Vol.29, NO.1, 2018
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Article Navigation >  Journal of Applied Meteorological Science  > 2018  >  29(1): 84-96
Cao Yang, Chen Hongbin, Su Debin. Identification and correction of the bright band using a C-band dual polarization weather radar. J Appl Meteor Sci, 2018, 29(1): 84-96. DOI:  10.11898/1001-7313.20180108.
Citation: Cao Yang, Chen Hongbin, Su Debin. Identification and correction of the bright band using a C-band dual polarization weather radar. J Appl Meteor Sci, 2018, 29(1): 84-96. DOI:  10.11898/1001-7313.20180108.
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Identification and Correction of the Bright Band Using a C-band Dual Polarization Weather Radar

DOI: 10.11898/1001-7313.20180108
  • 1.

    Key Laboratory of Middle Atmosphere and Global Environment Observation, Institute of Atmospheric Physics, Chinese Academy of Sciences, Beijing 100029

  • 2.

    University of Chinese Academy of Sciences, Beijing 100049

  • 3.

    Collaborative Innovation Center on Forecast and Evaluation of Meteorological Disasters, Nanjing University of Information Science & Technology, Nanjing 210044

  • 4.

    College of Electronic Engineering, Chengdu University of Information Technology, Chengdu 610225

  • Received Date: 2017-06-05
  • Rev Recd Date: 2017-10-09
  • Publish Date: 2018-01-31
    Abstract
  • The bright band is a layer of enhanced reflectivity due to melting of aggregated snow and ice crystals. The occurrence of a bright band causes significant overestimation in radar-based quantitative precipitation estimation (QPE). The bright band signature can be normally identified from vertical profiles of reflectivity (VPRs) of stratiform precipitation echoes and the freezing level height which is derived from radiosonde data. The VPRs correction is desirable to mitigate the bright band contamination and reduce the overestimation of the radar-based QPE. However, a well-defined bright band bottom, which is critical for the correction of bright band, is sometimes not found in VPRs. Fortunately, polarimetric variables, especially the correlation coefficient, can provide a much better depiction of vertical bright band structure than reflectivity.The volume scanning data of a C-band dual polarization radar from Beijing Meteorological Bureau, radiosonde data and measured rainfall data from ground rain gauge stations are used to test the methodology of the bright band identification and correction. Three bright band correction schemes including mean vertical profile of reflectivity (MVPR), apparent vertical profile of reflectivity (AVPR) and apparent vertical profile of correlation coefficient (AVPCC), which are derived from stratiform precipitation echoes, are applied to the reflectivity field in the given tilt, and radar-based QPEs are derived from the corrected reflectivity field based on traditional Z-R relations. Results indicate that the bright band top, peak and bottom can be easily identified from the volume scanning MVPR and the freezing level height, and most of bright band depths are between 0.8 km and 1.5 km. The AVPR and AVPCC schemes are shown to be more effective in mitigating the bright band contamination and reducing the overestimation of radar-derived QPE associated with the bright band than the MVPR correction. Corrected reflectivity fields are physically continuous in distribution, and the corrected radar-derived QPEs are close to the measured value of ground rain gauge stations.
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  • Fig. 1  Mean vertical profile of reflectivity

    (a)2029 BT 4 Aug 2013, (b)2103 BT 11 Aug 2013

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    Fig. 2  Time series of 0℃ isotherm height and top of bright band

    (a)4 Aug 2013, (b)11 Aug 2013

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    Fig. 3  Time series of top, bottom of bright band and the height of peak reflectivity

    (a)4 Aug 2013, (b)11 Aug 2013

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    Fig. 4  The PPI of correlation coefficient(a) and vertical profiles of correlation coefficient and reflectivity(b) at 3.4° elevation at 2029 BT 4 Aug 2013

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    Fig. 5  PPI of reflectivity at 2.4° elevation at 2029 BT 4 Aug 2013

    (a)before correction, (b)correction by MVPR, (c)correction by AVPR, (d)correction by AVPCC

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    Fig. 6  PPI of reflectivity at 2.4° elevation at 2103 BT 11 Aug 2013

    (a)before correction, (b)correction by MVPR, (c)correction by AVPR, (d)correction by AVPCC

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    Fig. 7  Distribution of the reflectivity and gauges shown in Fig. 5

    (triangles and squares denote gauges affected and unaffected by bright band in low tilt, respectively; circles denote gauges affected by bright band in high tilt, which are gauges unaffected by bright band in low tilt) (a)3.4° elevation, (b)5.3° elevation

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    Fig. 8  Distribution of the reflectivity and gauges shown in Fig. 6

    (triangles and squares denote gauges affected and unaffected by bright band in low tilt, respectively; circles denote gauges affected by bright band in high tilt, which are gauges unaffected by bright band in low tilt) (a)4.3° elevation, (b)6.69° elevation

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    Fig. 9  Time series of reflectivity and rainfall intensity from gauge observation effected by bright band

    (a)4 Aug 2013, (b)11 Aug 2013

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    Fig. 10  Scatter plot of reflectivity and rainfall intensity of gauge observation on 4 Aug 2013 and 11 Aug 2013

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    Fig. 11  Scatter plot of rainfall intensity between gauge observation and radar estimation on 4 Aug 2013 and 11 Aug 2013

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    • Received : 2017-06-05
    • Accepted : 2017-10-09
    • Published : 2018-01-31
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