The Southern Hemisphere subtropical anticyclones (SAs) are important features of the Earth's climate. A broad consensus among Coupled Model Intercomparison Project phase 3 and phase 5 climate models suggests an intensification of summer SAs over SH oceans in association with the increase in greenhouse gas concentrations in the atmosphere. Diagnostic and modeling analyses conducted here demonstrate that the strengthening of the SAs is primarily caused by enhanced diabatic heating over continents and cooling over oceans in austral summer. This enhancement of Southern Hemisphere near-surface SAs identified here together with the enhancement of their Northern Hemisphere counterparts as suggested by Li et al. (2012) indicates increasingly important roles played by SAs in modulating weather and climate on regional and global scales.
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 Connecting midlatitude westerlies with tropical easterlies, Southern Hemisphere subtropical anticyclones (SAs) are important elements of the summertime atmospheric circulation [Wu et al., 2009; Miyasaka and Nakamura, 2010; Lee et al., 2013]. In austral summer, SAs are closely related to the seasonal variation of moisture transport, precipitation [Lenters and Cook, 1999; Taschetto and Wainer, 2008], and tropical cyclone movement [Bannister et al., 1997]. The near-surface maritime anticyclonic systems could also strongly influence marine boundary layer (MBL) clouds and associated radiation budget [Garreaud et al., 2001; Wang et al., 2004] through their interaction with sea surface temperatures (SSTs) and the clouds [Klein and Hartmann, 1993; Rahn and Garreaud, 2010]. Thus, intensity changes of the SAs have major implications for climate change at both regional and global scales.
 Recent studies found that both Northern Hemisphere SAs have intensified in boreal summer [Zhou et al., 2009; Li et al., 2011, 2012]. The enhancement of the Northern Hemisphere SAs is primarily attributed to an increase in the land-sea thermal contrast during boreal summer in a warming climate [Li et al., 2012]. However, whether the intensity of the summertime SAs over Southern Hemisphere oceans is also changing has yet to be investigated. Climatologically, the Southern Hemisphere SAs share similar dynamics with their Northern Hemisphere counterparts [Wu et al., 2009; Miyasaka and Nakamura, 2010], i.e., they are forced by longwave (LO) radiative cooling over eastern oceans, sensible heating (SH) and condensational (CO) heating over western and eastern continents, respectively. Such heating patterns largely determine the strength of the SAs [Wu and Liu, 2003; Miyasaka and Nakamura, 2005; Wu et al., 2009]. It is unclear whether the physical mechanisms associated with the intensity changes of the SAs in Southern Hemisphere in a warming climate bear similarities with those responsible for the observed changes in their Northern Hemisphere counterparts. Understanding the intensity changes in the Southern Hemisphere SAs and the possible causes can help improve prediction of regional weather and climate.
 This work investigates the intensity change of the low-level summertime SAs over the Indian Ocean (IOSA), the South Pacific (SPSA), and the South Atlantic (SASA) through data diagnosis and numerical modeling. Possible mechanisms responsible for the intensity change of the Southern Hemisphere SAs are investigated.
2 Data and Methods
 Data used in this study consist of atmospheric circulation field from the 40 year European Centre for Medium-Range Weather Forecasts (ECMWF) Re-Analysis (ERA-40) from 1958 to 2002 [Uppala et al., 2005] and from both the Coupled Model Intercomparison Project phase 3 (CMIP3) and phase 5 (CMIP5) of the Intergovernmental Panel on Climate Change Fourth and Fifth Assessment Reports, respectively. An idealized general circulation model (IGCM) is adopted to further examine the processes responsible for the intensity change of the Southern Hemisphere SAs in a warming climate (see supporting information for more details).
3.1 Intensity Changes of the Southern Hemispheric SAs in Current and Future Climates
 Historically, there are two methods to define the intensity of SAs: the maximum stream function and the domain-averaged stream function over the climatological SA regions [Liu and Wu, 2004; Liu et al., 2007]. The domains used in the study are 40°S–20°S and 140°W–80°W for the SPSA, 35°S–25°S and 45°W–10°W for the SASA, and 35°S–20°S and 60°E–100°E for the IOSA, respectively. The two methods show similar results in the SAs' intensity change.
 Summertime climatological maritime anticyclonic systems from CMIP3 and CMIP5 models' simulation are first compared with those in ERA-40 that illustrate weaker low-level anticyclonic circulation over South Atlantic and Indian Ocean than that over South Pacific (Figure 1). During the period 1958–2002, the ERA-40 shows significant strengthening of all three SAs: the average stream function increased by −1.1 × 105 m2 s−2/decade, −6.9 × 105 m2 s−2/decade, and −3.1 × 105 m2 s−2/decade for the SPSA, the SASA, and the IOSA, respectively, and the trends of intensification are significant, with 95% confidence (the Mann-Kendall test).
 Compared to ERA-40, CMIP3 (CMIP5) model reasonably captures the shapes of the three maritime anticyclones in the twentieth century (1950–1999) (Figure 1a), but the intensities of the anticyclones are overestimated in CMIP3 and CMIP5 models. Specifically, multimodel ensemble (MME) mean intensity of the IOSA, the SPSA, and the SASA simulated by CMIP3 (CMIP5) model is systematically stronger by 6.6% (12.4%), 3.6% (13.7%), and 6.8% (19.9%), respectively.
 In the future, CMIP3 (CMIP5) model projects consistent expansion and center intensification for all three SAs in austral summer (Figure 1): The anticyclones tend to expand more zonally and westward, especially for the SPSA. Domain-averaged intensity of the SPSA simulated by the CMIP3 (CMIP5) model increases from −1.716 × 107 (−1.919 × 107) m2 s−2 (95% confidence interval based on t test: −1.695 × 107 and −1.74 × 107m2 s−2 for CMIP3 and −1.902 × 107 and −1.935 × 107m2 s−2 for CMIP5) in the twentieth century (1950–1999) to −1.77 × 107m2 s−2 (−1.955 × 107) m2 s−2 (95% confidence interval: −1.755 × 107 and −1.783 × 107m2 s−2 for CMIP3 and −1.94 × 107 and −1.97 × 107m2 s−2 for CMIP5) in the 21st century (2050–2099; Figures 2b and 2e). The difference between the SPSA intensity in the 21st and the 20th century simulations by CMIP3 and CMIP5 models are at 0.0001 significance level (χ2 test).
 Similar results are also found for the SASA and the IOSA using CMIP3 (CMIP5) models: domain-averaged SASA intensity is enhanced from−1.547 × 107m2 s−2 (−1.748 × 107) m2 s−2 in the twentieth century simulation to −1.597 × 107m2 s−2 (−1.765 × 107m2 s−2) in the 21st century simulation, and the MME mean intensity of the IOSA is enhanced from −1.277 × 107 m2 s−2 (−1.386 × 107 m2 s−2) during the period 1950–1999 to −1.335 × 107 (−1.428 × 107 m2 s−2) m2 s−2 during the period 2050–2099. The intensity differences of the SASA and the IOSA between the 20th and the 21st century simulations are significant at 0.01 level (χ2 test).
 In addition to the intensification of the anticyclonic circulations, the central areas of the anticyclones expand by about 500% (60%), 60% (30%), and 200% (100%) for the SPSA, the SASA, and the IOSA in CMIP3 (CMIP5) models, respectively. Overall, CMIP3 and CMIP5 model simulations indicate a consistent intensification of the three maritime anticyclonic systems during austral summer over Southern Hemisphere in a greenhouse gasses (GHGs) increase scenario.
3.2 Physical Mechanism for the Southern Hemisphere SAs' Strengthening
 Climatologically, Southern Hemisphere near-surface SAs share similar dynamics to their Northern Hemisphere counterparts [Wu et al., 2009; Miyasaka and Nakamura, 2010]. In the summer subtropics (15°S–45°S), the dominant diabatic heating is organized as follows: SH and CO heating over the western and eastern continents and LO cooling over eastern oceans, i.e., heat sources (sinks) over lands (oceans) [Wu and Liu, 2003; Miyasaka and Nakamura, 2005; Wu et al., 2009]. Corresponding to such heating patterns, atmospheric circulation in the subtropics is thus formed as anticyclonic (cyclonic) circulation over oceans and cyclonic (anticyclonic) circulation over continents in the lower (upper) troposphere [Wu and Liu, 2003; Miyasaka and Nakamura, 2005; Wu et al., 2009]. We will examine whether this diabatic heating critical to the summertime SAs in Southern Hemisphere changes and how the changes of heating alter the intensity of the near-surface SAs from the 20th to the 21st century, when GHGs increase through the analyses of CMIP3 models and IGCM experiments.
 Figure 3a demonstrates the column-integrated dominant heating change from the period of 1950–1999 to 2050–2099. Increases of SH (CO) heating are mainly over western subtropical Africa, southern Australia, and western South America (central and eastern subtropical Africa, North Australian monsoon region, the south Pacific convergence zone, and central to eastern South America between 20°S and 30°S), and enhanced LO cooling is mainly over the eastern South Atlantic, eastern South Pacific, and South Indian Ocean. Consistent with the changes in the dominant heating component, total diabatic heating increases (decreases) over continents (eastern oceans). Specifically, increased total heating over western continents is characterized by the maximum increase near the surface, and less changes with increasing altitude, suggesting that total diabatic heating change is dominated by SH heating change over the western continents (Figure 3c). Increased total heating over eastern continents from the 20th to 21st century are more obvious in the middle to upper troposphere, a prominent feature of CO heating (Figure 3b). LO cooling is also enhanced over eastern oceans (Figure 3d). Overall, the spatial pattern of diabatic heating enhancement from the 20th to 21st century (Figure 3) is similar to the heating climatology [Wu and Liu, 2003; Miyasaka and Nakamura, 2010] thus favors a stronger anticyclonic circulation over oceans, consistent with other studies [Seager et al., 2003; Liu et al., 2004; Nakamura et al., 2010].
 To verify the results from data analysis, we further perform simulations with an IGCM to study the impact of the heating changes discussed above on the intensity variations of the Southern Hemisphere SAs. Figure 4a compares the forced circulation field to the circulation in which only CMIP3 climatological planetary-scale flow is included in austral summer. Responding to the total diabatic heating change, the modeled intensity of the SPSA is enhanced, with maximum stream function changing from −2.04 × 107m2 s−2 to −2.26 × 107m2 s−2 and the anticyclone's central area (stronger than −2.0 × 107m2 s−2) expanding by about 375%. As we will show shortly, the intensification of the SPSA driven by the total diabatic heating changes (Figure 4a) is stronger than the sum of the modeled stream function responses to three individual heating changes (Figures 4b–4d), suggesting the existence of strong nonlinearity in the system. Similar to the SPSA, the intensities of the IOSA and SASA increase (Figure 4a), with a relatively uniform expansion for the SASA, more westward expansion for the IOSA (Figure 4a).
 We also investigate the changes of the SA intensities (Figures 4b–4d) associated with changes in SH heating over the western continents (Figures 3a and 3c), CO heating over eastern continents (Figures 3a and 3d), and LO cooling over eastern oceans (Figures 3a and 3b), separately. Figure 4c shows intensification and zonal expansion of the SPSA and IOSA responding to the increase of SH heating in the 21st century. The SASA shifts slightly eastward but no significant change of its intensity. Accompanying with the enhanced LO cooling over the eastern oceans, the three SAs all intensify (Figure 4b). The intensification is more apparent around the center of the SPSA and the SASA, and the former shifts eastward. The IOSA expands westward slightly (Figure 4b). Figure 4b suggests an important role of the LO cooling associated with MBL clouds over the eastern south Pacific and Atlantic in the SAs intensity. Note that the IGCM used here does not include the two-way coupling processes between the SAs and diabatic heating anomalies associated with local SSTs and MBL clouds variations; additional experiments with a fully coupled atmosphere-ocean model are needed to further confirm the findings here, which constitute our next research step. Corresponding to the changes of CO heating, the IOSA intensifies, especially at its center, while the SPSA expands westward slightly (Figure 4d), but the SASA does not change much. Figure 4 thus suggests that the intensification of the three southern hemisphere SAs is closely related with collectively diabatic heating changes from the 20th to the 21st century. IGCM experiments further prove that the enhancement of the low-level subtropical anticyclonic circulations over Southern Hemisphere oceans largely results from the stronger diabatic heating over land and is associated with LO cooling over oceans during austral summer in the future.
 Using the ERA-40, 23 CMIP3 and 30 CMIP5 model outputs, and IGCM simulations, this study assesses current and future changes in the strength of the summertime near-surface SAs over Southern Hemisphere oceans. CMIP3 and CMIP5 models project an unambiguous intensification of the three SAs in austral summer when GHGs increase. CMIP3 and CMIP5 models and the IGCM experiments suggest that the projected strengthening of these SAs can be interpreted as a collective response to the enhanced warming over continents and cooling over oceans and also to the possible feedbacks between the SAs and the MBL clouds especially over the South Pacific and South Atlantic, which is consistent with the current understanding of the dynamical forcings of SAs [Liu et al., 2004; Miyasaka and Nakamura, 2005; Seager et al., 2003; Nakamura, 2012]. These results along with those from Li et al.  demonstrate that intensification of summer SAs over oceans is a global phenomenon in the current and future climates. These results imply increasingly important roles played by global subtropical anticyclones in modulating regional and global weather and climate patterns as their intensities rise.
 We acknowledge the World Climate Research Programme's Working Group on Coupled Modelling, which is responsible for CMIP, and we thank the international modeling groups for producing and making available their model output. For CMIP, the U.S. Department of Energy's Program for Climate Model Diagnosis and Intercomparison provides coordinating support and led development of software infrastructure in partnership with the Global Organization for Earth System Science Portals. We also thank Guoxiong Wu and Gudrun Magnusdottir for helpful discussion, Cuihua Li for graphic help, and Ming Cai and an anonymous reviewer for insightful comments. This work is supported by the NSF AGS 1147608, NSF AGS 1147601, NSF ATM 07-39983, and NOAA grant NA10OAR4320137.
 The Editor thanks an anonymous reviewer and Tianjun Zhou for their assistance evaluating this manuscript.