anthropogenic, passive, conservative, and inert tracer, and in contrast to anthropogenic carbon, it is directly measurable. The CFC-12 atmospheric concentration increased from zero in the 1930s to its peak in the 2000s, since declining as a result of the Montreal protocol. Thus, CFC-12 is a transient tracer similar to anthropogenic carbon but for which there exist extensive direct measurements, all carried out with high precision during the WOCE (World Ocean Circulation Experiment) and CLIVAR (Climate and Ocean – Variability, Predictability and Change) era. Nowadays, ocean models are often evaluated with CFC-11 or CFC-12, especially those used to assess anthropogenic carbon uptake (Dutay et al., 2002; Orr et al., 2017).

The CFC-12 observations used in this study come from two trans-Arctic cruises: the 1994 Arctic Ocean Section (AOS94) (Jones et al., 2007) and the Beringia 2005 expedition (Anderson et al., 2011) (Fig. 1). AOS94 started on 24 July and was completed on 1 September, during which CFC-12 measurements were made at 39 stations. That section began in the Bering Strait, entered the Canada Basin adjacent to Mendeleev Ridge, continued to the Makarov Basin, and ended at the boundary of the Nansen Basin and the Barents Sea. The Beringia expedition started on 19 August and ended on 25 September 2005. It began off the coast of Alaska, went through the Canada and Makarov basins and crossed the Lomonosov Ridge, and its last CFC-12 station was taken on the Gakkel Ridge. These two cruises were chosen from among others because they cross large parts of the Arctic, including almost all four major basins.

2.8 Data-based estimates of anthropogenic carbon

Our simulated C_ant was compared to data-based estimates from Tanhua et al. (2009) for the year 2005 and from GLODAPv2 for the year 2002 (Lauvset et al., 2016), both based on the TTD approach.

3.1 Physical evaluation

3.1.1 Lateral water fluxes

The lateral water flux across each of the four Arctic boundaries is a fundamental reference for the simulated physical transport, especially given our goal to construct a budget that includes the lateral transport of passive tracers. Results for lateral water transport in the three model resolutions may be grouped into two classes: coarse resolution and higher resolutions. In ORCA2, water enters the Arctic Ocean from the Barents Sea and the Bering Strait (2.1 Sv split evenly), with 86 % of that total leaving the Arctic via the Fram Strait and the remaining 14 % flowing out via the CAA (Table 5). Conversely, outflow through the CAA is 7 times larger for ORCA05 and 9 times larger for ORCA025, being fueled by 26 % to 46 % more inflow via the Bering Strait and 110 % to 170 % more inflow via the Barents Sea. Outflow via the Fram Strait is 1.76 Sv in ORCA2, 1.42–1.75 Sv in ORCA05, and 1.46–1.80 Sv in ORCA025, depending on the time period (Table 5).

Schauer et al. (2008)Rudels et al. (2008)Skagseth et al. (2008)Smedsrud et al. (2010)Woodgate et al. (2010)Curry et al. (2014)Jeansson et al. (2011)Stöven et al. (2016)Jeansson et al. (2011)Olsen et al. (2015)Olsen et al. (2015)Olsen et al. (2015)

Table 5Lateral transport of water and C_ant across Arctic Ocean boundaries with average simulated values calculated for the same time period as observations.

^* Observational year or period impossible to identify exactly as C_ant and velocity measurements are not from the same year.

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Relative to the observed CAA outflow of 2.7 Sv (Curry et al., 2014; Straneo and Saucier, 2008), only ORCA05 and ORCA025 simulate similar results. In contrast, ORCA2's simulated CAA outflow is about one-ninth of that observed. Likewise, its inflow via the Barents Sea is half of that observed, while the two higher-resolution simulations have Barents Sea inflows that are 20 % and 40 % larger than observed. Yet for inflow through the Bering Strait, it is ORCA2 that is closest to the observed estimate, overestimating it by 30 %, while ORCA05 and ORCA025 overestimate it by 60 % and 90 %. Thus, too much Pacific water appears to be entering the Arctic Ocean. All resolutions underestimate the central observational estimate for the Fram Strait outflow by ∼12 % but still easily fall within the large associated uncertainty range.

Summing up, the net water transport across all four boundaries is not zero. A net Arctic outflow between 0.12 and 0.17 Sv is found for the three model resolutions owing to river inflow and precipitation as well as artifacts caused by using monthly averages. In contrast, when the observed water transport estimates at all four boundaries are summed up, there is a net outflow of 1.9 Sv, more than 10 times larger. This strong net outflow is also much larger than freshwater input from rivers of 0.08 Sv (McClelland et al., 2006) and precipitation of 0.12 Sv (Yang, 1999). It can only be explained by uncertainties in the data-based estimates of water transport, which are at least ±2.7 Sv for the net transport based on the limited uncertainties available for transport across the individual boundaries (Table 5). The excessive central observational estimate for the net outflow might be explained by a data-based estimate for the Barents Sea inflow that is too weak combined with a data-based estimate for the Fram Strait outflow that is too strong, a possibility that is consistent with results from the higher-resolution models ORCA05 and ORCA025.

3.1.2 Sea ice

Because sea-ice cover affects the air–sea CO₂ flux and hence anthropogenic carbon concentrations in the ocean, we compare the modeled sea-ice cover to that observed by the US National Snow and Ice Data Center (Walsh et al., 2015). Yearly averages of sea-ice extent agree within 2 % between the observations and models. Only in summer are simulated sea-ice concentrations slightly too high (by 0.25–0.5×10⁶ km³, e.g., 5 %). Despite this overall agreement in integrated sea-ice extent, regionally differences are larger. During winter (Fig. 3), all three model configurations slightly overestimate the sea-ice extent northeast of Iceland and north of the Labrador Sea, while the simulated sea-ice extent in the Barents Sea and the Bering Strait are similar to observations. During summer, the simulated sea-ice extent resembles that observed in the western Arctic particularly near the Pacific, but all model resolutions slightly overestimate sea-ice extent in the Nordic Seas, north of the Barents Sea, the Kara Sea, and the Laptev Sea. This overestimation should reduce air–sea CO₂ fluxes locally in these regions. Overall, the close model–data agreement for sea-ice extent in terms of the total amount, its trend and seasonal coverage, as well as regional coverage in winter contrasts with the tendency of the models to overpredict sea-ice cover in summer at the highest latitudes of the eastern Arctic.

Figure 3Sea-ice extent (a, b) and sea-ice concentration (c, d) over the Arctic from 1960 to 2012 comparing microwave-based observations from the National Oceanic and Atmospheric Administration (NOAA) (black) to simulated results from ORCA2 (green dots), ORCA05 (red dashes), and ORCA025 (blue dot–dash). Shown are the yearly averages (a), the average (climatological) seasonal cycle over 1958–2010 (b), and the average sea-ice extent in winter (December, January, February) (c) and summer (July, August, September) (d). The lines on the maps show the 50 % sea-ice cover for the three model resolutions and the observations, while the color indicates the observed sea-ice concentration.

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3.1.3 Atlantic water

In the Arctic Ocean, water temperature is used to help identify water masses, with values above 0 ^∘C typically coming from the Atlantic Ocean (Woodgate, 2013). The observed temperature along the 1994 and 2005 sections (Fig. 4) indicates that Atlantic Water (AW) is found between 200 and 1000 m, penetrating laterally below the strongly stratified Arctic Ocean surface waters. In ORCA025, this AW layer is deeper and more diffuse, lying between 500 and 1500 m and thus leading to a cold bias around 500 m and a warm bias around 1000 m. The Beringia station at the boundary between the Barents Sea and the Nansen Basin indicates that AW lies between 200 m (2.5 ^∘C) and the seafloor at 1000 m (0 ^∘C). Conversely in the same location in ORCA025, model temperatures remain above 1.5 ^∘C throughout the water column. That lower maximum temperature and weaker vertical gradient suggest that when ORCA025's Atlantic water enters the Arctic Ocean through the Barents Sea, it is too diffuse, being well mixed throughout the water column. Weaker maxima in ORCA025's simulated temperature relative to observations are also found further west in the Canada Basin along both sections. There, observed temperatures reach maxima of 1.1 ^∘C, while simulated temperature maxima reach only 0.5 ^∘C.

Figure 4Temperature along the 1994 Arctic Ocean Section (AOS94) cruise (a, c, e) and the Beringia 2005 section (b, d, f), both trans-Arctic transects (Fig. 1). The observations (a, b) are compared to simulated results from ORCA025 averaged over the summer of the respective year (c, d). The model–data difference is shown at the bottom.

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The two lower resolutions represent lateral invasion of AW less successfully than does ORCA025. Both simulations show water with temperatures higher than 0 ^∘C only at the southern end of the Nansen Basin. Vertically, these water masses are situated around 400 m for ORCA2 and between 200 and 1300 m for ORCA05.

3.2 CFC-12

Simulated CFC-12 was compared among the three resolutions and with observations, focusing first on basin-scale tendencies based on vertical profiles of the distance-weighted means along the Beringia 2005 section (Fig. 5). This comparison reveals that among resolutions, simulated CFC-12 concentrations differ most between 400 and 1900 m; conversely, above and below that intermediate zone, simulated average profiles are nearly insensitive to resolution. In that intermediate zone and above, simulated concentrations are also generally lower than observed. The only exception is the top 100 m in the Canada Basin where all resolutions overestimate observed concentrations by 10 %. Between 200 and 400 m, all resolutions underestimate observations by ∼50 %. Below 400 m, the ORCA2 CFC-12 concentrations decline quickly to zero by ∼1000 m, while the ORCA05 and ORCA025 concentrations continue to increase, both being 15 % greater at 900 m than at 400 m. Below that depth, the ORCA05 concentrations decline, quickly reaching zero at 1350 m, while ORCA025 concentrations remain above 1 pmol kg⁻¹ until 1400 m. Between 1100 and 1500 m, average CFC-12 concentrations along the Beringia section in ORCA025 are up to ∼10 % larger than observed. This overestimation of CFC-12 by ORCA025 reaches up to 40 % in the Canada and Makarov basins. Below 1900 m, the simulated concentrations are essentially zero, while the observations are slightly higher (0.12 pmol kg⁻¹). For comparison, the reported detection limit for CFC-12 for the Beringia 2005 expedition is 0.02 pmol kg⁻¹ (Anderson et al., 2011).

Figure 5Profiles of observed CFC-12 (black solid) and simulated CFC-12 in ORCA2 (green dots), ORCA05 (red dashes), and ORCA025 (blue dot–dash) along the Beringia 2005 section. Shown are distance-weighted means across that entire section (a) as well as over that section covering the Nansen and Amundsen basins (b), the Makarov Basin (c), and the Canada Basin (d). Shown in light grey is the vertical profile in 1958, the branching point for the three resolutions.

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Given the closer overall agreement of the ORCA025 simulated CFC-12 to the observations, let us now focus on its evaluation along the 1994 and 2005 sections (Fig. 6). On the Atlantic end of the Beringia 2005 section, where water enters the Nansen Basin from the Barents Sea, the water column in ORCA025 appears too well mixed, having CFC-12 concentrations that remain above 2.0 pmol kg⁻¹. Conversely, observed CFC-12 is less uniform, varying from 2.8 pmol kg⁻¹ at the surface to 1.3 pmol kg⁻¹ in bottom waters at 1000 m, thereby indicating greater stratification. A similar contrast in stratification was deduced from modeled and observed temperature profiles at the same location (Sect. 3.1.3). On the other side of the Arctic in the Canada Basin, there are observed local chimneys of CFC-12 where concentrations remain at about 2.0 pmol kg⁻¹ from near the surface down to 1000 m, particularly along the 1994 section. These chimneys suggest localized mixing that is only barely apparent in ORCA025 (Fig. 6). Such localized features are absent at lower resolution. The CFC-12 inventories were also calculated along the two sections, integrated over depth and distance (Table 7). Depending on the expedition, ORCA025 underestimates the observed CFC-12 section inventories by 13 %–18 %, ORCA05 by 36 %–38 %, and ORCA2 by 47 %–61 %.

Figure 6CFC-12 concentrations along the AOS94 section (a, c, e) and the Beringia section (b, d, f) for the observations (a, b), the simulated summer means in ORCA025 (c, d), and the model–data difference (e, f).

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3.3 Anthropogenic carbon inventories and concentrations

Simulated global ocean C_ant inventories are 152 Pg C in ORCA2, 146 Pg C in ORCA05, and 148 Pg C in ORCA025 in 2008, after accounting for corrections for the earlier starting date of 1765 using our perturbation simulations (P1765–P1870). The correction is similar for each resolution, e.g., 24–25 Pg C in 1995, and is consistent with our biogeochemical model simulation strategy (all three resolutions initialized with the ORCA05 output in 1958). Furthermore, these model-based corrections fall within the 29±5 Pg C correction calculated for the same 1765–1995 period with a data-based approach (Bronselaer et al., 2017). For the 1765–2008 period, the data-based global C_ant inventory estimate from (Khatiwala et al., 2009) is 140±24 Pg C, the range of which encompasses the results from all three model resolutions.

Table 6Total inventory, its change during 1960–2012, the cumulative air–sea flux, and the lateral flux of C_ant in Pg C.

^a Numbers in parentheses show the uncorrected value (starting date 1870). ^b Data-based inventory in 2002: 2.95 Pg C (GLODAPv2). ^c Data-based inventory in 2005: 3.03 Pg C (2.5–3.3) (Tanhua et al., 2009). ^d Computed as inventory change minus cumulative air–sea flux.

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In the Arctic Ocean, the corrected modeled C_ant inventories range from 1.9 to 2.5 Pg C in 2002 and from 2.0 to 2.6 Pg C in 2005, in each case with the low from ORCA2 and the high from ORCA025 (Table 6 and Fig. 2). These simulated basin-wide Arctic Ocean C_ant inventories were compared to the TTD-based estimates of anthropogenic carbon from (1) the GLODAPv2 assessment (Lauvset et al., 2016) normalized to the year 2002 and (2) the Tanhua et al. (2009) assessment normalized to 2005. The data-based assessment from GLODAPv2 suggests that 2.9 Pg C of anthropogenic carbon was stored in the Arctic Ocean in 2002, while that from Tanhua et al. (2009) suggests that 2.5–3.3 Pg C was stored there in 2005. In 2002, the upper limit of the modeled C_ant inventory range remains 0.4 Pg C lower than the GLODAPv2 data-based estimate, but the ORCA025 result in 2005 falls within the data-based uncertainty range of Tanhua et al. (2009). As for the global estimates, the modeled Arctic Ocean C_ant inventories include corrections for the late starting date of the biogeochemical simulations. This correction is 0.4 Pg C in 2005 for each of the three resolutions (Table 6).

Table 7Along-section CFC-12 inventories (µmol m⁻¹) integrated over depth and distance along the AOS94 and Beringia 2005 sections vs. colocated results in ORCA2, ORCA05, and ORCA025.

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Figure 7Area-weighted basin-wide average vertical profiles of C_ant concentration in 2002 for GLODAPv2 data-based estimates (black solid), ORCA2 (green dots), ORCA05 (red dashes), and ORCA025 (blue dot–dash) over the entire Arctic (a) as well as over the Nansen and Amundsen basins (b), the Makarov Basin (c), and the Canada Basin (d). Ocean corrected for the starting year by the perturbation approach simulations. Shown are the vertical profile in 1958 (dashed, light grey), the branching point for the three resolutions, and results from ORCA2^* for 2002 (magenta dots).

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The differences in basin-wide inventory estimates were further studied by comparing vertical profiles of C_ant from the models to those from the GLODAPv2 data-based estimates (Fig. 7). Surface concentrations in ORCA05 and ORCA025 are up to ∼35 % larger (+12 µmol kg⁻¹) than the data-based estimate, whereas the ORCA2 concentration is ∼22 % larger (+7 µmol kg⁻¹). By 150 m, the simulated concentrations in all resolutions have dropped below the data-based estimates and remain so, except for ORCA025, down to the ocean bottom. Data–model differences are largest at 400 m, with all resolutions underestimating data-based C_ant estimates by up to ∼28 % (9 µmol kg⁻¹). Below that depth, results from the three resolutions differ more. The C_ant concentration in ORCA2 decreases monotonically reaching 11 µmol kg⁻¹ at 1000 m and essentially zero by 2300 m. The vertical penetration of C_ant in ORCA2^* (the simulation without branching from ORCA05 in 1958) is shallower, reaching zero by 1400 m. In ORCA05, C_ant concentrations decrease slowly to 19 µmol kg⁻¹ at 1000 m, below which they decline rapidly, reaching zero at 2300 m. Only in ORCA025 do C_ant concentrations increase again below 400 m, reaching a local maximum at 900 m, an increase that causes the ORCA025 results to exceed data-based estimates by up to 2 µmol kg⁻¹ (∼11 %) at 1100 m. A similar maximum and excess are also seen in the CFC-12 profile for ORCA025 as is the minimum around 400 m (Fig. 5). Below 1500 m, the ORCA025 C_ant concentrations decline quickly, essentially reaching zero at 2300 m. Conversely, data-based C_ant concentrations remain roughly constant at 6 µmol kg⁻¹ down to the seafloor. Thus, the largest vertically integrated differences between ORCA025 and data-based estimates are found in the deep Arctic Ocean below 1600 m.

3.4 Anthropogenic carbon budget

For the budget of C_ant, we focused on the final decades over which the model resolutions differed (Tables 5 and 6). During 1960 to 2012, the C_ant inventory in ORCA025 increased by 1.98 Pg C, 80 % of which is stored in the four major Arctic Ocean basins: the Nansen Basin (0.30 Pg C), the Amundsen Basin (0.34 Pg C), the Makarov Basin (0.33 Pg C), and the Canada Basin (0.61 Pg C). Although the Canada Basin C_ant inventory increased most, its volume is larger so that its average C_ant concentration increased less than in the other basins (Fig. 7). Of the total inventory stored in the Arctic Ocean during that time, only about one-fourth (0.48 Pg C) entered the Arctic Ocean via the air–sea flux, most of which was transferred from the atmosphere through the surface of the Barents Sea (Fig. 8). The remaining 75 % (1.50 Pg C) entered the Arctic Ocean via lateral transport. This net lateral influx is the sum of the fluxes (1) from the Atlantic to the Barents Sea (1.98 Pg C), (2) from the Pacific through the Bering Strait (1.03 Pg C), (3) to the Atlantic via the Fram Strait (−0.06 Pg C), and (4) to the Atlantic via the CAA (−1.50 Pg C). Summed up, the net lateral inflow of anthropogenic carbon across the four boundaries is 1.45 Pg C. This lateral flux computed from monthly mean C_ant concentrations and flow fields is 0.05 Pg C (∼3 %) smaller than the lateral flux computed from the change in inventory minus the cumulative air–sea flux (Fig. 8). Within the Arctic, coastal regions typically exhibit net lateral losses, while the deep basins exhibit net lateral gain. The largest lateral loss occurs in the Barents Sea, where the cumulative air–sea flux of C_ant is also largest.

Figure 8Inventory change (a, d, g), cumulative air–sea flux (b, e, h), and the lateral flux calculated as the inventory change minus the cumulative air–sea flux (c, f, i) of C_ant over 1960–2012 for ORCA025 (a–c), ORCA05 (d–f), and ORCA2 (g–i).

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The budget of C_ant changes notably with resolution. Higher resolution results in more simulated C_ant being stored in the Arctic region, with increases in both the cumulative air–sea flux and lateral transport. The C_ant inventory change from 1960 to 2012 nearly doubles with the resolution increase between ORCA2 and ORCA025 (from 1.08 to 1.98 Pg C). Of that additional C_ant, 93 % is found between 300 and 2200 m, with the maximum being located at 1140 m. The remaining 7 % is located in the upper 300 m (Fig. 7). Resolution also affects the regional partitioning of C_ant (Figs. 7 and 8). When refining resolution from ORCA2 to ORCA05, the Arctic Ocean C_ant inventory increases by 0.47 Pg C, 72 % of which occurs in the Eurasian basins: the Nansen Basin (0.19 Pg C) and Amundsen Basin (0.15 Pg C). Another 23 % of that increase occurs in the Amerasian basins: the Makarov Basin (0.06 Pg C) and Canada Basin (0.05 Pg C). Coastal regions account for only 5 % of the total inventory increase. In contrast, the subsequent resolution enhancement between ORCA05 and ORCA025 results in little increase in inventory in the Eurasian basins (0.03 Pg C) but much more in the Amerasian basins (0.37 Pg C).

As resolution is refined between ORCA2 and ORCA025, the Arctic C_ant inventory increases as a result of a 66 % increase in the air–sea flux (+0.19 Pg C) and a 90 % increase in the lateral flux (+0.71 Pg C). Thus, the relative contribution of the lateral flux increases from 73 % to 76 %. Changing model resolution also affects the pathways by which C_ant enters the Arctic Ocean (Table 5). The most prominent change occurs in the CAA. From ORCA2 to ORCA025, the net outflow of C_ant through the CAA increases 7-fold (from −0.22 to −1.50 Pg C). Other notable changes include (1) the net outflow through the Fram Strait declining 12-fold from -0.74 to −0.06 Pg C, (2) the inflow through the Barents Sea increasing by 150 % (from 0.79 to 1.98 Pg C), and (3) the inflow of C_ant through the Bering Strait increasing by 39 % (from 0.74 to 1.03 Pg C).

4.1 CFC-12

The simulated CFC-12 in ORCA025 underestimates observed concentrations between 100 and 1100 m, slightly overestimates them on average between 1100 and 1500 m, and again underestimates the low observed concentrations below 1500 m. The temperature sections suggest that excess simulated CFC-12 between 1100 and 1500 m is due to a vertical displacement of inflowing Atlantic water, which descends too deeply into the Arctic (Fig. 4). Such vertical displacement would indeed reduce simulated CFC-12 concentrations above 1000 m and enhance them between 1100 and 1500 m. Yet the underestimation of integrated CFC-12 mass above 1100 m is larger than the overestimation below 1100 m. Thus, vertical displacement of Atlantic water cannot provide a full explanation. Simulated CFC-12 concentrations above 1100 m could also be too low because ventilation of subsurface waters is too weak, a hypothesis that is consistent with the simulated vertical gradients in both temperature and CFC-12 that are too strong between 100 and 1100 m.

4.2 Anthropogenic carbon

Vertical profiles of C_ant and CFC-12 are similar. Above 1000 m, ORCA025 underestimates data-based estimates of C_ant as well as observed CFC-12 owing to weak ventilation in the model. Between 1000 and 1500 m, simulated C_ant and CFC-12 in ORCA025 exhibit local maxima, which make them on average slightly higher than data-based and observed concentrations. These local maxima can be explained by the simulated Atlantic water masses, rich in both tracers, being too deep. However, the slight overestimation between 1000 and 1500 m is much smaller than the underestimation between 200 and 1000 m. Below 2000 m, simulated C_ant largely underestimates data-based estimates. The low simulated C_ant stems from too little deep-water formation in the model as indicated by the absence of simulated CFC-12 below 2000 m, an absence that contrasts with the observed CFC-12 concentrations that remain detectable all the way down to the ocean floor (Fig. 5).

A second reason for the low simulated Arctic C_ant inventory in ORCA025 is that it was initialized with ORCA05 results in 1958. Had ORCA025 been initialized in 1765, which was not computationally feasible, its simulated inventory would be larger, given that both C_ant and CFC-12 storage for ORCA025 are larger than those for ORCA05 over 1958–2012. That hypothesis is consistent with our finding that ORCA2^* (complete simulation at 2^∘ without branching from the 0.5^∘ configuration) takes up less C_ant than does ORCA2 (0.5^∘ until 1958 then 2^∘ afterwards), which is in line with ORCA2 taking up less C_ant and CFC-12 than ORCA05 (Figs. 2, 5, and 7). The initialization of ORCA2 with ORCA05 output in 1958 mainly affects C_ant storage between 1000 and 2000 m, the same depth range over which differences in simulated CFC-12 concentrations are largest between ORCA2 and ORCA05. Nevertheless, that 1958 initialization has little effect on subsequent changes in C_ant storage, cumulative lateral flux, and air–sea flux (Fig. 9). Rather it is the changes before 1958 that dominate the difference between ORCA2 and ORCA2^*.

Figure 9Comparison of results for the Arctic Ocean from ORCA2, ORCA05, ORCA025, and ORCA2^* and the nine earth system models that participated in CMIP5. Shown are the C_ant inventory in 2005 (black), the inventory change of C_ant (dark grey) between 1960 and 2012, the corresponding cumulative air–sea flux of C_ant (light grey), and the cumulative lateral flux of C_ant (white). Also indicated are the data-based estimate from Tanhua et al. (2009) (dashed black line) along with its associated uncertainty range (grey background). The inventory correction for the late starting date for our forced simulations is indicated as striped bars.

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All our model configurations underestimate C_ant concentrations in the deep waters of the Arctic Ocean based on the CFC-12 model evaluation. The same conclusion is drawn from comparing simulated to data-based estimates of C_ant. However, results from different data-based approaches to estimate C_ant can differ substantially in the deep ocean (e.g., Vázquez-Rodríguez et al., 2009). Furthermore, the TTD approach typically produces the highest values in deep waters due to its assumption of constant air–sea disequilibrium (Khatiwala et al., 2013). Hence applying other data-based approaches to assess the Arctic Ocean inventory of the C_ant inventory would eventually help to further constrain uncertainties.

4.3 Lateral flux

In our model, about three-fourths of the net total mass of C_ant that accumulates in the Arctic Ocean enters laterally from the Atlantic and Pacific oceans, independent of model resolution. Our simulated lateral fluxes of C_ant in ORCA025 were compared to data-based estimates from studies that multiply data-based C_ant concentrations (TTD estimates) along the Arctic boundaries by corresponding observation-based estimates of water transport.

The simulated lateral transport of C_ant in ORCA025 generally agrees with data-based estimates within their large uncertainties. These uncertainties result from uncertainties in data-based estimates of C_ant and from uncertainties in observational constraints on water flow, which also varies interannually (Jeansson et al., 2011). For the Fram Strait, Jeansson et al. (2011) estimated a net C_ant outflux (from the Arctic) of 1±17 Tg C yr⁻¹ in 2002, while for 2012 Stöven et al. (2016) estimate an outflux of 12 Tg C yr⁻¹ without indicating uncertainties. For the same years, ORCA025 simulates a net outflux of 8 Tg C yr⁻¹ in 2002 but a net influx (to the Arctic) of 5 Tg C yr⁻¹ in 2012. Both model and data-based estimates vary greatly between 2002 and 2012. Across the Barents Sea Opening, there is a consistent net influx from the Atlantic to the Arctic Ocean, i.e., 41±8 Tg C yr⁻¹ in 2002 for the data-based estimate (Jeansson et al., 2011) and 50 Tg C yr⁻¹ for ORCA025 in the same year.

More recently, Olsen et al. (2015) added data-based estimates of lateral fluxes of C_ant across the two other major Arctic Ocean boundaries, completing the set of four boundaries that define the perimeter. They estimate a C_ant influx of ∼18 Tg C yr⁻¹ from the Pacific through the Bering Strait and a C_ant outflux through the CAA of ∼29 Tg C yr⁻¹, both for the 2000s. For the same time period, ORCA025 simulates 50 % more inflow through the Bering Strait (∼27 Tg C yr⁻¹) and 24 % more outflow through the CAA (∼36 Tg C yr⁻¹). The larger Bering Strait C_ant influx in ORCA025 is consistent with its overestimated Bering Strait water inflow (Table 5, Sect. 3.1.1). Integrating over all four lateral boundaries, Olsen et al. (2015) found a total net C_ant influx of ∼29 Tg C yr⁻¹, which is 24 % less than that simulated in ORCA025 averaged over 2000–2010 (∼38 Tg C yr⁻¹). Olsen et al. (2015) did not provide uncertainties, but the uncertainty of their net lateral flux estimate is at least ±18 Tg C yr⁻¹ based on the data-based transport estimates at the two other Arctic boundary sections where uncertainties are available (Table 5).

Weighing in at about one-fourth of the lateral flux is the simulated air–sea flux of C_ant in ORCA025 of 10 Tg C yr⁻¹ when both are averaged over 2000–2010. That simulated estimate is only about 40 % of the data-based estimate of 26 Tg C yr⁻¹ from Olsen et al. (2015). Although no uncertainty is provided with that data-based air–sea flux estimate, it too must be at least ±18 Tg C yr⁻¹ given that it is calculated as the difference between the data-based storage estimate (Tanhua et al., 2009) and the Olsen et al. (2015) data-based net lateral flux. The simulated air–sea flux of C_ant falls within that assigned uncertainty range for the data-based estimate. In any case, both the model and data-based estimates suggest that the air–sea flux of C_ant is not the dominant contributor to the anthropogenic carbon budget of the Arctic Ocean, respectively representing 21 % and 47 % of the total C_ant input averaged over 2000–2010. For both, the lateral flux dominates.

4.4 Model resolution

Basin inventories of simulated anthropogenic carbon differ between model configurations because of how resolution affects their volume, bathymetry, circulation patterns, and source waters. Much of the water in the Nansen and Amundsen basins has entered laterally from the Atlantic Ocean through the Fram Strait and the Barents Sea (Jones et al., 1995). Water inflow through the Barents Sea increases by 150 % when moving from ORCA2 to ORCA05 but only by 20 % more between ORCA05 and ORCA025. Water inflow in those two higher-resolution models is also closer to observational estimates. Along with the increase in water inflow, higher resolution also increases the lateral influx of C_ant. Yet despite this increase in the C_ant lateral influx, the air–sea C_ant flux into the Arctic Ocean also increases with resolution. This finding can be explained by two mechanisms:(1) higher resolution decreases the outflux of C_ant through the Fram Strait, which mainly occurs in subsurface currents and thus does not greatly affect surface C_ant concentrations nor air–sea exchanges of C_ant, and (2) higher resolution enhances deep-water formation, mainly in the Barents Sea, which reduces surface C_ant and thus enhances the air-to-sea flux of C_ant. Although the air–sea flux of C_ant increases slightly, the larger lateral water fluxes in ORCA05 and ORCA025 mainly explain their higher C_ant concentrations in the Nansen and Amundsen basins. Some of this inflowing water continues to flow further along the slope, across the Lomonosov Ridge into the Makarov Basin, and then across the Mendeleev Ridge into the Canada Basin. Yet how well models simulate that flow path depends on lateral resolution. Between ORCA2 and ORCA05, C_ant inventories increase by 16 % in the Canada Basin (+0.05 Pg C) and by 40 % the Makarov Basin (+0.06 Pg C). But between ORCA05 and ORCA025, increases are 2 to 5 times greater: +0.25 Pg C in the Canada Basin and +0.12 Pg C in the Makarov Basin (Sect. 3.4). The change from ORCA2 to ORCA05 mainly seems to improve lateral exchanges with adjacent oceans, while the change from ORCA05 to ORCA025 improves interior Arctic Ocean circulation.

As the increase from ORCA05 to ORCA025 stems from a finer, more realistic representation of lateral transport within the Arctic, it would appear that eddying ocean models may be needed to adequately simulate the interior circulation in terms of its effect on C_ant storage in the Arctic Ocean. In the Canada Basin, such lateral inflow may not be the only source of C_ant. Another major source appears to come from density flows along the continental slope, driven by brine rejection from sea-ice formation over the continental shelves (Jones et al., 1995). A signature of this source in the observed sections may be the chimneys of constant CFC-12 concentration from the surface to about 1000 m in the Canada Basin, features for which only ORCA025 exhibits any such indication, albeit faint. To adequately model lateral exchanges of C_ant in the Arctic Ocean, at least a resolution comparable to that used in ORCA05 may be needed, while resolutions comparable to that in ORCA025 or above may well be required to begin to capture the effects from density flows along the slope. As a consequence of the deficient representation of these density flows, we would expect to see an increase in C_ant when using even higher resolution.

Improved modeled circulation from higher model resolution has also been shown to be critical to improving simulated anthropogenic tracers in the Southern Ocean (Lachkar et al., 2007) and simulated oxygen concentrations in the tropical Atlantic (Duteil et al., 2014).

Table 8CMIP5 models used in this study and the corresponding model groups.

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4.5 CMIP5 comparison

For a wider perspective, we compared results from our forced NEMO-PISCES simulations to those from nine ocean biogeochemical models that were coupled within different earth system modeling frameworks as part of CMIP5 (Table 8, Fig. 9). When the CMIP5 models are compared to the data-based estimate of the C_ant inventory, only the MIROC-ESM with its inventory of 2.7 Pg C falls within the data-based uncertainty estimate (2.5 to 3.3 Pg C in 2005). The next closest CMIP5 models are NorESM1-ME and HadGEM2-ES, which fall below the lower limit of the data-based range by 0.1 and 0.5 Pg C. Then come the MPI-ESM and GFDL-ESM models with their C_ant inventories in 2005 that are 0.9 to 1.5 Pg C lower than the lower limit. The lowest CMIP5 estimates are from both versions of the IPSL model, whose inventories reach only ∼20 % of the data-based range. Adjusting all the CMIP5-model Arctic inventories upward by ∼0.4 Pg C to account for their late start date in 1850, as we did for our three simulations, would place two of them (MIROC-ESM and NorESM1-ME) above the lower boundary of the data-based uncertainty estimate and another (HadGEM2-ES) just 0.1 Pg C below this lower boundary. Lateral fluxes over 1958–2012 also vary between CMIP5 models from an outflow of 0.3 Pg C in the IPSL-CM5A-LR model to an inflow of 1.1 Pg C in the MIROC-ESM model. Only the first three CMIP5 models mentioned above exhibit large net inflow of C_ant into the Arctic Basin (between 0.7 and 1.1 Pg C during 1960–2012), a condition that appears necessary to allow a model to approach the estimated data-based inventory range. Indeed, the six other CMIP5 models have lower lateral fluxes (−0.5 to 0.5 Pg C) and simulate low C_ant storage in 2005.

What is perhaps most surprising are the large differences between our forced ORCA2^* model and the IPSL-CM5A-LR and IPSL-CM5A-MR ESMs. All three of those models use the same coarse-resolution ocean model, although both ESMs rely on an earlier version with a different vertical resolution (31 instead of 46 vertical levels). The contrast in vertical resolution may explain part of the large difference in inventories (1.3 Pg C for our forced version that is not corrected for the late starting date vs. 0.3–0.6 Pg C for the two coupled versions) but the forcing could also play a role. Lateral resolution is not the only factor when aiming to provide realistic simulations of C_ant storage and lateral transport in the Arctic. Sensitivity studies testing other potentially critical factors are merited.

Figure 10Profiles of Ω_A for ORCA05 in 1960 (black solid) as well as ORCA2 (green dots), ORCA05 (red dashes), and ORCA025 (blue dot–dash) in 2012. The vertical black dashed line indicates the chemical threshold where Ω_A=1. The point where that vertical line intersects the other curves indicates the depth of the ASH.

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Figure 11Surface Ω_A for ORCA2, ORCA05, and ORCA025 (a–c) in August 2012.

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4.6 Effect on aragonite saturation state

Given that simulated C_ant is affected by lateral model resolution, so must be simulated ocean acidification. The aragonite saturation state (Ω_A) was computed for each resolution from the historical run's C_T, A_T, T, S, P_T, and Si_T, after correcting C_T and A_T for drift based on the control run. The higher concentrations of C_ant in the ORCA05 and ORCA025 simulations reduces Ω_A between 1960 and 2012 by more than twice as much as found with ORCA2 during the same period (Fig. 10). These differences translate into different rates of shoaling for the aragonite saturation horizon (ASH), i.e., the depth where Ω_A=1. During 1960–2012, the ASH shoals by ∼50 m in ORCA2, while it shoals by ∼150 m in ORCA05 and ∼210 m in ORCA025. Thus, model resolution also affects the time at which waters become undersaturated with respect to aragonite with higher resolution producing greater shoaling.

Although basin-wide mean surface Ω_A does not differ among resolutions, there are regional differences such as over the Siberian Shelf (Fig. 11). The minimum Ω_A in that region reaches 0.9 in ORCA2, while it drops to 0.3 in ORCA05 and 0.1 in ORCA025. That lower value in ORCA025 is more like that observed, e.g., down to 0.01 in the Laptev Sea (Semiletov et al., 2016). As these lows in Ω_A are extremely local, they cannot be expected to be captured in coarse-resolution models such as ORCA2. Higher-resolution models are needed in the Arctic to assess local extremes not only in terms of ocean acidification but also other biogeochemical variables.