Research Article The Impact of Typhoon Danas (2013) on the...

Research ArticleThe Impact of Typhoon Danas (2013) on the Torrential RainfallAssociated with Typhoon Fitow (2013) in East China

Hongxiong Xu1 and Bo Du2

1State Key Laboratory of Severe Weather, Chinese Academy of Meteorological Sciences, Beijing 100081, China2China Meteorological Administration Meteorological Observation Center, Beijing 100081, China

Correspondence should be addressed to Hongxiong Xu; [email protected]

Received 30 September 2014; Revised 20 January 2015; Accepted 20 January 2015

Academic Editor: Hann-Ming H. Juang

Copyright © 2015 H. Xu and B. Du. This is an open access article distributed under the Creative Commons Attribution License,which permits unrestricted use, distribution, and reproduction in any medium, provided the original work is properly cited.

When typhoon Danas (2013) was located at northeast of Taiwan during 6–8 October 2013, a torrential rainfall brought by typhoonFitow (2013) occurred over the east of China. Observations show that the rainband of Fitow, which may be impacted by Danas,caused the rainfall over north of Zhejiang. The Advanced Research version of the Weather Research and Forecast (ARW-WRF)model was used to investigate the possible effects of typhoon Danas (2013) on this rainfall event. Results show that the modelcaptured reasonably well the spatial distribution and evolution of the rainband of Fitow. The results of a sensitivity experimentremoving Danas vortex, which is conducted to determine its impact on the extreme rainfall, show that extra moist associated withDanas plays an important role in the maintenance and enhancement of the north rainband of Fitow, which resulted in torrentialrainfall over the north of Zhejiang. This study may explain the unusual amount of rainfall over the north of Zhejiang provincecaused by interaction between the rainband of typhoon Fitow and extra moisture brought by typhoon Danas.

1. Introduction

Extreme rainfall is responsible for a variety of societalimpacts, including flash flooding that can lead to damage,injury, and fatalities [1]. Tropical cyclones (TCs) are oftenheavy rain producers [2]. Thus, it is of great interest toaccurately predict extreme rainfall caused by TCs. However,heavy rainfall (including TCs rainfall) interweavesmultiscalenonlinear interactions among different physical processesand weather systems [3–5]. Such interactions include envi-ronmental moisture transport and binary TC (BTC) interac-tion [6].

Binary tropical cyclones (BTCs) can interact with eachother when they are close enough [7–10]. Their interactiondepends on the distance of two TCs, the differences inTC size, intensity, and the variations in the currents [11].Based on the results of numerical experiments, Shin et al.[10] suggested that the critical separation distance of binaryvortices is slightly less than twice the radius at which therelative vorticity of one vortex becomes zero. Concerningthe observations of binary tropical cyclones and realisticflow patterns surrounding tropical cyclones, studies by Carr

III et al. [12] and Carr III and Elsberry [13] proposed fourconceptual models of track-altering binary tropical cyclonesthat occurred in the Pacific Ocean.

If there is another typhoon near the area of disaster,the effects of binary tropical cyclone interaction make theprocess of precipitation become much more complicated.Studies [14, 15] showed that BTC processes may associatewith torrential rainfall in favorable environment conditions.Wu et al. [14] found that tropical Storm Paul (1999) plays animportant role in impeding the movement of Rachel, thusbecoming one of the key factors in enhancing the rainfallamount in southern Taiwan. Xu et al. [15] found that Goni(2009, 08W) transported a large amount of moisture andenergy into Morakot (2009, 09W). The interaction betweenGoni and Morakot accounts for about 30% of precipitationover Taiwan.

In this study, we discussed the role of the circulationassociated with Danas (2013) played in the extreme rainfallcaused by Fitow (2013). Specifically, the purpose of this paperis to quantify the distant effects of typhoon Danas on theextreme rainfall brought by rainband of Fitow in the east ofChina on 8–10 October 2013. In Section 2, we described the

Hindawi Publishing CorporationAdvances in MeteorologyVolume 2015, Article ID 383712, 11 pageshttp://dx.doi.org/10.1155/2015/383712

2 Advances in Meteorology

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Advances in Meteorology 3

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model configuration and design of numerical experimentsused in this study. We presented the results of numericalsimulations in Section 3. Finally we summarize conclusionsin Section 4.

2. Overview of 8–10 October 2013Torrential Rainfall

Figure 1 shows 500 hPa geopotential height and wind fromthe National Centers for Environmental Prediction (NCEP)

FNL analysis. It shows a South Asian anticyclone over theTibetan Plateau in southwestern China, and a west windtrough extended from north of China to Sichuan province(Figure 1(a)). In the mid-latitudes over the Japan Sea, therewas a subtropical anticyclone. During the typhoon Fitowlandfall over east of China (Figures 1(b), 1(c), and 1(d)),subtropical anticyclone moved to east. Warm and moistureof typhoon interacted with cold air after the westerly trough.This condition was favorable for the development of convec-tion and result of rainfall.


Typhoon Fitow hit north of Fujian province during 6–8 October 2013 and produced extreme rainfall and broughtabout catastrophic flash flooding to Zhejiang province. Theobserved 48 h rainfall is shown in Figure 2. The extremerainfall areas are mainly located in the coast and north ofZhejiang province. The exceptional rainfall with a recordamount of 700mm (northeast of Zhejiang) exceeded the 60-year recurrence.The southeast coast ofmainlandChina expe-riences several hits of landfalling typhoons every year [15].However, the amount of rainfall over Zhejiang (especially,north of Zhejiang) brought by Fitow is quite rare.Thus, it is ofgreat interest to explore the possible mechanism responsiblefor the unusual heavy rainfall.

Radar mosaic reflectivity (Figure 3) shows a quasistation-ary rainband, which was nearly in east-west direction overthe north of Zhejiang province. Along the band, there wereseveral echo centers of 45–55 dBz embedded in line, whichcorresponded to the north rainband of typhoon Fitow. Insidethe north rainband, there was another rainband occurringover the south of Zhejiang province. The inner echo bandwas also composed of a lot of echo centers. Inside the tworadar echo bands, there were a few echo blocks extendingto the eyewall along the radial, which corresponded to theconnecting spiral rainband.

Studies have shown that rainbands of a TCmoving slowlyoutward along the radial [16–18] may remain stationarywith new cells forming on the upwind edge [19, 20]. Thisprocess also occurred to the rainbands of typhoon Fitow(Figure 3). The north rainband remained stationary overZhejiang province. However, the south rainband movedfurther to the south when typhoon Fitow was to the south-west. The two rainbands were maintained by a differentsource of moisture. The north rainband was sustained bythe east flow for transporting warm and moisture water tothe region, with new convective cells repeat initiated in theupwind of rainband. However, the south rainband of Fitowwas maintained by both east flow and typhoon circulationassociated with typhoon Danas. The north quasistationaryrainbands began to decay, as typhoon Danas was movingfurther to the southwest.

The rainfall brought by typhoon Fitow is similar to thecase in typhoon Wipha (2007, 13W) [21, 22], but with largeramount and more severe disaster. Besides the favorable envi-ronments similar to Wipha, what other factor contributed tothe extreme rainfall caused by Fitow?

3. Model Description and Experimental Design

The WRF model version 3.4.1 [23] was utilized here atconvection-permitting resolutions to simulate the extremerainfall event. The model is initiated at 1800 UTC 5 October2013, but the domain D03 is activated at 6 h later. Figure 4shows the domain and topography for two experiments. Themodel horizontal spacing is 30 km, 10 km, and 3.3 km for d01,d02, and d03. Sizes of model grids are 375 × 246, 238 × 160,and 394 × 286, respectively. 30 sigma levels were defined withthe model top at 100 hPa.

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Themodel physical options include theThompsonmicro-physics scheme [24], the YSU planetary boundary layerscheme [25], the Kain-Fritsch cumulus parameterizationscheme [26, 27], the Noah land surface model [28, 29], therapid radiative transfermodel [30] longwave, and the Dudhiashortwave radiation scheme [31]. The cumulus parameteri-zation scheme was not applied to the finest (3.3 km) griddomain to explicitly resolve the convective rainfall.

Control (CTRL) and sensitive experiments (No Danas)were performed to investigate the impact of Danas on theextreme rainfall. In the control experiment, the initializedcondition was from NCEP-NCAR reanalysis data (1∘× 1∘)[32], while, in the sensitive experiment, the Danas vortexin the reanalysis data is removed. The method to removea vortex in the analysis field is the tropical cyclone (TC)bogussing scheme in the ARW-WRF [23]. The scheme canremove an existing tropical storm and was used to removetyphoon Danas vortex in No Danas experiment.

4. Result and Discussion

We first examine the structure of the rainband and its rainfallin CTRL experiment. Figure 5 presents the simulated radarreflectivity (DBZ) from CTRL experiment. In the CTRLexperiment, there are two rainbands over the north andsouth of Zhejiang province, respectively, in good agreementwith observation (Figure 5(a)). The north rainband extendedoutward of typhoon. New convective cells repeat initiated atupwind and move along rainband (Figures 5(b) and 5(c)).However, the simulated north rainband develops west of thelocation and more intense in northwest of Zhejiang provinceof the observed rainband (Figures 5 and 4).

The simulated 48 h accumulated rainfall of CTRL isshown in Figure 7(a). The distribution and intensity of


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simulated rainfall is nearly the same as what was observed(Figures 7(a) and 2). The maximum rainfall in CTRL experi-ment is 550mm, compared with 570mm that was observed.There are broad regions of the north and coast of Zhejiangexceeding 300mm. The horizontal distribution of simulated48 h accumulated precipitation is also similar to that of theobservation, but the location is incorrect to the southwest. Ingood agreement with the simulated distribution of the rain-bands, there is a westward and southward displacement of the

simulated precipitation and overestimate over northwest ofZhejiang province. Figure 11 presents time series of hourlyarea averaged rainfall, from the CMORPH-Gauge mergeddata and the CTRL and No Danas experiments. Comparedwith observation, the CTRL experiment underpredicted thetotal rainfall in the north Zhejiang province; the under-prediction occurred mainly during 1500 UTC 6 October–0000 UTC 8 October 2013, namely, the time of the heaviestrainfall. In spite of the underestimation of the peak rainfall


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intensity of Fitow, the simulated in CTRL experiment showthe reasonable evolution and distribution of rainfall.

Figure 6 shows the simulated track of CTRL, during0000 UTC 6 October-0000 UTC 7 October 2013, ChinaMeteorological Administration-Shanghai Typhoon Institute(CMA-SH). The model simulated the intensity of typhoonFitow reasonably well at the first 12 h of integration butconsiderably underpredicted the weakening rate of typhoonFitow (Figure 6(a)). On the other hand, the simulatedtrack of Saomai is nearly the same as the observed track

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over the ocean. After Fitow landfall, there is a westwardand southward displacement of the simulated precipitation(Figure 6(b)).

Figure 8 compares CTRL and No Danas simulated mois-ture flux (vector) and specific humidity (shaded, unit: g/Kg)at 0100 UTC 7 October 2013. In the two experiments, highvalues ofmoisture over east of China are brought westward bythe strong southeast flow (Figure 8). In theCTRL experiment,the Danas-related moisture exhibited spiral band-shapedbridge Fitow and Danas, which result in more moisturebrought to north of Zhejiang (Figure 8(a)). On the otherhand, the No Danas experiment shows only two narrowmoisture bands connecting to typhoon Fitow in the southof Zhejiang province (Figure 8(b)), and the high values(>14 g/Kg) of moisture over Zhejiang province are confinedmainly around typhoon Fitow, and there is not a band of highmoisture (>14 g/Kg) over the north of Zhejiang. The resultsindicate that one of the significant differences between thetwo experiments was the moisture transported by typhoon


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Danas. Previous research has shown that low-level moisturefrom the ocean can produce more rainfall [27, 33].

Prior to interaction between binary typhoon Danas andFitow, the rainbands distribution in the two experimentswas nearly identical (Figures 5(a) and 9(a)). This agreementsuggests that removal of typhoon Danas had little impacton formation of north-rainband farther west previous to thearrival of the typhoon Danas-related moisture [34]. As inthe CTRL experiment, two rainbands appear over the northand south of Zhejiang province about 1900 UTC 06 October.However, the north rainband disappeared and is displacedwith little scattered convective cells, and its convection haslittle area of stratiform rainfall brought with it. During 1900UTC 06 to 0100 UTC 07, the differences between the twosimulations became even better defined, as convective cellsrepeated initiation on upwind and move alone the rainbandin the CTRL experiment, but this process did not happen inNo Danas. Accordingly, by 0100 UTC 07 (Figures 5(d) and9(d)), there is still a rainband over the north of Zhejiangprovince in the CTRL simulation, while it disappeared inNo Danas. As a result, the extreme rainfall of the northof Zhejiang occurs in the CTRL experiment, but not inNo Danas.

Much of the reason for these differences in the mainte-nance of the north rainband can be attributed to the eastwardtransport of moisture associated with Danas. Figure 10 showscross sections along A1-A2 (Figures 10(a) and 1(c)) and B1-B2 (Figures 10(b) and 10(d)) at 0000 UTC 7 October 2013. Ascan be seen, there are convective cells lining from northwestto southeast along the north rainband. The radar reflectivitygreater than 35 DBZ extended from surface to ∼8Km. Onthe contrary, in the No Danas simulation, the developmentof convective cells ceases. This suggests that typhoon Danas

provided extramoisture for rainband and allowed it to persistfor a longer period.

The importance of the moisture becomes clear. In theCTRL simulation, there is a seemingly unlimited supplyof moisture to the north rainband of Fitow, whereas theNo Danas experiment has a less source of moisture. Conse-quently, new convection continues to initiate on the westernside of rainband in theCTRL, asmoremoist air is transportedinto the area. As a result of the rainband moving slowly overthe north of Zhejiang province, this allows more rainfall toaccumulate at the north of Zhejiang province. On the otherhand, once the instability from nearby sources is releasedin the No Danas experiment, the development of rainbandceases and weakens. These results indicate that the moist airfrom east coast of China played an important role inmoistureconvergence and the formation of north rainband regardlessofwhetherDanas existed and that theDanas-relatedmoistureprovided an additional source of fuel for this rainband andallowed the convection along the rainband to persist for alonger period.

In summary, the No Danas experiment shows that theextra moisture associated with typhoon Danas caused about2 times of the maximum precipitation from the outerrainbands of typhoon Fitow over the north of Zhejiangprovince—the maximum 48 h total in the No Danas runwas ∼220mm compared with more than 500mm in theCTRL experiment and observation (Figures 1, 3, and 10).This indicates about 55% reduction in total precipitationfrom the CTRL to No Danas. Namely, extra moisture fromthe typhoon Danas led to more than 55% enhancementof the total rainfall over the north of Zhejiang province.Thus, the interaction between typhoon Fitow and Danasduring 1900 UTC 06 and 0400 UTC 07 October (Figure 11)


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transported extra moisture to the north of Zhejiang provinceand resulted in the maintenance of north rainband oftyphoon Fitow. Consequently, this process made the greatestdifference in the precipitation happen at the north of Zhejiangprovince.

5. Conclusion

The ARW-WRF model is used to investigate the impact oftyphoon Danas (2013) over the western North Pacific ontorrential rainfall produced by typhoon Fitow (2013) over eastof China. In this case, when typhoon Danas was located innortheast of Taiwan, torrential precipitation occurred far tothe west over Zhejiang province of east China and its coastalarea. In CTRL simulation, the model reasonably reproducedthe major features of typhoon Fitow rainband and the

torrential rainfall over Zhejiang province. To investigate thecontribution of typhoon Danas to the rainfall in Zhejiangprovince, a sensitive experiment (No Danas) was performedin which the typhoon Danas vortex was removed. As a resultof absence of typhoon Danas, rainfall over the north ofZhejiang associated with north rainband of typhoon Fitowrapidly disappeared, indicating that typhoonDanas played animportant role in the rainfall produced by typhoon Fitow forthe case studied.

The major process involved in the effects of typhoonDanas is through the enhanced westward moisture transportinto the north rainband of typhoon Fitow. As a result,typhoon Danas played an important role in the torrentialrainfall in the north of Zhejiang province, although thetyphoon Danas was more than 1000 km to the east overnortheast of Taiwan.


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Conflict of Interests

The authors declare that there is no conflict of interestsregarding the publication of this paper.

References

[1] R. S. Schumacher and R. H. Johnson, “Mesoscale processescontributing to extreme rainfall in a midlatitude warm-seasonflash flood,”MonthlyWeather Review, vol. 136, no. 10, pp. 3964–3986, 2008.

[2] Y.Wang and H. Fudeyasu, “The role of Typhoon Songda (2004)in producing distantly located heavy rainfall in Japan,”MonthlyWeather Review, vol. 137, no. 11, pp. 3699–3716, 2009.

[3] F. D. Marks, L. K. Shay, G. Barnes et al., “Landfalling tropicalcyclones: forecast problems and associated research opportuni-ties,” Bulletin of the AmericanMeteorological Society, vol. 79, no.2, pp. 305–323, 1998.

[4] B.-W. Shen,W.-K. Tao,W.K. Lau, andR. Atlas, “Predicting trop-ical cyclogenesis with a global mesoscale model: hierarchicalmultiscale interactions during the formation of tropical cycloneNargis (2008),” Journal of Geophysical Research D: Atmospheres,vol. 115, no. 14, Article ID D14102, 2010.

[5] M. Zhang and D.-L. Zhang, “Subkilometer simulation of atorrential-rain-producing mesoscale convective system in EastChina. Part I: model verification and convective organization,”Monthly Weather Review, vol. 140, no. 1, pp. 184–201, 2012.

[6] H. Xu, X. Zhang, and X. Xu, “Impact of tropical storm bophaon the intensity change of super typhoon Saomai in the 2006typhoon season,” Advances in Meteorology, vol. 2013, Article ID487010, 13 pages, 2013.

[7] S. Fujiwhara, “The mutual tendency towards symmetry ofmotion and its application as a principle in meteorology,”Quarterly Journal of The Royal Meteorological Society, vol. 47,pp. 287–293, 1921.

[8] S. Fujiwhara, “The mutual tendency towards symmetry ofmotion and its application as a principle in meteorology,”Quarterly Journal of the RoyalMeteorological Society, vol. 49, pp.287–293, 1923.

[9] S. Fujiwhara, “On the growth and decay of vortical systems,”Quarterly Journal of the RoyalMeteorological Society, vol. 49, pp.75–104, 1931.

[10] S.-E. Shin, J.-Y. Han, and J.-J. Baik, “On the critical separationdistance of binary vortices in a nondivergent barotropic atmo-sphere,” Journal of the Meteorological Society of Japan, Series II,vol. 84, no. 5, pp. 853–869, 2006.

[11] S. Brand, “Interaction of binary tropical cyclones of the westernNorth Pacific Ocean,” Journal of Applied Meteorology, vol. 9, no.3, pp. 433–441, 1970.

[12] L. E. Carr III, M. A. Boothe, and R. L. Elsberry, “Observationalevidence for alternate modes of track-altering binary tropicalcyclone scenarios,”Monthly Weather Review, vol. 125, no. 9, pp.2094–2111, 1997.

[13] L. E. Carr III and R. L. Elsberry, “Objective diagnosis of binarytropical cyclone interactions for the western north pacificbasin,” Monthly Weather Review, vol. 126, no. 6, pp. 1734–1740,1998.

[14] C.-C. Wu, K. K. W. Cheung, J.-H. Chen, and C.-C. Chang,“The impact of tropical storm paul (1999) on the motionand rainfall associated with tropical storm rachel (1999) nearTaiwan,”MonthlyWeather Review, vol. 138, no. 5, pp. 1635–1650,2010.

[15] X. Xu, C. Lu, H. Xu, and L. Chen, “A possible mechanismresponsible for exceptional rainfall over Taiwan from TyphoonMorakot,” Atmospheric Science Letters, vol. 12, no. 3, pp. 294–299, 2011.

[16] H. V. Senn and H. W. Hiser, “On the origin of hurricane spiralrain bands,” Journal of Meteorology, vol. 16, no. 4, pp. 419–426,1959.

[17] H. E. Willoughby, “A possible mechanism for the formation ofhurricane rainbands,” Journal of the Atmospheric Sciences, vol.35, no. 5, pp. 838–848, 1978.

[18] P. T. May, “The organization of convection in the rainbands ofTropical Cyclone Laurence,”Monthly Weather Review, vol. 124,no. 5, pp. 807–815, 1996.

[19] L. Zhou, G. Zhai, and B. He, “Numerical study of the mesoscalesystems in the spiral rainband of 0509 Typhoon Matsa,”Advances inAtmospheric Sciences, vol. 28, no. 1, pp. 118–128, 2011.

[20] D. Atlas, K. Hardy, R. Wexler, and R. Boucher, “On the originof hurricane spiral bands,” Geof́ısica Internacional, vol. 3, no. 4,pp. 123–132, 1963.

[21] H. Zhou, “Mesoscle spiral rainband structure of super typhoonwipha(0713) observed by dual-doppler radar,” Transactions ofAtmospheric Sciences, vol. 33, no. 3, pp. 271–284, 2010 (Chinese).

[22] L. Zhou, G. Zhai, and D. Wang, “Mesoscale numerical studyof the rainstorm and asymmetric structure of 0713 typhoonwipha,” Chinese Journal of Atmospheric Sciences, vol. 35, no. 6,pp. 1046–1056, 2011 (Chinese).

[23] W. C. Skamarock, J. B. Klemp, J. Dudhia et al., “A description ofthe advanced research WRF version 3,” NCAR Technical NoteNCAR/TN-475+STR, 2008.


[24] G. Thompson, P. R. Field, R. M. Rasmussen, and W. D. Hall,“Explicit forecasts of winter precipitation using an improvedbulk microphysics scheme. Part II. Implementation of a newsnow parameterization,” Monthly Weather Review, vol. 136, no.12, pp. 5095–5115, 2008.

[25] S.-Y. Hong and H.-L. Pan, “Nonlocal boundary layer verticaldiffusion in a medium-range forecast model,”Monthly WeatherReview, vol. 124, no. 10, pp. 2322–2339, 1996.

[26] J. S. Kain, “The Kain—Fritsch convective parameterization: anupdate,” Journal of Applied Meteorology, vol. 43, no. 1, pp. 170–181, 2004.

[27] M. Lonfat, R. Rogers, T. Marchok, and F. D. Marks, “A paramet-ric model for predicting hurricane rainfall,” Monthly WeatherReview, vol. 135, no. 9, pp. 3086–3097, 2007.

[28] F. Chen and J. Dudhia, “Coupling an advanced land surface–hydrology model with the Penn State–NCAR MM5 modelingsystem. Part II: preliminarymodel validation,”MonthlyWeatherReview, vol. 129, no. 4, pp. 587–604, 2001.

[29] F. Chen and J. Dudhia, “Coupling an advanced land surface-hydrology model with the Penn State-NCAR MM5 modelingsystem. Part I: model implementation and sensitivity,”MonthlyWeather Review, vol. 129, no. 4, pp. 569–585, 2001.

[30] E. J. Mlawer, S. J. Taubman, P. D. Brown, M. J. Iacono, and S. A.Clough, “Radiative transfer for inhomogeneous atmospheres:RRTM, a validated correlated-k model for the longwave,”Journal of Geophysical Research D: Atmospheres, vol. 102, no. 14,pp. 16663–16682, 1997.

[31] J. Dudhia, “Numerical study of convection observed dur-ing the winter monsoon experiment using a mesoscale two-dimensionalmodel,” Journal of theAtmospheric Sciences, vol. 46,no. 20, pp. 3077–3107, 1989.

[32] National Weather Service/NOAA/U.S. Department of Com-merce/NCEP, CEP FNL Operational Model Global TroposphericAnalyses, Continuing from July 1999, Research Data Archive atthe National Center for Atmospheric Research, Computationaland Information Systems Laboratory, Boulder, Colo, USA,2000.

[33] J.M.Medlin, S. K. Kimball, andK.G. Blackwell, “Radar and raingauge analysis of the extreme rainfall during hurricane Danny’s(1997) landfall,” Monthly Weather Review, vol. 135, no. 5, pp.1869–1888, 2007.

[34] R. S. Schumacher, T. J. Galarneau Jr., and L. F. Bosart, “Distanteffects of a recurving tropical cyclone on rainfall in a midlati-tude convective system: a high-impact predecessor rain event,”Monthly Weather Review, vol. 139, no. 2, pp. 650–667, 2011.

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