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local topography. 2. Methods a. Study domain This study area is focused on west Java including Jakarta. This region is characterized by complex topography, including 1) the urban area of Jakarta at low altitude in the northern part of the radar domain and bordered by coastal areas, 2) suburban areas at slightly higher altitudes, and 3) high mountains extending from the west to the east in the southern part of the radar domain. The radar also covers the bay of Jakarta in the northern part of
local topography. 2. Methods a. Study domain This study area is focused on west Java including Jakarta. This region is characterized by complex topography, including 1) the urban area of Jakarta at low altitude in the northern part of the radar domain and bordered by coastal areas, 2) suburban areas at slightly higher altitudes, and 3) high mountains extending from the west to the east in the southern part of the radar domain. The radar also covers the bay of Jakarta in the northern part of
Climate Forecast System version 2 (CFSv2) 6-hourly products ( Saha 2011 ). The CLIVAR MJO Working Group diagnostics package ( Waliser et al. 2009 ) is used to isolate and analyze the intraseasonal (20–100 day) variability. MJO phase composites are computed based on the Real-Time Multivariate MJO index ( Wheeler and Hendon 2004 ). We use the ECHAM5.4 ( Roeckner 2003 ) AGCM coupled with the Snow-Ice-Thermocline (SIT) one-column ocean model ( Tu and Tsuang 2005 ; Tsuang et al. 2009 ) to simulate the
Climate Forecast System version 2 (CFSv2) 6-hourly products ( Saha 2011 ). The CLIVAR MJO Working Group diagnostics package ( Waliser et al. 2009 ) is used to isolate and analyze the intraseasonal (20–100 day) variability. MJO phase composites are computed based on the Real-Time Multivariate MJO index ( Wheeler and Hendon 2004 ). We use the ECHAM5.4 ( Roeckner 2003 ) AGCM coupled with the Snow-Ice-Thermocline (SIT) one-column ocean model ( Tu and Tsuang 2005 ; Tsuang et al. 2009 ) to simulate the
different resolutions, the area covered by the coarsest resolution buffer zone was removed from all experiments. Thus, in the 2-km runs, this means that the outer 80 grid points in each direction were not considered. This ensure a like-to-like comparison across resolutions. The model parameterization suite was configured based on a combination of information from previous studies on the region ( Argüeso et al. 2016 ; Li et al. 2017 ; Vincent and Lane 2016 ; 2017 ) and schemes that have been
different resolutions, the area covered by the coarsest resolution buffer zone was removed from all experiments. Thus, in the 2-km runs, this means that the outer 80 grid points in each direction were not considered. This ensure a like-to-like comparison across resolutions. The model parameterization suite was configured based on a combination of information from previous studies on the region ( Argüeso et al. 2016 ; Li et al. 2017 ; Vincent and Lane 2016 ; 2017 ) and schemes that have been
there is rainfall of ~20 mm day −1 over much of the region, there are not as clear of peaks over the islands as compared to the easterly regime. This difference may owe to suppressed shortwave surface heating due to greater cloud cover in this regime ( Oh et al. 2012 ; Hagos et al. 2016 ; Sakaeda et al. 2017 ; Zhang and Ling 2017 ; Ling et al. 2019 ). This regime is nonetheless characterized by prominent diurnal variation of convection, as described later. Hovmöller diagrams for CTL (the
there is rainfall of ~20 mm day −1 over much of the region, there are not as clear of peaks over the islands as compared to the easterly regime. This difference may owe to suppressed shortwave surface heating due to greater cloud cover in this regime ( Oh et al. 2012 ; Hagos et al. 2016 ; Sakaeda et al. 2017 ; Zhang and Ling 2017 ; Ling et al. 2019 ). This regime is nonetheless characterized by prominent diurnal variation of convection, as described later. Hovmöller diagrams for CTL (the
et al. (2011) , Vincent and Lane (2016a) , and Hassim et al. (2016) . While it is not clear what causes this deficit over the ridge, it is interesting to note that there may be snow cover for some of the period over these highest peaks, which may contaminate the satellite precipitation estimates (e.g., Chen et al. 2013 ). 7. The impact of the sea breeze The variations in the diurnal precipitation cycle with MJO phase are partly controlled by the intensity of the sea-breeze circulation, both
et al. (2011) , Vincent and Lane (2016a) , and Hassim et al. (2016) . While it is not clear what causes this deficit over the ridge, it is interesting to note that there may be snow cover for some of the period over these highest peaks, which may contaminate the satellite precipitation estimates (e.g., Chen et al. 2013 ). 7. The impact of the sea breeze The variations in the diurnal precipitation cycle with MJO phase are partly controlled by the intensity of the sea-breeze circulation, both
