Vol.28, NO.3, 2017
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Article Navigation >  Journal of Applied Meteorological Science  > 2017  >  28(3): 340-356
Zhao Qiang, Wang Nan, Li Pingyun, et al. Diagnosis of thermal and dynamic mechanisms of two rainstorm processes in Northern Shaanxi. J Appl Meteor Sci, 2017, 28(3): 340-356. DOI:  10.11898/1001-7313.20170308.
Citation: Zhao Qiang, Wang Nan, Li Pingyun, et al. Diagnosis of thermal and dynamic mechanisms of two rainstorm processes in Northern Shaanxi. J Appl Meteor Sci, 2017, 28(3): 340-356. DOI:  10.11898/1001-7313.20170308.
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Diagnosis of Thermal and Dynamic Mechanisms of Two Rainstorm Processes in Northern Shaanxi

DOI: 10.11898/1001-7313.20170308

  • Shaanxi Provincial Meteorological Observatory, Xi'an 710014

  • Received Date: 2016-11-30
  • Rev Recd Date: 2017-03-31
  • Publish Date: 2017-05-31
    Abstract
  • Based on the conventional meteorological observations and 6 h 1°×1° NCEP FNL analysis data, two heavy rain processes occurred on 21-22 July 2013 and 8-9 July 2014 in northern Shaanxi are diagnosed with synoptic method and dynamic diagnosis method. It shows that both processes can be attributed to the intersection of the warm moist air flow along the edge of subtropical high at 500 hPa and the cold air brought from plateau troughs. Low-level jet plays an important role, as it provides adequate water vapor and water vapor convergence lifts on the left side of the shear line. The vertical secondary circulation produced by the coupling of upper-and low-level jet is an important triggering factor. Heavy rainfall in "0721" process occurs mainly at Yan'an where strong coupling of upper-level jet and low-level jet is located. There is strong convective instability in the atmosphere in the initial stage of precipitation during both rainstorm processes. Convergence lifting from the low-level shear line triggers convection energy, resulting in strong precipitation. The latent heat of condensation released by the precipitation extends downward to the middle atmosphere, and leads to thermal discontinuity of the middle and lower atmosphere. Atmospheric wet baroclinicity and frontogenesis significantly enhances, causing the uplift of whole layer saturated atmosphere and strong precipitation, finally producing heavy rainfall process. Because the convective precipitation is stronger and latent heat released is greater in "0721" rainstorm process, the feedback of the low-level jet and the middle atmosphere frontogenesis is stronger, and therefore the precipitation is heavier. The vertical component of generalized convective vorticity vector describes the enhancing of vertical wind shear very well, and describes the frontogenesis which is increased by condensation latent heat that released by water vapor phase transition in the middle and lower layers very well. Therefore, the changing trend of generalized convective vorticity vector can reflect the development and decrease of precipitation. The large value center and high gradient area on the south side of the vertically integrated moist thermodynamic advection parameters is consistent with rainstorm fall area, and it appears about 6 hours before the precipitation, indicating it can be used to effectively forecast regional precipitation.
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    References(34)

  • Fig. 1  The accumulated precipitation of Shaanxi (unit:mm)

    (a) from 2000 BT 21 Jul to 2000 BT 22 Jul in 2013, (b) from 2000 BT 8 Jul to 2000 BT 9 Jul in 2014

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    Fig. 2  500 hPa height (the contour, unit:dagpm), wind at 0800 BT 22 Jul 2013(a) and 2000 BT 8 Jul 2014(b) with 700 hPa height (the contour, unit:dagpm), wind, vorticity (the shaded) at 0800 BT 22 Jul 2013(c), 2000 BT 8 Jul 2014(d)

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    Fig. 3  The evolution of upper level and low level jet (the wind vector and the wind direction denote wind at 200 hPa and 700 hPa, the contour and the shaded denote wind speed at 200 hPa and 700 hPa, unit:m·s-1)

    (a)2000 BT 21 Jul 2013, (b)0800 BT 22 Jul 2013, (c)0200 BT 9 Jul 2014, (d)0800 BT 9 Jul 2014

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    Fig. 4  The evolution of upper level and low level divergence

    (the contour denotes divergence at 200 hPa, the shaded denotes divergence at 700 hPa, unit: 10-5 s-1) (a)0800 BT 22 Jul 2013, (b)0200 BT 9 Jul 2014

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    Fig. 5  The vertical circulation (profile along the oblique line in Fig.3b, the shaded denotes terrain)

    (a)0800 BT 22 Jul 2013, (b)0200 BT 9 Jul 2014

    DownLoad: Full-Size Img PowerPoint

    Fig. 6  The profile of the equivalent potential temperature along 110°E (unit:K)(the shaded denotes terrain)

    (a)2000 BT 21 Jul 2013, (b)0800 BT 22 Jul 2013, (c)0800 BT 8 Jul 2014, (d)2000 BT 8 Jul 2014

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    Fig. 7  The vertical profile of latent heat of condensation heating rate (unit: J·kg-1·s-1) at 0800 BT 22 Jul 2013(a), 2000 BT 8 Jul 2014(b), generalized potential temperature (unit:K) at 0800 BT 22 Jul 2013(c), 2000 BT 8 Jul 2014(d), and the profile of frontogenesis function along 110°E (unit:10-10 K·m-1·s-1) at 0800 BT 22 Jul 2013(e), 2000 BT 8 Jul 2014(f)(the shaded denotes terrain)

    DownLoad: Full-Size Img PowerPoint

    Fig. 8  The distribution of vertical integration of moist thermodynamic advection (the contour, unit:10-9(K2·Pa)/(m2·s))(the shaded denotes column cloud water)

    (a)0800 BT 22 Jul 2013, (b)0800 BT 9 Jul 2014

    DownLoad: Full-Size Img PowerPoint

    Fig. 9  The distribution of generalized convective vorticity vector (the contour, unit:10-4 K·s-1)(the shaded denotes column cloud water)

    (a)0800 BT 22 Jul 2013, (b)0800 BT 9 Jul 2014

    DownLoad: Full-Size Img PowerPoint
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    • Received : 2016-11-30
    • Accepted : 2017-03-31
    • Published : 2017-05-31
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