Vol.33, NO.2, 2022
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Article Navigation >  Journal of Applied Meteorological Science  > 2022  >  33(2): 244-256
Chen Jinqiu, Shi Xiaohui. Possible effects of the difference in atmospheric heating between the Tibetan Plateau and the Bay of Bengal on spatiotemporal evolution of rainstorms. J Appl Meteor Sci, 2022, 33(2): 244-256. DOI:  10.11898/1001-7313.20220210.
Citation: Chen Jinqiu, Shi Xiaohui. Possible effects of the difference in atmospheric heating between the Tibetan Plateau and the Bay of Bengal on spatiotemporal evolution of rainstorms. J Appl Meteor Sci, 2022, 33(2): 244-256. DOI:  10.11898/1001-7313.20220210.
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Possible Effects of the Difference in Atmospheric Heating Between the Tibetan Plateau and the Bay of Bengal on Spatiotemporal Evolution of Rainstorms

DOI: 10.11898/1001-7313.20220210

  • State Key Laboratory of Severe Weather, Chinese Academy of Meteorological Sciences, Beijing 100081

  • Received Date: 2021-09-24
  • Rev Recd Date: 2022-12-20
  • Publish Date: 2022-03-31
    Abstract
  • Based on the climatical daily meteorological data from May to August during 1979-2019, using the methods of empirical orthogonal function (EOF) and multivariate empirical orthogonal function (MV-EOF), correlation analysis and synthetic analysis, the characteristics of the temporal and spatial evolution of atmospheric heat sources around the Tibetan Plateau (TP) and the Bay of Bengal (BOB) are investigated, and their relationships with the rainstorm in eastern China are analyzed. It's found that MV-EOF can well show the relationship between the spatial distribution characteristics of different elements and their temporal evolution.The results reflect the close relationship between the thermal condition of TP and its surrounding areas, the summer monsoon circulation, and the rainstorm in eastern China.Correspondingly, the rainstorm events occur in Southeast China and the middle and lower reaches of the Yangtze River, respectively. The spatial variation characteristics of the atmospheric heating in TP and surrounding areas show significant differences in the second and the third modes of MV-EOF, especially in the reversal of the thermal contrast between TP and BOB. The atmospheric heating in TP and BOB shows an opposite trend, which indicates that the sea-land thermal comparison between TP and BOB is likely to be one of the key factors leading to the occurrence of rainstorm events in different places in eastern China. The results of the synthetic analysis suggest a possible physical mechanism: When the atmospheric heating is weak over TP and strong over BOB, there is a strong ascending motion over BOB and its surrounding areas, which is conducive to the maintaining of South Asian high (SAH) and the northwestern Pacific subtropical high (WPSH) in southward position, and also conducive to the occurrence of cyclonic water vapor transportation circulation in Southeast China-South China Sea-Northwest Pacific. It weakens the southwesterly water vapor transportation, thus induces the continuous heavy precipitation in South China.After the increasing of the atmospheric heating over TP, the convergence and ascending motion of the lower atmosphere are strengthened, which attracts the SAH to move northward to TP, with an enhancement and eastward extension. The WPSH then lift northward, and the airflows around it convey more water vapor to West China and the middle and lower reaches of the Yangtze River, resulting in heavy precipitation. The above results show that in the climate average state, the thermal contrast change of the TP and BOB can change the atmospheric vertical circulation through modulation, affect the location and intensity of the SAH and WPSH, and then change the water vapor transportation. It has an important impact on the spatiotemporal variation of the rainstorm events in the eastern China.
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  • Fig. 1  The spatial distribution of rainstorm precipitation(a) with the time coefficient(b) of the second mode of MV-EOF decomposition and the spatial distribution of rainstorm precipitation(c) with the time coefficient(d) of the third mode of MV-EOF decomposition

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    Fig. 2  The spatial distribution of the apparent heat source of the atmosphere of the second mode(a) and the third mode(b) of MV-EOF decomposition

    (the thick solid line denotes the scope of the Tibetan Plateau)

    DownLoad: Full-Size Img PowerPoint

    Fig. 3  The spatial distribution of the second mode and the third mode of MV-EOF decomposition

    (the thick solid line denotes the scope of the Tibetan Plateau)
    (a)500 hPa geopotential height of the second mode, (b)500 hPa geopotential height of the third mode, (c)integrated water transport flux (the vector) and its divergence (the shaded) of the second mode, (d)integrated water transport flux (the vector) and its divergence (the shaded) of the third mode

    DownLoad: Full-Size Img PowerPoint

    Fig. 4  The spatial distribution and time coefficient of the apparent heat source of the atmosphere of the second and the third modes of EOF decomposition

    (the thick solid line denotes the scope of the Tibetan Plateau)
    (a)the spatial distribution of the second mode of EOF decomposition, (b)the time coefficient of the second mode of EOF decomposition, (c)the spatial distribution of the third mode of EOF decomposition, (d)the time coefficient of the third mode of EOF decomposition

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    Fig. 5  The distribution of synthetic rainstorm precipitation in eastern China in the PC2 high value stage (from 13 Jun to 12 Jul) (a) and in the PC3 high value stage (from 15 May to 12 Jun) (b) based on EOF decomposition of the apparent heat source of the atmosphere

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    Fig. 6  The correlation coefficients between the PC2(a), PC3(b) of EOF decomposition of the apparent heat source of the atmosphere and vertical velocity at 500 hPa respectively

    (only the contours passing the test of 0.05 level respectively are drawn, the thick solid line denotes the scope of the Tibetan Plateau)

    DownLoad: Full-Size Img PowerPoint

    Fig. 7  Distribution of composited geopotential heights at 200 hPa(a), 500 hPa(b) in the PC2 high value stage (from 13 Jun to 12 Jul) and 200 hPa(c), 500 hPa(d) in the PC3 high value stage based on EOF decomposition of the apparent source of the atmosphere (from 15 May to 12 Jun)(unit: dagpm)

    (the thick solid line denotes the scope of the Tibetan Plateau)

    DownLoad: Full-Size Img PowerPoint

    Fig. 8  The correlation coefficients between the PC2(a), PC3(b) of EOF decomposition of the apparent heat source of the atmosphere and integrated water transport flux (the vector), rainstorm precipitation in eastern China (the shaded, dark(light) red and dark(light) blue denote the positive and the negative passing the test of 0.05(0.1) level, respectively)

    (the thick solid line denotes the scope of the Tibetan Plateau)

    DownLoad: Full-Size Img PowerPoint

    Fig. 9  Distribution of composited geopotential heights at 200 hPa(a), 500 hPa(b) in Aug (unit: dagpm)

    (the thick dotted line denotes the trough line, the thick solid line denotes the Tibetan Plateau)

    DownLoad: Full-Size Img PowerPoint
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    • Received : 2021-09-24
    • Accepted : 2022-12-20
    • Published : 2022-03-31
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