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Biao Geng and Masaki Katsumata

-dB Z echo-top height in each grid was defined as the maximum height of the specified echo intensity in the column of the grid. Echo areas, echo-top heights, and volumetric rainfall values were derived for both convective and stratiform echoes. Relationships between the radar-derived variables and the MJO, ERW, KW, and MRGW events were investigated by performing a simple linear regression (SLR) analysis and a standardized multiple linear regression (MLR) analysis. Each time series of the radar

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Arun Kumar, Jieshun Zhu, and Wanqiu Wang

. From the time series of RMM indices over the analysis period (1998–2017 for rainfall and 1988–2017 for others), the corresponding spatial patterns in other fields are obtained on the basis of regressions of unfiltered daily anomalies of respective fields against daily values of RMM indices. From the spatial regression patterns and RMM indices, daily values of MJO-related components are linearly reconstructed for the fields of interest. Variance percentage associated with MJO variability is then

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Joshua Chun Kwang Lee, Anurag Dipankar, and Xiang-Yu Huang

as statistical linear regression or analytical balance operators) between them. These multivariate relationships can be extracted by inserting a single observation of a specific variable and assessing the resulting analysis increments from all other variables. To illustrate, a pseudo-single observation of θ , which is 1 K above the background is inserted at around 1 km altitude near the center of the domain ( Fig. 1a ) with an observation error of 0.2 K. We focus on the prescribed relationship

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Satoru Yokoi, Shuichi Mori, Masaki Katsumata, Biao Geng, Kazuaki Yasunaga, Fadli Syamsudin, Nurhayati, and Kunio Yoneyama

). The cooling dominated only during period I, whereas warming took place in the following days (13 December onward) when the diurnal cycle of precipitation was obscured. Using this time series in period I as a reference, we then perform regression analysis of daily time series of the radar-estimated precipitation at a particular location and hour of day ( Fig. 12b ). The top of this figure plots the regression coefficients between the late-afternoon cooling and precipitation at 0700 LT of the same

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