The Uncharacteristic Occurrence of the June 2013 Biomass-Burning Haze Event in Southeast Asia: E ﬀ ects of the Madden-Julian Oscillation and Tropical Cyclone Activity

: One of the worst haze events to ever hit Peninsular Malaysia occurred in June 2013 due to smoke from Riau, Central Sumatra. While biomass-burning in the region is common, the early occurrence of a haze episode of this magnitude was uncharacteristic of the seasonality of extreme ﬁre events, which usually occur between August and October in the Maritime Continent (MC). This study aims to investigate the phenomenology of the June 2013 haze event and its underlying meteorological forcing agents. The aerosol and meteorological environment during the event is examined using the Moderate Resolution Imaging Spectroradiometer (MODIS) active ﬁre hotspot detections and aerosol optical thickness retrievals, satellite-based precipitation retrievals, and meteorological indices. These datasets are then supported by a WRF-Chem simulation to provide a comprehensive picture of the event’s meteorology and aerosol transport phenomenology. While extreme ﬁre events are more characteristic of El Nino years, the MODIS ﬁre count over the MC in June for the years 2001–2015 was highest in 2013 when neutral El Nino / Southern Oscillation (ENSO) conditions prevailed. Although, the mean daily precipitation for June 2013 was below average for June 2003–2015. An early active tropical cyclone (TC) season occurred in 2013, and results show that the combined induced subsidence and ﬂow enhancement due to TC Bebinca and the dry phases of a strong Madden–Julian Oscillation (MJO) event contributed to the event intensiﬁcation. Results also show that Bebinca induced a decrease in surface relative humidity of at least 10% over Riau, where ﬁre hotspots were concentrated.


Introduction
Biomass-burning haze (BBH) in Southeast Asia (SEA) is an environmental concern that has attracted much attention during the past decade. Consequently, numerous studies have been performed to understand and characterize the occurrence of regularly occurring haze episodes [1][2][3][4]. Throughout the Maritime Continent (MC), agricultural waste burning, intentional forest fires to convert forests to agricultural land, and related peat burning have been the major causes of extreme haze episodes [1,2,5,6]. Such events are reported to have had alarming detrimental health effects on the populations affected most by the respective episodes [7][8][9][10]. Fire in the MC is most widespread during the drier boreal summer southwest monsoon season with a fire season that usually runs from June to October with the bulk of the fire occurring between August and early October [4]. In contrast, agricultural and forest fire activity peaks in boreal spring from late February to early May in northern SEA, when dry monsoonal conditions prevail over that region [2,6,[11][12][13]. Fire activity generally starts earlier in the west of the MC with the start date propagating eastward. In fact, fire activity is a combination of economic factors and environmental opportunity. The economic factors of land clearing and agricultural maintenance are well entrenched in SEA. The meteorology of dry spells provides an opportunity to burn. Therefore, if we understand the meteorological phenomenology that leads to favourable fire weather, we can then start to understand and predict burning and its consequences.
There are several meteorological factors that influence observed burning activity at different temporal scales in the MC [4]. El Nino/Southern Oscillation (ENSO) [14,15] is the strongest indicator of total burning in the MC, and during El Nino years, the already prevailing drier conditions are generally intensified, which results in more intense haze events [4,[16][17][18][19]. While ENSO influences inter-annual fire activity, the wet and dry phases of the Madden-Julian Oscillation (MJO) [20][21][22][23] over the MC largely modulate intra-seasonal fire activity in the region [4,24]. The MJO is a 30-90 day large-scale coupled pattern of meso-synoptic scale circulation and deep convection that propagates eastward at a speed of~5 m s −1 through regions of the Indian Ocean and the Pacific Ocean where the sea surface is warm [20,21,23]. MJO activity can be classified into eight phases. In phase 1, enhanced convection associated with MJO genesis occurs over Africa and the western Indian Ocean. By phases 2 and 3, convection is present over the Indian Ocean and approaches the MC by phase 4. Convection enters the Pacific Ocean during phase 5, which induces significant drying over the MC. Maximum drying occurs over the MC during phases 6 and 7 as convection propagates further over the Pacific Ocean. The convection regime ultimately terminates in phase 8, and the cycle repeats itself. Fire activity usually peaks over the MC during phases 5 to 7 as MJO induced subsidence inhibits precipitation over the region [4,21], with burning over Sumatra being influenced by the phase of the MJO more than other regions in the MC [4]. Tropical cyclone (TC) activity in the SCS is a high-frequency phenomenon, which also induces subsidence over the MC and which was shown to have an important impact on forest fire occurrence and BBH transport [4,25].
The most recent El Nino related extreme episodes [4,[16][17][18][19] occurred in 1997, 2006, 2009, and 2015. However, severe events can occur in any year, with Central Sumatra and its Riau province being less influenced by ENSO than other regions of the MC [4]. Indeed, one of the worst cases of biomass-burning haze occurred in 2013 [26], a year of neutral ENSO conditions. The Air Pollution Index (API) in Malaysia and the Pollution Standard Index (PSI) in Singapore reached hazardous levels in June 2013, and a state of emergency was declared in Malaysia [27]. The source was clear.  While the most significant fire events in the MC usually occur between August and early October, small fire events in June are not uncommon [4]. However, the extreme magnitude of this June 2013 haze event is unique in the modern data record and thus has garnered significant attention. Previous studies on the June 2013 haze event mostly include statistical studies of the impacts of haze on air quality and health [27][28][29]. Vadrevu et al. [26] assessed the June 2013 episode based on satellite retrievals and showed that the aerosol optical thickness (AOT) for June 2013 was significantly higher than the previous years. Oozeer et al. [25] identified the convective mechanisms that uplifted the haze emissions from Sumatra to the upper troposphere and reported the influence of low-pressure systems over the SCS on the transport of these emissions over Peninsular Malaysia during the 2013 event. More recently, Koplitz et al. [30] investigated the effect of anomalous westerlies during the late phases of the MJO on the transport of haze the June 2013 episode. However, despite these efforts, to date, there has yet to be an overarching discussion of the overall meteorology that led to this unprecedented event. While the most significant fire events in the MC usually occur between August and early October, small fire events in June are not uncommon [4]. However, the extreme magnitude of this June 2013 haze event is unique in the modern data record and thus has garnered significant attention. Previous studies on the June 2013 haze event mostly include statistical studies of the impacts of haze on air quality and health [27][28][29]. Vadrevu et al. [26] assessed the June 2013 episode based on satellite retrievals and showed that the aerosol optical thickness (AOT) for June 2013 was significantly higher than the previous years. Oozeer et al. [25] identified the convective mechanisms that uplifted the haze emissions from Sumatra to the upper troposphere and reported the influence of low-pressure systems over the SCS on the transport of these emissions over Peninsular Malaysia during the 2013 event. More recently, Koplitz et al. [30] investigated the effect of anomalous westerlies during the late phases of the MJO on the transport of haze the June 2013 episode. However, despite these efforts, to date, there has yet to be an overarching discussion of the overall meteorology that led to this unprecedented event.
Atmosphere 2020, 11, 55 4 of 24 This study seeks to investigate the meteorological environment that prevailed during the haze episode, the parameters that have contributed to its intensification, and its peculiarity with regards to past extreme haze events. Here, we systematically examine the strong scale dependencies that interact to create such a significant event, starting with inter-seasonal ENSO [14,15], followed by the MJO [20][21][22][23] and TC activity over the SCS [31,32]. We also investigate, in detail, the relative influence of TC Bebinca over the SCS, and its interaction with the MJO, on the intensification of the June 2013 haze event. This is achieved by using the Weather Research and Forecasting model coupled with Chemistry (WRF-Chem) [33,34], which was shown to simulate well the distribution and evolution of biomass-burning aerosols, as well as their radiative impacts on the atmosphere [18,25,[35][36][37][38][39].
This article is organized in the following manner. Section 2 provides an overview of the datasets and methods employed to study the aerosol and meteorological characteristics of the June 2013 haze event, as well as a description of the WRF-Chem model used. Section 3 discusses the aerosol and meteorological characteristics of the haze event and its peculiarity in relation to past extreme haze episodes. Section 4 discusses the evaluation of the model, the interaction between TC Bebinca and the MJO and their influence on the occurrence and intensification of the haze event. Finally, Section 5 concludes this article.

Episode Characteristics
The study region in this paper covers the MC and the SCS and extends from 10 • S to 10 • N and 90 • E to 150 • E, as shown in Figure 2a. We begin by investigating the aerosol and meteorological characteristics over the study region in June 2013, using satellite-derived datasets and meteorological indices, which are selected based on Reid et al. [4]. The combined MODIS Terra (~10:30 LST) and Aqua (~13:30 LST) 1 km daily active fire products are used to depict the overall fire activity during the June 2013 haze episode. Reid et al. [6] have pointed out that these data can only be considered semi-quantitatively since cloud cover can block the heat signature of fires. Fires in the MC are also sometimes too small to be detected by fire hotspot satellite products [40]. NASA MODIS col 6 Level 3 [41] aerosol optical thickness (AOT) at 550 nm are used to show the overall aerosol environment during the duration of the haze event in June 2013. Similar to fire data, AOT data in this region can be problematic due to high cirrus cover but nevertheless can track the location and relative intensity of individual events [6]. We then analyse the overall meteorological environment during the haze event using storm track, precipitation, and MJO characteristics data. The storm track data are obtained from the Unisys Weather hurricane archive database (weather.unisys.com/hurricane). Precipitation data are obtained from the high-resolution Climate Prediction Center MORPHing technique product (CMORPH) [42] for which the 3-h interval and 0.25 • resolution data are used in our analysis. CMORPH data are used as it best represents the temporal and spatial patterns of precipitation in the MC [43][44][45][46]. Finally, the MJO characteristics are analysed using the Wheeler and Hendon [47] product of the MJO phase and amplitude, available on the MJO page of the Bureau of Meteorology website (http://www.bom.gov.au/climate/mjo/).
We also use historical fire count, precipitation, and ENSO and MJO conditions data to investigate the peculiarity of the June 2013 haze event with regards to past extreme haze events in terms of its timing, ENSO and MJO conditions and fire count ratios. The MODIS Terra MOD14CM1 [48] and Aqua MYD14CM1 [49] 1 degree gridded monthly active fire products are used for the temporal analysis of fire activity over regions of interest in the MC for the years 2000-2015, for which a complete record exists [50,51]. The multivariate indices of Wolter and Timlin [52] and Wheeler and Hendon [47] are used for the temporal analysis of ENSO and MJO, respectively. The Multivariate ENSO Index (MEI) is a measure of the ENSO signal, which is based on six observed variables over the tropical Pacific, namely, sea-level pressure, surface zonal and meridional wind components, sea surface temperature, surface air temperature, and cloudiness [52]. Monthly MEI data from the year 1950 onwards can be

Model Setup
The WRF-Chem model [33,34] is an online-coupled regional meteorological model that can simultaneously simulate weather, aerosol life cycle, aerosol-cloud-radiation interactions, and gasphase chemistry. The selection of the model chemistry settings for the simulations in this study is based on Sessions et al. [53], Wang et al. [18], and Ge et al. [39], which all use the Fire Locating and Modeling of Burning Emissions (FLAMBE) dataset to simulate the forest fire smoke emissions. The main model chemistry and physics settings are shown in Table 1. Sensitivity WRF simulations (plots not shown here) were previously run with three cumulus parameterization schemes, namely, Betts-Miller-Janjic (BMJ) [54,55], Kain-Fritsch (KF) [56] and Grell 3D (G3D) cumulus scheme [57] over the model domain for the same study period. In summary, the BMJ scheme showed the best agreement to CMORPH data, and hence, all WRF-Chem simulations for this episode are run with BMJ, which is consistent with a recent study by Ge et al. [58] for the case of September 2011 in the Maritime Continent. Pennelly et al. [59] also report that BMJ simulates precipitation with better accuracy than KF and G3D at 30 km grid resolution. The overall model configuration is outlined below.
The model domain and nest used in this study are presented in Figure 2a. Domain d01 contains 160 × 150 27 km grid points and serves to capture the large-scale dynamics and smoke transport over the study region. The nest d02 contains 172 × 172 9 km grid points and is used to investigate the presence of subsidence and its influence on forest fire occurrence over Sumatra. The model consists of 50 vertical sigma levels with about 12 layers concentrated in the lowest 1 km of the atmosphere

Model Setup
The WRF-Chem model [33,34] is an online-coupled regional meteorological model that can simultaneously simulate weather, aerosol life cycle, aerosol-cloud-radiation interactions, and gas-phase chemistry. The selection of the model chemistry settings for the simulations in this study is based on Sessions et al. [53], Wang et al. [18], and Ge et al. [39], which all use the Fire Locating and Modeling of Burning Emissions (FLAMBE) dataset to simulate the forest fire smoke emissions. The main model chemistry and physics settings are shown in Table 1. Sensitivity WRF simulations (plots not shown here) were previously run with three cumulus parameterization schemes, namely, Betts-Miller-Janjic (BMJ) [54,55], Kain-Fritsch (KF) [56] and Grell 3D (G3D) cumulus scheme [57] over the model domain for the same study period. In summary, the BMJ scheme showed the best agreement to CMORPH data, and hence, all WRF-Chem simulations for this episode are run with BMJ, which is consistent with a recent study by Ge et al. [58] for the case of September 2011 in the Maritime Continent. Pennelly et al. [59] also report that BMJ simulates precipitation with better accuracy than KF and G3D at 30 km grid resolution. The overall model configuration is outlined below.
The model domain and nest used in this study are presented in Figure 2a. Domain d01 contains 160 × 150 27 km grid points and serves to capture the large-scale dynamics and smoke transport over the Atmosphere 2020, 11, 55 6 of 24 study region. The nest d02 contains 172 × 172 9 km grid points and is used to investigate the presence of subsidence and its influence on forest fire occurrence over Sumatra. The model consists of 50 vertical sigma levels with about 12 layers concentrated in the lowest 1 km of the atmosphere and a model top set at 50 hPa. The initial and boundary meteorological conditions are provided by the European Centre for Medium-range Weather Forecast (ECMWF) ERA-Interim analyses [60] with a resolution of 0.7 • at 6 h intervals. Analysis nudging is also used to nudge the model towards the ERA-Interim analyses. The four nudged fields are the u and v horizontal wind components, temperature and specific humidity, while a nudging coefficient of 0.0003 s −1 , corresponding to a timescale of 1 h, is used for the present simulations. The FLAMBE database, which provides the smoke emission flux (kg h −1 ) for each fire pixel detected by MODIS [3], is used to specify the smoke emission rate in the simulations based on the parameterizations described by Reid et al. [3] and Wang et al. [18]. The FLAMBE smoke emission values were tripled before being integrated into the simulations since FLAMBE emissions have a low bias over the study region [3,70,71] and a tripling of the FLAMBE emissions is recommended to remove the bulk of that bias over the study region [3]. The emissions injection height is set at 0.8 km based on the sensitivity studies done by Wang et al. [18]. It is important to note that since the focus of this study is the transport of smoke particles, background aerosols and aerosol radiative feedback are not included in the simulation. The simulations are initialized at 00UTC on 14 June 2013 and end at 00UTC on 27 June 2013. The FLAMBE emissions are updated for each day of the simulation, and the first 3 days of the run are considered as spin-up.

Model Evaluation
The model performance is evaluated in terms of its ability to reproduce the monsoonal precipitation and meteorological environment, as well as aerosol transport, over the study region before analysis. the simulated AOT before performing a quantitative comparison with MODIS AOT. Vertical profiles from the Cloud-Aerosol Lidar with Orthogonal Polarisation (CALIOP) [72] instrument onboard the Cloud-Aerosol Lidar and Infrared Pathfinder Satellite Observation (CALIPSO) are used to evaluate the aerosol vertical profile simulated by the WRF-Chem simulations. The CALIOP Level 2 product at a horizontal and vertical resolution of 5 km and 60 m, respectively, under 20 km is used in this study. The WRF-Chem simulated PM 2.5 concentrations on 24 June 2013 at 07:00 UTC extracted along the corresponding CALIPSO track is compared with the CALIOP-derived extinction coefficient at 532 nm.

Overall Aerosol and Meteorological Environment during the June 2013 Haze Event
The start of the biomass burning season in the MC generally starts in Riau Province, Central Sumatra, in June through early August [4]. While significant events existed in 2004 and 2005, the worst biomass burning haze episodes to affect air quality in major cities of the MC occurred in June 2013 [25][26][27][28][29]. Figure 2b shows the MODIS fire hotspot detections over SEA during the study period. Fire activity was largely concentrated over the Riau region in Central Sumatra, while sparse hotspots occurred over Peninsular Malaysia and Borneo during the study period.
Reid et al. [4] gives an overview of the seasonal fire behaviour in the MC and notes that fire activity peaks over the MC as the Intertropical Convergence Zone (ITCZ) migrates northward during the summer monsoon. The southwest summer monsoon (SWM) season in SEA usually occurs from April to October, and prevailing surface winds generally blow from the southwest over the MC towards the monsoonal trough east of the Philippines [73][74][75]. The summer monsoonal trough extends from the West Pacific, through the Northern South China Sea, and further over land in PSA and into the Indian monsoon. However, part of the monsoonal trough precipitation is a result of cyclone activity rather than simple ITCZ convection, as was the case when tropical storm Bebinca occurred over the SCS. Figure 3a shows the storm tracks of TCs that prevailed in June 2013, including storm Bebinca. The CMORPH precipitation fields in Figure 2c for the 17 to 25 June 2013 event period show that precipitation was a maximum over the SCS and Eastern PSA while a distinct region of dryness prevailed over Sumatra, Peninsular Malaysia, and Western Borneo. In fact, as Figure 2 shows, Central Sumatra received less than 2 mm of rainfall per day. TC activity over the SCS and its associated induced dryness over the MC in June 2013 is further discussed in Section 4.2. In addition, the observed fire activity corresponded with high AOT values over the region, as can be seen in Figure 2d. AOT retrievals, at 550 nm, of at least 1.8 can be observed over Central Sumatra and all across southern Peninsular Malaysia through Southern SCS. Figure 2d also shows that smoke was transported all over the SCS by the prevailing southwesterlies and was eventually scavenged out by precipitation associated with tropical storm Bebinca. These winds were intensified as a result of TC activity over the SCS and the associated inflow arm enhancement, as discussed in Section 4.2. Figure 3b shows the Wheeler and Hendon [47] product of the MJO phase and amplitude for the months of May, June, and July 2013, while Figure 4 shows the CMORPH daily precipitation plots for the period 10 to 28 June 2013 over the region 30 • S to 30 • N and 30 • E to 150 • W. Generally, MJO exists when amplitudes are higher than 1 and is deemed strong when amplitudes exceed 1.5. On 10 June, a weak phase 3 of the MJO prevailed, and precipitation occurred along the Eastern Indian Ocean, as shown in Figure 4a. Phase 4 of the MJO then prevailed until 14 June as convection and precipitation gradually shifted from Central MC towards Eastern MC, as shown in Figure 4b,c. Precipitation then increased over the Western Pacific Ocean as phase 5 of the MJO prevailed from 15 to 18 June. The occurrence of the haze episode over SPM between 17 and 25 June 2013 coincided with the dry phases of the MJO over the MC. The MJO transitioned from phase 5 to phase 6 from 18 to 19 June, and from phase 6 to 7 on 21 June. During these periods, maximum drying due to induced subsidence can be observed over the MC while precipitation due to TC Bebinca prevailed over the SCS, as shown in Figure 4f,g. The amplitude of the MJO was higher than 1 throughout the haze episode and exceeded 1.5 from 23 June onwards. The MJO transitioned to phase 8 on 24 June marking the end of the dry phase over the MC. Figure 4h-j indeed show that precipitation gradually increased over the MC from 24 to 28 June. Similar mechanisms are also described in Reid et al. [24,76], showing the contribution of MJO related subsidence to increased biomass burning over the MC. Figure 3b also shows that the strong MJO event of June 2013 is lagged and followed by weak MJO events with amplitudes of less than 1 from mid-May to the beginning of June and for most of July. This behaviour of the MJO was discussed by Napitu et al. [77] where the authors suggest that it is the result of vigorous cooling of the sea surface temperature (SST) by the previous strong MJO. The migration of the MJO from 17 to 25 June also coincided with the passage of tropical storm Bebinca over the SCS. This is further discussed in Section 4.2.
Atmosphere 2020, 11, 55 8 of 24    [76], where amplitudes greater than 1 and 1.5 are considered as significant and strong, respectively. The grey shaded area represents the period 18-25 June when the haze episode occurred.
Atmosphere 2020, 11, 55 9 of 24 discussed by Napitu et al. [77] where the authors suggest that it is the result of vigorous cooling of the sea surface temperature (SST) by the previous strong MJO. The migration of the MJO from 17 to 25 June also coincided with the passage of tropical storm Bebinca over the SCS. This is further discussed in Section 4.2.

2013 in Context: Time-Series of Fire, ENSO, and MJO Characteristics
The MEI time-series for the years 1980 to 2016 is shown in Figure 5a. Also included are markers that represent major haze episodes that occurred during that time period. Red markers represent episodes that occurred during ENSO warm phases while the yellow marker represents the June 2013 episode. As highlighted by Reid et al. [4], interannual fire variability is highly correlated to the ENSO warm phase, which can be observed in Figure 5a. The worst episodes occurred in 1982-1983, 1997-1998, and 2015 [19,78] and the peak MEI values during these three episodes were 2.909, 3.038, and 2.527, respectively. Typically, El Nino events correspond to MEI values of greater than 0.5. Interestingly, the June 2013 haze episode, which is classified as one of the worst haze episodes in the region [27], occurred when neutral ENSO conditions prevailed. The MEI value during that month was −0.144. In contrast, all major red marked haze episodes occurred when warm conditions prevailed.
The inter-annual MODIS fire counts are also compared to show that the occurrence of the intense haze episode of June 2013 was indeed anomalous. While short pulses of fire activity over Central

2013 in Context: Time-Series of Fire, ENSO, and MJO Characteristics
The MEI time-series for the years 1980 to 2016 is shown in Figure 5a. Also included are markers that represent major haze episodes that occurred during that time period. Red markers represent episodes that occurred during ENSO warm phases while the yellow marker represents the June 2013 episode. As highlighted by Reid et al. [4], interannual fire variability is highly correlated to the ENSO warm phase, which can be observed in Figure 5a. The worst episodes occurred in 1982-1983, 1997-1998, and 2015 [19,78] and the peak MEI values during these three episodes were 2.909, 3.038, and 2.527, respectively. Typically, El Nino events correspond to MEI values of greater than 0.5. Interestingly, the June 2013 haze episode, which is classified as one of the worst haze episodes in the region [27], occurred when neutral ENSO conditions prevailed. The MEI value during that month was −0.144. In contrast, all major red marked haze episodes occurred when warm conditions prevailed.
2013 than for any other year since both satellites came into operation. In fact, the average fire count over SPM recorded by Aqua and Terra for the month of June since they came into operation are 2745 and 1692, respectively. In contrast, for June 2013, Aqua and Terra fire counts over SPM were 7453 and 6928, respectively. In addition, a ratio of fire count for SPM to MC, for the years 2001-2015, shows that the highest recorded ratio of 0.89 occurred in June 2013. Therefore, fire activity over SPM in June 2013 was indeed anomalous for that period of the year under the prevailing neutral ENSO conditions.  The inter-annual MODIS fire counts are also compared to show that the occurrence of the intense haze episode of June 2013 was indeed anomalous. While short pulses of fire activity over Central Sumatra in June are not new [4], major fire episodes usually occur between August and October, as can be seen in Figure 5a. Figure Figure 5b. While bearing in mind that MODIS fire products may only be considered semi-quantitatively, it is important to note that the fire counts recorded by both Aqua and Terra over the MC and SPM for the month of June were higher in 2013 than for any other year since both satellites came into operation. In fact, the average fire count over SPM recorded by Aqua and Terra for the month of June since they came into operation are 2745 and 1692, respectively. In contrast, for June 2013, Aqua and Terra fire counts over SPM were 7453 and 6928, respectively. In addition, a ratio of fire count for SPM to MC, for the years 2001-2015, shows that the highest recorded ratio of 0.89 occurred in June 2013. Therefore, fire activity over SPM in June 2013 was indeed anomalous for that period of the year under the prevailing neutral ENSO conditions. Figure 6 shows the time series data for ENSO, precipitation, fire count, and the MJO in June. While ENSO is a good indicator of seasonal burning, it cannot explain all dry spells and corresponding burning episodes. Figure 6b shows a good indicator of seasonal burning, the intensity of burning activity does not only depend on ENSO conditions. Comparing June 2013 to June 2003 and 2004, the daily precipitation rates over SPM were only slightly higher in 2013 at 1.5 mm day −1 . However, it needs to be reiterated that, interestingly, the highest fire count in June was recorded in 2013 for the period 2001-2015. This indicates that the days during which the haze episode occurred in June 2013 were much drier than the rest of the month since very dry conditions must have prevailed to sustain the intense burning episode of June 2013.

Model Evaluation Results
Overall, WRF-Chem successfully captures the location and magnitude of precipitation over the northern domain area but with a slight westward phase shift in intensity, as shown in Figure 7a,b. Since the model is nudged to ERA-Interim analyses, a plot of ERA-Interim accumulated precipitation is included in Figure 7c. While ERA-Interim successfully captures the location of precipitation, it fails to capture the regions of high precipitation over the SCS as compared to CMORPH and WRF-Chem. This indicates that the BMJ cumulus parameterization in WRF-Chem is able to resolve convection over the model domain. Pennelly et al. [59] reported a similar phase shift in intensity to that observed in Figure 7b, which occurs with simulations run with BMJ cumulus parameterization at 30 km resolution but not 15 km resolution. The shift in precipitation intensity can, therefore, be attributed to the relatively coarse grid resolution of 27 km used in this study. CMORPH, WRF-Chem, and ERA-Interim all show that while precipitation prevailed over the northern half of the domain, a distinct region of dryness can be observed over Peninsular Malaysia, Sumatra, and Borneo. This precipitation pattern is indeed characteristic of the SWM season [73][74][75], which was described in Section 3.1. The model succeeds at producing similar patterns and magnitudes of AOT over the MC, as shown in Figure 8a,b. However, the MODIS AOT retrieval in Figure 8a is an aggregation of 6 days of individual retrievals from MODIS Terra, which contain missing cells of AOT data for the model domain, particularly for very high AOT smoke in which the retrieval fails. Huang et al. [87] and Reid et al. [6] advise caution when evaluating AOT maps in the study region, where cirrus contamination in the MODIS products can also increase the baseline AOT throughout the region. This explains the relatively low AOT values retrieved from MODIS Terra as compared to the model. Observed AOTs over the domain are at least 2.4 while over the corresponding regions, the WRF-Chem simulations produce AOTs of at least 3. However, the spatial correlation between the masked simulated AOT and MODIS AOT is as high as 0.71, showing that the model successfully captures the smoke northeasterly smoke transport pattern towards the SCS. The model also successfully captures the variations in plume height as shown by the plume peaks between latitudes 1° S and 2° N, and 4° N, and 7° N in   [83][84][85], particularly in areas of complex terrain where topographic features cannot be explicitly considered by the coarse resolution of the model. This implies that smoother orography underestimates the terrain roughness, which eventually leads to an excess of wind speed [86]. Therefore, the overestimation of the 10 m wind speed in this study is likely due to the relatively coarse 27 km resolution of the domain. Nevertheless, for 10 m wind speed, the highest correlation, r 2 = 0.98, was observed at the Johor station while the lowest root mean square error (RMSE), RMSE = 1.0 m s −1 was recorded at Perak. The highest correlation and lowest RMSE for 2 m temperature were also observed at Perak and were r 2 = 0.96 and RMSE = 0.7 • C, respectively. The correlations and RMSEs for each station are shown at the bottom of each figure.
The model succeeds at producing similar patterns and magnitudes of AOT over the MC, as shown in Figure 8a,b. However, the MODIS AOT retrieval in Figure 8a is an aggregation of 6 days of individual retrievals from MODIS Terra, which contain missing cells of AOT data for the model domain, particularly for very high AOT smoke in which the retrieval fails. Huang et al. [87] and Reid et al. [6] advise caution when evaluating AOT maps in the study region, where cirrus contamination in the MODIS products can also increase the baseline AOT throughout the region. This explains the relatively low AOT values retrieved from MODIS Terra as compared to the model. Observed AOTs over the domain are at least 2.4 while over the corresponding regions, the WRF-Chem simulations produce AOTs of at least 3. However, the spatial correlation between the masked simulated AOT and MODIS AOT is as high as 0.71, showing that the model successfully captures the smoke northeasterly smoke transport pattern towards the SCS. The model also successfully captures the variations in plume height as shown by the plume peaks between latitudes 1 • S and 2 • N, and 4 • N, and 7 • N in Figure 8c,d. The plume peaks in these two regions reached 3 km in height. Both plots also show that the smoke particles were confined to within 3 km in height along the CALIPSO track.

Combined Effect of Tropical Cyclone Bebinca and MJO
During the summer monsoon, as the ITCZ migrates northwards, southwesterlies tend to prevail over the western MC and the SCS. Furthermore, the Western North Pacific (WNP) is the most active basin of tropical cyclogenesis [88], and 80% of the TCs develop within or in the surroundings of the ITCZ, where low-level convergence occurs between the trade easterlies and the southwesterlies [89,90]. In 2013, the TC season in the WNP was marked by an above average genesis of TCs and was characterized by an early active TC season in June [32]. In fact, four TCs were generated in June 2013, which is twice the climatological average of 1.8 TCs. These four TCs, namely Tropical Storm Yagi (8-12 June), Tropical Storm Leepi (17-20 June), Tropical Storm Bebinca (20-23 June), and Typhoon Rumbia (28 June-2 July), are shown in Figure 3a. Bebinca, which coincided with the extreme haze event over Sumatra, Singapore, and Malaysia, began to develop on 18 June and rapidly intensified

Combined Effect of Tropical Cyclone Bebinca and MJO
During the summer monsoon, as the ITCZ migrates northwards, southwesterlies tend to prevail over the western MC and the SCS. Furthermore, the Western North Pacific (WNP) is the most active basin of tropical cyclogenesis [88], and 80% of the TCs develop within or in the surroundings of the ITCZ, where low-level convergence occurs between the trade easterlies and the southwesterlies [89,90]. In 2013, the TC season in the WNP was marked by an above average genesis of TCs and was characterized by an early active TC season in June [32]. In fact, four TCs were generated in June 2013, which is twice the climatological average of 1.8 TCs. These four TCs, namely Tropical Storm Yagi (8-12 June), Tropical Storm Leepi (17)(18)(19)(20), Tropical Storm Bebinca (20)(21)(22)(23), and Typhoon Rumbia (28 June-2 July), are shown in Figure 3a. Bebinca, which coincided with the extreme haze event over Sumatra, Singapore, and Malaysia, began to develop on 18 June and rapidly intensified into a Tropical Depression (TD) migrating northwards over the SCS. By 21 June Bebinca had intensified into a Tropical Storm (TS) and started migrating westwards towards PSA, and maximum wind speeds of 18 m s −1 were recorded. By 24 June, Bebinca had lost strength as it made landfall over PSA. More details about the mentioned storms can be found in the Joint Typhoon Warning Center Annual Tropical Cyclone Report for 2013 (http://www.usno.navy.mil/NOOC/nmfc-ph/RSS/jtwc/atcr/2013atcr.pdf).
The increase in fire activity in the southern MC and transport of smoke over the SCS as TCs transit the SCS has been reported by Reid et al. [4,24]. Wang et al. [18] also showed how cyclone Xangsane enhanced southwesterly winds and induced large scale subsidence over the MC, which contributed to fire propagation over Kalimantan and Sumatra in October 2006. However, these events occurred when TCs are climatologically more prevalent in the South China Sea/Philippines region. In June, the storm tracks are typically further north. In June 2013, however, TCs were abnormally south. Weather in the MC was influenced by an intensification of the low-pressure belt of the northern ITCZ, which drew stronger winds from the Indian Ocean towards the northeast [25]. This intensification was in fact Bebinca. The coevolution of Bebinca and the haze event is depicted in Figure 9, which shows MODIS images from the Terra and Aqua satellites for 17 to 26 June 2013, the corresponding WRF-Chem simulated daily averaged sea level pressure (SLP), and near-surface wind patterns, as well as daily averaged and vertically integrated PM 2.5 concentrations (darker red plumes indicate higher concentrations of PM 2.5 ). On 17 June, very few fire hotspots can be observed over the MC with westerlies and southwesterlies blowing over Sumatra and Peninsular Malaysia, as shown in Figure 9a,g. On 19 June, increased cloud cover can be observed over the SCS, as Bebinca gradually generated into a TD near 16 • N and 115 • E over the SCS, while the reverse occurred over Sumatra and Peninsular Malaysia, as shown in Figure 9b. An increase in fire hotspots over Central Sumatra can also be observed, as well as smoke being transported in a northeasterly direction from the hotspots over Sumatra to Western Borneo and the SCS by enhanced monsoonal flow. The eastward motion of the emissions plume is aided by winds associated with the Sumatran low located near 5 • S and 105 • E, as shown in Figure 9h,n, as well as the prevailing westerlies, which persist over Sumatra during the dry phase of the MJO over the MC.
By 21 June, cyclone Bebinca had intensified into a TS, as shown by increased cloud cover over the SCS in Figure 9c, and reduced SLP and stronger associated winds, as shown in Figure 9i. As Bebinca started moving westward toward PSA, relatively dry weather persisted over Central Sumatra, except for some scarce clouds associated with Bebinca. A high number of fire hotspots prevailed over Sumatra, as well as continued haze propagation over the MC. Despite the fact that part of the smoke seemed to be confined within the clouds in Figure 9c, a similar widespread smoke pattern is simulated by the model, as shown in Figure 9o. On 22 June, the intense TC Bebinca had already reached the east coast of PSA, and the winds over Sumatra and Peninsular Malaysia had shifted to higher flow in a north-northeasterly direction. This also resulted in a gradual shift in the plume flow from Sumatra, as shown in Figure 9p. In fact, the most intense and widespread emissions seem to have occurred between 21 and 22 June, as shown by Figure 9o,p. This period also corresponds to the period during which TC Bebinca was the strongest, as shown in Figure 9i,j. Figure 10 shows the vertical velocity over cross-sections YY' and ZZ', which are marked in Figure 9j, on 22 June. The wind fields for each cross-section were calculated from the horizontal velocity along that cross-section and 10 times the vertical velocity. The intensification and propagation of hotspots and emissions over Sumatra can be attributed to the large-scale subsidence and induced dryness due to cyclone Bebinca, as shown in Figure 10a. Deep convection can be observed between 15 • N and 22 • N resulting in large scale divergence near the upper troposphere. Air over Sumatra, near the equator, is, in turn, accelerated towards the convection centre of Bebinca through the inflow arm of the cyclone. Upper level winds are accelerated towards the equator where upper level convergence occurs, resulting in subsidence over Sumatra and the formation of a deep convective cell between the equator and 22 • N along cross-section YY'. Orographic motion over the mountains of Sumatra can also be observed. The influence of dry air due to mountain flow on increased fire activity over Central Sumatra in June 2013 is discussed by Oozeer et al. [25]. Figure 9, which shows MODIS images from the Terra and Aqua satellites for 17 to 26 June 2013, the corresponding WRF-Chem simulated daily averaged sea level pressure (SLP), and near-surface wind patterns, as well as daily averaged and vertically integrated PM2.5 concentrations (darker red plumes indicate higher concentrations of PM2.5). On 17 June, very few fire hotspots can be observed over the MC with westerlies and southwesterlies blowing over Sumatra and Peninsular Malaysia, as shown in Figure 9a,g. On 19 June, increased cloud cover can be observed over the SCS, as Bebinca gradually generated into a TD near 16° N and 115° E over the SCS, while the reverse occurred over Sumatra and Peninsular Malaysia, as shown in Figure 9b. An increase in fire hotspots over Central Sumatra can also be observed, as well as smoke being transported in a northeasterly direction from the hotspots over Sumatra to Western Borneo and the SCS by enhanced monsoonal flow. The eastward motion of the emissions plume is aided by winds associated with the Sumatran low located near 5° S and 105° E, as shown in Figure 9h,n, as well as the prevailing westerlies, which persist over Sumatra during the dry phase of the MJO over the MC. By 21 June, cyclone Bebinca had intensified into a TS, as shown by increased cloud cover over the SCS in Figure 9c, and reduced SLP and stronger associated winds, as shown in Figure 9i. As Bebinca started moving westward toward PSA, relatively dry weather persisted over Central Sumatra, except for some scarce clouds associated with Bebinca. A high number of fire hotspots prevailed over Sumatra, as well as continued haze propagation over the MC. Despite the fact that part of the smoke seemed to be confined within the clouds in Figure 9c, a similar widespread smoke pattern is simulated by the model, as shown in Figure 9o. On 22 June, the intense TC Bebinca had already reached the east coast of PSA, and the winds over Sumatra and Peninsular Malaysia had shifted to higher flow in a north-northeasterly direction. This also resulted in a gradual shift in the plume flow from Sumatra, as shown in Figure 9p. In fact, the most intense and widespread emissions seem to have occurred between 21 and 22 June, as shown by Figure 9o,p. This period also corresponds to the period during which TC Bebinca was the strongest, as shown in Figure 9i,j. Figure 10 shows  To further investigate the proposed subsidence mechanisms induced by TC Bebinca over Riau, SLP and 700 hPa geopotential height maps, as well as 700 hPa geopotential height and surface relative humidity anomalies from the WRF-Chem simulations, are shown in Figure 11. The plots in Figure 11 were extracted from the model output for the nest d02. Figure 11a shows the daily averaged SLP for To further investigate the proposed subsidence mechanisms induced by TC Bebinca over Riau, SLP and 700 hPa geopotential height maps, as well as 700 hPa geopotential height and surface relative humidity anomalies from the WRF-Chem simulations, are shown in Figure 11. The plots in Figure 11 were extracted from the model output for the nest d02. Figure 11a shows the daily averaged SLP for the period 17-26 June 2013, while Figure 11b shows the daily averaged geopotential height plots overlaid with the total fire hotspots for the same period. Figure 11a indicates that relatively high pressure prevailed over SPM during the period 17-26 June, where the minimum prevailing daily averaged SLP was as high as 1006 hPa. Relatively weak southwesterlies also prevailed over Riau during that period. While high pressure prevailed over the entire nest during the 17-26 June period, Figure 11b shows that higher pressure particularly prevailed over the Riau region as compared to the rest of Sumatra. The daily averaged 700 hPa geopotential height over Riau was at least 3136 m. More importantly, Figure 11b shows that the fire hotspots detected by MODIS were concentrated over that region of higher 700 hPa geopotential height over Sumatra. This indicates that the overall subsidence and higher pressure over Riau intensified the June 2013 fire episode. Figure 11c,d show the 700 hPa geopotential height anomaly overlaid with 10 m wind anomaly vectors, and surface relative humidity anomaly, respectively, between the period 21-23 June and the remaining days of the 10-day period 17-26 June. These three days were selected since TC Bebinca reached maximum intensity between 21 and 23 June. Figure 11c shows that TC Bebinca induced a high-pressure system over the eastern part of the nest in addition to the prevailing high pressure conditions over the entire nest during the 10-day period. Indeed, a clockwise wind motion can be observed near the eastern coast of SPM while positive geopotential anomalies can be observed over the same region and over Peninsular Malaysia and northern Sumatra. This suggests that these regions of positive geopotential height anomalies might have had a "dam effect", which confined the bulk of the PM 2.5 concentrations over SPM, as shown in Figure 9m-r. In addition, Figure 11d indicates that TC Bebinca induced more dryness over Riau as the surface relative humidity anomaly plot shows a decrease in relative humidity of at least 10%. More importantly, the MODIS fire hotspots for the period 21-23 June shown in Figure 11d coincide exactly with the regions of negative surface relative humidity anomaly over Riau. This further shows the fire hotspots over Riau during the 21-23 June period were indeed the result of the dryness induced by Bebinca. Figure 9k shows that cyclone Bebinca had lost in intensity by 24 June, but induced subsidence and dryness prevailed over Sumatra, and emissions were still strong on that day with the plume flowing in a northerly direction. By 26 June, Bebinca had weakened into a low-pressure system, and the subsidence over Sumatra had subsided, as shown by the increase in cloud cover in Figure 9f. Fire hotspots had also drastically reduced over Sumatra and so did the emissions as a result. The weakening of cyclone Bebinca marked the end of the haze episode over Peninsular Malaysia and Sumatra thus indicating a significant correlation between the intensification and propagation of forest fires and the transport of BBH over the MC due to TC activity over the SCS. More importantly, this shows that improving the ability to predict extreme TC episodes over the SCS can, in turn, help improve our ability to model and predict intense BBH episodes over the MC.
It is also important to note that the migration of the MJO discussed in Sections 3.1 and 3.2 coincided with the train of TC activity over the SCS and NWP in June 2013, as was the case in Reid et al. [24] during the Vasco Cruise in September 2011. Maloney and Hartmann [91] reported that the transit and departure of the MJO from the MC is often associated with an increase in TC formation in the region. The favourable conditions for TC formation set by the transit of the MJO in June 2013, which are growing eddies, strong surface convergence, and high sea surface temperatures [91], could have, therefore, contributed to the formation of the four TCs shown in Figure 3a. Two characteristics of the MJO-TC relationship for June 2013 are of note. Firstly, out of the four TCs, only Bebinca and Rumbia crossed the SCS while Yagi and Leepi migrated northwards over WNP, and the seesaw shift of the preferable cyclogenesis region discussed in Kim et al. [92] can be observed in June 2013. Usually, when the MJO related convection centre is located over the Indian Ocean, TCs tend to migrate eastward, and westward when the MJO convection centre occurs over the WNP. As can be seen in Figure 5, Yagi occurred during phases 2-4 of the MJO, Leepi occurred during phase 5, Bebinca occurred during phases 6-7, and Rumbia occurred during phase 8. This leads to the second characteristic of the MJO-TC relationship over the MC in June 2013. The migration of Bebinca over the SCS coincided with the dry phases of the MJO over the MC, and therefore, the combined subsidence due to Bebinca and the MJO lead to intense fire activity occurring over Central Sumatra. Figure 10b shows the cross-section ZZ' marked over Figure 9j. Low level westerlies and upper level easterlies can be observed along ZZ' with subsidence occurring throughout the cross-section over the MC, especially between 96 • E and 107 • E. The convective centre is not visible in Figure 10b since by phases 6-7 of the MJO, convection occurs to the east of the model domain. It is also interesting to note that no major haze event occurred when Rumbia, which had intensified into a Category 1 Typhoon with maximum wind speeds of 36 m s −1 (twice as fast as Bebinca), migrated westwards over the SCS. This suggests that Rumbia related subsidence was not enough to suppress the MJO related convection over the MC. Rumbia coincided with phase 8 of the MJO when the MJO cycle was about to terminate over the Pacific and restart over the Indian Ocean. MJO amplitudes were higher than 1.5 from 23 June to 8 July. The uncharacteristically early and strong June 2013 event, therefore, occurred as a result of the combined subsidence from Bebinca and the MJO.
Atmosphere 2020, 11, 55 17 of 24 of the nest in addition to the prevailing high pressure conditions over the entire nest during the 10day period. Indeed, a clockwise wind motion can be observed near the eastern coast of SPM while positive geopotential anomalies can be observed over the same region and over Peninsular Malaysia and northern Sumatra. This suggests that these regions of positive geopotential height anomalies might have had a "dam effect", which confined the bulk of the PM2.5 concentrations over SPM, as shown in Figure 9m-r. In addition, Figure 11d indicates that TC Bebinca induced more dryness over Riau as the surface relative humidity anomaly plot shows a decrease in relative humidity of at least 10%. More importantly, the MODIS fire hotspots for the period 21-23 June shown in Figure 11d coincide exactly with the regions of negative surface relative humidity anomaly over Riau. This further shows the fire hotspots over Riau during the 21-23 June period were indeed the result of the dryness induced by Bebinca. Figure 9k shows that cyclone Bebinca had lost in intensity by 24 June, but induced subsidence and dryness prevailed over Sumatra, and emissions were still strong on that day with the plume flowing in a northerly direction. By 26 June, Bebinca had weakened into a low-pressure system, and the subsidence over Sumatra had subsided, as shown by the increase in cloud cover in Figure 9f. Fire hotspots had also drastically reduced over Sumatra and so did the emissions as a result. The weakening of cyclone Bebinca marked the end of the haze episode over Peninsular Malaysia and Sumatra thus indicating a significant correlation between the intensification and propagation of forest fires and the transport of BBH over the MC due to TC activity over the SCS. More importantly,

Summary and Conclusions
One of the worst episodes of biomass-burning haze over the MC occurred in June 2013. However, the magnitude for this timing was uncharacteristic of the seasonality of extreme fire events in the region. In order to study this peculiar case, the aerosol and meteorological characteristics over SEA during the study period of 17 to 25 June were investigated. MODIS fire hotspot detections showed that fire activity was concentrated over Central Sumatra during the haze episode, which corresponded to high AOD retrievals of at least 1.8 over the region. CMORPH precipitation fields for the same period also showed that precipitation was a maximum over the SCS while Central Sumatra was particularly dry. The AOT retrievals indicated that smoke was transported by southwesterlies, which prevail during the SWM season, towards the SCS where it was eventually scavenged out by precipitation associated with TC Bebinca.
Fire activity is a combination of economic need and meteorological opportunity. By the start of the drier southwest monsoon season, farmers have begun to clear land and prepare for burning. This study focused on three features of interest that created highly favourable fire weather in the study region, namely, ENSO, the MJO, and TC activity. The MEI time-series from 1980 to 2016 showed that neutral ENSO conditions prevailed during the June 2013 haze episode with an MEI value of −0.144 for that month. In contrast, the three worst episodes over the MC during that period occurred in 1982 to 1983, 1997 to 1998, and 2015 when warm conditions prevailed. Major fire episodes usually occur between August and October in the MC. Therefore, the overall MODIS fire count over the MC in June 2013 expectedly ranked low as compared to bulk-burning months, which occurred during El-Nino years but were comparable to those during non-El Nino years. Comparing fire counts that occurred over only SPM WRF-Chem was used to investigate the influence of TC Bebinca over the SCS on the haze event and was run from 14 to 27 June 2013. The model performance was evaluated by comparing the model results to CMORPH precipitation data, measured data at selected ground stations over Malaysia and CALIPSO and MODIS satellite data. The model succeeded to capture the location and magnitude of precipitation over the domain area and to predict the diurnal variation of 10 m wind speed and 2 m temperature, respectively. The modelled AOTs at 550 nm were also very similar to the observed MODIS AOT in patterns and magnitudes. WRF-Chem also successfully captured the variations in plume height as compared to the CALIOP-derived extinction profile. In 2013, the TC season over WNP was marked by an above average number of TCs. TC Bebinca was generated over the SCS during this active and early period of cyclone genesis, which could have been the result of the transiting MJO, and was found to have serious intensifying effects on the propagation of forest fires over Sumatra and the transport of haze over the MC. The model results showed that subsidence associated with Bebinca and the dry phases of the MJO contributed to regions of dryness over Central Sumatra and the migration of Bebinca from the SCS onto Indochina governed the direction of plume flow from Sumatra. In fact, the extreme haze event of June 2013 coincided with the presence of TC Bebinca. The WRF-Chem model results showed that while high pressure and dry conditions prevailed over SPM during the simulation period 17-26 June 2013, TC Bebinca induced further subsidence and dryness over Riau causing a 10% decrease in surface relative humidity during the three days when it was most intense. Therefore, intense and early TC seasons over the WNP can be an indication of the occurrence of early and extreme haze events over the MC. More importantly, the combined subsidence due to both Bebinca and the MJO is a phenomenon which requires further attention since no haze event occurred when stronger Category 1 Rumbia crossed the SCS during the lesser dry phase 8 of the MJO over the MC.