This study disentangles the changes in Indian Ocean (IO) dipole (IOD)-related SST and rainfall variability under global warming projected by the RCP8.5 runs in 29 CMIP5 models. The IOD rainfall changes consist of the thermodynamic component due to the surface moisture increase and the dynamic component due to the changes in IOD-related circulation. The IOD circulation changes are dominated by the IOD SST changes, which were further clarified using the amplitude and structural decomposition. The amplitudes of IOD SST and circulation are both decreased at rates of around 7.2% and 13.7% °C−1, respectively. The structural changes in IOD SST and circulation show a pattern with increases from the eastern to the western coast of the equatorial IO, similar to the pattern of so-called extreme IOD events in previous studies. Disentangling previous mechanisms and projections, we conclude that the increased atmospheric stability suppresses the amplitudes in IOD SST and circulation, whereas the positive IOD (pIOD)-like mean-state SST changes, leading to greater warming in the west than the east, mainly alter the structure of IOD SST and circulation. Both the amplitude and structural changes in the IOD SST and circulation are robust among the CMIP5 models, but their distinct patterns and out-of-step changes lead to an uncertain projection of IOD changes defined by the dipole mode index or EOF analysis in previous studies. Furthermore, the structural changes, dominated by the pIOD-like mean-state SST changes, are significantly correlated with the historical IOD amplitude among the models. Considering the commonly overestimated IOD amplitude as an emergent constraint, the structural changes in IOD SST and circulation should not be as robust as the original multimodel projection.
The Indian Ocean dipole (IOD) mode is a dominant interannual variability of sea surface temperature (SST) anomalies in the tropical Indian Ocean (IO) (Saji et al. 1999; Webster et al. 1999; Yu and Rienecker 1999; Murtugudde et al. 2000). The IOD features a zonal dipole pattern of SST anomalies (SSTAs) between the eastern equatorial IO (EEIO) off Sumatra and Java and the western equatorial IO (WEIO). A positive IOD (pIOD) event is defined by negative SSTAs in the EEIO and positive SSTAs in the WEIO, and the SST pattern of a negative IOD is an approximate mirror opposite to a pIOD. The SST pattern of the IOD is coupled with surface wind anomalies and a dipole pattern of rainfall anomalies over the equatorial IO (e.g., Yamagata et al. 2004; Schott et al. 2009; Cai et al. 2013). The prominent circulation and rainfall anomalies associated with the IOD often induce extreme disasters in the IO-rim regions (Ashok et al. 2003; Zubair et al. 2003; Behera et al. 2005; Kripalani et al. 2010).
The tropical IO also shows apparent warming with greenhouse gases increasing (e.g., Du and Xie 2008). How the IOD mode and its impact on regional climate will respond to global warming is one of the most significant issues (Ihara et al. 2009; Zheng et al. 2010; Cai et al. 2013; Zheng et al. 2013; Cai et al. 2014a). Apart from basin-uniform warming in IO, most state-of-the-art models project a robust pattern of mean-state SST changes with more warming in the WEIO and less in the EEIO, often called a pIOD-like pattern (Fig. 1) (Abram et al. 2008; Zheng et al. 2010, 2013; Liu et al. 2015; Luo et al. 2016). The pIOD-like mean-state SST changes will shoal the thermocline in the EEIO and deepen that in the WEIO, and the shoaling thermocline in the EEIO can enhance the local thermocline feedback, leading to an intensified local SST variability (Abram et al. 2008; Zheng et al. 2010). In contrast, global mean warming can increase the static stability of the tropical atmosphere (Knutson and Manabe 1995; Lu et al. 2008), leading to a decreased air–sea interaction variability in the tropics (Zheng et al. 2013; P. Huang et al. 2017). The opposite roles of the two processes result in an uncertain change in IOD-related SST variability projected in state-of-the-art models (Ihara et al. 2009; Cai et al. 2013; Zheng et al. 2013; Hui and Zheng 2018).
Although the changes in IOD-related SST variability (referred to simply as “IOD SST”) are projected with large intermodel spread, some studies reported that the extreme pIOD events using a rainfall-based definition are likely to increase in a warmer climate (Cai et al. 2014a; Wang et al. 2017). The robust pIOD-like pattern in mean-state SST change (Fig. 1), with weakened equatorial westerly winds and eastward oceanic currents was suggested to cause increased frequency of extreme pIOD events (Cai et al. 2014a). The distinct projections of IOD SST and IOD-driven rainfall variability (hereafter referred to as “IOD rainfall”) show that the relationship among the changes in IOD SST, IOD rainfall, and mean-state SST is still unclear.
There is a similar question with regard to the changes in ENSO-related SST and rainfall variability (Collins et al. 2010; Power et al. 2013). Recently, great progress has been made based on moisture budget decompositions for change in the interannual variability of tropical rainfall (Seager et al. 2012; Chung et al. 2014; Huang and Xie 2015; Huang 2016). A simplified moisture budget decomposition proposed in Huang and Xie (2015) defines change in the interannual variability of tropical rainfall as
where P is tropical rainfall, ω is pressure velocity at 500 hPa representing vertical motion, q is surface specific humidity, Δ denotes future change, and the prime denotes interannual variability. The term Δqω′ due to the mean-state moisture change Δq is defined as the thermodynamic component, and qΔω′ due to the change in circulation variability Δω′ is defined as the dynamic component. The moisture budget decomposition clearly presents the relationship among rainfall variability change ΔP′, circulation variability change Δω′, and mean-state moisture change Δq under global warming. Furthermore, for ENSO-related variability, the circulation variability change Δω′ is closely tied to the SST variability change and mean-state SST change pattern (Huang and Xie 2015; Huang 2016). This decomposition was also applied to study the rainfall variability change in South America and North America (Tedeschi and Collins 2017; Dong et al. 2018). The effectiveness of the simplified moisture budget decomposition for analyzing ENSO-related SST and rainfall variability provides a helpful method to disentangle the puzzling changes in IOD SST and IOD rainfall in a warmer climate.
In this study, we used the decomposition method in Huang and Xie (2015) to explore the mechanisms of IOD rainfall changes and the relationship with IOD SST changes, based on the outputs of 29 CMIP5 models in the historical and the +8.5 W m−2 representative concentration pathway (RCP8.5) runs. Our analyses show that the moisture decomposition method is also practicable to IOD rainfall changes: the thermodynamic component due to the mean-state moisture increase and the dynamic component due to IOD circulation changes can accurately describe the pattern of IOD rainfall changes. The relationship between changes in IOD circulation and IOD SST is also disentangled based on an amplitude and structural decomposition with an intermodel correlation analysis.
The rest of the paper is organized as follows. Section 2 describes the CMIP5 models and methods; section 3 presents the thermodynamic and dynamic decomposition of IOD rainfall changes; the relationship between changes in IOD SST and IOD circulation is presented in section 4; section 5 discusses the intermodel spread of changes in IOD-related variability projected in CMIP5; and conclusions and discussions are given in section 6.
2. Models and methods
The models, the definition of climatology and interannual anomaly, the moisture budget decomposition, and the amplitude and structural decomposition used in the present study are similar to that in Huang and Xie (2015) and Huang (2016), and are briefly reviewed here. The following introduction of the models and methods is derived from Huang (2016) with minor modifications.
a. Models and the definition of climatology and IOD-related variability
This study used the historical runs from 1971 to 2005 and the RCP 8.5 runs from 2006 to 2100 from 29 models of the CMIP5 (Taylor et al. 2012). The 29 models are ACCESS1.0, ACCESS1.3, BCC_CSM1.1, BCC_CSM1.1(m), BNU-ESM, CanESM2, CCSM4, CESM1(BGC), CMCC-CESM, CMCC-CM, CMCC-CMS, CNRM-CM5, GFDL CM3, GFDL-ESM2G, GFDL-ESM2M, GISS-E2-H, GISS-E2-R, HadGEM2-ES, IPSL-CM5A-LR, IPSL-CM5A-MR, IPSL-CM5B-LR, MIROC5, MIROC-ESM, MIROC-ESM-CHEM, MPI-ESM-LR, MPI-ESM-MR, MRI-CGCM3, NorESM1-M, and NorESM1-ME (expansions of acronyms are available online at http://www.ametsoc.org/PubsAcronymList). The oceanic and atmospheric outputs in all models were interpolated onto a 2.5° × 2.5° grid, which is effective for the large-scale interannual variability.
The calculation of interannual anomalies followed Zheng et al. (2013), removing the seasonal cycle, performing a 3-month running mean, and removing the 9-yr running mean. Then, the 1976–2005 period was selected as the current climate, and the eighteen 30-yr segments starting from 1981 with 5-yr leaps (i.e., 1981–2010, 1986–2015, 1991–2020, …, 2061–90, 2065–95) were selected as periods in the warming climate, and the beginning and ending 5-yr data were abandoned. The mean of each 30-yr segment in the RCP8.5 runs and the 1976–2005 in the historical runs defined the respective climatology. Here, the 30-yr division does not influence the conclusions. Because IOD typically matures in the months from September to November (SON) in observations and CMIP5 models (e.g., Zheng et al. 2013), we calculated the SON seasonal mean of the filtered SST anomalies to extract the IOD in the following steps. Considering the discrepancies of model simulation skill for the SST pattern of IOD, we defined the IOD pattern using the dipole mode index (DMI; Saji et al. 1999), which is the different regional-mean SST anomalies in the WEIO (50°–70°E, 10°S–10°N) minus the EEIO (90°–110°E, 10°S–0°), the two green boxes in Fig. 2a. The interannual anomalies of SST, rainfall, and circulation were regressed onto the standardized DMI to define IOD SST, IOD rainfall, and IOD circulation for each model and each 30-yr segment.
The average of all models defines the multimodel ensemble mean (MME). Four popular SST observation datasets were used to measure IOD amplitude in observations. They are NOAA ERSST version 4 from https://www1.ncdc.noaa.gov/pub/data/cmb/ersst/v4/netcdf/ (B. Huang et al. 2015), NOAA ERSST version 5 from https://www1.ncdc.noaa.gov/pub/data/cmb/ersst/v5/netcdf/ (B. Huang et al. 2017), HadISST from https://www.metoffice.gov.uk/hadobs/hadisst/ (Rayner et al. 2003), and COBE SST2 from https://www.esrl.noaa.gov/psd/data/gridded/data.cobe2.html (Hirahara et al. 2014).
b. Decompositions for IOD rainfall changes
Moisture budget decomposition is often used to investigate the formation mechanism of tropical rainfall changes in climatological mean state (Held and Soden 2006; Chou et al. 2009; Seager et al. 2010; Huang et al. 2013; Huang 2014) and in interannual variation (Seager et al. 2012; Chung et al. 2014; Huang and Xie 2015). In the present study, we applied the simplified moisture budget decomposition method proposed in Huang and Xie (2015) [Eq. (1)] to study IOD rainfall changes. In Eq. (1), the constant coefficient of the moisture budget equation is omitted for simplicity, as in previous studies (Huang et al. 2013; Huang and Xie 2015). Resultantly, the units on the two sides of Eq. (1) differ by a constant, which does not influence the conclusions.
Following Huang and Xie (2015) and Huang (2016), the changes in IOD circulation Δω′ can be further decomposed into amplitude and structural changes: . The amplitude changes were obtained by projecting the total Δω′ onto the historical ω′, and the residual was defined as the structural changes . Similarly, the changes in IOD SST ΔT′ were decomposed as . With the decomposition of IOD circulation changes, changes in IOD rainfall can be written as
where Δqω′ is the thermodynamic component, represents the amplitude changes in the dynamic component, and the structural changes in the dynamic component.
3. IOD rainfall changes and moisture budget decomposition
Figures 2a and 2b show the patterns of IOD SST and IOD rainfall, respectively, of the MME simulated in the CMIP5 models. The models’ performance in reproducing the IOD mode has been evaluated in previous studies (e.g., Zheng et al. 2013). The CMIP5 models can basically reproduce a realistic IOD mode. Here, the IOD SST and rainfall patterns were defined by the regression of the standardized DMI. As a result, the defined IOD-related patterns must be closer to the observations than the definition based on empirical orthogonal function (EOF) analysis in Zheng et al. (2013), especially for the models with a relatively unrealistic IOD pattern. On the other hand, the IOD SST is overestimated in the models compared with the observation, as reported in previous studies (Cai and Cowan 2013; Liu et al. 2014; Li et al. 2015).
The MME changes in IOD SST and IOD rainfall in the period of 2066–95 of the RCP8.5 run are shown in Figs. 2c and 2d, respectively. The pattern of IOD SST changes is roughly opposite that of the pIOD pattern (Fig. 2a). However, differing from the pIOD pattern, the western negative SST changes extend to the eastern coast of the equatorial IO and are much stronger than the positive SST changes off the Sumatra–Java coast, whereas the positive SST changes are only located in the Southern Hemisphere. The pattern of IOD SST changes will be discussed in section 4 in detail. For the IOD rainfall changes ΔP′, there are robust negative rainfall changes extending from the EEIO to the western coast of the equatorial IO and weak positive rainfall in the southeastern IO. The pattern of ΔP′ is similar to the pattern of extreme pIOD events defined by the second mode of EOF analysis for the rainfall anomalies in Cai et al. (2013), and consists of the projection of increased frequency of extreme pIOD events. The ΔP′ pattern basically corresponds to the ΔT′ pattern, except that the range of negative SST changes in ΔT′ is wider than that of the negative rainfall changes inΔP′.
Following the moisture budget decomposition, the total ΔP′ is decomposed into the thermodynamic (Δqω′; Fig. 3a) and dynamic (qΔω′; Fig. 3b) components. The pattern of the thermodynamic component is identical to the historical IOD circulation and rainfall (Fig. 2b) because the spatial gradient of mean-state moisture changes is much weaker than that of the historical IOD circulation. As a result, the thermodynamic component due to the surface moisture increase enhances IOD rainfall with the increase rate of surface moisture under global warming, around 7%–8% °C−1 following the Clausius–Clapeyron relationship. On the other hand, the dynamic component of ΔP′ due to the IOD circulation changes Δω′ shows a pattern with decreases extending from the EEIO to the western coast of the equatorial IO and weak increases in the southeastern IO, following the pattern of Δω′ (Fig. 4). The sum of the thermodynamic and dynamic components (Fig. 3c) accurately describes the pattern of ΔP′ (Fig. 2d and contours in Fig. 3c), indicating the simplified moisture budget decomposition [Eq. (1)] proposed in Huang and Xie (2015) for ENSO rainfall changes is also feasible for the IOD rainfall changes. The magnitude of the dynamic component (Fig. 3b) is around twice that of the thermodynamic component (Fig. 3a) and thus basically dominates the total ΔP′ (Fig. 3c). The contribution of the thermodynamic component is visible off the eastern coast of Africa and the western coast of Sumatra and Java. Obviously, the sum of the thermodynamic and dynamic components (Fig. 3c) is closer to ΔP′ than the dynamic component (Fig. 3b), showing that the thermodynamic component cannot be ignored.
4. Amplitude and structural decomposition for IOD SST and circulation
From Fig. 4, the pattern of IOD circulation changes Δω′ is roughly consistent with that of IOD SST changes ΔT′, both enhanced off the Sumatra–Java coast and decreased from the EEIO to the WEIO. On the other hand, the patterns of ΔT′ and Δω′ exhibit apparent discrepancies, especially the opposite changes at around 80°–100°E and 10°S–0°. Following the amplitude and structural decomposition introduced in section 2c, we decomposed ΔT′ and Δω′ into amplitude and structural changes, respectively. Dependent on the decomposition method, the amplitude changes of IOD SST (; Fig. 5a) have an identical pattern to the historical IOD SST (Fig. 2a), whereas the structural changes of IOD SST (; Fig. 5c) are spatially orthogonal to the historical IOD SST. Similarly, the pattern of the amplitude changes of IOD circulation () is identical to that of historical IOD circulation, and the pattern of the structural changes of IOD circulation () is orthogonal to the historical IOD circulation (not shown). Both and show a robust decrease relative to the pIOD pattern (Figs. 2a and 5a,b), which could be induced by the increased static stability (Knutson and Manabe 1995; Lu et al. 2008; Zheng et al. 2013; P. Huang et al. 2017). The pattern of is closely consistent with that of , both of which are similar to the pattern of extreme pIOD defined in Cai et al. (2014a).
The intermodel agreement test suggests that both and are robust among the models, which seems controversial given the conclusion that the IOD SST changes are not robust in the CMIP5 projections (Cai et al. 2013; Zheng et al. 2013). This result can be explained by the distinct patterns of and , which are a zonal dipole pattern and a monopole pattern with maximum in the central-eastern equatorial IO, respectively. Especially, is opposite to off the Sumatra–Java coast, the EEIO domain to calculate DMI, resulting in the nonrobust changes in IOD SST in the EEIO (Fig. 2c). To illustrate the robustness more clearly, we further calculated an IOD SST change index, which represents the different regional-mean IOD SST changes in the WEIO (50°–70°E, 10°S–10°N) minus the EEIO (90°–110°E, 10°S–0°), that is, the two green boxes for calculating DMI in Fig. 2a. The IOD SST change index is equal to the change in the standard deviation of DMI, hereafter referred to as the total DMI change. In Fig. 6a, the total DMI changes show an apparent intermodel spread, increased in 10 models and decreased in 19 models. The regional mean of IOD SST changes in the EEIO domain (90°–110°E and 10°S–0°) has similarly large intermodel spread (Fig. 6b), with an increase (decrease) in 15 (14) models. In contrast, the DMI mean of has very high intermodel agreement (Fig. 6c), being increased (decreased) in 6 (23) models; and represented by the regional mean over the central equatorial IO (60°–100°E, 5°S–5°N) is increased (decreased) in 25 (4) models (Fig. 6d).
Apart from the MME analysis, the intermodel relationship analysis is an effective way to study the mechanism of regional climate change (e.g., Huang and Xie 2015), which is further used to study the relationship between the changes in IOD SST and circulation. In Fig. 7a, the change percentage of is significantly correlated with that of in the 29 models, indicating the dominant role of in the intermodel spread of . It is noteworthy that the intercept of the – linear regression is not zero but around −21.7% at 2.6°C tropical-mean warming during 2066–95 in RCP8.5 runs (Fig. 7a). The negative intercept of the – linear regression indicates a faster decrease of than . Separately considered, decreases at a rate of around 13.7% per 1°C tropical-mean warming (Fig. 7b), and the rate for is around 7.2% °C−1 (Fig. 7c). As a result, the response of IOD circulation to IOD SST decreases at a rate of around 7.6% °C−1 (Fig. 7d), which is close to the Clausius–Clapeyron relationship. These change rates reveal that the increased atmospheric stability under global warming, following the Clausius–Clapeyron relationship (Knutson and Manabe 1995), directly influences the response efficiency of atmospheric circulation to external forcing (P. Huang et al. 2017), such as the SST anomalies here. Weakening of the IOD circulation response to IOD SST in turn influences the SST variability through the Bjerknes feedback. This process is robust among the models and does not depend on the model’s mean-state performance. On the other hand, the response of SST variability to atmospheric anomalies would be enhanced under global warming, which could be induced by the uniform decrease in the thermocline depth with the increased temperature stratification in the ocean subsurface (Pierce et al. 2006; Capotondi et al. 2012; P. Huang et al. 2015). The decreased response of circulation to SST anomalies is the dominant source of the decreased IOD SST amplitude under global warming, but must be balanced by the enhancement process to form a stable change in IOD SST and circulation variability.
Similar to the relationship between and , the structural changes in IOD circulation are also significantly correlated with the structural changes in IOD SST (Fig. 8a). Both and are linearly enhanced along with the tropical-mean SST increase during the calculation periods (Figs. 8b,c), but they also show different rates in the early and late twenty-first century, reflecting the non-unidirectional response of mean SST to global warming over the Indo-Pacific basin (Kim et al. 2014). In contrast to the progressive decrease in the amplitude of IOD circulation response to IOD SST (Fig. 7d), the strength of response to almost does not vary along the enhancement of global warming (Fig. 8d) and stays around the historical response strength of the IOD circulation to the IOD SST (dashed line in Fig. 8d). This result indicates that the atmospheric static stability changes and other possible mechanisms do not contribute to , and that is dominated by . The relationship between IOD-related and is different from that between the structural changes in ENSO-related SST and circulation (Huang and Xie 2015; Huang 2016), in which the structural changes in ENSO-related circulation can also be modified by the spatial pattern of the tropical Pacific SST increase via the atmospheric convection process (Cai et al. 2014b; Huang and Xie 2015). This result suggests that the oceanic mechanism proposed in Cai et al. (2014a) to explain the increased extreme pIOD events could form the structural changes in IOD SST and circulation. The pIOD-like mean-state SST changes (Fig. 1) associated with shoaling thermocline and weakening of equatorial eastward oceanic currents and westerly winds benefit the westward extension of the SSTAs in EEIO to form the structural changes in IOD SST and circulation relative to the historical patterns of IOD SST and circulation (Cai et al. 2014a). Because of the different change rates of , , , and , the pattern of is mismatched with that of shown in Fig. 4, although their subcomponents correspond well with each other (Fig. 5). This result disentangles the puzzle of the mismatch between ΔT′ and Δω′ shown in Fig. 4, which is crucial to understand the mismatch between ΔT′ and ΔP′ shown in Figs. 2c and 2d.
5. Intermodel uncertainty and the effect of model bias
Although CMIP5 models project a robust change in the structure of IOD SST and circulation associated with the pIOD-like mean-state SST changes (Fig. 1), Li et al. (2016) reported that the robust pIOD-like pattern of mean-state SST changes could be an artificial projection induced by the commonly overestimated IOD amplitude in the CMIP5 models, implying the projected increases in the extreme pIOD events would also be artificial. We defined a DMI-like SST index to represent the zonal pattern of mean-state SST changes in the models following Li et al. (2016), and used the standard deviation of DMI to represent the simulated historical IOD amplitude. Indeed, there are significant correlation between the zonal pattern of mean-state SST changes and the historical IOD amplitude among the models (Fig. 9), and the IOD amplitude is commonly overestimated in the models compared with the observation in four SST datasets ERSST version 4, ERSST version5, HadISST, and COBE SST2 (blue, red, brown, and green lines in Fig. 9, respectively) although the IOD amplitude in the four datasets shows some discrepancies varying from 0.37° to 0.42°C (Cai and Cowan 2013; Liu et al. 2014; Li et al. 2015). Under a spatial observational constraint strategy (Boé et al. 2009; Bracegirdle and Stephenson 2012; Collins et al. 2012; Bracegirdle and Stephenson 2013; Cox et al. 2013; Huang and Ying 2015), we can see that the robust pIOD-like pattern of mean-state SST could be overestimated, being twice constrained by the IOD amplitude.
We further investigated the relationship between the zonal pattern of mean-state SST changes with the amplitude and structural changes of IOD circulation and SST. The mean-state SST change pattern is not significantly correlated with the change percentages of and (Fig. 10), further verifying that and are dominated by the increase in atmospheric stability increase (Fig. 7) and the spatial pattern of mean-state SST changes does not play a remarkable role. For the structural changes, the mean-state SST change pattern and the historical IOD amplitude both significantly correlate with and (Figs. 11 and 12), no matter whether the intermodel spread of historical IOD amplitude associated with the sensitivity of air–sea coupling is removed from and in respective models (Figs. 11c,d and 12c,d) or not (Figs. 11a,b and 12a,b). While the historical IOD amplitude in the models is commonly overestimated with respect to the observations (Fig. 12), the robust structural changes in IOD circulation and IOD SST, associated with the increase in extreme pIOD events, could be overestimated. Even though there is a significant correlation of the historical IOD amplitude with the mean-state SST change pattern (Fig. 9), and (Fig. 12), we must notice that the intermodel spread of historical IOD amplitude only can explain about 14% (r2 in Fig. 9) of the intermodel variance of the mean-state SST change pattern, and around 40%–50% (r2 in Figs. 12a,b) of the intermodel variance of and . Therefore, the projected robust changes in and with increased extreme pIOD events cannot be totally erased by the emergent constraint considering the overestimated historical IOD bias. Some other processes suggested in Wang et al. (2017) could also contribute to the mean-state SST change pattern and the structural changes in IOD circulation and SST.
6. Conclusions and discussion
The present study investigated the changes in IOD-related SST and rainfall variability under global warming through a moisture budget decomposition for IOD-related rainfall variability and an amplitude and structural decomposition for IOD-related SST and circulation variability, based on 29 CMIP5 models in RCP8.5 simulations. The results show that the moisture budget decomposition proposed for the changes in ENSO-related rainfall variability (Huang and Xie 2015) is also practicable to disentangle the changes in IOD rainfall. The changes in IOD-related circulation are closely related to the changes in IOD-related SST through the amplitude and structural decomposition.
The total IOD rainfall changes can be decomposed into a thermodynamic component due to the increase in mean-state moisture and a dynamic component induced by the changes in IOD circulation. The sum of the thermodynamic and dynamic components can accurately describe the pattern of IOD rainfall changes. The thermodynamic component enhances the amplitude of IOD rainfall with an identical pattern to the historical IOD rainfall, whereas the pattern of the dynamic component dominated by the pattern of IOD circulation changes features an increase from the EEIO to the western coast of the equatorial IO.
The moisture budget decomposition converts the question of IOD rainfall changes to that of IOD circulation changes. We further decomposed the changes in IOD SST and circulation into the amplitude and structural components, inspired by the success of a similar decomposition in Huang and Xie (2015) to reveal the close relationship between the changes in ENSO-related circulation and SST variability. The amplitude changes in IOD circulation are significantly correlated with that of IOD SST among the models , both of which show a robust decrease. Moreover, the decrease rate of , around 13.7% °C−1, is about twice of the decrease rate of because of the decrease in the response of atmospheric circulation to local SST anomalies under global warming (P. Huang et al. 2017). In turn, the decreased atmospheric response to local SST anomalies suppresses the variability of IOD SST. The pattern of the structural changes in IOD circulation is similar to that of the structural changes in IOD SST, similar to the pattern of the extreme IOD rainfall defined in Cai et al. (2014a).
The present study can more clearly explain two conflicting processes resulting in an uncertain IOD change suggested in Zheng et al. (2013). The suppression of increased atmospheric stability is basically uniform (P. Huang et al. 2017) and mainly results in the amplitude changes of IOD, whereas the pIOD-like mean-state SST changes associated with the shoaling thermocline mainly modify the structure of IOD as suggested in Cai et al. (2014a). Both of them are robust in the CMIP5 projections, but because of the distinct patterns between them the predefined DMI changes would project an uncertain IOD change. Another noteworthy result is that the time scale of the response of IOD SST with circulation to global warming could be different between their amplitude and structural changes: the amplitude changes could be more exactly linear along with the tropical-mean temperature increase, whereas the structural change shows pronounced differences between the early and late twenty-first century.
The intermodel spread analysis for the structural changes in IOD SST and circulation indicates that the robust structural changes in IOD SST and circulation are significantly associated with the pIOD-like pattern of mean-state SST changes, which could be overestimated by the common overly IOD amplitude in the models (Li et al. 2016). When this bias is considered in the emergent constraint, the robust structural changes in IOD SST and circulation associated with the extreme pIOD evernts projected in the CMIP5 models should be weakened. However, only a part of intermodel variance of the mean-state SST change pattern (around 14%) and (around 40%–50%) can be explained by the historical IOD amplitude. This agrees with the suggestions in Wang et al. (2017) that there could be other mechanisms also contribute to the robust structural changes in IOD circulation and SST, which cannot be erased by the emergent constraint with the IOD amplitude bias.
The present study only analyzed the changes under the RCP8.5 scenario, which could be different from the changes in other pathway scenarios. However, this issue could not influence the main conclusions drawn in the present study. First, the moisture budget decomposition for IOD rainfall change was checked for the other 17 periods with lower warming except for the period 2066–95. The moisture budget decomposition can also accurately describe the IOD rainfall changes in the lower warming scenarios as in 2066–95 (not shown). Second, the amplitude and structural decompositions for IOD SST and circulation changes in lower warming scenarios have been shown in Figs. 7 and 8. The relationships of the amplitude and structural changes in IOD SST and circulation with tropical-mean warming are mainly linear, and the main conclusions drawn here were also based on these linear relationships. Indeed, there are some obvious nonlinear evolutions in the structural changes of IOD SST and circulation (Figs. 8b,c). It could reflect the non-unidirectional response of mean SST to global warming over the Indo-Pacific basin (Kim et al. 2014) and be associated with the scenarios, which would be an interesting issue in the future.
All of the present conclusions are based on the initial definition of IOD, the regression onto the DMI. This method greatly locks the related patterns to correlate with the dipole pattern of the two regions to calculate DMI both in the present-day and future climate. As a result, the possible changes independent of the DMI, such as the so-called extreme IOD events based on the second EOF mode of IO SST anomalies, are greatly removed relative to the results based on EOF analysis (Cai et al. 2013; Zheng et al. 2013). Even so, there are remarkable structural changes found in the DMI-regressed IOD SST and circulation patterns. This result implies that the structural changes in the IOD pattern could be underestimated in this study. The distinct method could also contribute to the more robust projections in the amplitude and structural changes of the IOD SST and circulation (Figs. 5 and 6). The method removed some structural changes and simplified the question to obtain a clearer conclusion, which would be a solid foundation to further study other aspects of IOD changes in future.
The work was supported by the National Natural Science Foundation of China (Grants 41722504, 41476003, 41575088, 41706024, 41690121, and 41690120), the Youth Innovation Promotion Association CAS, and the Fundamental Research Funds for the Central Universities. I acknowledge the World Climate Research Programme’s Working Group on Coupled Modeling, which is responsible for CMIP5, and the climate modeling groups (listed in section 2a) for producing and making available their model output. We also thank two anonymous reviewers for their constructive suggestions.