Michael, J. - P., Misra, V., & Chassignet, E. P. (2013). The El Niño and Southern Oscillation in the historical centennial integrations of the new generation of climate models. Reg Environ Change , 13 (S1), 121–130.
Misra, V. (2008). Coupled Air, Sea, and Land Interactions of the South American Monsoon. J. Climate , 21 (23), 6389–6403.
Misra, V. (2009). Harvesting model uncertainty for the simulation of interannual variability. J. Geophys. Res. , 114 (D16).
Misra, V. (2009). The Amplification of the ENSO Forcing over Equatorial Amazon. J. Hydrometeor , 10 (6), 1561–1568.
Misra, V. (2010). Interaction of interannual and diurnal variations over equatorial Africa. J. Geophys. Res. , 115 (D1).
Misra, V. (2013). A multi-disciplinary assessment of the southeastern United States climate. Reg Environ Change , 13 (S1), 1–3.
Misra, V. (2013). The NOAA MAPP Climate Prediction Task Force. U.S. CLIVAR Variations , 11 (2), 27–28.
Misra, V., & Bastola, S. (2016). Reconciling droughts and landfalling tropical cyclones in the Southeastern United States. Clim Dyn , 46 (3-4), 1277–1286.
Misra, V., & Bhardwaj, A. (2019). Defining the Northeast Monsoon of India. Mon. Wea. Rev. , 147 (3), 791–807.
Abstract: This study introduces an objective definition for onset and demise of the Northeast Indian Monsoon (NEM). The definition is based on the land surface temperature analysis over the Indian subcontinent. It is diagnosed from the inflection points in the daily anomaly cumulative curve of the area-averaged surface temperature over the provinces of Andhra Pradesh, Rayalseema, and Tamil Nadu located in the southeastern part of India. Per this definition, the climatological onset and demise dates of the NEM season are 6 November and 13 March, respectively. The composite evolution of the seasonal cycle of 850hPa winds, surface wind stress, surface ocean currents, and upper ocean heat content suggest a seasonal shift around the time of the diagnosed onset and demise dates of the NEM season. The interannual variations indicate onset date variations have a larger impact than demise date variations on the seasonal length, seasonal anomalies of rainfall, and surface temperature of the NEM. Furthermore, it is shown that warm El Niño�Southern Oscillation (ENSO) episodes are associated with excess seasonal rainfall, warm seasonal land surface temperature anomalies, and reduced lengths of the NEM season. Likewise, cold ENSO episodes are likely to be related to seasonal deficit rainfall anomalies, cold land surface temperature anomalies, and increased lengths of the NEM season.
Misra, V., & Bhardwaj, A. (2019). Understanding the seasonal variations of Peninsular Florida. Clim Dyn , 54 (3-4), 1873–1885.
Abstract: This study accounts for varying lengths of the seasons, which turns out to be an important consideration of climate variability over Peninsular Florida (PF). We introduce an objective definition for the onset and demise of the winter season over relatively homogenous regions within PF: North Florida (NF), Central Florida (CF), Southeast Florida (SeF), and Southwest Florida (SwF). We first define the summer season based on precipitation, and follow this by defining the winter season using surface temperature analysis. As a consequence, of these definitions of the summer and the winter seasons, the lengths of the transition seasons of spring and fall also vary from year to year. The onset date variations have a robust relationship with the corresponding seasonal length anomalies across PF for all seasons. Furthermore, with some exceptions, the onset date variations are associated with corresponding seasonal rainfall and surface temperature anomalies, which makes monitoring the onset date of the seasons a potentially useful predictor of the following evolution of the season. In many of these instances the demise date variations of the season also have a bearing on the preceding seasonal length and seasonal rainfall anomalies. However, we find that variations of the onset and the demise dates are independent of each other across PF and in all seasons. We also find that the iconic ENSO teleconnection over PF is exclusive to the seasonal rainfall anomalies and it does not affect the variations in the length of the winter season. Given these findings, we strongly suggest monitoring and predicting the variations in the lengths of the seasons over PF as it is not only an important metric of climate variability but also beneficial to reduce a variety of risks of impact of anomalous seasonal climate variations.
