• <tr id="yyy80"></tr>
  • <sup id="yyy80"></sup>
  • <tfoot id="yyy80"><noscript id="yyy80"></noscript></tfoot>
  • 99热精品在线国产_美女午夜性视频免费_国产精品国产高清国产av_av欧美777_自拍偷自拍亚洲精品老妇_亚洲熟女精品中文字幕_www日本黄色视频网_国产精品野战在线观看 ?

    Impact of the Monsoonal Surge on Extreme Rainfall of Landfalling Tropical Cyclones

    2021-04-20 00:42:02DajunZHAOYubinYUandLianshouCHEN
    Advances in Atmospheric Sciences 2021年5期

    Dajun ZHAO, Yubin YU, and Lianshou CHEN

    1State Key Laboratory of Severe Weather, Chinese Academy of Meteorological Sciences, Beijing 100081, China

    2University of Chinese Academy of Sciences, Beijing 100049, China

    ABSTRACT A comparative analysis and quantitative diagnosis has been conducted of extreme rainfall associated with landfalling tropical cyclones (ERLTC) and non-extreme rainfall (NERLTC) using the dynamic composite analysis method. Reanalysis data and the tropical cyclone precipitation dataset derived from the objective synoptic analysis technique were used. Results show that the vertically integrated water vapor transport (Qvt) during the ERLTC is significantly higher than that during the NERLTC. The Qvt reaches a peak 1?2 days before the occurrence of the ERLTC and then decreases rapidly. There is a stronger convergence for both the Qvt and the horizontal wind field during the ERLTC. The Qvt convergence and the wind field convergence are mainly confined to the lower troposphere. The water vapor budget on the four boundaries of the tropical cyclone indicates that water vapor is input through all four boundaries before the occurrence of the ERLTC,whereas water vapor is output continuously from the northern boundary before the occurrence of the NERLTC. The water vapor inflow on both the western and southern boundaries of the ERLTC exceeds that during the NERLTC, mainly as a result of the different intensities of the southwest monsoonal surge in the surrounding environmental field. Within the background of the East Asian summer monsoon, the low-level jet accompanying the southwest monsoonal surge can increase the inflow of water vapor at both the western and southern boundaries during the ERLTC and therefore could enhance the convergence of the horizontal wind field and the water vapor flux, thereby resulting in the ERLTC. On the other hand, the southwest monsoonal surge decreases the zonal mean steering flow, which leads to a slower translation speed for the tropical cyclone associated with the ERLTC. Furthermore, a dynamic monsoon surge index (DMSI) defined here can be simply linked with the ERLTC and could be used as a new predictor for future operational forecasting of ERLTC.

    Key words: landfalling tropical cyclones, extreme rainfall, monsoon surge, dynamic composite analysis

    1. Introduction

    Tropical cyclones are major synoptic systems and often produce destructive rainstorms. There are many records of extreme rainfall related to the activity of tropical cyclones(Tao, 1980). For example, the maximum 24-h rainfall record for China (1748.5 mm on 1 August 1996) was recorded at Ali Mountain in Taiwan Province during Typhoon Herb (1996). The maximum 24-h rainfall record of 1062 mm in the Chinese mainland was recorded during the “75.8 extraordinary rainstorm in Henan province ” caused by Typhoon Nina (1975) (975) (Chen et al., 2012). Rainstorms associated with tropical cyclones have a widespread impact in terms of both their duration and range (Lei, 2020) and can lead to both economic and social losses, making disaster prevention and mitigation challenging (Chen et al.,2012). Previous studies have shown that the highest proportions of rainfall induced by tropical cyclones occur in East Asia (Khouakhi et al., 2017), and that heavy rainfall in this region is more sensitive to changes in the water vapor content of the atmosphere than general rainfall (Trenberth,1999). The Intergovernmental Panel on Climate Change Fifth Assessment Report noted that the frequency and intensity of extreme rainfall have been increasing as a result of global warming and increasing amounts of atmospheric water vapor. We therefore need to carry out systematic studies on landfalling tropical cyclone extreme rainfall(ERLTC).

    Extreme rainfall events have caused great losses in recent years as a result of their high frequency and widespread impact, but are still a great challenge in operational forecasting. Extreme rainfall is generally defined by either the relative (95th or 99th percentiles) or absolute (daily or accumulated rainfall during the precipitation process)threshold methods. The relative method focuses on the climatology of extreme rainfall to determine a pattern (Chris et al., 2002; Knight and Davis, 2009). The absolute method is commonly used in synoptic studies. For example, a typhoon-induced extraordinary rainstorm in China with 24-h rainfall ≥1000 mm was defined as an extreme rainfall by Chen and Xu (2017), although there have been seven extreme rainfall associated with typhoons that have met this criterion since 1960. Six of these extreme rainfall occurred in Taiwan, but only one in the Chinese mainland. A maximum daily rainfall ≥50 mm is also used to define an extreme rainfall during a typhoon (hoon (Jiang et al., 2018;Qiu et al., 2019). Using this definition, the operational forecasting terms of typhoon-induced torrential rain, heavy torrential rain and extraordinary storm all refer to the extreme rainfall associated with typhoons.

    As a crucial component of the Earth’s atmospheric circulation, monsoons are essential for the occurrence of rainfall.China is located in the world’s largest monsoonal climate zone, the Asian?Australian monsoon region, and therefore the Asian monsoon has a great impact on rainstorms in China (Zhao et al., 2019). Statistical and numerical studies have shown that low-level jets (LLJs) mainly consist of boundary layer jets (BLJs) and synoptic system-related LLJs (SLLJs) over southern China, which are the key factors in regulating heavy rainfall (Du and Chen, 2019a),convection initiation (Du and Chen, 2019b) and the subsequent upscale convective growth (Du et al., 2020). Chen et al. (2010) concluded that the heavy rainfall from landfalling typhoons depends upon the transport of water vapor, the extratropical transition process, land surface processes, topography, and mesoscale convective systems. The relationship between the rainfall associated with landfalling tropical cyclones and summer monsoon jets has also been investigated. Results show that the tropical cyclones causing widespread heavy rainfall are often consistently associated with a low-level jet after landfall and the water vapor flux and latent heat are significantly higher than tropical cyclones that only cause weak rainfall (Cheng et al., 2012). The summer monsoon is not constant in its intensity after onset and shows marked low-frequency oscillations. A monsoon surge occurs when the wind speed increases dramatically, followed by significant changes in the weather (Dictionary of Atmospheric Science 1994). Monsoon surge is usually defined as the band-pass filtered zonal wind at 850 hPa (Ju et al., 2005, 2007) or regional mean of total wind at 850 hPa over a specific area (Dong et al., 2010). In addition, the monsoon surge is always identified with southeast oriented cloud clusters in infrared satellite imagery in real time operational forecasting. When the southwest monsoonal is strong,a low-level jet tends to form and approach typhoons from their south side to transport sufficient water vapor, which is conducive to the formation and maintenance of heavy rainfall (Tao, 1980). Monsoon surges are crucial in rainstorms that cause flooding and provide the water vapor required for the rainstorm (Tao and Wei, 2007).

    The southeastern coast of China is the most active area in the East Asian summer monsoon region, and landfalling typhoons often occur where monsoon surges and typhoons have more opportunity to interact with each other (Chen and Xu, 2017). Dong et al. (2010) reported that a southwesterly monsoonal surge can intensify the transport of water vapor to westward-moving typhoons, and that the enhanced southwesterly flow increases the convergence near the typhoon,which favors the development of ascending motion and intensifies the rainfall. Based on these studies, it is easy to associate monsoon surges with LTCER and the surges may influence the occurrence of such rainfall. Wang et al. (2010) also showed that the monsoon surge can increase the torrential rains induced by the landfalling typhoon.

    Extreme rainfall, including ERLTC, has increased in frequency within the current backdrop of global warming,hence we need to improve our understanding of the causative mechanisms for these events. The main objective of this study is to conduct a dynamic composite analysis of the occurrence of ERLTC and to focus on the impact of the monsoonal surge on it. Landfalling tropical cyclones with nonextreme rainfall (NERLTC) are also analyzed.

    The rest of the paper is organized as follows. Section 2 describes the data and methods. Section 3 details the water vapor flux composite and comparative analysis in terms of the vertically integrated water vapor transport (Q), the Qconvergence, lateral boundary budget and the vertical distribution. Section 4 discusses the impacts of the low-level jet and steering flow associated with the monsoon surge. Our discussion and conclusions are presented in section 5.

    2. Data and methods

    The 6-h reanalysis data from the National Centers for Environmental Prediction?National Center for Atmospheric Research dataset with a spatial resolution of 2.5°×2.5° and the tropical cyclone best-track dataset from the China Meteorological Administration (Ying et al., 2014) are used. In addition, the tropical cyclone precipitation dataset identified by objective synoptic analysis (Ren et al., 2001,2007) is also employed, which partitions the rainfall induced by tropical cyclones from the total rainfall based on station observations from the Chinese mainland, Macau,Hong Kong and Taiwan Island. The dataset also includes rainfall record over land induced by side-swiping tropical cyclones which did not make landfall (fall (Feng et al., 2020),in addition to the rainfall from tropical cyclones that do make landfall. These data have been widely applied in studies of typhoon-induced rainfall over China (Ren et al., 2006;Jiang et al., 2018; Qiu et al., 2019; Liu and Wang, 2020).

    Our study has taken more factors into consideration in defining typhoon extreme rainfall, including the number of samples and the representativeness of the tropical cyclones triggering the extreme rainfall, the differences among typhoon-induced torrential rain, heavy torrential rain and extraordinary storms, and extreme rainfall caused by typhoons on Taiwan, Hainan Island and the Chinese mainland. We defined typhoon-induced extraordinary rainstorms in China as a rainfall event in which the 24-h rainfall was ≥600 mm at a single rain gauge station. Statistically, there are 38 records of single-station typhoon extreme rainfall from 1960 to 2019, caused by a total of 26 typhoons. Among these 26 typhoons, 14 resulted in extreme rainfall in Taiwan, 5 resulted in extreme rainfall in Hainan and 7 resulted in extreme rainfall in the Chinese mainland.Seven ERLTC occurred at the same rain gauge station at Ali Mountain, Taiwan Island, which is more than 25% of all the typhoons according to our definition. These typhoons are the main object of study in this paper. We carried out comparative analysis and dynamic diagnosis of the large-scale circulations of selected tropical cyclones using dynamic composite analysis (e analysis (Li et al., 2004). The ERLTC and NERLTC were identified based on the similarities of the season of occurrence (major season, July?September), track(northwestward), and location (Ali Mountain in Taiwan Island) of the tropical cyclones. On this basis, typhoons 9608, 0908, 6312, 1307 and 0813 were selected as associated with ERLTC, whereas typhoons 9417, 1315, 0713,0505 and 0605 were selected as associated with NERLTC.This research focuses on the precipitation induced by tropical cyclones over land. The term “l(fā)andfalling tropical cyclones” refers to the landfall of either the center of the tropical cyclone or the tropical cyclone rain belt. Thus, it covers both the landfalling tropical cyclones and side-swiping tropical cyclones in the operational forecasting definition.The average daily rainfall during ERLTC and NERLTC is 1223.0 and 165.7 mm, respectively (Table 1). We are more concerned with the differences between extreme rainfall and ordinary torrential rain accompanied with landfalling typhoons, not the so-called “dry typhoon” which can only generate precipitation over 24-h≤50 mm.

    Figure 1 shows the tracks and intensity categories of the tropical cyclones during the ERLTC (Fig. 1a) and NERLTC (Fig. 1b). These tropical cyclones occurred during the peak season of tropical cyclone activity (July?September)and showed a mainly northwestward movement. All these tropical cyclones made landfall or affected Taiwan and the Chinese mainland, reaching the category of a typhoon or above before landfall. To avoid the influence of terrain and to make the tropical cyclone samples more comparable, we selected the tropical cyclones associated with ERLTC and NERLTC in Ali Mountain, Taiwan. This paper focuses on the main differences between the tropical cyclones that bring extreme rainfall and those that bring non-extreme rainfall under similar backgrounds of atmospheric circulation and the same terrain.

    3. Comparative analysis of water vapor flux

    3.1. Vertically integrated water vapor transport

    The vertically integrated water vapor transport (Q) of an air column is defined as (Ding, 1989; Chen and Huang,2007):

    where

    q

    (kg kg) and

    V

    (m s) are the specific humidity and wind vector for each layer of the air column, respectively,

    u

    and

    v

    are the zonal and meridional wind components, respectively,

    P

    (Pa) is the surface air pressure,

    g

    is the gravitational acceleration and the unit of

    Q

    is kg ms.

    Table 1. Overview of selected ERLTCs and NERLTCs.

    Fig. 1. Track and intensity categories of the selected (a) ERLTC and (b) NERLTC during periods of extreme rainfall. TD, TS, STS, TY, STY and SupTY are representing the tropical depression, tropical storm, severe tropical storm, typhoon, strong typhoon and super typhoon, respectively.

    We aimed to explore the evolutionary characteristics and compare the differences of water vapor between ERLTC and NERLTC. Figure 2 shows the evolution of the area-averaged Qduring ERLTC and NERLTC, where rectangles of different colors indicate the overall evolution of the water vapor flux of the typhoon and the surrounding environmental field as a function of the side lengths relative to the eye of the typhoon center.

    The different variation trends for the Qare consistent with each other. The Qincreases continuously, reaching a maximum 1.5 days before the occurrence of extreme rainfall and then decreases rapidly. This evolutionary trend is most pronounced within the rectangles with side lengths of 5° and 10°, indicating that there are significant differences in the water vapor fluxes within the typhoon circulation before and after the occurrence of extreme rainfall. This is an indication of the occurrence of extreme rainfall. A comparison between ERLTC (Fig. 2a) and NERLTC (Fig. 2b)shows that the Qin the tropical cyclone circulation and the surrounding environmental field is significantly higher for the ERLTC than for the NERLTC.

    Fig. 2. Variations in the regional average Qvt during (a) ERLTC and (b) NERLTC (units: kg m?1 s?1). The horizontal axis shows the time in days relative to the occurrence of rainfall, ?1 (?2) means the day (two days) before the extreme rainfall occurrence, and so on. Color curves indicate distances from TC centers in degrees latitude and longitude.

    Fig. 3. The Qvt (units: kg m?1 s?1) for (a, d, g, j) ERLTC and (b, e, h, k) NERLTC and their differences (c, f, i, l) (units:kg m?1 s?1). (a?c) and (d?f) show the Qvt two days and one day before rainfall, respectively, (g?i) shows the Qvt on the day when the rainfall occurred and (j?l) show the Qvt one day after rainfall. The center of the tropical cyclone is set as the origin of the coordinates, which are positive to the north and east direction and negative to the south and west. Horizontal and vertical axes indicate the distance in latitude and longitude degree from the composite TC center.

    Differences in the water vapor fields can result in very different intensities and distributions of rainfall, which could, in turn, determine the spatiotemporal distribution and intensity of typhoon rainstorms (Ye and Li, 2011). To further investigate the main water vapor transport channels in the tropical cyclones that trigger extreme rainfall, Fig. 3 shows the Qbetween 1000 and 300 hPa during ERLTC and NERLTC and their differences. There are two major channels for the transport of water vapor from the southwest and southeast regions for both types of tropical cyclone, but the southwestern water vapor channel of a tropical cyclone associated with the ERLTC is much broader and continuously provides water vapor for the development of the cyclone.However, the southeastern oriented water vapor channel interacts with the two types of tropical cyclones in different quadrants–in the first quadrant (northeast relative to the typhoon center) for ERLTC and in the fourth quadrant (southeast relative to the typhoon center) for NERLTC. In other words, the environmental southeastern oriented water vapor channel combines with the typhoon in its northeast (southeast) direction in ERLTC (NERLTC). Tropical cyclones associated with the ERLTC have a continuous and stable inflow of water vapor from the southeastern sector. The differences in water vapor transport (Figs. 3c, 3f, 3i and 3l) show that the southwestern channels for the transport of water vapor is powerful and long-lasting in the environmental field for tropical cyclones associated with the ERLTC. A continuous inflow of water vapor from the southwest for tropical cyclones associated with the ERLTC occurs from two days before the extreme rainfall to one day after its occurrence, intensifying the water vapor flux on the southwestern side of the tropical cyclones. Thus, a more intense southwesterly transport of water vapor in the environment is a key feature differentiating tropical cyclones associated with the ERLTC from those associated with the NERLTC.

    3.2. Qvt divergence and decomposition terms

    The Qcan reflect the source of the water vapor for rainfall and the relationship between the transport of water vapor and the weather systems in the environment. The location and intensity of the rainfall are more closely related to the divergence of the Q.

    The

    Q

    divergence

    C

    of the air column is decomposed as follows (Chen and Huang, 2007):

    where

    C

    is the source (sink) for water vapor transport.

    C

    >0 (

    C

    < 0) indicates the convergence (divergence) of water vapor, meaning a water vapor transport sink (source).

    C

    consists of two components: the convergence of the wind [the first term on the right-hand side of Eq. (2)] and the advection term for water vapor [the second term on the right-hand side of Eq. (2)]. A positive (negative) value of the wind field convergence or the wet (dry) advection of water vapor facilitate (suppresses) the convergence of water vapor.

    Figure 4 shows the spatial distributions of the Qdivergence and the two components (convergence and advection of water vapor) during the ERLTC and the NERLTC on the date when extreme rainfall occurred. On the day on which the extreme rainfall occurred, strong convergence of water vapor was located within 10° of the center of the tropical cyclone related to ERLTC, where there are large areas of water vapor convergence on the southwestern and southeastern sides, associated with the southwestern and southeastern water vapor fluxes, respectively (Fig. 4a). Although there is also a strong area of convergence of water vapor near the center of the tropical cyclone related to NERLTC (Fig. 4b), the corresponding intensity and range are significantly smaller than those in ERLTC. There is also an area of strong water vapor divergence within 10° northeast of the center of tropical cyclone related to the NERLTC. These characteristics are unchanged during the two days before the occurrence of extreme rainfall (figure not shown). The distribution of the water vapor flux divergence for both types of tropical cyclone is mainly determined by the wind field convergence term (Figs. 4c?f), indicating that the contribution of wind convergence to water vapor flux convergence is significantly greater than that of water vapor advection. Specifically,wind convergence is mainly within the circulation of the two types of tropical cyclones as well as the environmental fields on their southeastern and southwestern sides (Figs. 4c?d). The wind convergence is much wider and stronger within the circulation of tropical cyclones associated with ERLTC and within the environmental field on its southwestern side compared with tropical cyclones associated with NERLTC. For the water vapor advection term, wind convergence (Figs. 4e, 4f) contributes less (relatively more) to the total water vapor flux convergence in ERLTC (NERLTC).However, such difference does not have a significant effect on the total water vapor flux convergence. Therefore, tropical cyclones associated with ERLTC are associated with strong wind convergence to their southwestern and southeastern sides–that is, with the presence of stronger moisture advection in the environment–resulting in a stronger water vapor flux convergence in the circulation of the tropical cyclones. However, the wind convergence in the environment to the southwest and southeast of tropical cyclones associated with NERLTC is relatively weak and the northern side of the tropical cyclones is dominated by dry advection, making a negative contribution to the water vapor flux convergence in NERLTC.

    3.3. Qvt budget on the lateral boundaries of tropical cyclones

    We used the regional average water vapor budget proposed by Ding (1989):

    Fig. 4. Distributions of (a, b) Qvt (vector) and Qvt divergence (shaded), (c, d) convergence and (e, f) water vapor advection during ERLTC and the NERLTC for the day on which extreme rainfall occurs (units: 10?5 kg m?2 hPa?1 s?1).ERLTC are shown on the left panels, NERLTC on the right panels.

    The four terms on the right-hand side of Eq. (4) represent the amount of water vapor entering the selected region from the southern, northern, western and eastern boundaries, respectively, where

    k

    and

    n

    are the number of grids along the meridional and zonal directions in the selected region, and ?

    l

    , ?

    l

    , ?

    l

    and ?

    l

    are the grid spacings along the four boundaries. Our study area is a square with sides of 10° longitude/latitude centered on the eye of the typhoon.The variations in the water vapor flux at each lateral boundary and the total water vapor flux during the ERLTC and the NERLTC were calculated to determine the characteristics of the water vapor budget in the typhoon area during the ERLTC.

    We investigated the evolution of the Qin ERLTC and NERLTC along the four boundaries (east, west, south and north) of the rectangular region with side lengths of 10°from the center of the typhoon to quantitatively determine the transport of water vapor between the environment and the tropical cyclones (Fig. 5). The water vapor flows enter through all four boundaries during ERLTC (Fig. 5a), with the largest (smallest) inflow on the southern (northern) boundary. The inflow of water vapor increases on the southern and western boundaries before the occurrence of ERLTC,reaching a peak 1?2 days before the occurrence of extreme rainfall, respectively, and then decreases rapidly once the extreme rainfall begins. However, there is no significant difference between the inflow of water vapor on the northern and eastern boundaries before and after the occurrence of extreme rainfall. Similarly, there are also water vapor inflows on the southern, western and eastern boundaries of the rectangular region for tropical cyclones associated with NERLTC. However, there is a continuous outflow of water vapor on the northern boundary before the occurrence of rainfall (Fig. 5b), which is consistent with previous findings(Ding and Liu, 1986). The inflows of water vapor on both the western and southern boundaries during ERLTC are larger than those during NERLTC, but there is no obvious difference in the water vapor budget between the two types of tropical cyclones on the eastern boundary. Therefore the inflow of water vapor on the northern boundary is an important feature that distinguishes ERLTC from NERLTC.

    3.4. Vertical distribution of water vapor flux

    Figure 6 shows the vertical profiles of the water vapor fluxes averaged over the rectangular area with side lengths of 10° from the center of the typhoon for the two types of tropical cyclones. These profiles were used to determine the distribution of water vapor fluxes in different layers.

    The fluxes of water vapor in both types of tropical cyclones decrease with height as a result of their structural characteristics–i.e., areas with high wind speeds and large amounts of water vapor are located in the lower and middle troposphere. However, the water vapor flux is significantly higher in the tropical cyclones associated with ERLTC than those associated with NERLTC and can be almost twice as large in the same layer. The regionally averaged water vapor flux below 850 hPa in ERLTC is at a maximum from two days before the occurrence of extreme rainfall until the day on which the extreme rainfall occurs. By contrast, the regionally averaged water vapor flux in NERLTC reaches a maximum three days before the occurrence of rainfall and then decreases from two days before the occurrence of rainfall. Combined with the results for the Q(Fig. 3), this shows that the lower troposphere makes the highest contribution to the Q, and therefore the water vapor flux in the lower troposphere is significantly different between the ERLTC and NERLTC.

    Fig. 5. Evolution of the Qvt budget for ERLTC and NERLTC along the four boundaries of the rectangular region with side lengths of 10° from the center of the typhoon (units: kg m?1 s?1).

    Fig. 6. Vertical profiles of the average water vapor flux in the rectangular area with side lengths of 10° from the center of the two types of tropical cyclone for (a) ERLTC and (b) NERLTC (units: kg m?1 s?1).

    4. Impact of the monsoonal surge

    4.1. Monsoon surge and low-level jet

    Our analyses show the strong convergence of Qduring ERLTC, which is mainly caused by the strong convergence of wind. This section further explains the configuration of circulation that allows for such a strong convergence of the water vapor flux during ERLTC. Figure 7 shows the configuration of the wind and humidity fields at 850 hPa and the west Pacific subtropical high at 500 hPa for the same time period.

    There is no significant difference between the humidity fields of the two types of tropical cyclones. The tropical cyclone itself and its western side are both areas of high humidity and these areas are slightly larger in regions with ERLTC. However, the configurations of the wind field are markedly different for the two types of tropical cyclone. During ERLTC, the tropical cyclones are linked to the southwestern low-level jet and interact with each other for a long time(Figs. 7a and 7c), causing the southern monsoonal trough to advance eastward and the subtropical high to retreat eastward and then move northward. This is consistent with the conclusions in Cheng et al. (2012) that the water vapor and instability energy associated with low-level jet have an important influence on landfalling typhoon induced extraordinary rainstorms. However, the tropical cyclone associated with the NERLTC does not interact with the southwestern lowlevel jet. The area near the tropical cyclone with high wind speeds is always to the east, mainly as a result of the strong pressure gradient between the subtropical high and the tropical cyclone.

    4.2. Monsoon surge slows the movement of tropical cyclones

    Many previous studies have documented that a slower translation speed of a tropical cyclone favors local extreme rainfall by extending the impact period of the typhoon, especially on Taiwan Island (Chien and Kuo, 2011; Su et al.,2012; Wu, 2013; Chen and Xu, 2017). Figure 8 shows the translation speed of our selected examples of ERLTC (NERLTC) and the average speed calculated using the latitudinal and longitudinal position at 6-h intervals in the best-track dataset.

    Figure 8 clearly shows that the average translation speed of the ERLTC (NERLTC) is slower (faster) during the period of extreme rainfall. Specifically, the average translation speed of the ERLTC (NERLTC) is 15.5 (20.5) km h.The average translation speed of the ERLTC is only 75% of the average for the NERLTC. Tu and Chou (2013) suggested that intense and long-lasting typhoon rainfall is mainly a result of this slower translation speed, which may be associated with weakening of the steering flow. Figure 9 shows the zonal component of the steering flow of ERLTC and NERLTC at each level between 1000 and 200 hPa and the whole-layer zonal mean component of the steering flow.Before the occurrence of extreme rainfall, the direction of the zonal steering flow in ERLTC and NERLTC were similar at the middle and higher levels, but were different in magnitude. The tropical cyclones associated with ERLTC had a much stronger westward zonal steering flow while the NERLTC had an eastward zonal steering flow in the lower troposphere. This directly affected the whole-layer zonal mean steering flow and therefore the ERLTC had a relatively weak eastward zonal mean steering flow, which contributed to the slower translation speed relative to the NERLTC.

    Fig. 7. Specific humidity (shading; units: 10?2 kg kg?1) at 850 hPa, wind speed ≥12 m s?1 (black contours), zonal wind u=0(red solid line; units: m s?1) and the 500-hPa geopotential height (blue solid line; units: 10 gpm) for the (a, c) ERLTC and (b,d) NERLTC (a, b) one day before and (c, d) on the day on which the extreme rainfall occurred.

    4.3. Dynamic monsoon surge index

    Within the background of the East Asian summer monsoon, the activities of monsoonal surges are characterized by a clear increase in wind speed, possibly associated with the activity of low-level jets. Monsoon surges have previously been defined as the regional average of the zonal wind at 850 hPa in a given region (Dong et al., 2010; Hai et al., 2017). As a landfalling typhoon generally moves from east to west after formation, it is often difficult to distinguish the circulation of the typhoon itself from the monsoon surge circulation during and after the landfalling. We therefore define a dynamic monsoon surge index (D MSI)as:

    Fig. 8. Translation speed (units: km h?1) of the five selected ERLTC (red dashed lines) and their average (red solid line) and the five NERLTC (blue dashed lines) and their average (blue solid lines)calculated from their latitudinal and longitudinal position records at 6-h intervals in the best-track dataset.

    Fig. 9. Time series of the zonal component of steering flow (vectors) and its magnitude (shading; units: m s?1) at each level between 1000 and 200 hPa of (a) ERLTC and (b) NERLTC. The vectors in the lower box of each panel show the wholelayer zonal mean component of steering flow.

    where

    U

    denotes the zonal wind at 850 hPa,

    x

    indicates the longitude range from 40° to 10° west of the center of the tropical cyclone and similarly

    y

    indicates that the latitude varies within 20° south of the center of the tropical cyclone (as shown in the rectangle in Fig. 10a). The DMSI is the average of

    N

    grid values in the region, which means that the location of the center of the tropical cyclone at each time is taken as the dynamic regional center. This ensures that, in dynamic coordinates, the tropical cyclone is always at the center of the study area, whereas the monsoon surge is always to the southwest of the tropical cyclone.

    Fig. 10. (a) Domain for the definition of the DMSI overlain by the 850 hPa wind field (units: m s?1) of the ERLTC one day before the occurrence of extreme rainfall. (b) Evolution of the DMSI for the two types of tropical cyclone (units: m s?1).

    Figure 10b shows the evolution of the DMSI during the ERLTC and NERLTC. The DMSI clearly distinguishes ERLTC from NERLTC, with the DMSI of ERLTC being significantly greater than that of NERLTC before and after rainfall. The DMSI increases continuously three days before the extreme rainfall in ERLTC, peaks on the day on which the rainfall occurs, and then decreases rapidly. The DMSI also increases before the occurrence of rainfall in NERLTC, but with a relatively small magnitude. The DMSI proposed here indicates significance for ERLTC and could be taken as a predictor of ERLTC in operational forecasting.

    5. Discussion and conclusions

    We carried out composite and comparative analyses of two types of tropical cyclone (10 cases in total) based on an objective definition of ERLTC from the perspective of monsoon surges.

    (1) The Qpeaks 1?2 days before the occurrence of the ERLTC and decreases dramatically after the occurrence of rainfall. The Qin the circulation of the tropical cyclone and its surrounding environmental field during the ERLTC is significantly larger than that during the NERLTC. In terms of the regionally averaged water vapor fluxes, both the circulation of the ERLTC and its environment are moister than that of the NERLTC.

    (2) There is a wider and more persistent water vapor channel to the southwest of the tropical cyclone during the ERLTC than during the NERLTC. The low-level jet to the southwest of the tropical cyclone during the ERLTC is connected to the tropical cyclone for a long time and continuously enhances the cyclonic circulation of the tropical cyclone. The Qconvergence is stronger during the ERLTC than during the NERLTC. The wind convergence term contributes the most to the environmental fields in both types of tropical cyclones, whereas the water vapor advection term has a relatively minor role. The strong wind convergence in the ERLTC is mainly caused by the low-level jet overlain by the circulation of the tropical cyclone, whereas there is no low-level jet in the environment of cyclones associated with NERLTC.

    (3) The water vapor flux budget on the boundaries indicates that there is inflow of water vapor from the four boundaries 10° from the center of the tropical cyclone during the ERLTC, whereas there is a continuous outflow of water vapor on the northern boundary during the NERLTC before the rainfall occurs. Quantitatively, the inflow of water vapor is larger on both western and southern boundaries during the ERLTC than during the NERLTC, but there is little difference on the eastern boundary.

    (4) The southwest monsoonal surge can decrease the zonal mean steering flow, which leads to a slower translation speed and extends the period of influence of the ERLTC. The circulation of the landfalling typhoon and the monsoon circulation can be clearly distinguished by our newly defined DMSI. The DMSI is significantly higher during the ERLTC than during the NERLTC and increases dramatically before the occurrence of ERLTC. Given its clear physical implications, the DMSI could be used as a predictor for ERLTC and could be used in operational forecasting.

    Our conclusions suggest that monsoon surge activity has a significant impact on ERLTC. Previous reports of ERLTC have mainly focused on a single case (Ge et al.,2010; Chien and Kuo, 2011; Ding, 2015), whereas our findings are based on several and are an extension of previous studies concluding that low-level jets have an important influence on the formation of typhoon-induced extraordinary storms (Cheng et al., 2012). From the perspective of monsoon surges, understanding the formation and development of low-level jets and their interaction with tropical cyclones can help to improve our understanding of the mechanisms of ERLTC. Nevertheless, this study is limited to synopticscale analyses and more detailed processes; in particular,mesoscale, convective, and microphysical processes during the ERLTC have not been investigated as a result of the coarse resolution of the data. We are planning numerical experiments to explore this further in future studies.

    This work was supported by the National Science Foundation of China (Grant Nos. 41775048,42030611), National Basic Research Program of China (Grant No.2015CB452804), the Open Grants of the State Key Laboratory of Severe Weather (Grant No. 2020LASW-B06). The authors thank Dr. Fumin REN for providing the TC-induced OSAT precipitation dataset over China in this study. The best-track data is from http://tcdata.typhoon.org.cn and the NCEP/NCAR reanalysis data is from https://rda.ucar.edu/datasets/. The authors are grateful to the editor and the three anonymous reviewers for providing insightful comments that significantly improved the quality of this paper.

    两个人的视频大全免费| 成人欧美大片| 白带黄色成豆腐渣| 97人妻精品一区二区三区麻豆| 一边亲一边摸免费视频| 69人妻影院| 肉色欧美久久久久久久蜜桃 | eeuss影院久久| av在线天堂中文字幕| 久久久久网色| 成人欧美大片| 国产亚洲5aaaaa淫片| 国产成年人精品一区二区| 午夜福利在线观看吧| 特大巨黑吊av在线直播| 不卡视频在线观看欧美| 亚洲国产精品sss在线观看| 淫秽高清视频在线观看| 精品人妻熟女av久视频| 精品一区二区三卡| 日韩av不卡免费在线播放| 亚洲av.av天堂| 美女内射精品一级片tv| 亚洲精品乱码久久久v下载方式| 啦啦啦韩国在线观看视频| 岛国毛片在线播放| 波野结衣二区三区在线| 黄色一级大片看看| 久久热精品热| 亚洲美女视频黄频| 亚洲av电影在线观看一区二区三区 | 91狼人影院| 日本-黄色视频高清免费观看| 国产精品福利在线免费观看| 久久久久久伊人网av| 99久久中文字幕三级久久日本| 丰满乱子伦码专区| 亚洲精品成人av观看孕妇| 午夜免费观看性视频| 午夜福利网站1000一区二区三区| 国产精品三级大全| 国产精品一二三区在线看| 国产精品人妻久久久久久| 国产乱人视频| 偷拍熟女少妇极品色| 久久精品国产亚洲网站| 久久久欧美国产精品| 国产爱豆传媒在线观看| 成人漫画全彩无遮挡| 麻豆精品久久久久久蜜桃| 国产午夜精品一二区理论片| 国产黄频视频在线观看| 在线观看免费高清a一片| 亚洲精品国产av蜜桃| 免费大片黄手机在线观看| 只有这里有精品99| 亚洲av男天堂| 噜噜噜噜噜久久久久久91| 久久精品综合一区二区三区| 日本猛色少妇xxxxx猛交久久| 2018国产大陆天天弄谢| 高清日韩中文字幕在线| 日韩av免费高清视频| 观看美女的网站| 精品久久久精品久久久| 丝瓜视频免费看黄片| 色综合色国产| 亚洲国产av新网站| 男人爽女人下面视频在线观看| 精品一区二区三卡| 亚洲自拍偷在线| 欧美性猛交╳xxx乱大交人| videossex国产| av在线天堂中文字幕| 波野结衣二区三区在线| 亚洲av日韩在线播放| 成人国产麻豆网| 激情五月婷婷亚洲| 国产免费视频播放在线视频 | 日韩欧美国产在线观看| 精品久久久久久久久久久久久| 天堂网av新在线| 中文字幕人妻熟人妻熟丝袜美| 免费少妇av软件| 18+在线观看网站| 免费看光身美女| 老司机影院毛片| 免费av不卡在线播放| 午夜福利高清视频| 日本色播在线视频| 一级片'在线观看视频| 午夜福利视频精品| 久久精品夜色国产| 精品酒店卫生间| 免费播放大片免费观看视频在线观看| 99久久精品国产国产毛片| 精品久久久噜噜| 亚洲精品aⅴ在线观看| 激情五月婷婷亚洲| 国产91av在线免费观看| 纵有疾风起免费观看全集完整版 | 亚洲图色成人| ponron亚洲| 听说在线观看完整版免费高清| 成人鲁丝片一二三区免费| 亚洲欧美日韩东京热| 欧美bdsm另类| 在线 av 中文字幕| 麻豆成人av视频| 日韩伦理黄色片| 亚洲国产最新在线播放| 成人综合一区亚洲| 国产 一区精品| 亚洲欧美日韩卡通动漫| 精品一区二区三卡| 91av网一区二区| 日韩av在线大香蕉| 日韩电影二区| 亚洲精品成人久久久久久| 午夜福利视频精品| 真实男女啪啪啪动态图| 国产亚洲5aaaaa淫片| 一区二区三区四区激情视频| 黄色欧美视频在线观看| 男人舔奶头视频| 18禁在线播放成人免费| 久久久色成人| 国产伦理片在线播放av一区| 精品国产三级普通话版| 午夜爱爱视频在线播放| 高清视频免费观看一区二区 | 欧美一级a爱片免费观看看| 中文字幕av成人在线电影| 激情 狠狠 欧美| 亚洲av电影不卡..在线观看| ponron亚洲| 青青草视频在线视频观看| 女的被弄到高潮叫床怎么办| 国内精品美女久久久久久| 一级毛片电影观看| 亚洲精品中文字幕在线视频 | 一级毛片久久久久久久久女| 国产日韩欧美在线精品| 免费高清在线观看视频在线观看| 能在线免费看毛片的网站| 中文字幕久久专区| 蜜臀久久99精品久久宅男| av一本久久久久| 亚洲精品日本国产第一区| 亚洲人成网站在线播| 久99久视频精品免费| 丰满少妇做爰视频| 亚洲欧美一区二区三区国产| 国产一区有黄有色的免费视频 | ponron亚洲| 亚洲国产精品专区欧美| 97在线视频观看| 最近手机中文字幕大全| 午夜精品国产一区二区电影 | 精品亚洲乱码少妇综合久久| 久久久久免费精品人妻一区二区| 人体艺术视频欧美日本| 国产黄频视频在线观看| 爱豆传媒免费全集在线观看| 亚洲国产精品成人综合色| 久久精品夜色国产| 日本一本二区三区精品| 亚洲丝袜综合中文字幕| 人体艺术视频欧美日本| 美女主播在线视频| 国产精品爽爽va在线观看网站| 国产淫片久久久久久久久| 国产成人精品一,二区| 91久久精品电影网| 黑人高潮一二区| 毛片女人毛片| 丝袜喷水一区| 三级国产精品欧美在线观看| 最近最新中文字幕免费大全7| 91精品伊人久久大香线蕉| 少妇丰满av| 亚洲精品日韩在线中文字幕| 亚洲自偷自拍三级| 最后的刺客免费高清国语| 亚洲精品国产av蜜桃| 免费无遮挡裸体视频| 亚洲伊人久久精品综合| 久久国内精品自在自线图片| 少妇裸体淫交视频免费看高清| 欧美 日韩 精品 国产| 久久鲁丝午夜福利片| 亚洲成人精品中文字幕电影| 噜噜噜噜噜久久久久久91| 国产精品精品国产色婷婷| 国产69精品久久久久777片| 人人妻人人看人人澡| 亚洲精品久久久久久婷婷小说| 亚洲av成人av| 男插女下体视频免费在线播放| 久久久久久久亚洲中文字幕| 国产午夜福利久久久久久| 欧美另类一区| 青春草国产在线视频| 色5月婷婷丁香| 免费播放大片免费观看视频在线观看| 成人午夜高清在线视频| av一本久久久久| 日韩亚洲欧美综合| 真实男女啪啪啪动态图| 精品熟女少妇av免费看| 2021天堂中文幕一二区在线观| 欧美性猛交╳xxx乱大交人| 51国产日韩欧美| 国产色爽女视频免费观看| 黄色配什么色好看| 色吧在线观看| 亚洲精品国产av成人精品| 国产久久久一区二区三区| 最近中文字幕2019免费版| 亚洲丝袜综合中文字幕| 永久网站在线| 国产欧美另类精品又又久久亚洲欧美| 日本爱情动作片www.在线观看| 床上黄色一级片| 狂野欧美白嫩少妇大欣赏| 看免费成人av毛片| 久久久久久久久大av| 日韩亚洲欧美综合| 麻豆成人av视频| 亚洲精品乱码久久久v下载方式| 麻豆成人av视频| 婷婷六月久久综合丁香| 欧美一区二区亚洲| av线在线观看网站| 欧美激情国产日韩精品一区| 亚洲成人精品中文字幕电影| 亚洲欧美日韩卡通动漫| 午夜精品国产一区二区电影 | 亚洲人成网站在线播| 美女脱内裤让男人舔精品视频| 国产精品国产三级国产av玫瑰| 三级毛片av免费| 91狼人影院| 国产 一区精品| 看非洲黑人一级黄片| 看非洲黑人一级黄片| 69人妻影院| 女的被弄到高潮叫床怎么办| 99re6热这里在线精品视频| 秋霞在线观看毛片| 97超碰精品成人国产| 国内少妇人妻偷人精品xxx网站| 国产黄a三级三级三级人| 麻豆成人午夜福利视频| 十八禁国产超污无遮挡网站| 99视频精品全部免费 在线| 国产精品一及| 嫩草影院精品99| 亚洲自偷自拍三级| 国产在视频线精品| 日韩视频在线欧美| 亚洲精品亚洲一区二区| 欧美性感艳星| 欧美极品一区二区三区四区| 欧美日韩综合久久久久久| 国产男人的电影天堂91| 国产中年淑女户外野战色| 国产伦在线观看视频一区| 男人舔女人下体高潮全视频| 一区二区三区乱码不卡18| 成年女人在线观看亚洲视频 | 久久久久久九九精品二区国产| 最近视频中文字幕2019在线8| 91精品国产九色| 亚洲成色77777| 中文精品一卡2卡3卡4更新| 国产成人aa在线观看| 91狼人影院| 菩萨蛮人人尽说江南好唐韦庄| 男插女下体视频免费在线播放| 国产欧美日韩精品一区二区| av播播在线观看一区| 六月丁香七月| 国产探花在线观看一区二区| 自拍偷自拍亚洲精品老妇| 色播亚洲综合网| 一级爰片在线观看| 久久99精品国语久久久| 卡戴珊不雅视频在线播放| 老师上课跳d突然被开到最大视频| 1000部很黄的大片| 偷拍熟女少妇极品色| 久久国产乱子免费精品| 国产高清国产精品国产三级 | 亚洲电影在线观看av| 日韩制服骚丝袜av| 成年人午夜在线观看视频 | eeuss影院久久| 亚洲va在线va天堂va国产| 啦啦啦韩国在线观看视频| 国产精品福利在线免费观看| 国产精品久久久久久av不卡| 国产成人a区在线观看| 汤姆久久久久久久影院中文字幕 | 老师上课跳d突然被开到最大视频| 国产精品综合久久久久久久免费| 18禁在线播放成人免费| 精品人妻一区二区三区麻豆| 国产黄色免费在线视频| 少妇猛男粗大的猛烈进出视频 | 日韩一区二区视频免费看| 黄片无遮挡物在线观看| 一区二区三区乱码不卡18| 亚洲在线观看片| freevideosex欧美| 欧美zozozo另类| 九九爱精品视频在线观看| 欧美三级亚洲精品| 丰满乱子伦码专区| 亚洲av电影不卡..在线观看| 国产精品一区二区性色av| 嫩草影院新地址| 久久久久久久亚洲中文字幕| 亚洲美女视频黄频| 免费黄网站久久成人精品| 哪个播放器可以免费观看大片| 免费在线观看成人毛片| 国产三级在线视频| 欧美3d第一页| 亚洲熟女精品中文字幕| 免费看日本二区| 街头女战士在线观看网站| 国产麻豆成人av免费视频| 99视频精品全部免费 在线| 午夜亚洲福利在线播放| av黄色大香蕉| 欧美精品一区二区大全| 青青草视频在线视频观看| av黄色大香蕉| 黄片无遮挡物在线观看| 午夜老司机福利剧场| 国产成人午夜福利电影在线观看| 亚洲欧美精品专区久久| 六月丁香七月| 免费av观看视频| 亚洲伊人久久精品综合| 国产黄色视频一区二区在线观看| 国产精品精品国产色婷婷| av黄色大香蕉| 日韩av在线免费看完整版不卡| 永久网站在线| 国产欧美另类精品又又久久亚洲欧美| 国产乱来视频区| 人人妻人人澡人人爽人人夜夜 | 国产综合精华液| 亚洲av成人精品一区久久| 日本色播在线视频| 少妇人妻精品综合一区二区| 久久久久久久久久久免费av| 久久久精品94久久精品| 汤姆久久久久久久影院中文字幕 | 男人狂女人下面高潮的视频| 夫妻性生交免费视频一级片| 2018国产大陆天天弄谢| av女优亚洲男人天堂| 人妻少妇偷人精品九色| 伦理电影大哥的女人| 国产精品一及| 成人性生交大片免费视频hd| www.av在线官网国产| 2018国产大陆天天弄谢| 极品教师在线视频| 久久热精品热| 精品久久国产蜜桃| 一级av片app| 成年女人看的毛片在线观看| 国产精品爽爽va在线观看网站| 如何舔出高潮| 国产高潮美女av| 国产精品久久久久久av不卡| 91精品一卡2卡3卡4卡| 久久久久久伊人网av| 亚洲欧美一区二区三区国产| 黄色日韩在线| 少妇猛男粗大的猛烈进出视频 | 久久热精品热| 成年免费大片在线观看| 久久精品久久久久久噜噜老黄| 麻豆成人午夜福利视频| 亚洲精品日韩在线中文字幕| 最近的中文字幕免费完整| 午夜日本视频在线| 天堂俺去俺来也www色官网 | 熟女人妻精品中文字幕| 男女啪啪激烈高潮av片| 啦啦啦啦在线视频资源| 国内揄拍国产精品人妻在线| 国产综合懂色| 精品久久久久久久久av| 日韩在线高清观看一区二区三区| 最近中文字幕高清免费大全6| 少妇高潮的动态图| 午夜免费激情av| 国内精品美女久久久久久| 人妻少妇偷人精品九色| 国产三级在线视频| 99热这里只有精品一区| 久久久久久久久久黄片| 久久这里有精品视频免费| 男女国产视频网站| 国产成人freesex在线| 女人十人毛片免费观看3o分钟| 国产精品.久久久| 欧美成人一区二区免费高清观看| 身体一侧抽搐| 国产乱来视频区| 国产 一区精品| 蜜桃久久精品国产亚洲av| 久久精品久久久久久噜噜老黄| 久久久久久久久久久丰满| 97超视频在线观看视频| 波多野结衣巨乳人妻| av在线天堂中文字幕| 天天一区二区日本电影三级| 午夜老司机福利剧场| 寂寞人妻少妇视频99o| 亚洲欧美一区二区三区国产| 日产精品乱码卡一卡2卡三| 国产麻豆成人av免费视频| 一区二区三区高清视频在线| 舔av片在线| av卡一久久| 国产探花极品一区二区| 少妇的逼好多水| 尤物成人国产欧美一区二区三区| eeuss影院久久| 国产黄色视频一区二区在线观看| 三级男女做爰猛烈吃奶摸视频| 一夜夜www| 特级一级黄色大片| 国产视频首页在线观看| 国产成人精品一,二区| 国产成人91sexporn| 国产亚洲一区二区精品| 国产毛片a区久久久久| 国产欧美另类精品又又久久亚洲欧美| 中文字幕免费在线视频6| 亚洲精品乱码久久久久久按摩| av国产久精品久网站免费入址| 中文字幕久久专区| 日韩av不卡免费在线播放| 日韩成人av中文字幕在线观看| 国产大屁股一区二区在线视频| 全区人妻精品视频| 搡老妇女老女人老熟妇| 午夜免费男女啪啪视频观看| 七月丁香在线播放| 成人亚洲精品av一区二区| 久久国产乱子免费精品| 麻豆av噜噜一区二区三区| 一区二区三区高清视频在线| 丰满少妇做爰视频| h日本视频在线播放| 久久精品久久精品一区二区三区| 97在线视频观看| 在线观看人妻少妇| 免费不卡的大黄色大毛片视频在线观看 | 亚洲精品国产av蜜桃| 国产 一区精品| 日韩 亚洲 欧美在线| 成年女人看的毛片在线观看| 欧美日韩国产mv在线观看视频 | 日韩 亚洲 欧美在线| 边亲边吃奶的免费视频| 男人和女人高潮做爰伦理| 九九在线视频观看精品| 丰满少妇做爰视频| 久久热精品热| 成人亚洲精品av一区二区| 日韩欧美三级三区| 91精品一卡2卡3卡4卡| 亚洲aⅴ乱码一区二区在线播放| 国产亚洲av片在线观看秒播厂 | 国产 一区 欧美 日韩| 97在线视频观看| 免费av观看视频| 卡戴珊不雅视频在线播放| 天堂中文最新版在线下载 | 久久精品国产亚洲av天美| 丰满人妻一区二区三区视频av| a级一级毛片免费在线观看| 欧美日韩视频高清一区二区三区二| 欧美最新免费一区二区三区| 久久久久网色| av国产免费在线观看| 国产高清三级在线| 欧美一区二区亚洲| 美女脱内裤让男人舔精品视频| 午夜精品在线福利| 大话2 男鬼变身卡| 亚洲最大成人手机在线| xxx大片免费视频| 国产片特级美女逼逼视频| 免费观看av网站的网址| 成人无遮挡网站| .国产精品久久| 午夜福利在线观看吧| 夫妻性生交免费视频一级片| 国产成人aa在线观看| eeuss影院久久| 午夜精品一区二区三区免费看| 免费大片18禁| 夜夜看夜夜爽夜夜摸| a级毛色黄片| 国产成人91sexporn| 国产午夜精品一二区理论片| 六月丁香七月| 91午夜精品亚洲一区二区三区| 亚洲人成网站在线播| 床上黄色一级片| 久久久久国产网址| 成人av在线播放网站| eeuss影院久久| 亚洲三级黄色毛片| 成人午夜高清在线视频| 国产高潮美女av| 中文字幕亚洲精品专区| 久久久国产一区二区| 久久久久国产网址| 亚洲欧美中文字幕日韩二区| 3wmmmm亚洲av在线观看| 亚洲丝袜综合中文字幕| 少妇猛男粗大的猛烈进出视频 | 少妇人妻一区二区三区视频| 国产 一区 欧美 日韩| 成人漫画全彩无遮挡| 免费av不卡在线播放| 亚洲精品第二区| 搡女人真爽免费视频火全软件| 成人欧美大片| 毛片一级片免费看久久久久| 亚洲精品自拍成人| 又爽又黄a免费视频| 乱人视频在线观看| 欧美区成人在线视频| 日韩一区二区三区影片| 丰满人妻一区二区三区视频av| 人妻一区二区av| 毛片女人毛片| 欧美日韩精品成人综合77777| 久久久a久久爽久久v久久| 亚洲av一区综合| 免费观看av网站的网址| 99久国产av精品| 国产成人福利小说| 99久久九九国产精品国产免费| 精品一区二区三区视频在线| 久久精品久久久久久噜噜老黄| 日韩欧美一区视频在线观看 | 国内精品美女久久久久久| 99久国产av精品| 床上黄色一级片| h日本视频在线播放| 午夜激情福利司机影院| 一级毛片 在线播放| 国产在线男女| 能在线免费看毛片的网站| freevideosex欧美| 十八禁国产超污无遮挡网站| 啦啦啦中文免费视频观看日本| 成人毛片a级毛片在线播放| 丝瓜视频免费看黄片| 成人特级av手机在线观看| 国产高清不卡午夜福利| 久久精品久久久久久久性| 国产精品一区二区三区四区久久| 大香蕉久久网| 99热6这里只有精品| 国产精品国产三级国产av玫瑰| 一个人看视频在线观看www免费| 亚洲国产色片| 久久99热这里只有精品18| 色5月婷婷丁香| 国产老妇伦熟女老妇高清| 亚洲美女视频黄频| 亚洲无线观看免费| 男人爽女人下面视频在线观看| 亚洲美女视频黄频| 人妻一区二区av| av女优亚洲男人天堂| 99久久精品热视频| 国产精品99久久久久久久久| 亚洲欧美中文字幕日韩二区| 亚洲国产精品专区欧美| 亚洲在久久综合| 熟女人妻精品中文字幕| 高清日韩中文字幕在线| 亚洲欧美日韩东京热| 午夜激情欧美在线| 国产成年人精品一区二区| 黄色配什么色好看| 久久精品国产亚洲网站| 欧美精品国产亚洲| av天堂中文字幕网| 成人二区视频| 丰满乱子伦码专区| 国产午夜福利久久久久久| 内地一区二区视频在线| 国产精品女同一区二区软件| 国产精品一区二区性色av| 直男gayav资源| 国产黄色小视频在线观看| 一区二区三区高清视频在线| 天堂影院成人在线观看| 啦啦啦中文免费视频观看日本|