• <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 ?

    Distinctive MJO Activity during the Boreal Winter of the 2015/16 Super El Ni?o in Comparison with Other Super El Ni?o Events

    2021-04-07 10:20:50XubenLEIWenjunZHANGPangChiHSUandChaoLIU
    Advances in Atmospheric Sciences 2021年4期

    Xuben LEI,Wenjun ZHANG,Pang-Chi HSU,and Chao LIU

    Key Laboratory of Meteorological Disaster, Ministry of Education/Joint International Research Laboratory of Climate and Environmental Change/Collaborative Innovation Center on Forecast and Evaluation of Meteorological Disasters, Nanjing University of Information Science &Technology, Nanjing 210044, China

    ABSTRACT Many previous studies have demonstrated that the boreal winters of super El Ni?o events are usually accompanied by severely suppressed Madden-Julian oscillation (MJO) activity over the western Pacific due to strong descending motion associated with a weakened Walker Circulation.However,the boreal winter of the 2015/16 super El Ni?o event is concurrent with enhanced MJO activity over the western Pacific despite its sea surface temperature anomaly (SSTA)magnitude over the Ni?o 3.4 region being comparable to the SSTA magnitudes of the two former super El Ni?o events (i.e.,1982/83 and 1997/98).This study suggests that the MJO enhanced over western Pacific during the 2015/16 super El Ni?o event is mainly related to its distinctive SSTA structure and associated background thermodynamic conditions.In comparison with the previous super El Ni?o events,the warming SSTA center of the 2015/16 super El Ni?o is located further westward,and a strong cold SSTA is not detected in the western Pacific.Accordingly,the low-level moisture and air temperature (as well as the moist static energy,MSE) tend to increase in the central-western Pacific.In contrast,the low-level moisture and MSE show negative anomalies over the western Pacific during the previous super El Ni?o events.As the MJO-related horizontal wind anomalies contribute to the further westward warm SST-induced positive moisture and MSE anomalies over the western tropical Pacific in the boreal winter of 2015/16,stronger moisture convergence and MSE advection are generated over the western Pacific and lead to the enhancement of MJO convection.

    Key words:super El Ni?o,Madden-Julian oscillation,moisture diagnosis

    1.Introduction

    The Madden-Julian oscillation (MJO,Madden and Julian,1971) is the most significant mode of atmospheric intraseasonal variability over the tropics.The MJO usually initiates over the western Indian Ocean,slowly propagates eastward through the Maritime Continent to the central Pacific,and dissipates near the dateline (Madden and Julian,1972).MJO-related circulations/convection and heating anomalies can influence various weather events and climate variability,such as tropical cyclone activity (Liebmann et al.,1994;Camargo et al.,2009),monsoons (Yasunari,1979;Li et al.,2018),mid-latitude storm tracks (Zheng et al.,2018),and the North Atlantic oscillation (Cassou,2008).

    Significant progress has been made over the past few decades in revealing the basic features and underlying physical mechanisms of the MJO (e.g.,Weickmann et al.,1985;Ferranti et al.,1990;Sperber,2003;Kiladis et al.,2005).Previous studies have emphasized the importance of moisture processes and associated moist static energy (MSE) in the initiation,propagation,and intensity of the MJO (Kemball-Cook and Weare,2001;Maloney,2009;Andersen and Kuang,2012;Adames and Wallace,2014;Pritchard and Bretherton,2014).For example,the horizontal transportation of moisture/MSE plays a crucial role in both the initiation (Zhao et al.,2013;Maloney and Wolding,2015) and development (Andersen and Kuang,2012;Adames and Wallace,2014) of MJO-related convection.The low-level moistening ahead of the MJO convection results in a relatively unstable stratification that favors the eastward development of the deep convection (Hsu and Li,2012;Kim et al.,2014).

    The El Ni?o—Southern Oscillation (ENSO) is the most dominant coupled ocean—atmosphere phenomenon on the interannual timescale.Numerous studies have demonstrated its significant influences on global climate,mostly through so-called atmospheric bridge mechanisms (e.g.,Bjerknes,1969;Wallace et al.,1998;Alexander et al.,2002;Lau and Nath,2006;Zhang et al.,2015).The relationship of ENSO with the MJO has also been largely documented.Observations show that El Ni?o events are usually accompanied by active and continuous eastward-propagating MJO events (Kessler et al.,1995;Zhang and Gottschalck,2002;Zavala-Garay et al.,2005).In the spring and summer of years with developing El Ni?o events,the intraseasonal zonal westerly winds associated with the active MJO can force an eastward extension of the tropical Pacific warm pool edge,and thus contribute to warming sea surface temperature (SST) anomalies (SSTAs) in the central to eastern tropical Pacific (Vecchi and Harrison,2000;Hendon et al.,2007;Tang and Yu,2008).

    El Ni?o is also able to influence initiation,intensity,propagation,and other basic characteristics of the MJO by modulating the SST distribution (Kim et al.,2010;Kapur and Zhang,2012;Wang et al.,2019).During the mature and decaying phases of El Ni?o,MJO intensity is normally weakened in the western tropical Pacific (Chen et al.,2015).The frequency of intraseasonal oscillation is higher over the western Pacific,and mainly characterized by northwestward propagation during decaying El Ni?o events in summer (Liu et al.,2016a).Correspondingly,the eastward propagation of the MJO is also weakened at the equator(Lin and Li,2008).Roughly opposite responses of the MJO can be found for La Ni?a events.In recent years,another type of El Ni?o event has occurred much more frequently with a maximum SSTA center located in the central Pacific(CP) (Larkin and Harrison,2005;Ashok et al.,2009;Kao and Yu,2009;Kug et al.,2009;Ren and Jin,2011;Zhang et al.,2014).In contrast to traditional El Ni?o events,the CP El Ni?o is usually accompanied by enhanced MJO activity and further eastward propagation during its mature and decaying phases (e.g.,Gushchina and Dewitte,2012;Feng et al.,2015;Chen et al.,2016;Hsu and Xiao,2017).

    Among El Ni?o events,so-called super El Ni?o events have extremely warm SSTAs in the tropical Pacific and are of considerable public concern since they can lead to more severe global catastrophic disasters compared to normal El Ni?o events (Smith et al.,1999;Zhang et al.,2016;Geng et al.,2017).Since the late 1970s when satellite observation began,three super El Ni?o events (i.e.,1982/83,1997/98,and 2015/16) have been well-observed.These three events share similar characteristics in terms of evolution and intensity,and exhibit similar MJO-associated westerly wind anomalies during their development stages (McPhaden,1999;Levine and McPhaden,2016;Chen et al.,2017).However,the 2015/16 super El Ni?o event does exhibit some unique characteristics and climate impacts compared to the two prior super El Ni?o events (Jacox et al.,2016;L’Heureux et al.,2017;Paek et al.,2017;Lyu et al.,2018).Considering the different oceanic/atmospheric features of the 2015/16 super El Ni?o event,some MJO features during its mature phase may also differ from the other two super El Ni?o events.We observe that the 2015/16 super El Ni?o event coincides with enhanced MJO activity over the western Pacific,which is very different from the previous super El Ni?o events.This observation deserves further investigation in order to understand the possible reasons for this uniqueness during the boreal winter of the 2015/16 super El Ni?o event.

    In this study,we analyze the differences in MJO activity of the 2015/16 super El Ni?o event compared to the previous two super El Ni?o events.Possible physical reasons for the unique MJO feature of the 2015/16 super El Ni?o event are further investigated based on the diagnoses of moisture and MSE budget equations.First,the data and methodology used in this study are described in section 2.Then,the distinct MJO feature associated with the 2015/16 super El Ni?o event is displayed through inter-comparison with the other two super El Ni?o events in section 3.Possible reasons for the unique MJO activity during the 2015/16 El Ni?o are examined in section 4.Finally,conclusions and discussions are summarized in section 5.

    2.Data and methodology

    2.1.Datasets

    In this study,daily mean outgoing longwave radiation data (OLR,Liebmann and Smith,1996) and monthly global gridded precipitation data (Xie and Arkin,1997) with horizontal resolution of 2.5° × 2.5° from the National Oceanic and Atmospheric Administration (NOAA) are used to identify convective activity at the intraseasonal and interannual timescales,respectively.Monthly SST data with horizontal resolution of 1° × 1° is obtained from the Hadley Centre Sea Ice and Sea Surface Temperature datasets(HadISST1;Rayner et al.,2003).To understand the physical processes related to MJO development,the three-dimensional dynamic and thermodynamic fields,including daily averaged horizontal winds,vertical pressure velocity,air temperature,specific humidity,and geopotential height,are collected from the European Centre for Medium-Range Weather Forecasts (ECMWF) interim reanalysis (ERAInterim,Dee et al.,2011).The sensible heat flux (SHF),latent heat flux (LHF),and longwave (LW) and shortwave(SW) radiation fluxes at the bottom and top of the atmosphere from the ERA-Interim reanalysis are also used.The horizontal resolution of all ERA-Interim datasets is 1.5° ×1.5°.We also use the all-season real-time multivariate MJO(RMM) index (Wheeler and Hendon,2004;http://www.bom.gov.au/climate/mjo/graphics/rmm.74toRealtime.txt) to examine the MJO amplitude over the tropics.

    2.2.Methodology

    To extract the MJO-associated intraseasonal variability(30—90 days),a 201-point Lanczos bandpass filter is used(Duchon,1979).The monthly mean amplitude of the MJO is measured as the square root of the filtered OLR variance within a 3-month running window centered on that calendar month (Hendon et al.,2007).Ni?o3.4 index is used for defining a super El Ni?o event as the intensity of El Ni?o,which is calculated by the standardized area-averaged SSTA in the Ni?o3.4 region (5°S—5°N,120°—170°W),and the Ni?o3.4 index during the mature phase of super El Ni?o events is usually above the 2 standard deviations.Anomalies were calculated as the departures from the climatological average over the entire study period (1979—2018).The monthly RMM amplitude is calculated by following steps:first calculate the 90 days running averaged of daily RMM amplitude [(RMM1+RMM2)],and then calculate the monthly mean RMM amplitude of every single month.

    Column-integrated MSE and low-level moisture are important factors for the development and maintenance of the MJO (Maloney,2009;Hsu and Li,2012;Sobel and Maloney,2013;Adames and Wallace,2014;Kim et al.,2014).The moisture and MSE budget terms are diagnosed to understand the key processes contributing to the distinct MJO activity in the boreal winter of 2015/16.The moisture budget equation at the intraseasonal timescale is based on Eq.(1) (Yanai et al.,1973):

    where

    q

    is the specific humidity,and

    V

    and ω represent horizontal wind and vertical pressure velocity,respectively.

    Q

    and

    L

    denote the apparent moisture sink and latent heat of condensation,and Q/L is regarded as a residual of the moisture budget.Prime notation indicates the intraseasonal(30—90 day) component.Here,the vertical integral of Eq.(1) is calculated from 1000 hPa to 700 hPa,considering that low-level moisture plays a key role in development of the MJO.

    The MSE budget at intraseasonal timescales is defined by Eq.(2) (Neelin and Held,1987):

    where

    m

    denotes MSE,defined by

    m

    =

    CT

    +

    Lq

    +

    gz

    ,and

    C

    is the heat capacity of dry air at constant pressure (1004 J Kkg),

    L

    is the specific latent heat for a unit substance(2.5 × 10J kg),

    g

    is the gravitational constant (9.8 m s),and

    z

    is geopotential height.The left-hand term and first two terms of the right-hand side of Eq.(2) are vertically integrated from 1000 hPa to 100 hPa.The net heat flux terms are calculated as the differences between the top and surface level of the atmosphere.

    3.Distinct MJO activity during the 2015/16 super El Ni?o

    Fig.1.(a) Time evolutions of the Ni?o3.4 index (°C) for 1982/83 (red),1997/98 (orange) and 2015/16 (blue) events relative to the climatological state in 1979—2018.Notation of 0 (1) in parentheses on the x-axis represents the El Ni?o developing (decaying) year.(b) Anomalies of monthly RMM index amplitude in the boreal winters of three super El Ni?o events.

    Figure 1 a shows the Ni?o3.4 index evolutions for the three super El Ni?o events.With the exception of some differences at the developing and decaying stages,the general evolutions and magnitudes are quite similar for these three events.The magnitude of the 2015/16 super El Ni?o event is slightly larger,relative to the other two super El Ni?o events during their respective peak seasons.To display the MJO intensity during each of the three super El Ni?o events,the amplitudes of the RMM index during their boreal winters (during which the MJO and ENSO signals are the most vigorous) are shown in Fig.1b.Consistent with previous studies (e.g.,Gushchina and Dewitte,2012;Chen et al.,2016;Wang et al.,2018),overall MJO activity is strongly suppressed during boreal winters of the 1982/83 and 1997/98 super El Ni?o events.In contrast,the 2015/16 super El Ni?o event exhibits a very different MJO response with enhanced MJO activity during boreal winter.From the phase space diagram of the MJO (Fig.2a) during boreal winters of the three super El Ni?o events,the eastward propagation of the MJO during 2015/16 is clearly more robust and of obviously higher amplitude over the Maritime Continent compared to the central-western Pacific area.In contrast,the MJO intensity over the Indian Ocean (phases 1—3) is nearly comparable for the three super El Ni?o events.The monthly averaged RMM amplitude anomalies (Fig.1b) represents the overall states of the MJO in the equatorial region for each of the three super El Ni?o events.To reveal the geographical distribution of MJO activity and quantify the contributions of frequency effect and magnitude effect to the distinct MJO enhancement during 2015/16,we compare the frequency of active MJO days (RMM amplitude greater than 1) and the averaged amplitude for each phase during boreal winters between the three super El Ni?o events (Figs.2b and 2c).Instances of an active MJO were more frequent in phases 4—7 (especially phase 4) during the boreal winter of 2015/16,while they were less frequent in other phases(phases 1—3 and 8) when compared to the boreal winters of 1982/83 and 1997/98 (Fig.2b).The active MJO over the Maritime Continent and Pacific area (phases 4—8) also had a stronger amplitude during 2015/16 than during the previous two events (Fig.2c).Thus,the most significant enhancement of MJO activity during 2015/16 occurred over the Maritime Continent to western Pacific (phases 5—8),where the MJO was more active in terms of amplitude and frequency.

    Fig.2.(a) MJO phase space diagrams for the boreal winters of 1982/83 (red),1997/98 (yellow),and 2015/16 (blue).(b) The frequency of each MJO phase during the boreal winters of 1982/83,1997/98,and 2015/16.(c) Same as (b)but for the MJO intensity.

    To clearly identify the key region with significant MJO changes associated with super El Ni?o events,Figure 3 shows the spatial patterns of the MJO-related (30—90 day filtered) convection variability.For the 1982/83 and 1997/98 super El Ni?o events,the MJO intensity is significantly suppressed over most of the tropical Indo-Pacific region (Figs.3a,b).A slightly weakened MJO can also be seen in the tropical Indian Ocean during the boreal winter of the 2015/16 super El Ni?o,while the MJO is remarkably strengthened over the Maritime Continent and the tropical western Pacific of the Southern Hemisphere (Fig.3c),which is consistent with the results shown in Fig.2.The enhanced MJO activity during the 2015/16 super El Ni?o event experienced a maximum over the western Pacific near 10°S,which is climatologically the region with the most vigorous MJO activity.Previous studies have also found similar intraseasonal variability with this enhanced activity (Liu et al.,2016b).The unique change in MJO amplitude during boreal winter of the 2015/16 super El Ni?o event can also be clearly seen when the difference is taken between it and the previous two super El Ni?o events (Figs.3d—f).The remarkable enhancement of MJO intensity during the 2015/16 super El Ni?o event is observed more consistently over the tropical western Pacific (green boxes in Fig.3,120°—170°E,5°—15°S) relative to the 1982/83 super El Ni?o event (Fig.3d),the 1997/98 super El Ni?o event (Fig.3e),and their average (Fig.3f).This region will be our focus since the largest difference appears here.

    Considering modulation of the background oceanic-atmospheric conditions on MJO activity,Figure 4 displays anomalous SST and precipitation patterns associated with the boreal winters of three super El Ni?o events.All three events are characterized by extremely warm SSTAs and above average precipitation over the central to eastern tropical Pacific.Compared to the previous two super El Ni?o events,the warm SSTA center is clearly displaced westward by about 20 degrees of longitude for the 2015/16 super El Ni?o event (Figs.4a—c).This observation is further supported by the SSTA difference between the 2015/16 case and the average of the other two cases (Fig.4d).Figure 4d also shows that the precipitation anomalies are stronger in the central Pacific and weaker in the eastern Pacific during the 2015/16 boreal winter compared to the other two cases.In the western Pacific,negative SSTAs and reduced precipitation are evident for the boreal winters of the 1982/83 and 1997/98 super El Ni?o events (Figs.4a,b).However,slightly negative SSTAs can be found in the western Pacific with very small negative precipitation anomalies during the boreal winter of 2015/16 (Fig.4c).These observations suggest that the distinct oceanic and atmospheric anomalies in the western Pacific during the boreal winter of the 2015/16 super El Ni?o event (Fig.4d) provide different background conditions for MJO activity and may possibly lead to unique MJO anomalies in contrast to the previous super El Ni?o events.The possible effects of the background conditions will be investigated in detail in the next section.

    4.Possible mechanisms responsible for enhanced MJO activity during the boreal winter of 2015/16

    Fig.3.Anomalous distributions of 30—90 d filtered OLR standard deviation (shading,W m—2) during the boreal winters of(a) 1982/83,(b) 1997/98,and (c) 2015/16,superimposed on the climatology (contours,W m—2).The corresponding differences between (d) 2015/16 minus 1982/83,(e) 2015/16 minus 1997/98,(f) 2015/16 minus the average of 1982/83 and 1997/98.

    Fig.4.Seasonal SST (shading,°C) and precipitation (contours,mm d—1) anomalies in the boreal winters of (a)1982/83,(b) 1997/98,and (c) 2015/16.(d) Their differences between 2015/16 and the average of 1997/98 and 1982/83.

    The development of MJO convection is closely linked with the low-level moisture and MSE since these factors are providing the favorable preconditioning for the convection.(Maloney,2009;Andersen and Kuang,2012;Hsu and Li,2012;Kim et al.,2014).We diagnose the low-level moisture budget,Eq.(1),and the column-integrated MSE budget,Eq.(2),over the western tropical Pacific (5°—15°S,120°—170°E,the green box in Fig.3) to investigate key processes causing unique MJO activity during the boreal winter of 2015/16.

    Composite OLR anomalies at the intraseasonal timescale are used to represent local MJO evolution in the western Pacific.Active MJO events were selected for the composite when the 30—90 day filtered OLR over the western Pacific was greater than 1 standard deviation.The date with the minimum 30—90 day OLR is defined as day 0.As shown in Fig.5a,the OLR anomalies change their signs from positive to negative around day -10,when the MJO convective signal initiates and develops.For low-level moisture,its maximum tendency also occurs around day -10,leading the MJO convection maximum by about 10 days (Fig.5b).The phase relationship between the MJO-related convection and moisture suggests an important effect of the leading low-level moisture accumulation on the growth of the MJO convection.Despite similar evolutions of MJO convection and moisture anomalies for all three super El Ni?o events,the amplitude of moisture tendency in the 2015/16 event is about twice as strong as those of the 1982/83 and 1997/98 events (Figs.5a,b).The enhanced moisture tendency is likely contributing to the strong amplitude of MJO convection in the 2015/16 event (Fig.5a) during its development stage (from day —10 to 0,when the OLR ranges from zero to its minimum).Focusing on the MJO development period,the moisture tendency is positive and the vertical moisture advection shows a large contribution.Although the horizontal moisture advection is in phase with the moisture tendency,it has a relatively small contribution compared to vertical advection and latent heating processes during the MJO development stage (Figs.5c—d).Note that the moisture begins discharging through apparent moisture sinking and latent heat of condensation when the MJO convection is established,which is represented as

    Q

    /

    L

    in Eq.(1) (Kemball-Cook and Weare,2001;Kiladis et al.,2005).

    Figure 6 further compares the moisture budget terms and the c ontributionsof scale interactions to the key processes during day ?10 to day 0,when MJO convection grows quickly.During the developing stage of MJO convection,the moisture tendency (?q/?t) of the 2015/16 event is much stronger thanthose of the 1982/83 and 1997/98 events,which comes mainly from vertical moisture advection,consistent with the results shown in Fig.5.According to the continuity equation,the vertical advection term (the second term on the right-hand side of Eq.(1)) can be further decomposed as follows:

    where the right-hand side terms represent horizontal moisture convergence and vertical moisture flux convergence,respectively.To elucidate the importance of scale interactions for vertical moisture advection,

    q

    and

    V

    are decomposed into low-frequency background state (LFBS,longer than 90 days),intraseasonal component (30—90 days),and higher-frequency disturbances (less than 30 days) as depicted in the following equation:

    The overbar,prime,and asterisk indicate LFBS,intraseasonal,and higher-frequency components,respectively.Based on this,the zonal moist convergence can be separated into 9 terms representing the interactions between different timescales:

    Fig.5.Composites of (a) 30—90 day filtered OLR anomaly (W m—2) averaged over the western Pacific region(120°—170°E,5°—15°S) with day 0 as the occurrence of maximum MJO OLR anomaly.The blue,orange and red lines represent MJO evolutions during the boreal winters of 2015/16,1997/98 and 1982/83,respectively.(b—e) Same as (a) except for column-integrated (1000—700 hPa) intraseasonal moisture budget terms (10—6 kg m—2 s—1) for (b)moisture tendency,(c) horizontal advection,(d) vertical advection,and (e) residual of the moisture budget.

    In addition to the preconditioning effect of low-level moisture,the positive MSE anomalies associated with the MJO are also argued to be important for the initiation and growth of MJO convection (e.g.,Maloney,2009;Andersen and Kuang,2012;Zhao et al.,2013;Maloney and Wolding,2015;Hsu and Xiao,2017).Although the MSE variability is dominated by the moisture change at the MJO timescale(Maloney,2009),its budget diagnosis,shown in Eq.(2),could provide additional insights about the effects of radiative heating and surface fluxes on the MJO evolution.We analyze the MSE evolution and its related physical processes for MJO initiation and development during the three super El Ni?o events.Figure 8 shows temporal evolutions of the MSE anomalies averaged over the western Pacific(5°—15°S,120°—170°E,green box in Fig.3).A positive MSE tendency is detected during the initiation and development stages of the MJO convection (Fig.8a),when the OLR anomaly shows a negative tendency from day —20 to 0(Fig.5a).For the 2015/16 super El Ni?o event,the MSE tendency is larger than the other two events during the MJO initiation and development stages,resulting in enhanced MSE given the same time period for MJO development (from day—20 to 0),corresponding to the much stronger MJO activity.Evolutions of each column-integrated MSE budget term are displayed in Fig.9 to inspect their respective contribution.The column-integrated MSE tendency (?m/?t)reaches the peak around day —10 (Fig.9a),consistent with the moisture tendency (Fig.5b).In comparison,the vertically integrated horizontal MSE advection resembles the phase evolution of the MSE tendency and can well explain the amplitude difference for the three events (Fig.9b),suggesting its important contribution to the differences in MJO activity.The column vertical MSE advection shifts its phase by about a quarter period respective to the MSE tendency and displays comparable amplitudes for the 1997/98 and 2015/16 events (Figs.9c).The surface turbulent fluxes (Figs.9d,e) and shortwave radiation (Fig.9g) seem to have a minor contribution to the different MSE tendency.The evolution of longwave radiation(Fig.9f) is in phase with the evolution of MJO convection.The amplitude of longwave radiation in the boreal winter of 2015/16 is larger than the other two events,indicating that the longwave radiation may maintain the stronger MJO convection in 2015/16 (Fig.9f).The role of longwave radiation in supporting the MJO convection was highlighted by previous studies (Andersen and Kuang,2012;Maloney and Wolding,2015;Hsu and Xiao,2017).

    Fig.6.Difference in lower troposphere (1000—700 hPa) column-integrated (a) intraseasonal moisture budget terms(10—6 kg m?2 s?1) and(b) individual decomposition terms of(V?q/?p)′ between the boreal winter of 2015/16 and the average of the boreal winters of 1982/83 and 1997/98 over the western tropical Pacific (120°—170°E,5°—15°S) from day —10 to day 0.

    Fig.7.Vertically averaged (1000—700 hPa) LFBS moisture (shading,g kg—1) and MJO-related horizontal wind(vectors,m s—1) anomalies for (a) 1982/83,(b) 1997/98,(c) 2015/16 and (d) difference between 2015/16 and the average of 1982/83 and 1997/98 from day —10 to day 0.The green boxes denotes the western tropical Pacific(5°—15°S,120°—170°E).

    Fig.8.Evolutions of intraseasonal MSE anomalies (kJ kg—1) over the western Pacific (120°—170°E,5°S—15°S) during the boreal winters of (a) 1982/83,(b) 1997/98,and (c) 2015/16.Note the day 0 represents the date of maximum MJO convection.

    Fig.9.Temporal evolutions of the column-integrated (1000—100 hPa) intraseasonal MSE budget terms (W m—2) during the boreal winters of 1982/83 (red line),1997/98 (orange line),and 2015/16 (blue line) over the western Pacific region(120°—170°E,5°—15°S).Day 0 denotes the date of the maximum MJO convection.

    For a purely quantitative comparison,we show the changes in amplitude of each budget term over the western Pacific during the initiation and development stages of the MJO convection (from day ?20 to day 0).The differences in the MSE budget terms between the 2015/16 super El Ni?o and the other two super El Ni?o events are displayed in Fig.10a.Note that the sum of the right-hand side terms is approximate to the left-hand side term (i.e.,the MSE tendency),suggesting that our calculations are nearly balanced.The growth rate of MSE (?m/?t)during the 2015/16 super El Ni?o event is much larger than those during the 1982/83 and 1997/98 super El Ni?o events,consistent with the enhanced MJO activity.The horizontal advection here is the most dominant term for the growth rate of the MSE.In addition,the longwave radiation during the 2015/16 El Ni?o event is the secondary contributor for the growth of the MSE,and the larger longwave radiation has more positive feedback for the MJO convection,since increased cloudiness could produce larger longwave radiation.The other terms are relatively small and play minor roles on the MSE tendency.The MSE diagnostic results indicate that the horizontal advection of MSE is the key process inducing the enhancement of MJO convection during the 2015/16 super El Ni?o event.We next examine relative contributions of processes from different time-scale interactions to the horizontal MSE advection based on the following equation:

    The decomposition of different time-scale interactions is the same as with Eqs.(4—5).As shown in Fig.10b,the increased horizontal MSE advection in the 2015/16 super El Ni?o event is mostly attributable to the strengthened horizontal advection of the LFBS MSE by MJO-related horizontal wind.This result highlights the importance of interaction between the LFBS MSE and the MJO-related horizontal wind anomalies,as also revealed from the low-level moisture diagnosis (Figs.6b,7c).Figure 11 displays the vertically (1000—100 hPa) averaged distributions of LFBS MSE and intraseasonal horizontal wind anomalies.The boreal winters of 1982/83 and 1997/98 show negative LBFS MSE anomalies over the western Pacific (Figs.11a,b),which are related to the below average SST anomalies (

    CT

    )(Figs.4a,b) and the below average moisture (

    Lq

    ) (Figs.7a,b).In contrast,the LBFS MSE is increased over the western equatorial Pacific during boreal winter of the 2015/16 super El Ni?o (Fig 11c),which is closely related to the westward displacement of the warm SSTAs and convection(Fig.4c).The MJO-related wind anomalies tend to transport the relatively higher MSE toward the western Pacific,causing the increased MSE over the active MJO region(Figs.11c and d).The MSE diagnostic results suggest that the warmer SSTs and thus low-level moistening during the 2015/16 super El Ni?o event could be the key factors responsible for the stronger MJO through enhancing the MSE over the western Pacific.

    Fig.10.Differences of column-integrated (1000—100 hPa) intraseasonal (a) MSE budget terms (W m?2) and (b)individual terms of averaged over the western Pacific region (120°—170°E,5°—15°S) at the initiating and developing stages of MJO convection (from day ?20 to day 0) between 2015/16 and the average of 1982/83 and 1997/98.

    Fig.11.Vertically averaged (1000—100 hPa) LFBS MSE anomalies (shading,1 × 103 J kg?1) and low-level(1000—700 hPa) MJO-related zonal wind anomalies (vectors,m s?1) for (a) 1982/1983,(b) 1997/1998,(c) 2015/2016,and (d) difference between 2015/16 and the average of 1982/83 and 1997/98 from day ?20 to day 0.The green boxes denote the western tropical Pacific (5°—15°S,120°—170°E).

    Fig.12.Column-integrated intraseasonal (a) ·? term (1000—700 hPa,g kg?1) and (b) ·? term (1000—100 hPa,W m?2,where represents the averaged V′ at the MJO developed stage during boreal winters of 1979—2018.

    5.Conclusion and discussion

    Previous observation shows that western Pacific MJO activity is strongly suppressed during the mature and decaying phases of super El Ni?o events (e.g.,1982/83 and 1997/98 El Ni?o events).The SSTAs of the most recent super El Ni?o event (i.e.,2015/16) also exhibit a very similar evolution and amplitude as the previous super El Ni?o events.However,this super El Ni?o event is accompanied by very different MJO activity with enhanced convection over the western Pacific during its peak phase.Compared to the 1982/83 and 1997/98 super El Ni?o events,the SSTA center during the 2015/16 super El Ni?o event shifts westward by about 20 degrees of longitude,which can provide sufficient moisture/MSE for MJO development over the western Pacific.The low-level moisture budget shows that vertical moisture advection is the major contributor to the enhancement of the MJO in 2015/16.This intensified vertical advection could be attributed to the interaction between the enhanced MJO-related zonal wind and the abundant low-frequency background moisture field over the centralwestern Pacific.The column-integrated MSE budget also suggests the interaction between MJO zonal wind anomalies and the background MSE field plays a key role in the enhancement of the MJO during the boreal winter of 2015/16.In other words,the increases in background moisture and MSE associated with the warm SSTAs over the central-western Pacific in the 2015/16 super El Ni?o event were important for the enhanced MJO activity.

    Previous studies have revealed different MJO features,in terms of intensity and propagation,for the eastern Pacific(EP) and central Pacific (CP) El Ni?o.The MJO intensity and El Ni?o amplitude exhibit a certain degree of linear relationship for the EP and CP El Ni?o,respectively (Gushchina and Dewitte,2012;Feng et al.,2015;Chen et al.,2016;Hsu and Xiao,2017;Wang et al.,2018).Our study finds that MJO intensity is very sensitive to SSTA zonal location of El Ni?o,even the super El Ni?o (usually regarded as a same type) events have different impact.It highlights that the ENSO zonal structure and SSTA distribution need to be considered due to their possible modulations on MJO development.Only three super El Ni?o events are investigated to observe their differences in this study.However,to which extent the normal El Ni?o spatial SSTA patterns modulate on MJO development remains unclear and deserves further investigation.

    Acknowledgements

    .This work was supported by the National Key R&D Program of China (2018YFC1505804),and the National Nature Science Foundation of China (42088101).

    国产精品九九99| 真人做人爱边吃奶动态| 老司机午夜福利在线观看视频| 中文字幕人妻熟女乱码| 天天添夜夜摸| 在线永久观看黄色视频| 18禁观看日本| 亚洲一区二区三区色噜噜| 97人妻天天添夜夜摸| 中出人妻视频一区二区| 国产高清有码在线观看视频 | 91成年电影在线观看| 久久精品国产亚洲av香蕉五月| 波多野结衣av一区二区av| 亚洲欧美激情在线| 一区二区三区国产精品乱码| 50天的宝宝边吃奶边哭怎么回事| 欧美大码av| 国产人伦9x9x在线观看| 久久天躁狠狠躁夜夜2o2o| 日韩欧美一区视频在线观看| 天天躁夜夜躁狠狠躁躁| 窝窝影院91人妻| 操美女的视频在线观看| 精品欧美国产一区二区三| 久久亚洲真实| cao死你这个sao货| 亚洲av熟女| 电影成人av| 国产av精品麻豆| 91成人精品电影| 亚洲中文字幕日韩| 国产亚洲精品av在线| 久久久久久久久中文| 亚洲在线自拍视频| 国内精品久久久久久久电影| 国产欧美日韩综合在线一区二区| 国产色视频综合| 一级,二级,三级黄色视频| 欧美在线一区亚洲| 最近最新中文字幕大全免费视频| 国产av精品麻豆| 俄罗斯特黄特色一大片| 精品国产乱码久久久久久男人| 婷婷精品国产亚洲av在线| 在线观看舔阴道视频| 99久久国产精品久久久| 99国产精品免费福利视频| 国产午夜福利久久久久久| 夜夜躁狠狠躁天天躁| 国产精品久久电影中文字幕| 亚洲aⅴ乱码一区二区在线播放 | 国产区一区二久久| 国产成人av教育| 久久九九热精品免费| 久久久久国内视频| 日日干狠狠操夜夜爽| 亚洲成人国产一区在线观看| 日韩精品青青久久久久久| 国产精品亚洲美女久久久| 最近最新中文字幕大全电影3 | 国产精品av久久久久免费| 精品国产亚洲在线| 无限看片的www在线观看| 久久久久久久久免费视频了| 精品日产1卡2卡| x7x7x7水蜜桃| 久久这里只有精品19| av福利片在线| 久久这里只有精品19| 在线av久久热| 一进一出抽搐动态| 一进一出抽搐动态| 亚洲第一欧美日韩一区二区三区| 青草久久国产| 亚洲av熟女| 亚洲人成电影观看| 18禁裸乳无遮挡免费网站照片 | 中文字幕精品免费在线观看视频| 一级毛片女人18水好多| 亚洲色图综合在线观看| 精品卡一卡二卡四卡免费| 大码成人一级视频| 欧美丝袜亚洲另类 | 91老司机精品| 制服诱惑二区| 日本 欧美在线| 女性生殖器流出的白浆| 国产高清激情床上av| 国产野战对白在线观看| 村上凉子中文字幕在线| 国产高清激情床上av| 午夜福利高清视频| 韩国精品一区二区三区| 大型黄色视频在线免费观看| 日日爽夜夜爽网站| 亚洲人成伊人成综合网2020| 久久亚洲真实| 午夜亚洲福利在线播放| 51午夜福利影视在线观看| 男女之事视频高清在线观看| videosex国产| 国产一区二区在线av高清观看| 国产黄a三级三级三级人| 亚洲精品粉嫩美女一区| 亚洲av日韩精品久久久久久密| 国产三级黄色录像| 成在线人永久免费视频| 男女之事视频高清在线观看| 久久久久国内视频| 国产熟女午夜一区二区三区| 啦啦啦 在线观看视频| 日本欧美视频一区| 国产99白浆流出| 丝袜美足系列| 亚洲第一电影网av| 国产麻豆69| 老司机午夜十八禁免费视频| 夜夜爽天天搞| 国产精品久久视频播放| 国产亚洲av嫩草精品影院| 免费在线观看黄色视频的| 免费不卡黄色视频| 老司机福利观看| 亚洲欧美日韩高清在线视频| 色播在线永久视频| 国产精品亚洲美女久久久| 看片在线看免费视频| 成人亚洲精品av一区二区| 久久这里只有精品19| 麻豆国产av国片精品| 日韩av在线大香蕉| 久久精品影院6| 午夜a级毛片| 亚洲国产精品999在线| 人人妻,人人澡人人爽秒播| 男人舔女人的私密视频| 97碰自拍视频| 纯流量卡能插随身wifi吗| av天堂在线播放| 人人妻人人澡欧美一区二区 | 国产精华一区二区三区| 日本一区二区免费在线视频| 成人亚洲精品av一区二区| 久久国产亚洲av麻豆专区| 久久精品国产综合久久久| 亚洲成国产人片在线观看| 老司机福利观看| 久久影院123| 色播在线永久视频| 天天一区二区日本电影三级 | 天堂√8在线中文| 不卡一级毛片| 成人av一区二区三区在线看| 久久国产乱子伦精品免费另类| 嫩草影视91久久| 亚洲欧美日韩无卡精品| 他把我摸到了高潮在线观看| 久久久国产精品麻豆| 1024视频免费在线观看| 国产精品精品国产色婷婷| 精品乱码久久久久久99久播| 久久国产乱子伦精品免费另类| 老司机靠b影院| 精品高清国产在线一区| 我的亚洲天堂| 免费一级毛片在线播放高清视频 | 18禁国产床啪视频网站| 国产精品日韩av在线免费观看 | 十分钟在线观看高清视频www| 91国产中文字幕| 99riav亚洲国产免费| 国产亚洲av嫩草精品影院| 国产97色在线日韩免费| 亚洲avbb在线观看| 色尼玛亚洲综合影院| 精品国内亚洲2022精品成人| 搞女人的毛片| 久久婷婷成人综合色麻豆| 波多野结衣av一区二区av| 岛国视频午夜一区免费看| 俄罗斯特黄特色一大片| 这个男人来自地球电影免费观看| 99香蕉大伊视频| 午夜久久久在线观看| 日韩大尺度精品在线看网址 | 一边摸一边抽搐一进一出视频| 国产亚洲精品综合一区在线观看 | 国产一区二区三区视频了| 91在线观看av| 丁香六月欧美| 国产精品一区二区免费欧美| 9色porny在线观看| 日韩大尺度精品在线看网址 | 少妇被粗大的猛进出69影院| 免费高清视频大片| 男女之事视频高清在线观看| 久久香蕉激情| 成人亚洲精品av一区二区| 丁香六月欧美| 欧美日韩精品网址| av天堂在线播放| 亚洲精品在线观看二区| 村上凉子中文字幕在线| 国产又色又爽无遮挡免费看| 美女午夜性视频免费| 成人三级黄色视频| 最好的美女福利视频网| 色在线成人网| 搡老岳熟女国产| av视频免费观看在线观看| 亚洲久久久国产精品| 亚洲中文av在线| 黄频高清免费视频| 嫁个100分男人电影在线观看| 久久午夜亚洲精品久久| 日韩有码中文字幕| 中文字幕最新亚洲高清| 啦啦啦韩国在线观看视频| 97人妻天天添夜夜摸| 大型黄色视频在线免费观看| 动漫黄色视频在线观看| 亚洲精品在线观看二区| 男女做爰动态图高潮gif福利片 | 啪啪无遮挡十八禁网站| 国产熟女午夜一区二区三区| 免费久久久久久久精品成人欧美视频| 午夜福利影视在线免费观看| 久久香蕉精品热| 999精品在线视频| www.自偷自拍.com| 亚洲国产看品久久| 亚洲久久久国产精品| 久久天躁狠狠躁夜夜2o2o| 久久久国产成人免费| 午夜精品久久久久久毛片777| 久久草成人影院| 国产精品一区二区免费欧美| 不卡av一区二区三区| 丝袜在线中文字幕| 亚洲片人在线观看| 亚洲av第一区精品v没综合| 欧美成狂野欧美在线观看| 国产亚洲欧美精品永久| 看片在线看免费视频| 老司机靠b影院| 日韩国内少妇激情av| 久久国产精品男人的天堂亚洲| 高清在线国产一区| 精品不卡国产一区二区三区| cao死你这个sao货| 国产精品免费视频内射| 国产成人欧美在线观看| 麻豆av在线久日| 人人妻人人爽人人添夜夜欢视频| 亚洲国产日韩欧美精品在线观看 | 亚洲精品中文字幕一二三四区| 99国产综合亚洲精品| 国产成人精品在线电影| or卡值多少钱| 中文字幕另类日韩欧美亚洲嫩草| 少妇裸体淫交视频免费看高清 | 亚洲av熟女| 国产高清有码在线观看视频 | 国产精品野战在线观看| 精品欧美国产一区二区三| 欧美黑人欧美精品刺激| 九色亚洲精品在线播放| 亚洲全国av大片| 一级毛片女人18水好多| 中文字幕色久视频| 成年人黄色毛片网站| 国产精品精品国产色婷婷| 美女大奶头视频| 动漫黄色视频在线观看| 欧美日韩乱码在线| 久久青草综合色| 亚洲第一av免费看| 天天躁夜夜躁狠狠躁躁| 国产亚洲精品一区二区www| 国产一区二区三区综合在线观看| 中文字幕精品免费在线观看视频| av片东京热男人的天堂| 美女大奶头视频| 免费在线观看视频国产中文字幕亚洲| 国产精品永久免费网站| 美女高潮喷水抽搐中文字幕| 国产1区2区3区精品| 丝袜美腿诱惑在线| 久久人人97超碰香蕉20202| 国产亚洲精品一区二区www| 777久久人妻少妇嫩草av网站| 麻豆成人av在线观看| 精品福利观看| 日韩欧美国产一区二区入口| 亚洲成人国产一区在线观看| 亚洲七黄色美女视频| 日本撒尿小便嘘嘘汇集6| 亚洲精品国产一区二区精华液| 一级毛片精品| 亚洲一区中文字幕在线| 亚洲全国av大片| 亚洲av美国av| 亚洲av电影在线进入| 露出奶头的视频| 亚洲一卡2卡3卡4卡5卡精品中文| 波多野结衣巨乳人妻| 一二三四在线观看免费中文在| 午夜两性在线视频| 午夜免费观看网址| 99在线视频只有这里精品首页| 国产1区2区3区精品| 精品久久久久久,| 亚洲激情在线av| 国产三级黄色录像| 99在线视频只有这里精品首页| 黄色丝袜av网址大全| 亚洲欧美日韩高清在线视频| 日韩中文字幕欧美一区二区| 男女午夜视频在线观看| 1024香蕉在线观看| 搡老妇女老女人老熟妇| 操美女的视频在线观看| 91大片在线观看| 久久国产精品男人的天堂亚洲| 91麻豆精品激情在线观看国产| 亚洲aⅴ乱码一区二区在线播放 | 久久青草综合色| 日韩中文字幕欧美一区二区| 国产一区在线观看成人免费| 99在线人妻在线中文字幕| 在线观看免费午夜福利视频| 亚洲精品av麻豆狂野| 老熟妇仑乱视频hdxx| 女性生殖器流出的白浆| 国内精品久久久久久久电影| 欧美 亚洲 国产 日韩一| 国产又色又爽无遮挡免费看| 啪啪无遮挡十八禁网站| 午夜福利成人在线免费观看| 人妻丰满熟妇av一区二区三区| 国产精品免费视频内射| 国产精品二区激情视频| 一进一出抽搐动态| 99久久99久久久精品蜜桃| 亚洲美女黄片视频| 午夜免费激情av| 少妇的丰满在线观看| 国产精品亚洲美女久久久| 久久婷婷人人爽人人干人人爱 | 午夜激情av网站| 成人免费观看视频高清| 国产成人欧美在线观看| 国产99白浆流出| 精品国产乱码久久久久久男人| 午夜福利成人在线免费观看| 国产欧美日韩一区二区三区在线| 精品久久久久久,| 黑丝袜美女国产一区| 国产欧美日韩综合在线一区二区| 国产熟女xx| 久久狼人影院| 男人操女人黄网站| 亚洲午夜精品一区,二区,三区| 国产黄a三级三级三级人| 女人被狂操c到高潮| 夜夜看夜夜爽夜夜摸| 黄色视频,在线免费观看| 首页视频小说图片口味搜索| 国产精品一区二区在线不卡| 午夜日韩欧美国产| 国产视频一区二区在线看| www.www免费av| 欧美日韩福利视频一区二区| 色综合欧美亚洲国产小说| 亚洲在线自拍视频| 91在线观看av| 一区二区三区激情视频| 午夜福利18| 午夜福利,免费看| 免费看美女性在线毛片视频| 一区二区三区精品91| 国产亚洲欧美98| 9色porny在线观看| 国产成+人综合+亚洲专区| av中文乱码字幕在线| 亚洲精华国产精华精| 50天的宝宝边吃奶边哭怎么回事| 国产野战对白在线观看| 色精品久久人妻99蜜桃| 麻豆一二三区av精品| 一区二区日韩欧美中文字幕| 久久精品成人免费网站| 久久午夜综合久久蜜桃| 欧美精品亚洲一区二区| 国产精品久久久av美女十八| 亚洲精品久久国产高清桃花| 丝袜美腿诱惑在线| 日韩欧美国产在线观看| 久久欧美精品欧美久久欧美| 桃红色精品国产亚洲av| 国产成+人综合+亚洲专区| 女人爽到高潮嗷嗷叫在线视频| 亚洲伊人色综图| 成在线人永久免费视频| 国产精品久久电影中文字幕| 妹子高潮喷水视频| 久久精品国产清高在天天线| 成人手机av| 成人国产综合亚洲| 国产成人欧美| 久久天堂一区二区三区四区| 国产成人精品久久二区二区91| 老司机午夜十八禁免费视频| 9色porny在线观看| 国产精品99久久99久久久不卡| 亚洲国产精品999在线| 国产三级黄色录像| 香蕉国产在线看| √禁漫天堂资源中文www| 香蕉久久夜色| 亚洲专区中文字幕在线| 日韩欧美三级三区| 亚洲国产欧美一区二区综合| 久久久久国产一级毛片高清牌| 亚洲一区二区三区色噜噜| 亚洲精品美女久久av网站| 久久久久国内视频| 亚洲欧洲精品一区二区精品久久久| 一区二区三区激情视频| 国产精品久久久久久精品电影 | 免费少妇av软件| 电影成人av| 人妻久久中文字幕网| 亚洲自偷自拍图片 自拍| 亚洲国产精品sss在线观看| 性色av乱码一区二区三区2| 国内久久婷婷六月综合欲色啪| 午夜免费观看网址| 可以在线观看毛片的网站| 琪琪午夜伦伦电影理论片6080| 国产1区2区3区精品| 大陆偷拍与自拍| 亚洲专区字幕在线| 啪啪无遮挡十八禁网站| 亚洲中文字幕一区二区三区有码在线看 | 欧美乱妇无乱码| 国产成人欧美| 桃色一区二区三区在线观看| 日本 av在线| 亚洲精品国产色婷婷电影| 亚洲av美国av| 亚洲av成人一区二区三| 亚洲国产精品成人综合色| 一边摸一边做爽爽视频免费| 日韩有码中文字幕| 丁香欧美五月| 在线播放国产精品三级| 19禁男女啪啪无遮挡网站| 亚洲av片天天在线观看| 亚洲aⅴ乱码一区二区在线播放 | 国产在线精品亚洲第一网站| 黄色视频不卡| 国产熟女xx| 日本免费a在线| 美女国产高潮福利片在线看| 十八禁人妻一区二区| 国产精品综合久久久久久久免费 | 亚洲精品中文字幕在线视频| 非洲黑人性xxxx精品又粗又长| 涩涩av久久男人的天堂| 亚洲avbb在线观看| 亚洲熟妇中文字幕五十中出| 精品久久久精品久久久| 午夜福利在线观看吧| 每晚都被弄得嗷嗷叫到高潮| 免费不卡黄色视频| 一区福利在线观看| 看免费av毛片| 亚洲九九香蕉| 又紧又爽又黄一区二区| 国产欧美日韩综合在线一区二区| 搡老岳熟女国产| 黄色丝袜av网址大全| 欧美激情极品国产一区二区三区| 好看av亚洲va欧美ⅴa在| 亚洲五月天丁香| 亚洲精品中文字幕在线视频| 女人被狂操c到高潮| 两个人免费观看高清视频| 精品一区二区三区av网在线观看| 国产精品av久久久久免费| 黄色成人免费大全| 在线观看日韩欧美| 亚洲国产看品久久| 免费在线观看日本一区| 亚洲av第一区精品v没综合| 中文亚洲av片在线观看爽| 非洲黑人性xxxx精品又粗又长| av在线播放免费不卡| 九色国产91popny在线| 一个人免费在线观看的高清视频| 美女国产高潮福利片在线看| 一级作爱视频免费观看| 不卡一级毛片| 一级作爱视频免费观看| 国产精品综合久久久久久久免费 | 欧美久久黑人一区二区| 中文字幕人成人乱码亚洲影| 亚洲精品一区av在线观看| 久久午夜亚洲精品久久| 欧美成人午夜精品| 可以在线观看的亚洲视频| 亚洲国产毛片av蜜桃av| 人人澡人人妻人| 亚洲九九香蕉| 日韩中文字幕欧美一区二区| 国产区一区二久久| 亚洲,欧美精品.| 精品国产国语对白av| 99国产精品一区二区蜜桃av| 亚洲精品国产区一区二| 桃色一区二区三区在线观看| 亚洲第一青青草原| 国产亚洲精品av在线| 久久久久久久久久久久大奶| 少妇粗大呻吟视频| 大码成人一级视频| 人人妻人人爽人人添夜夜欢视频| 无限看片的www在线观看| 大香蕉久久成人网| 日韩成人在线观看一区二区三区| 国产aⅴ精品一区二区三区波| 亚洲性夜色夜夜综合| 国产视频一区二区在线看| aaaaa片日本免费| 男人舔女人下体高潮全视频| 午夜影院日韩av| 国产精品永久免费网站| 日韩视频一区二区在线观看| 亚洲专区国产一区二区| 无人区码免费观看不卡| 亚洲片人在线观看| 热re99久久国产66热| 啪啪无遮挡十八禁网站| www.自偷自拍.com| 国产精品 欧美亚洲| 国产一级毛片七仙女欲春2 | 香蕉久久夜色| 久久午夜亚洲精品久久| 精品国产一区二区三区四区第35| 免费在线观看日本一区| 啪啪无遮挡十八禁网站| 神马国产精品三级电影在线观看 | www国产在线视频色| 亚洲av美国av| 在线十欧美十亚洲十日本专区| 制服诱惑二区| 免费少妇av软件| 中文字幕av电影在线播放| 日韩av在线大香蕉| 黑人巨大精品欧美一区二区蜜桃| 成人18禁在线播放| 丝袜美腿诱惑在线| 欧美亚洲日本最大视频资源| 精品午夜福利视频在线观看一区| 国产精品九九99| 变态另类成人亚洲欧美熟女 | 久久亚洲精品不卡| 99久久99久久久精品蜜桃| 夜夜爽天天搞| 午夜两性在线视频| 免费在线观看黄色视频的| 国产又色又爽无遮挡免费看| 99国产精品99久久久久| a在线观看视频网站| 国产成人系列免费观看| 国产人伦9x9x在线观看| 欧美黄色片欧美黄色片| 精品欧美国产一区二区三| 99久久精品国产亚洲精品| 搡老熟女国产l中国老女人| 视频区欧美日本亚洲| 熟妇人妻久久中文字幕3abv| 大型av网站在线播放| 欧美成人午夜精品| 成人手机av| 乱人伦中国视频| 亚洲国产精品久久男人天堂| 一a级毛片在线观看| 日本三级黄在线观看| 亚洲第一青青草原| 黄色毛片三级朝国网站| 丝袜美腿诱惑在线| www日本在线高清视频| 国产精品 国内视频| 不卡一级毛片| 日韩一卡2卡3卡4卡2021年| 美女午夜性视频免费| 级片在线观看| 国产一区二区激情短视频| 国产免费男女视频| av网站免费在线观看视频| 妹子高潮喷水视频| 免费在线观看亚洲国产| 欧美激情 高清一区二区三区| 少妇熟女aⅴ在线视频| 中文字幕人妻熟女乱码| 久久精品国产清高在天天线| 一级毛片高清免费大全| 亚洲aⅴ乱码一区二区在线播放 | 十八禁人妻一区二区| 亚洲 国产 在线| 亚洲一区高清亚洲精品| 色综合亚洲欧美另类图片|