Relationship of tropical-cyclone-induced remote precipitation with tropical cyclones and the subtropical high

doi:10.1007/s11707-015-0530-7

Front. Earth Sci.

2016, Vol. 10

Issue (3) : 595-606 https://doi.org/10.1007/s11707-015-0530-7

RESEARCH ARTICLE

Relationship of tropical-cyclone-induced remote precipitation with tropical cyclones and the subtropical high

Rui XING^1,²,Zhiying DING^1,^2,^*(

),Sangjie YOU^1,²,Haiming XU^1,²

¹. Key Laboratory of Meteorological Disasters of the Ministry of Education, Nanjing University of Information Science & Technology, Nanjing 210044, China
². Department of Atmospheric Sciences, Nanjing University of Information Science & Technology, Nanjing 210044, China

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Abstract

This study concerns the precipitation induced by a tropical cyclone (TC) before the TC arrives, which will be referred to as TC remote precipitation (TRP). Based on the distribution characteristics of the non-rotational wind and the divergent-wind vertical circulation related to TC, the subtropical high, and TRP of 45 TRP events during June, July, and August of 2000?2009, the relationships among these three entities (TC, subtropical high, and TRP) can be categorized into four patterns. The first pattern accounts for the highest proportion of the TRP events (59%), and a conceptual model is then provided for this pattern. The primary characteristics of this model are as follows: TC, the subtropical high, and TRP can interact with each other through the divergent-wind secondary circulation at both sides of the ridge line of the subtropical high (between the subtropical high and TC, and between the subtropical high and TRP). At the upper level (150 or 200 hPa), the northward non-rotational wind from the TC converged toward the subtropical high ridge line and subsided, and at 950 hPa the divergent wind from the ridge line of the subtropical high converged toward TC; these constructed the secondary circulation between TC and the subtropical high. In the meantime, the southward non-rotational wind at the upper level (150 or 200 hPa) from TRP and the divergent wind at 950 hPa from the subtropical high ridge line toward TRP constructed the secondary circulation between TRP and the subtropical high. As TC and TRP interacted with each other, the subtropical high ridge line was usually under the downdraft area of the whole atmosphere. The other three patterns are different from the first pattern mainly in terms of the intensity and position of the non-rotational-wind secondary circulation. The numerical simulation of the Beijing 7·21 rainstorm confirmed the relationship among TC, the subtropical high, and TRP, indicating that when the interaction weakened, the TRP also weakened.

Keywords tropical cyclone tropical cyclone remote precipitation subtropical high divergent wind numerical simulation

Corresponding Author(s): Zhiying DING

Just Accepted Date: 10 October 2015 Online First Date: 11 December 2015 Issue Date: 20 June 2016

Cite this article:

Rui XING,Zhiying DING,Sangjie YOU, et al. Relationship of tropical-cyclone-induced remote precipitation with tropical cyclones and the subtropical high[J]. Front. Earth Sci., 2016, 10(3): 595-606.

URL:

https://academic.hep.com.cn/fesci/EN/10.1007/s11707-015-0530-7
https://academic.hep.com.cn/fesci/EN/Y2016/V10/I3/595

Fig.1 Curve of the composite regionally-averaged divergent wind velocity (unit: m·s⁻¹) vs. pressure. The dashed lines denote the critical layers where the wind speed decreased or increased rapidly

Fig.2 Left column: composite geo-potential height (solid curve; units: dagpm), divergent wind (vector; unit: m·s⁻¹) with divergence (shading; units: 10⁻⁵s⁻¹ ) at 950 hPa. Middle column: composite geo-potential height at 950 hPa with divergent wind and divergence at 200 hPa or 150 hPa (b1 and b2 for 150 hPa and the remaining for 200 hPa). Right: composite geo-potential height at 500 hPa and precipitation (shading; units: mm) for the four patterns (panels c1 to c4). The elliptical area indicates the composite TRP area, the thick black line represents the convergent or divergent center near the SH ridge line, and the TC symbol denotes the composite TC center at 950 hPa (similarly hereinafter).

Fig.3 Composite vertical circulation of the v-component of non-rotational wind (shading denotes the velocity; unit: m·s⁻¹) and vertical velocity (unit: 10⁻² m·s⁻¹) along the longitude that passed through TC center and TRP area for patterns I (a), II (b), III (c), and IV (d). The TC symbol represents the location of the composite TC, the triangle symbol represents the divergent center at the lower level near the SH ridge, and the ellipse represents the latitude range of the composite TRP (similarly hereinafter).

Fig.4 A conceptual model for the whole-layer relationship pattern. The thin black contour indicates the geo-potential height at 950 hPa, and the brown line denotes the SH ridge. The arrows indicate airflow directions.

Tab.1 Statistical numbers of the four relationship patterns among TC, SH, and TRP

Tab.2 Average distance between TC and TRP for patterns I and II and their respective distances to the lower-level divergence center at 950 hPa

Fig.5 Maps of 850-hPa wind (arrows; unit: m·s⁻¹), water vapor flux (shading; unit: g·(s·hPa·cm)⁻¹), and 6-h accumulative precipitation (solid curve unit: mm) from the TRMM data at (a) 0600 UTC 21 July 2012 and (b) 1200 UTC 21 July 2012.

Fig.6 Geo-potential height, non-rotational wind with divergence at 950 hPa at 0600 UTC 21 July 2012 (a) and 1200 UTC 21 July (c). Geo-potential height at 950 hPa, non-rotational wind at 200 hPa at 0600 UTC 21 (b) and 1200 UTC 21 (d). (The units are the same as in Fig. 2.) Vertical circulation of the regionally-averaged v-component of divergent wind and vertical velocity at 0600 UTC 21 July (the region is 115°E−117°E) (e) and at 1200 UTC 21 July (the region is 115°E−118°E) (f). (The units are the same as in Fig. 3).

Fig.7 (a) Tracks of TC Vicente from the JMA best track dataset and the control run output at 6-h interval. (b) Corresponding time series of intensity.

Fig.8 Top: 18-h accumulative precipitation (shading; units: mm) from 0600 UTC 21 July 2012 to 0000 UTC 22 July for (a) the CMORPH data and (b) the control run. Bottom: divergent wind (vector; units: m·s⁻¹) and geo-potential height (solid contour; units: dagpm) at 950 hPa (c), the divergent wind at 150 hPa and geo-potential height at 950 hPa (d) at 1200 UTC 21 July in the control run.

Fig.9 (a) Comparison of the regionally-averaged (38.44°N−44.04°N, 109.98°E−121.48°E) accumulative precipitation every 3-h from 0600 UTC 21 July 2012 to 0000 UTC 22 July between control run and sensitivity test (no-TC). (b) 18-h accumulative precipitation in this time period in the sensitivity test. Units: mm.

Fig.10 Vertical cross section of regionally-averaged (120°E−123°E) v-component of the non-rotational wind (units: m·s⁻¹) in (a) the control and (b) the sensitivity test at 1200 UTC 21 July 2012.

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