PlioMIP2 simulations with NorESM-L and NorESM1-F
- 1Climate Change Research Center, Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing 100029, China
- 2NORCE Norwegian Research Centre, Bjerknes Centre for Climate Research, Bergen, Norway
- 3Department of Atmospheric Science, School of Environmental Studies, China University of Geosciences, Wuhan, China
- 4Nansen-Zhu International Research Centre, Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing 100029, China
Correspondence: Zhongshi Zhang (email@example.com)
As a continuation of the Pliocene Model Intercomparison Project (PlioMIP), PlioMIP Phase 2 (PlioMIP2) coordinates a wide selection of different climate model experiments aimed at further improving our understanding of the climate and environments during the late Pliocene with updated boundary conditions. Here we report on PlioMIP2 simulations carried out by the two versions of the Norwegian Earth System Model (NorESM), NorESM-L and NorESM1-F, with updated boundary conditions derived from the Pliocene Research, Interpretation and Synoptic Mapping version 4 (PRISM4). NorESM1-M is the version of NorESM that contributed to the Coupled Model Intercomparison Project Phase 5 (CMIP5). NorESM-L is the low-resolution of NorESM1-M, whereas NorESM1-F is a computationally efficient version of NorESM1-M, with similar resolutions and updated physics. Relative to NorESM1-M, there are notable improvements in simulating the strength of the Atlantic meridional overturning circulation (AMOC) and the distribution of sea ice in NorESM1-F, partly due to the updated ocean physics. The two NorESM versions both produce warmer and wetter Pliocene climate, with a greater warming over land than over ocean. Relative to the preindustrial period, the simulated Pliocene global mean surface air temperature is 2.1 ∘C higher with NorESM-L and 1.7 ∘C higher with NorESM1-F, and the corresponding global mean sea surface temperature enhances by 1.5 and 1.2 ∘C. The simulated precipitation for the Pliocene increases by 0.14 mm d−1 globally in both model versions, with large increases in the tropics and especially in the monsoon regions and only minor changes, or even slight decreases, in subtropical regions. The intertropical convergence zone (ITCZ) shifts northward in the Atlantic and Africa in boreal summer. In the simulated warmer and wetter Pliocene world, AMOC becomes deeper and stronger, with the maximum AMOC levels increasing by ∼9 % (with NorESM-L) and ∼15 % (with NorESM1-F), while the meridional overturning circulation slightly strengthens in the Pacific and Indian oceans. Although the two models produce similar Pliocene climates, they also generate some differences, in particular for the Southern Ocean and the northern middle and high latitudes, which should be investigated through PlioMIP2 in the future. As compared to PlioMIP1, the simulated Pliocene warming with NorESM-L is weaker in PlioMIP2 but otherwise shows very similar responses.
The mid-Pliocene warm period (mPWP, 3.0–3.3 million years ago), a warm and stable interval in the Earth's geological history with paleogeography configurations and greenhouse gas concentrations similar to today, provides an interesting case study for understanding possible warm climates in our future. During the mPWP, the estimated global mean temperature was about 2–3 ∘C higher than at present (e.g., Dowsett et al., 2009, 2010a). The global mean sea level was higher than that of today, with a peak of 22±10 m (Miller et al., 2012). Due to warm sea surface temperatures, the Arctic Ocean experienced seasonally sea-ice-free conditions (Cronin et al., 1993; Dowsett et al., 2010b; Robinson, 2009; Clotten et al., 2018). Ice sheets were smaller over western Antarctica and Greenland, and the vegetation belts were displaced poleward (Salzmann et al., 2008; Dowsett et al., 2010b).
The warm mPWP climate has been simulated with a suite of models under the framework of Pliocene Model Intercomparison Project Phase 1 (PlioMIP1), forced with the boundary conditions from Pliocene Research, Interpretation and Synoptic Mapping version 3 (PRISM3) (Dowsett et al., 2010a; Haywood et al., 2013). According to these simulations, the simulated global annual mean surface temperature during the mPWP was 1.8–3.6 ∘C above preindustrial levels (Haywood et al., 2010, 2013, 2016a). The high atmospheric CO2 level (405 ppmv) dominated the majority of warming in tropical regions, while clear-sky albedo was mainly responsible for a stronger warming at high latitudes (Hill et al., 2014). Furthermore, the Hadley cell became weaker and shifted poleward (Sun et al., 2013). Westerlies (Li et al., 2015) and global tropical cyclones (Yan et al., 2016) migrated poleward. Also, according to the models, the East Asian summer monsoon intensified in the Pliocene warm climate (R. Zhang et al., 2013), and the global monsoon system generally brought more precipitation into the expanded monsoon regions (Li et al., 2018). The simulated Arctic sea ice was less extensive and thinner than it is in modern times (Howell et al., 2016). The simulated Atlantic meridional overturning circulation (AMOC) and the associated ocean heat transport were similar to those of the preindustrial period (Zhang et al., 2013a). Despite the generally consistent features of the simulations, a large model–data mismatch in terms of the warming magnitude remained at the northern high latitudes (e.g., Atlantic, Arctic Ocean, and Asia) (Dowsett et al., 2013; Haywood et al., 2013; Salzmann et al., 2013).
To better understand the warm mPWP climate and to better constrain the model–data mismatch, PlioMIP Phase 2 (PlioMIP2) was launched in 2016. The modeling strategy adopted in PlioMIP2 has been revised to establish a better-balanced methodology for model–data comparisons. Instead of focusing on the time window between 3.0 and 3.3 Ma, PlioMIP2 identified the time slice of 3.205 Ma centered on an interglacial peak (marine isotope stage KM5c) as the key target for the model–data comparison (Haywood et al., 2016b). The updated boundary conditions taken from PRISM4 (Dowsett et al., 2016; Haywood et al., 2016b) are used in PlioMIP2.
In this study, we present PlioMIP2 simulations with two different versions of the Norwegian Earth System Model (NorESM), NorESM-L (Zhang et al., 2012), and NorESM1-F (Guo et al., 2019). In the following sections, we first introduce the two model versions and our experimental design. Next, we present the simulated results in Sect. 4 and discussions in Sect. 5. Finally, the last section gives the summary and conclusions.
The NorESM is developed based on the structure of the Community Climate System Model version 4 (CCSM4) from the National Center for Atmospheric Research (Gent et al., 2011). In the model, the atmospheric component is the Oslo version of CAM4 (Community Atmosphere Model version 4) (CAM4-Oslo), which implements an advanced scheme for interactions between aerosol and clouds (Kirkevåg et al., 2013). The oceanic component is the Miami Isopycnic Coordinate Ocean Model (MICOM) (Bleck and Smith, 1990; Bleck et al., 1992; Bentsen et al., 2013), with several improvements. To limit model complexity and speed up model integration, both NorESM-L and NorESM1-F use the standard, prescribed aerosol chemistry of CAM4 rather than that of CAM4-Oslo.
NorESM-L is a low-resolution of NorESM1-M (the version of NorESM that contributed to the Coupled Model Intercomparison Project Phase 5, CMIP5) and is developed for paleoclimate simulations (Zhang et al., 2012). The atmospheric component has a horizontal resolution of T31 (∼3.75∘) and 26 vertical levels. The ocean component employs a bipolar grid with a horizontal resolution of nominal 3∘ and uses 30 isopycnic vertical layers (Table 1). NorESM-L was used to simulate the Pliocene climate in PlioMIP1 (Zhang et al., 2012). Further information on NorESM-L is documented in Zhang et al. (2012).
NorESM1-F is assembled for long time simulations with relatively high resolutions and improved process representations and climate performance compared to NorESM1-M (Guo et al., 2019). In the model, the atmosphere component uses a horizontal resolution of 1.9∘ latitude and 2.5∘ longitude and uses 26 vertical levels. The ocean component employs a tripolar grid with a nominal 1∘ horizontal resolution and uses 53 vertical layers (Table 1).
In NorESM1-F, the change in ocean–sea-ice grid from bipolar in NorESM1-M to a tripolar configuration together with a reduction in model complexity by replacing the comprehensive aerosol–cloud process representations in NorESM1-M with the standard prescribed aerosol chemistry of CAM4 (as was done in NorESM-L) lead to large speedup of the model. In addition, the reduction in the coupling frequency between atmosphere–sea-ice and atmosphere–land and the dynamic subcycling of the sea ice is helpful to improve the computational performance with a relatively small effect on the modeled climate (Guo et al., 2019).
Compared to NorESM1-M, there are some updates in the ocean physics in NorESM1-F. NorESM1-F takes measures to reduce sea ice thickness biases in shelf regions and modifies the parameterization of oceanic mesoscale eddies and the vertical mixing (Guo et al., 2019). With those updates to the ocean physics, NorESM1-F provides reasonable simulations of sea ice and AMOC compared to NorESM1-M (Guo et al., 2019). In the atmosphere component, the model adopts the formulation for energy updates and energy conservation, changes the air–sea flux calculation, and modifies the calculation of the solar zenith angle (Guo et al., 2019). Compared to NorESM1-M, the seasonal cycle of sea surface temperature in the equatorial Pacific is markedly improved with NorESM1-F. There are also several important improvements on how precipitation is simulated, e.g., improvements in seasonality, reduced wet bias, and mitigation of the common double intertropical convergence zone (ITCZ) problem. Further details on the model performance of NorESM1-F can be found in Guo et al. (2019).
a In the preindustrial experiments, the ocean component of NorESM-L and NorESM1-F was initialized from rest in both cases. The ocean component of NorESM-L was initiated from Levitus temperature and salinity (Levitus and Boyer, 1994). The ocean component of NorESM1-F was initialized from the Polar Science Center Hydrographic Climatology (PHC) 3.0, updated from Steele et al. (2001). In the Pliocene experiments, the Pliocene T/S (temperature / salinity) with NorESM-L was initiated from T/S in the PlioMIP1 experiment with NorESM-L (Zhang et al., 2012). The Pliocene T/S with NorESM1-F was initiated from T/S in the preexisting experiment under a 2000-year spin-up with atmospheric CO2 concentration set to 400 ppmv. b After a 2000-year spin-up with atmospheric CO2 concentration set to 400 ppmv, the experiment is integrated for another 500 years forced with all Pliocene boundary conditions.
3.1 Preindustrial control experiment
According to the PlioMIP2 protocol (Haywood et al., 2016b), we use modern geographic boundary conditions, including modern land–sea mask, topography, and ice sheets and vegetation for the year 1850, in the preindustrial control experiments (Table 2). For NorESM-L, we set atmospheric CO2, N2O, and CH4 levels to the preindustrial values of 280 ppmv, 270 ppbv, and 760 ppbv, respectively. The orbital parameters apply values for the year 1950. For NorESM1-F, the default preindustrial atmospheric CO2, N2O, and CH4 levels are 284.7 ppmv, 275.68 ppbv, and 791.6 ppbv, respectively.
The preindustrial experiment with NorESM-L was run for 2200 years, and the experiment with NorESM1-F was run for 2000 years. Climatological means of the last 100 years were analyzed in this study.
3.2 Pliocene experiment
Following PlioMIP2 experimental guidelines (Haywood et al., 2016b), we close the Hudson Bay, Bering Strait, and straits through the Canadian Arctic Archipelago in the Pliocene land–sea configuration. The atmospheric CO2 concentration is set to 400 ppmv. Atmospheric N2O and CH4 concentrations, the solar constant, and orbital parameters are identical to preindustrial values (Table 2).
We use the “anomaly method” recommended in PlioMIP2 to create the paleogeography for the Pliocene experiment. We first calculate differences between the PRISM4 Pliocene and PRISM4 modern topography and interpolate these to a T31 resolution for NorESM-L and to a resolution for NorESM1-F. Then, we add the interpolated topography anomalies to modern topography in the preindustrial experiment.
To create vegetation in the Pliocene experiment, we first interpolate PRISM4 Pliocene vegetation to the resolution for NorESM-L and for NorESM1-F. Then, we convert biome vegetation types to LSM (land system model) vegetation types following the procedure outlined by Rosenbloom (2009). Lakes for the Pliocene are prescribed by adding the PRISM4 lake area anomaly to modern conditions. Pliocene soil conditions remain the same as the preindustrial conditions.
With NorESM-L, the Pliocene experiment was run for 1200 years. With NorESM1-F, the Pliocene experiment was first spun up for 2000 years with atmospheric CO2 concentration set to 400 ppmv and then run for 500 years forced with all Pliocene boundary conditions. Climatological means of the last 100 years were used for analysis.
a NH – Northern Hemisphere. b SH – Southern Hemisphere. c ANN – annual mean; JJA – June–July–August; DJF – December–January–February.
4.1 Surface air temperature
Relative to the preindustrial experiments, the simulated Pliocene climate is warmer according to both NorESM versions (Fig. 1). The global annual mean surface air temperature (SAT) increases by 1.7 and 2.1 ∘C under the NorESM1-F and NorESM-L Pliocene simulations, respectively. In particular, stronger warming appears at high latitudes (Fig. 1 and Table 3). The simulated Pliocene annual mean SAT increases by 5.2 ∘C (NorESM1-F) and 4.9 ∘C (NorESM-L) at the northern high latitudes and by 3.2 ∘C (NorESM1-F) and 7.6 ∘C (NorESM-L) at the southern high latitudes. Weak cooling appears in tropical Africa, India, northeastern Asia, northern Australia, and the southern Pacific close to western Antarctica, under the NorESM1-F and NorESM-L Pliocene simulations (Fig. 1a, b). Both NorESM1-F and NorESM-L simulate stronger warming over land than over ocean. Relative to the preindustrial period, the simulated Pliocene global mean surface air temperature (SAT) over land increases by 2.3 ∘C with NorESM-L and 2.0 ∘C with NorESM1-F, which is notably larger than the warming over ocean (2.0 and 1.6 ∘C for the NorESM-L and the NorESM1-F, respectively). This stronger warming over land is a common feature in most PlioMIP2 simulations. However, the simulated zonal mean SAT over land is nearly twice as large as in the ocean at the northern high latitudes (Fig. S1 in the Supplement).
Changes in seasonal SAT follow a similar pattern to those of the annual SAT. The two models generate strong seasonal warming in Circum-Arctic regions, e.g., Hudson Bay, the Canadian Arctic Archipelago, and Greenland, in the Pliocene experiment. However, NorESM-L produces larger Pliocene seasonal warming over the Southern Ocean and Antarctica than NorESM1-F.
The simulated Pliocene global mean annual precipitation increases by 0.14 mm d−1 according to the two NorESM versions (Fig. 2). The mean annual precipitation increases largely in the tropical regions and especially in monsoon regions of North Africa, Asia, and Australia. In subtropical regions, the zonal mean annual precipitation does not change markedly or slightly decreases. The changes in seasonal precipitation generally follow the pattern of annual precipitation. Both models suggest that the ITCZ shifts northward in the Atlantic and in Africa in the boreal summer but does not change considerably in the boreal winter.
4.3 Sea surface temperature
Both NorESM1-F and NorESM-L simulate higher sea surface temperatures (SSTs) in the Pliocene experiments compared to preindustrial experiments (Fig. 3). The simulated Pliocene global mean annual SST is 1.2 ∘C (NorESM1-F) and 1.5 ∘C (NorESM-L) higher than preindustrial levels (Fig. 3 and Table 3). Large increases in SST appear at the high latitudes of both hemispheres (Fig. 3 and Table 3). The simulated Pliocene annual mean SST increases by 2.4 ∘C (NorESM1-F) and 2.1 ∘C (NorESM-L) in the middle and high latitudes of the North Atlantic (north of 30∘ N) and by 1.4 ∘C (NorESM1-F) and 2.4 ∘C (NorESM-L) in the Southern Ocean. A slight cooling occurs in the South Pacific close to western Antarctica according to the Pliocene experiments for both NorESM model versions. The seasonal change in SST is largely consistent with the annual pattern.
4.4 Sea surface salinity
Changes in sea surface salinity (SSS) from the Pliocene experiments differ notably between NorESM1-F and NorESM-L. The global mean SSS decreases by 0.34 g kg−1 in the NorESM1-F Pliocene simulation, while it increases by 0.16 g kg−1 according to the NorESM-L Pliocene simulation (Fig. 4). With NorESM1-F, Pliocene SSS generally decreases in most oceans, except for Baffin Bay, the Labrador Sea, and the North Atlantic subpolar regions. With NorESM-L, Pliocene SSS increases slightly in most oceans, while it decreases in the Indian Ocean and in the Arctic.
The divergent responses in SSS in NorESM1-F and NorESM-L are most likely to be associated with the different vertical redistribution of salt in the two models, due to differences in, e.g., surface layer mixing, ocean ventilation, convection, and circulation. The two models have different vertical resolutions and horizontal or vertical mixing schemes. When the drift in global mean SSS is removed, NorESM-L and NorESM1-F show similar regional anomalies (Fig. S2). Both versions show that the SSS contrast among the Indian Ocean, the Arctic, and the rest of the oceans is intensified in the Pliocene experiment (Fig. S2).
4.5 Sea ice
The simulated Pliocene sea ice with NorESM1-F and NorESM-L is reduced both in terms of its thickness and its extent (Fig. 5). In the Northern Hemisphere, the simulated Pliocene sea ice thickness in the Arctic Ocean is reduced by 0.5 to 1 m in March and by more than 1 m in September. In September, NorESM1-F simulates an almost ice-free Arctic in the Pliocene experiment, while sea ice remains in the central Arctic according to the NorESM-L Pliocene simulation. In March, sea ice becomes thinner while still covering most of the Arctic Ocean in both models. In the Southern Hemisphere, although both models generate retreated sea ice extents for the Southern Ocean, NorESM-L simulates the larger sea ice responses. The Southern Ocean becomes almost ice-free specifically in March according to the NorESM-L Pliocene simulation.
The strength of shallower circulation in the subtropical gyre of the North Pacific is represented by the PMOC maximum north of 5∘ N above 500 m. The strength of Pacific Deep Water is represented by the PMOC minimum measured below the 500 m.
4.6 Meridional overturning circulation
The simulated Pliocene AMOC becomes stronger and deeper in both models compared to the preindustrial climate. With NorESM1-F, the maximum AMOC is 28.1 Sv in the Pliocene experiment, increasing by about 15 % (Fig. 6 and Table 4). With NorESM-L, the simulated maximum AMOC is 23.3 Sv in the Pliocene experiment, which is 2 Sv (about 9 %) larger than that in the preindustrial experiment. Both models suggest that the vertical extent of the AMOC cell penetrates deeper during the Pliocene relative to the preindustrial period (Fig. 6 and Table 4). Compared to the preindustrial period, Pliocene SSS increases in Baffin Bay, the Labrador Sea, and the North Atlantic subpolar gyre in both models (Fig. 4), reducing the surface stratification and tending to favor more open-ocean convection, thereby potentially contributing to the strengthened AMOC.
In the Pacific and Indian oceans, meridional overturning circulation is slightly stronger in the Pliocene experiments than in the preindustrial experiments. As for the shallower circulation in the North Pacific subtropical gyre, the maximum of the circulation is increased by 1.0 Sv with NorESM1-F (22.3 Sv for the preindustrial experiment vs. 23.3 Sv for the Pliocene experiment) and by 0.9 Sv with NorESM-L (30.7 Sv for the preindustrial experiment vs. 31.6 Sv for the Pliocene experiment) (Fig. 6 and Table 4). As for the deeper circulation associated with Pacific Deep Water, the strength is increased by 0.8 Sv with NorESM1-F (−13.6 Sv for the preindustrial experiment vs. −14.6 Sv for the Pliocene experiment) and by 4.6 Sv with NorESM-L (−17.0 Sv for the preindustrial experiment vs. −21.6 Sv for the Pliocene experiment) (Fig. 6 and Table 4). In the Pliocene experiments, both NorESM versions simulate an extended northward penetration of deep water.
5.1 NorESM1-F vs. NorESM1-L
Although the two versions of the NorESM simulate similar Pliocene climates, they still exhibit some differences. The most significant differences appear in the Southern Ocean (Fig. 1). SST increase over the Southern Ocean is ∼1 ∘C larger with NorESM-L than with NorESM1-F in the Pliocene experiments. This difference between the two model versions is likely to be associated with different responses in ocean heat transport and sea ice. Simulated Pliocene southward ocean heat transport to the Southern Ocean is reduced according to NorESM1-F but increased according to NorESM-L (Fig. 7a and c), which partly explains the reduction in the Southern Ocean sea ice extent being more pronounced for NorESM-L than it is according to NorESM1-F (Fig. 5). Pliocene (austral summer) sea ice is nearly absent according to NorESM-L, while it still covers part of the Southern Ocean according to NorESM1-F. On the one hand, the larger seasonal warming in the Southern Ocean favors less sea ice extent in the Pliocene experiment simulated with NorESM-L. On the other hand, the presence of less sea ice leads to a reduction in albedo and to a more active ocean–atmosphere interaction (e.g., ice–albedo feedback) and contributes to the higher levels of Southern Ocean warming in the Pliocene experiment simulated with NorESM-L.
NorESM-L also simulates increased ventilation in the Southern Ocean, while NorESM1-F does not. As is indicated by the changes in salinity, sea water over the Southern Ocean becomes less stratified according to the NorESM-L Pliocene simulation (Fig. 8). The weakened ocean stratification allows the Southern Ocean to be well ventilated. As a result, the simulated Pliocene deep water is much younger in the Southern Ocean (Fig. S3). This well-ventilated Southern Ocean also appeared from the PlioMIP1 simulation with NorESM-L (Zhang et al., 2013b). However, with NorESM1-F, simulated Pliocene Southern Ocean stratification appears similar to that simulated in the preindustrial experiment. Such divergent responses in Southern Ocean stratifications also appeared in the PlioMIP1 simulations (Zhang et al., 2013a). It remains difficult to fully explain the divergent responses. The explanation is likely related to the updated ocean physics and/or higher resolution in NorESM1-F when compared to NorESM-L.
The other remarkable differences in the Pliocene simulations with the two versions appear in the northern middle and high latitudes. Compared to NorESM-L, the increase in the Pliocene SST simulated with NorEMS1-F at the northern middle (high) latitudes is 0.2 ∘C (0.1 ∘C) larger (Fig. 3 and Table 3). The increase in the Pliocene annual mean SAT at the northern middle (high) latitudes with NorESM1-F is 0.2 ∘C (0.3 ∘C) larger (Fig. 1 and Table 3). The stronger Pliocene warming at the northern high latitudes is most likely related to the mechanism responsible for the larger responses in sea ice reduction with NorESM1-F since the clear-sky albedo, particularly in sea ice regions, dominates the high-latitude warming in the Pliocene (Hill et al., 2014). In association with the larger salinity increase in the northern North Atlantic (Fig. 4), the enhancement of AMOC is larger with NorESM1-F than with NorESM-L (∼15 % vs. ∼9 %), which favors the larger increases in the Pliocene northward ocean heat transport to the Atlantic with NorESM1-F (Figs. 6 and 7). Correspondingly, less sea ice simulated in the Pliocene experiment contributes to a larger warming at the high latitudes with NorESM1-F than with NorESM-L through the ice–albedo feedback (Figs. 1 and 3).
5.2 PlioMIP1 vs. PlioMIP2
With NorESM-L, the simulated Pliocene surface temperatures in PlioMIP2 are slightly cooler than those simulated in PlioMIP1. Simulated increases in global annual mean SAT and SST are 1.1 and 0.43 ∘C less in PlioMIP2 than those generated in PlioMIP1 (Fig. 9). At the northern middle and high latitudes, the simulated increases in annual mean SAT (SST) are 1.7 and 5.0 ∘C (1.0 and 0.7 ∘C) weaker, respectively, in PlioMIP2 than in PlioMIP1 (Fig. 9, and Table 5). Simulated weaker levels of Pliocene warming also appear in the PlioMIP2 experiment with HadCM3, according to which the Pliocene annual mean SAT is 0.4 ∘C cooler in PlioMIP2 (Hunter et al., 2019) than in PlioMIP1 (Bragg et al., 2012). However, MRI-CGCM2.3, CCSM4, and IPSL-CM5A all simulate a larger warming in the Pliocene experiments in PlioMIP2 (Kamae et al., 2016; Chandan and Peltier, 2017; Tan et al., 2020) than those in PlioMIP1 (Contoux et al., 2012; Kamae and Ueda, 2012; Rosenbloom et al., 2013).
The simulated weaker Pliocene warming is attributable to the modified boundary conditions used in PlioMIP2. Relative to PlioMIP1, the Pliocene atmospheric CO2 is 5 ppmv less in PlioMIP2 (400 ppmv in PlioMIP2 vs. 405 ppmv in PlioMIP1). The slight reduction in Pliocene atmospheric CO2 is not likely to induce a significant effect on the simulated Pliocene warming weakness. Compared to PlioMIP1, the seaways at the northern high latitudes (including the Bering Strait and Canadian Arctic Archipelago straits) are closed under the PlioMIP2 boundary conditions. Previous sensitivity investigations have demonstrated that the closure of the Bering Strait favors the formation of North Atlantic deep water and the intensification of AMOC by reducing freshwater transport from the Pacific to the Arctic Ocean and the North Atlantic (e.g., Hu et al., 2010; Brierley and Fedorov, 2016; Otto-Bliesner et al., 2017). In contrast, the closure of Canadian Arctic Archipelago Straits tends to weaken AMOC, by increasing fresh water transport through the Fram Strait and thereby leading to the freshening and subsequent cooling of the Labrador and Greenland–Iceland–Norwegian seas (Otto-Bliesner et al., 2017). However, the combined effects of closing these two seaways are complicated and appear to be model dependent. For example, with the Bering Strait and Canadian Arctic Archipelago Straits closed together, Pliocene ocean surface warming in the North Atlantic high latitudes is enhanced under the CCSM4 (Otto-Bliesner et al., 2017) and IPSL-CM5A simulations (Tan et al., 2020) but is weakened according to NorESM-L.
In this study, we used two versions of the NorESM (NorESM-L and NorESM1-F) to carry out core experiments designed in PlioMIP2, with boundary conditions derived from PRISM4. Relative to the preindustrial period, the simulated Pliocene global mean SAT is 2.1 ∘C higher according to NorESM-L and 1.7 ∘C higher according to NorESM1-F. The simulated Pliocene global mean SST is 1.5 ∘C warmer according to NorESM-L and 1.2 ∘C warmer according to NorESM1-F. Compared to NorESM1-F, the simulated Pliocene warming is larger with NorESM-L. In both model versions, Pliocene global mean precipitation increases by 0.14 mm d−1. Strong precipitation responses occur in tropical regions and especially in monsoon regions, and the ITCZ shifts northward in the Atlantic and in Africa in the boreal summer. According to the Pliocene experiments of both NorESM versions, AMOC becomes stronger and deeper, and meridional overturning circulation strengthens slightly in the Pacific and Indian oceans. Although the two models simulate similarly warm climates for the Pliocene, they also produce some differences, especially for the Southern Ocean and the northern middle and high latitudes. NorESM-L simulates increased ventilation in the Pliocene Southern Ocean, while NorESM1-F does not. Compared to the climate simulated with NorESM-L in PlioMIP1, the Pliocene warming simulated in PlioMIP2 (with the updated PRISM4 boundary conditions) is slightly less pronounced. A comparison of Pliocene climates simulated with NorESM-L in PlioMIP1 and PlioMIP2 shows a weaker warming in PlioMIP2. The Pliocene global mean SAT and SST are 1.1 and 0.43 ∘C lower, respectively, in PlioMIP2 than those in PlioMIP1. Sensitivity experiments testing the impacts of boundary condition modification made from PlioMIP1 to PlioMIP2, i.e., the effects of closing ocean gateways in the northern high latitudes, will be helpful in casting further light on these model discrepancies. The model–dependent sensitivity to the closure of the ocean gateways in the northern high latitudes will be an interesting question that is worth further attention within the PlioMIP2 community.
All PlioMIP2 boundary conditions are available on the USGS PlioMIP2 web page (https://geology.er.usgs.gov/egpsc/prism/7_pliomip2.html, last access: 19 January 2020). Climatological averages of the two NorESM versions will be uploaded to the PlioMIP2 data repository later (ftp://see-gw-01.leeds.ac.uk, last access: 18 January 2020). Request of access should be directed to Alan M. Haywood. Specific data can be obtained upon requests to the corresponding author Zhongshi Zhang (firstname.lastname@example.org).
The supplement related to this article is available online at: https://doi.org/10.5194/cp-16-183-2020-supplement.
ZZ and XL designed the study and developed the structure of this work. ZZ conducted the NorESM-L simulations. CG conducted the NorESM1-F simulations. XL analyzed all the data and wrote the paper. All co-authors contributed to writing the paper and discussing the data analysis.
The authors declare that they have no conflict of interest.
This article is part of the special issue “PlioMIP Phase 2: experimental design, implementation and scientific results”. It is not associated with a conference.
The NorESM simulations benefitted from resources provided by UNINETT Sigma2 – the National Infrastructure for High Performance Computing and Data Storage in Norway. We thank Baohuang Su for valuable discussion. We further thank the reviewers and editor for constructive suggestions and improvements to the paper.
This research has been supported by the National Key Research and Development Program of China (grant no. 2018YFA0605602), the National Natural Science Foundation of China (grant nos. 41888101, 41472160, and 41775088), the Norwegian Research Council (grant no. 221712, 229819), the Thousand Talents Program for Distinguished Young Scholars (Zhongshi Zhang), the China Scholarship Council (grant no. 201804910023), and the China Postdoctoral Science Foundation (grant no. 2015M581154).
This paper was edited by Wing-Le Chan and reviewed by two anonymous referees.
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