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Gerald A. Meehl, Julie M. Arblaster, Julie M. Caron, H. Annamalai, Markus Jochum, Arindam Chakraborty, and Raghu Murtugudde

CMIP3 that were assessed in the IPCC AR4. They concluded that apart from mean monsoon precipitation, models that correctly simulate the timing and location of SST and diabatic heating anomalies over the equatorial Pacific, and the associated changes to the large-scale east–west Walker circulation, capture the monsoon–ENSO relationship realistically. Following the conjectures of Annamalai et al. (2007) , we examine first the ability of CCSM4 in capturing the basic state over the South Asian summer

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Aneesh C. Subramanian, Markus Jochum, Arthur J. Miller, Raghu Murtugudde, Richard B. Neale, and Duane E. Waliser

bands of MJO generate excessive precipitation in the model. The intraseasonal variance of the diabatic heating caused by convection parameterized in the model has a spatial pattern that is similar to the variance of the precipitation ( Fig. 16 ). This supports the idea that the excessive precipitation in the model is due to large-scale convective systems (such as the MJO) in the intraseasonal band. In the Indian Ocean initiation region of MJO, during phases 2 and 3 of the composite MJO, the ratio of

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Jennifer E. Kay, Marika M. Holland, Cecilia M. Bitz, Edward Blanchard-Wrigglesworth, Andrew Gettelman, Andrew Conley, and David Bailey

Heat Transport Calculation Methods Assuming no atmospheric heat storage ( = 0), which is appropriate for equilibrium conditions, vertically integrated total northward heat transport (NHT) and atmospheric northward heat transport (NHT atm ) can be deduced from diabatic heating (e.g., Porter et al. 2010 ). As such, NHT and NHT atm across each latitude band shown in Fig. 6 and Fig. 8 were calculated using top of atmosphere and surface energy fluxes as follows: and where R e is radius of the

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Samantha Stevenson, Baylor Fox-Kemper, Markus Jochum, Richard Neale, Clara Deser, and Gerald Meehl

remote sources. The adjustment of the tropical thermocline to extratropical perturbations is therefore a combination of wave adjustment, advective supply, and diabatic balance (e.g., Cane and Sarachik 1979 ; Gu and Philander 1997 ; Boccaletti 2005 ). While estimates differ on the delay time scale because forcing of downwelling regions (and consequently the wave and advective pathways) differ substantially among models, most studies arrive at a decadal or multidecadal lag for the tropics after an

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