Journal of Arid Meteorology ›› 2022, Vol. 40 ›› Issue (3): 406-414.DOI: 10.11755/j.issn.1006-7639(2022)-03-0406
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JIAO Yang1,2(), ZHANG Yongjing1,2, YIN Chengmei1,2, CHU Yingjia1,2
Received:
2020-12-04
Revised:
2021-01-04
Online:
2022-06-30
Published:
2022-06-28
焦洋1,2(), 张永婧1,2, 尹承美1,2, 褚颖佳1,2
作者简介:
焦洋(1989—),女,工程师,从事天气预报和极端天气研究. E-mail: jiaoyang0621@foxmail.com。
基金资助:
CLC Number:
JIAO Yang, ZHANG Yongjing, YIN Chengmei, CHU Yingjia. Response of summer rainstorm in Shandong Province to change of spring atmospheric heat sources in southeastern Tibet Plateau and its adjacent areas[J]. Journal of Arid Meteorology, 2022, 40(3): 406-414.
焦洋, 张永婧, 尹承美, 褚颖佳. 山东夏季暴雨对青藏高原东南部及邻近区域春季大气热源变化的响应[J]. 干旱气象, 2022, 40(3): 406-414.
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URL: http://www.ghqx.org.cn/EN/10.11755/j.issn.1006-7639(2022)-03-0406
Fig.1 Spatial distribution of the first mode of standardized rainstorms days field decomposed by EOF (a) and its time coefficient series (b), and the tendency distribution (c, Unit: d·(10 a)-1) and anomaly series (d)of rainstorms days in summer from 1979 to 2018 in Shandong Province (The solid triangles and inverted triangles pass the significance test at 0.05 level)
Fig.2 The distribution of mean atmospheric heat source in spring (a) and summer (b) (Unit: W·m-2) (the black line for the Tibetan Plateau boundary with altitude more than 3000 m, and the red box for the strong center of atmospheric heat source. the same as below)
Fig.3 The correlation coefficients distribution between summer rainstorm index in Shandong Province and intensity of atmospheric heat source in spring (a) and summer (b), and the time series of atmospheric heat source intensity index over the Tibetan Plateau in spring (c) and its correlation coefficients distribution with summer rainstorm days in Shandong Province (d) from 1979 to 2018 (The dotted areas pass the significance test at 0.1 level. the same as below; the solid triangles from small to large pass the significances tests at 0.1 and 0.05 level, respectively)
Fig.4 The 200 hPa geopotential height field (a, Unit: gpm), 500 hPa geopotential height (color shaded areas, Unit: gpm)and integrated water vapor flux (vectors, Unit: g·cm-1·s-1) field (b) in summer regressed by spring atmospheric heat source intensity index over the Tibetan Plateau
Fig.5 The zonal vertical sections of relative vorticity (color shaded areas, Unit: 10-5 s-1) and wind field (vectors, Unit: m·s-1) along 30°N in the same period (a) and over 35°N-40°N area in summer (b) regressed by atmospheric heat source intensity index over the Tibetan Plateau in spring (The black area is the Tibetan Plateau, and black arrows pass the significance test at 0.1 level. the same as below)
Fig.6 The spatial distribution of the first mode of 200 hPa mean meridional wind anomaly field in summer decomposed by EOF (a, color shaded areas) and its standardized time coefficients series (b) (the black contours for the climatic average location of westerly jet with wind speed more than or equal to 20 m·s-1)
Fig.7 The meridional vertical section of average relative vorticity (color shaded areas, Unit: 10-5 s-1) and wind field (vectors, Unit: m·s-1) over 110°E-125°E in the same period regressed by SAH_int in summer
Fig.8 The lowpass filtered mean relative vorticity (color shaded areas, Unit: 10-5 s-1) and TN flux (vectors, Unit: m2·s-2) at 200 hPa in the same period regressed by Silk Road teleconnection correlation index in summer
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