• <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 ?

    Effect of tidal currents on the transport of saline water from the North Branch in the Changjiang River estuary*

    2018-12-22 07:00:02DINGJian丁堅SHAOYuchen邵雨辰WUDean吳德安
    Journal of Oceanology and Limnology 2018年6期
    關鍵詞:德安

    DING Jian (丁堅), SHAO Yuchen (邵雨辰) , WU De’an (吳德安),

    1 Key Laboratory of Coastal Disaster and Defence, Ministry of Education, Hohai University, Nanjing 210098, China

    2 Nanjing Water Planning and Design Institute Corp. Ltd., Nanjing 210022, China

    Abstract Based on the MIKE 21 numerical model combined with measured data, a numerical model for the coupling of water and salinity in the Changjiang (Yangtze) River estuary was established, and based on good verification, the influence of the tidal current intensity on the transport and variations of salinity concentrations in saline water from the North Branch to the South Branch was numerically evaluated. The time and space mean root mean square of the tidal current velocity can be expressed as a parabolic function of an adjustment coefficient for the amplitude of the M2 tidal constituent along the open boundaries of the model. Under the advection of runoff and tidal currents, the saline pool is transported downstream in an oscillatory pattern. With the enhancement of tidal current intensity, the oscillatory motion of the saltwater pool is increasingly significant in a tidal cycle forced by rising and falling tides. Along four set paths, the daily average concentrations of the saline core were generally similar, and in the process of transportation downstream, the concentrations of saltwater declined. The decay of the tidal-period-averaged salinity of the saltwater was linearly related to the square of the tidal current. Thus, the tidal current has a significant and direct impact on saltwater transport and diffusion in the Changjiang River estuary.

    Keyw ord: Changjiang River estuary; saltwater intrusion; numerical simulation; transport and diffusion;attenuation

    1 INTRODUCTION

    The Changjiang (Yangtze) River is the largest river of the china, with 9.24×1011m3freshwater discharged into the East China Sea each year (Wu et al., 2010).Runoff varies seasonally, with a maximum monthly mean of 49 500 m3/s in July and a minimum of 10 500 m3/s in January (Shen et al., 2003). The width of the river mouth is about 90 km, and the tidal limit reaches Anhui Datong station about 642 km from the river mouth. The Changjiang River estuary is a moderate tidal estuary with multi-level branching influenced by the interactions of runoff and tidal current. Chongming Island first divides the estuary into the North Branch and the South Branch. Then,the South Branch is bifurcated by Hengsha Island and Changxing Island into the North Channel and the South Channel. Finally, the South Channel is bifurcated into the North Passage and the South Passage by Jiuduansha. The runoff of the Changjiang River is ultimately discharged into the East China Sea through four outlets.

    Saltwater intrusion presents a specific pattern in the Changjiang estuary; in the dry season when river discharge is small, the water/salt mass in the North Branch can spill over into the South Branch under strong tidal conditions (Wu and Zhu, 2007; Xue et al.,2009; Wu et al., 2010). Previous studies have focused on the interactions between saltwater and freshwater,such as the length of saltwater intrusion (e.g., Shen et al., 2003; Kong et al., 2004). In early studies of saltwater intrusion length, it was assumed that the transport of runoff and tidal currents to saline water was balanced (Knudsen, 1900; Hansen and Rattray,1965), and based on this assumption, many researchers have proposed equilibrium equations of estuarine salinity transport. Festa and Hansen (1976) found that the length of salinity intrusion changes with water depth, the vertical diffusion coefficient, and runoff .Chatwin (1976) evaluated salinity intrusion length based on parameters including the depth of the estuary, runoff , the vertical diffusion coefficient and the salinity of the estuary (Chatwin, 1976). Based on in-situ data, investigation and analysis revealed that river discharge and tides were the main dynamic factors determining the features of saltwater intrusion in the Changjiang estuary during the dry season (Zhu et al., 2010; Li et al., 2012).

    Many researchers have explored the relationships between saltwater intrusion and various factors such as runoff , tides, topography and wind using numerical models. Park and Kuo (1996) used a two-dimensional numerical model to study the saltwater intrusion process and its response to changes in the tide cycle,and the results showed that the response of the estuary saltwater intrusion to the changes in tidal current velocity requires four months of adjustment time(Park and Kuo, 1996). Taking into account the complexity of saltwater intrusion in the Changjiang River estuary, researchers have mainly focused on the influence of runoff , tides, wind, topography and estuarine engineering on saltwater intrusion (Mao and Shen, 1993; Xiao and Shen, 1998; Shen et al., 2000;Zhu and Wu, 2013). Based on a three-dimensional numerical model with a high-resolution grid, the response time of saltwater intrusion to river discharge during different tidal patterns in the Changjiang River estuary was studied (Hou and Zhu, 2013). Saltwater diffusion forced by the M2 constituent and the quasisteady flow were studied using a numerical mode(Zhu and Wu, 2013), and it was pointed out that the M2 constituent has great influence on the mixing and transport of salinity. The quantitative relationships between saltwater intrusion from the North Branch and both river runoff and tidal range were analyzed(Wu et al., 2006) using the ECOM-si numerical model, and the modified ECOM model was used to study the impact of wind stress and the Coriolis force on the formation of a freshwater zone in the Meimaosha area of the South Passage of the Changjiang River estuary (Zhu et al., 2008). It was found that a freshwater zone existed in the Meimaosha area during the dry season, and its dynamic mechanisms of formation were mainly Changjiang River runoff and tidal current oscillation. Based on a three-dimensional numerical model, the transport mechanism of saltwater spilling over from the North Branch in the Changjiang River estuary was analyzed quantitatively using the flux analysis method. The Lagrange residual as well as the tidal pump were found to be the main dynamic factors (Wu and Zhu, 2007).

    In brief, these studies of saltwater intrusion in the Changjiang River estuary have mainly been based on the response of the Changjiang River estuary to runoff , tidal currents, circulation, tides, topography,hydraulic structure, and wind forcing (Gong and Shen, 2011; Fan et al., 2012; Wang et al., 2012; Shaha et al., 2013). A significant feature of saltwater intrusion in the Changjiang River estuary is the mixing of saltwater from the North Branch and saltwater from the South Branch (Mao and Shen,1993). It is particularly difficult to visually identify and analyze saltwater transport and the distribution of brine salinity from the North Branch. Previous studies have used the relationships between maximum salinity, minimum salinity, and the tide level, the phase relationship between salinity and flow velocity,or the vertical distribution characteristics of salinity to qualitatively interpret the source of the saltwater.However, these studies lacked clear and accurate methods to reflect the processes of saltwater intrusion from the North Branch and the characteristics of its transport and diffusion in the South Branch. Therefore,in this study, the MIKE 21 model has been applied to the Changjiang River estuary and adjacent Hangzhou Bay to simulate tidal currents and salinity transport and distribution. The effects of various tidal current intensities corresponding to the given amplitude of the M2 constituent along the open boundary on salt intrusion were investigated. Model calibration and verification were conducted by comparing the tidal level, tidal current velocity, and salinity with the available field data. The model was then applied to investigate the transport and diffusion of the salt mass in the South Branch, which originates only from the North Branch, under a given river discharge amount and various tidal current intensity conditions. The data of underwater topographic, current, sediment concentration, salinity used in this paper were surveyed and provided by “General Administration of hydrology of Shanghai” and “Survey Bureau of Hydrology and Water Resources of the Yangtze River Estuary, Changjiang Water Resources Commission”.

    The two hydrology survey basically covers the entire Changjiang estuary.

    Fig.1 Bathymetric map of water depth below 1985 elevation datum plane

    2 METHOD

    2.1 Governing equations for salinity

    The module was used to calculate temperature and salinity diffusion in the MIKE 21 model. The threedimensional salinity transport equation in a Cartesian coordinate system:

    was used, wheresis the salinity,Dvis the vertical diffusion coefficient of salinity, andssis the salinity discharge of point source. The variableFsis the horizontal salinity diffusion term, which can be defined as:

    whereDhis the horizontal diffusion coefficient of salinity,Dh=A/σT, andDv=vt/σT,σTis the Prandtl constant. The horizontal eddy viscosity coefficient is calculated using the Smagorinsky formula, which is based on the velocity gradient.

    whereCsis set to 0.28.

    Theσcoordinate transformation of the salinity transport equation is the same as the tidal flow equation. The expression after coordinate transformation is as follows:

    The two-dimensional salinity transport equation in a Cartesian coordinate system is as follows:

    2.2 The range of model and mesh partitioning

    To study saltwater intrusion from the North Branch,the range of the model was set to A and to B2, as shown in Figs.1 and 2, respectively. The range of model A is the maximum range. The western/upstream open boundary is at Datong Station in Anhui Province,about 500 km from Xuliuting in the Changjiang River estuary. The downstream boundaries of the model are three open boundaries to the south, north and east; the northern open boundary is along the latitude of 32.5°N, the southern open boundary is along the latitude of 29.5°N, and the eastern open boundary is along the longitude of 124.5°E. The eastern and western open boundaries are about 700 km apart, the northern and southern open boundaries are about 350 km apart.

    Fig.2 Bathymetric map for schematic B2

    In order to control the strength of the intrusion saltwater and study transport law of the saline water only from the North Branch, the model B2 was set up.For model B2, the upstream open boundary of the B2 model is along the section of Datong station. The start point of the downstream northern open boundary is set near Lianxinggang, and another open boundary of model B2 in the North Branch is located near the head of Chongming Island. The eastern open boundary is about 100 km from the estuary entrance, located near the 40 m isobath. The southern open boundary is from Luchaogang eastward.

    2.3 Computational grid

    The number of grid cells for model A is 115 780,the number nodes is 61 246, the largest off shore grid spacing is 8 000 m, and the minimum mesh inside the estuary mouth is 200 m. The mesh size decreases gradually from the open sea to the mouth. The number of grid cells for model B1 is 74 115, the number of nodes is 39 603, the maximum grid spacing is about 2 000 m, and the grid size is close to that of model A in the inner estuary. The number of grid cells for B2 is 32 311, the number of nodes is 60 368.

    2.4 The open boundary conditions

    The upstream boundaries of models A and B2 at Datong station are driven by daily flow measurements from February 11, 2002 to March 13, 2002. The boundary of model A in the open sea is driven by hourly water level data from February 11 to March 13, 2002. The water level data were obtained from the calculated results of the East China Sea Model(Zhang, 2005). The flow of the Qiangtangjiang boundary was set to 0 m3/s because of its small runoffvolume. For model B2, the open sea boundary and the Chongtou boundary in the North Branch are driven by the water level and flow processes from model A. For the initial conditions of models A and B2, a cold start was adopted, and the sea levels and flow rates for both models were set to 0 (Wu et al., 2015).

    The upstream boundary salinity for the model A was set to 0, and the salinity at the southern boundary was obtained through linear interpolation between 15 to the west and 30 to the east. The salinity at the eastern boundary was obtained through linear interpolation between 30 to the south and 35 to the north. The salinity of the northern boundary was obtained through linear interpolation between 25 to the west and 35 to the east. The salinity at the boundary of model B2 in the North Branch was extracted from salinity calculation results of model A, and the salinity at the boundary in the southern branch was set to 0.

    2.5 Model parameter setting

    (1) Time step: Δt=30 s.

    (2) The roughness field has great influence on the flow velocity and tidal range. Based on the water depths of different areas, after careful verification and calibration, the roughness was taken as 0.01+0.01/Hin the outer of the estuary area, and 0.015+0.015/Hin inner area of the estuary, whereHis the local water depth (relative to the average tidal level).

    (3) The horizontal diffusion coefficient of salinity has some influence on the simulated salinity field in the Changjiang estuary. The greater the horizontal diffusion coefficient, the faster the rate of salinity diffusion and the larger the diffusion range. Based on careful verification and calibration, the salinity diffusion coefficient is given as 100 m2/s.

    2.6 Model validation

    Model A was simulated for 120 days, repeatedly driven by the open boundary conditions from February 11, 2002 to March 12, 2002. Then, model B2 was simulated for 120 days. The initial salinity field of model B2 was provided by the simulation result of model A at the end of third interval of 30 days. The initial water level and velocity field values were 0;that is, using the initial dynamic conditions of the cold start for the model B2. The salinity values and water flux at the open boundary near the head of Chongming Island were obtained from the simulated results of model A. The water level along the rest of the open boundaries were given by model A, and the corresponding salinity values were set to 0 for investigating saltwater transport and diffusion in the South Branch, which represents intrusion of saltwater is from the North Branch. After 120 days of simulation of model B2, the last 15 days of the simulated results related to saltwater motion in the South Branch were used for verification and analysis. This 15-day period includes the typical tides types of full tide, spring tide and neap tide. Here, a percentage deviation model(Maréchal, 2004) was adopted to evaluate the simulation of models A and B2 for sea level and flow rate:

    i n the formula,Dis the measured data,Mis the model data, and the relationship between PB and the quality level of the simulation results is shown in Table 1.

    The percentage deviation model was used again to evaluate the simulation of salinity by models A and B2. The simulations of tide level, tide flow and salinity were good. The PB values (Maréchal, 2004)were generally less than 40. The tidal level, tidal current and salinity were well represented, and the PB values were less than 40. The model therefore meets the requirements (Shao, 2014).

    3 RESULT AND ANALYSIS

    3.1 Route setting

    It is very difficult to obtain detailed data on saltwater intrusion in the North Branch, with limited field data available. To better understand the process of the saltwater intrusion from the North Branch, the downward movement of the saltwater and salinity changes in the waterways of the South Branch were studied to reveal the transport pattern of the saline pool in the waterways of the South Branch. Therefore,the movement routes of saline pool were set as shown in Fig.3.

    Table 1 Relationship between PB and the quality level of the simulation results

    Table 2 Proportional coefficients of different schemes

    The influences of different flow intensities on saltwater migration from the North Branch were also studied. At the upstream boundary of model A, the water flow rate is 13 000 m3/s, and the salinity is zero.

    Tidal current character and tidal current elliptic factors in the Changjiang estuary were calculated and analyzed. The research shows that the tide characteristic coefficient values are less than 0.25 in the Deep Water Channel (Pan et al., 2016). The semidiurnal tidal current play major role (Jiang et al.,2013). M2 constituent is primary (Zhu et al., 1999)and the characters of tidal current are normal semidiurnal tidal rectilinear current in the sea area.Thus the hydrodynamic characteristics of the Changjiang estuary can be reflected in a better degree by using the M2 tide as the hydrodynamic opening boundary condition. The results of the East China Sea model provide the M2 tidal level from February 11,2002 to March 12, 2002. The product of M2 tidal amplitude and the scale coefficientfcan be used to represent the simulation of different flow intensities,as shown in Table 2.

    As mentioned above, the numerical results obtained from model A for the boundary conditions of model B2 were obtained.

    3.2 Response of tidal current to different proportions of M2 tide

    The amplitude of the M2 tide on the open boundary is multiplied by a certain proportional coefficient,which indicates the input conditions of different tidal current intensities. To study the response of tidal current velocity to different proportional coefficients,the hourly flow data of 15 days were extracted at 1-km-interval grids along paths b1, b2, b3 and b4.

    Fig.3 The routes b1, b2, b3 (a); route b4 (b)

    The points of each path were classified as the inner and outer parts of the estuary. As is shown in Fig.3,the area within 60 km of each path was defined as the inner area of the estuary, while the area outside the 60 km is defined as the outer area of the estuary. The calculation procedures are as follows:

    whereup,nrepresents thenth hourly-interval current velocity corresponding to pointpalong each path;Nrepresents the number ofup,n,N=24×15+1=361;upis the time root-mean-square (RMS) velocity at pointp;umis the space RMS ofupalong each path, andPrepresents the number of points used in the RMS calculation.

    Fig.4 Fitting relationships between the root mean square velocity u m and the coefficient f

    Fig.5 Fitting relationships between the root mean square velocity u m and the coefficient f

    Fig.6 Fitting relationships between the root mean square velocity u m and the coefficient f

    Fig.7 Fitting relationships between the root mean square velocity u m and the coefficient f

    As shown in Figs.4–7, there is a nonlinear correlation between the RMS velocity and the proportionality coefficient, and the above nonlinear relationship is more accurate in parabolic form:

    The coefficientsaandbreflect the sensitivity of the tidal current velocity to the proportionality coefficient. Based on the values ofaandb, the RMS velocity of the outer estuary is more sensitive than the RMS velocity of the inner estuary to the coefficientf.It is presumed that larger scale factors correspond to greater tidal current intensities.

    Fig.8 Positions of the saline core at hourly intervals along path b1 under different flow

    Fig.9 Positions of the saline core at hourly intervals along path b2 under different flow

    Fig.10 Positions of the saline core at hourly intervals on path b3 under different flow

    3.3 The influence of tidal current on the transport of the salt water

    To facilitate analysis of the transport and diffusion of saltwater in the South Branch, the locations of maximum salinity along each path are defined as the saline core. The variation of the saline core corresponding to different tidal boundary conditions are shown in Figs.8–11. Based on the variation of the saline core along each path under different flow conditions, during the spring tide period from third day to the sixth day, the saline core oscillates in the vicinity of the starting point. Greater tidal current velocities correspond to larger amplitudes of this oscillation. From the beginning of the sixth day, it is clear that the saline water pool is transported to the lower reaches. When the tidal current is weak, the salt water is transported to the lower reaches with little fluctuation. Under the advection transport of runoffand the tidal current, the core of the saline water pool is transported downstream at a constant velocity. With the enhancement of tidal current intensity, the core of saline group has clear fluctuations with the tidal cycle under the actions of flood and ebb currents.

    3.4 The salinity variation of the saline water core under different flow conditions

    Fig.11 Positions of the saline core at hourly intervals on path b4 under different flow

    Fig.12 The 24-hour-averaged salinity of the saline core along path b1 under different flow conditions

    Fig.13 The 24-hour-averaged salinity of the saline core along path b2 under different flow conditions

    Fig.14 The 24-hour-averaged salinity of the saline core along path b3 under different flow conditions

    The variation of the 24-hour-averaged salinity of the saline water core under different flow conditions are shown in Figs.12–15. On the fifth day, the core salinity of the reached its maximum value, and in the process of downstream transport, the salinity of the salt water decreased. For model B2, under the same boundary control conditions, the saltwater intrusion of the North Branch was affected little by the different tidal currents in the south branch. Therefore, the maximum values of salt concentration corresponding to each scheme were similar. As shown by project 1,under conditions of low tidal current intensity, the lateral diffusion of brine is suppressed, and highconcentration saltwater was restricted to the Baimaosha waterway in the South Branch, The salinity values near the starting point of each path were relatively small. With the enhancement of the tidal current (as in project 5), the salinity increased with transverse diffusion. However, with the increase of the turbulent diffusion (e.g., projects 7 and 8), the salinity of the saline water core in the vicinity of the starting point of each path began to decline.

    Fig.15 The 24-hour-averaged salinity of the saline core along path b4 under different flow conditions

    Fig.16 Relative salinity of the saltwater core on path b1 under different flow

    Fig.17 Relative salinity of the saltwater core on path b2 under different flow

    3.5 The dynamic process of relative salinity of the saline water core under different flow conditions

    The relative salinity, that is, the ratio of the salinity of the saline core and its initial salinity, can reflect the diffusion rate of the saltwater. The relative salinity variation of the saline water core under different flow conditions are shown in Figs.16–19. Under different flow conditions, the saltwater is transported downstream in each set path, and the change of the relative salinity of the tidal cycle in the brine mass is positively correlated with tidal current intensity.Stronger the tidal currents correspond to faster decrease of the salinity of the salt pool.

    To further elucidate the attenuation of the relative salinity of the salt core, the attenuation of this relative salinity was calculated, as shown in Figs.20 and 21.There is a strong linear relationship between the attenuation rate and the square of the RMS velocityuin the inner estuary; this expression is shown below:

    Fig.18 Relative salinity of the saltwater core on path b3 under different flow

    Fig.19 Relative salinity of the saltwater core on path b4 under different flow

    The value of the coefficientccorresponding to each path is about 0.20–0.42; the coefficientdis more stable at around 0.021. The value of the coefficientcdetermines the decay of the salt core caused by flow velocity, whereas the value of the coefficientdis relatively constant, and its relationship with flow velocity is not explicit.

    The decay ratersis similar to that used in study of pollutant diffusion in the estuary. In the longitudinal mixing process of pollutants in the waterway, the longitudinal diffusion effect is mainly caused by dispersion induced by the inhomogeneous distribution of transverse or vertical flow velocity and turbulent diffusion. In fact, because the former is larger than the latter, and the two factors always work together.Therefore, turbulent diffusion is often neglected. This study is focused on longitudinal diffusion and the longitudinal diffusion coefficient (Fischer, 1967).

    Because diffusion coefficients are affected by many factors, simplified theoretical analysis is often limited in practical application. Diffusion coefficients are calculated with semi-theoretical and semi-empirical formulae, which are calibrated based on field measurements or laboratory experimental data. These formulae include factors such as velocity, tidal period,water depth, and parameters reflecting river shape. It can be inferred that the coefficientcin Eq.8 should be related to the tidal cycle, channel depth and channel shape parameters. In the formula, the value of the coefficientdis relatively stable, which should be related to the dilution effect caused by runoff and turbulent diffusion.

    4 CONCLUSION

    Under the conditions of upstream runoff of 13 000 m3/s, without wind force, and during the spring tide, the saline cores maintain an oscillating motion forced by the action of the flood and ebb currents along the Baimaosha waterway, with a range of oscillating motion below the head area of Chongming of about 0–14 km. Net transport of salt water to the lower reaches occurred in the transition period between spring tide and middle tide, the saline cores along each path were transported to downstream within 90 km below the tail of Baimaosha, and the fluctuation range of the saline core along each path in one tidal cycle was about 10–20 km. The average downward velocity of the saline core along each path in the inner estuary was about 8–10 km/d, whereas the average downward velocity in the outer estuary was about 2–4 km/d. Because of the influence of the double guide channel of the Changjiang estuary Deepwater Channel on water flow, the average downward velocity of the saline group core along path b2 in the outer estuary was about 10 km/d. The attenuation rate of the salinity of the salt core along each path was 0.08–0.1/d in the inner estuary and 0.24/d in the outer estuary, also because of the influence of the double guide channel of the Changjiang estuary Deepwater Channel on the water flow. The attenuation rate of salinity of the salt core along path b2 was about 0.1/d.

    Saline water transport is the result of interactions of runoff and tidal currents. Under the actions of different flow intensities, the fluctuation range of the saline core in a tidal cycle increases with tidal current intensity. The attenuation of the average relative salinity of the saline core is linearly related to the square of the tidal current. This attenuation may be related to the tidal cycle, channel depth, and channel shape parameters, which may correspond to dilution and molecular diffusion caused by runoff .

    In this study, under the condition of constant runoff ,the response of the transport and diffusion of saline water from the North Branch to different tidal current intensities was studied. In practice, the influence of highly saline water from the South Branch on the transport of saline water from the North Branch is ignored, which means that this exploratory study of the transport of saltwater from the North Branch was carried out without considering the interactions between saline water from the North Branch and high-salinity water from the open sea passing through the South Branch. However, in the vicinity of the Changjiang estuary near the sea, tidally averaged circulation has the following feature: despite net seaward flow caused by the river through the crosssection, the deeper half of the water typically flows landward. This inflow gradually rises and joins the river flowing outward in the upper half of the estuary,which results in an overall pattern called exchange flow, and would affect the transport and diffusion of the saline water.

    Only a two-dimensional numerical model was used in this study to simulate and analyze the movement of saline water from the North Branch. In fact, there is a strong stratification phenomenon in the vicinity of Chongming Island, which causes more complex brine movement. A follow-up study will employ a threedimensional numerical model to simulate the threedimensional movement of saltwater in the Changjiang estuary, considering only saltwater spilling over from the North Branch, only saltwater intrusion from the downstream though the South Branch, as well as the actual situation of brine movement in the Changjiang River estuary. Through comparative analysis, the interactions of these two different sources of brine and their contributions to the saltwater intrusion may be determined.

    5 DATA AVAILABILITY STATEMENT

    Sequence data used to calibrate the mode and support the findings of this study have been deposited in the Survey Bureau of Hydrology and Water Resources of the Changjiang River estuary. http://www.cjh.com.cn/pages/swcy_jj.html.

    猜你喜歡
    德安
    簽名少寫一個字, 影響遺囑最終效力嗎?
    婦女生活(2023年5期)2023-05-31 14:13:48
    沈稼青 肖德安 張 穎 劉桂云 蒯淵智 邵 源 宋志強 趙 林 王志敏
    大江南北(2022年7期)2022-07-13 02:09:20
    中德安聯(lián)人壽完成股權變更登記
    中德安聯(lián)人壽保險有限公司上海分公司損益表(2019)
    2018德安杯挑戰(zhàn)賽將重新起航
    汽車與運動(2018年3期)2018-06-21 17:51:44
    劁豬
    四川文學(2017年11期)2017-11-09 21:15:00
    耳 疾
    飛天(2017年1期)2017-02-16 23:25:24
    呂德安作品
    詩書畫(2016年3期)2016-08-22 03:18:52
    “寫微不足道的事物,順便將黑暗沉吟”——讀呂德安
    詩書畫(2016年3期)2016-08-22 03:18:52
    抒懷
    老年世界(2016年3期)2016-04-26 07:20:05
    波多野结衣高清无吗| 亚州av有码| 在线观看美女被高潮喷水网站| 日本一二三区视频观看| 欧美成人免费av一区二区三区| 免费一级毛片在线播放高清视频| 永久网站在线| 国产成人精品婷婷| 男人和女人高潮做爰伦理| 99热全是精品| kizo精华| 国产精品久久久久久亚洲av鲁大| 欧美性感艳星| 一级黄片播放器| 丝袜喷水一区| 天堂中文最新版在线下载 | 51国产日韩欧美| 校园春色视频在线观看| 国产探花极品一区二区| 亚洲欧美精品专区久久| 超碰av人人做人人爽久久| 国产亚洲av嫩草精品影院| 直男gayav资源| 亚洲最大成人中文| 色噜噜av男人的天堂激情| 成年女人永久免费观看视频| 日韩高清综合在线| 国产精品永久免费网站| 99视频精品全部免费 在线| 国产 一区精品| 嫩草影院精品99| 熟女人妻精品中文字幕| 十八禁国产超污无遮挡网站| 色哟哟哟哟哟哟| 亚州av有码| 男人的好看免费观看在线视频| 人妻久久中文字幕网| 欧美人与善性xxx| 日日啪夜夜撸| 狂野欧美激情性xxxx在线观看| 亚洲国产色片| 久久久精品大字幕| 两个人的视频大全免费| 国产成人精品婷婷| 99热6这里只有精品| 天堂网av新在线| 日本成人三级电影网站| 少妇被粗大猛烈的视频| 能在线免费看毛片的网站| 亚洲第一电影网av| 在线天堂最新版资源| 国内揄拍国产精品人妻在线| 少妇猛男粗大的猛烈进出视频 | 亚洲自偷自拍三级| 精品人妻熟女av久视频| 欧美最黄视频在线播放免费| 午夜福利高清视频| av在线天堂中文字幕| 秋霞在线观看毛片| 免费看光身美女| 色哟哟哟哟哟哟| 色吧在线观看| 99久久无色码亚洲精品果冻| 亚洲美女搞黄在线观看| 欧美日韩一区二区视频在线观看视频在线 | 亚洲av成人av| 国产成人aa在线观看| 晚上一个人看的免费电影| 亚洲不卡免费看| 国内久久婷婷六月综合欲色啪| 又黄又爽又刺激的免费视频.| 国产精品不卡视频一区二区| 悠悠久久av| 精品久久久久久久久亚洲| 亚洲美女视频黄频| 国产精品av视频在线免费观看| 久久精品夜夜夜夜夜久久蜜豆| 久久婷婷人人爽人人干人人爱| 一本—道久久a久久精品蜜桃钙片 精品乱码久久久久久99久播 | 国产亚洲5aaaaa淫片| 国产一区二区在线观看日韩| 久久婷婷人人爽人人干人人爱| 免费av毛片视频| www.色视频.com| 国产成人精品婷婷| 日韩欧美精品免费久久| 欧美日韩国产亚洲二区| 国产乱人视频| 中文字幕熟女人妻在线| 婷婷色av中文字幕| 欧美激情国产日韩精品一区| 少妇被粗大猛烈的视频| 久久久色成人| 国产高清三级在线| 亚洲欧美精品自产自拍| 色综合站精品国产| 99久国产av精品| 伦精品一区二区三区| 日韩欧美精品v在线| 天堂√8在线中文| 国产精品久久久久久精品电影小说 | 老司机福利观看| 亚洲在久久综合| 亚洲成人中文字幕在线播放| 女人十人毛片免费观看3o分钟| 国产精品久久久久久久久免| 老熟妇乱子伦视频在线观看| 亚洲一级一片aⅴ在线观看| 99久国产av精品国产电影| 可以在线观看毛片的网站| 中文字幕av成人在线电影| 亚洲内射少妇av| 精品一区二区三区视频在线| 欧美变态另类bdsm刘玥| 国产一区二区在线观看日韩| 欧美色视频一区免费| 啦啦啦韩国在线观看视频| 国产乱人视频| 少妇裸体淫交视频免费看高清| 成人二区视频| 在线天堂最新版资源| 黑人高潮一二区| 国产人妻一区二区三区在| 久久久久久久久中文| 国产亚洲5aaaaa淫片| 亚洲欧美日韩卡通动漫| 精品久久久久久久久久免费视频| 国产极品天堂在线| 亚洲婷婷狠狠爱综合网| 久久这里有精品视频免费| 亚洲精品亚洲一区二区| 一夜夜www| 日本三级黄在线观看| 免费观看在线日韩| 九九热线精品视视频播放| 少妇熟女欧美另类| 色5月婷婷丁香| 欧美bdsm另类| 一级毛片我不卡| 午夜精品一区二区三区免费看| 日本黄大片高清| 国产一区二区激情短视频| 午夜福利视频1000在线观看| 看黄色毛片网站| 成人三级黄色视频| 国产精品久久久久久av不卡| 国产伦精品一区二区三区四那| 久久久午夜欧美精品| 日本爱情动作片www.在线观看| 尤物成人国产欧美一区二区三区| 国产高潮美女av| 精品久久久久久久久av| 欧美丝袜亚洲另类| av福利片在线观看| 国国产精品蜜臀av免费| 亚洲欧美精品综合久久99| 国产高清不卡午夜福利| 国产一区二区三区在线臀色熟女| 尤物成人国产欧美一区二区三区| 欧美+亚洲+日韩+国产| 一级二级三级毛片免费看| 成人亚洲精品av一区二区| 夜夜看夜夜爽夜夜摸| 一级毛片电影观看 | 性欧美人与动物交配| 一个人看的www免费观看视频| 久久久久久久久大av| 久久韩国三级中文字幕| 又黄又爽又刺激的免费视频.| 神马国产精品三级电影在线观看| 日韩成人av中文字幕在线观看| 女的被弄到高潮叫床怎么办| 成人毛片a级毛片在线播放| 免费看美女性在线毛片视频| 国产精品麻豆人妻色哟哟久久 | 日本黄色视频三级网站网址| 校园人妻丝袜中文字幕| 99久久精品一区二区三区| 国产av在哪里看| 好男人视频免费观看在线| 99精品在免费线老司机午夜| 国内揄拍国产精品人妻在线| 国产黄色视频一区二区在线观看 | 婷婷色综合大香蕉| 99久国产av精品国产电影| 日日摸夜夜添夜夜添av毛片| 深夜精品福利| 成熟少妇高潮喷水视频| 一区二区三区高清视频在线| 色播亚洲综合网| 成人美女网站在线观看视频| 深夜a级毛片| 日本一二三区视频观看| 久久久久久久久久成人| 色哟哟·www| 亚洲av不卡在线观看| 熟女电影av网| 国产精品精品国产色婷婷| 亚洲精品乱码久久久v下载方式| 国产精品一区二区性色av| 深爱激情五月婷婷| 老师上课跳d突然被开到最大视频| 中文字幕av成人在线电影| 69人妻影院| 又爽又黄a免费视频| 国内少妇人妻偷人精品xxx网站| 亚洲欧洲日产国产| 直男gayav资源| 亚洲精品亚洲一区二区| 日韩av在线大香蕉| 亚洲国产日韩欧美精品在线观看| 国产高清视频在线观看网站| 极品教师在线视频| 边亲边吃奶的免费视频| 国产成人影院久久av| 91狼人影院| 丰满人妻一区二区三区视频av| 麻豆精品久久久久久蜜桃| av天堂中文字幕网| 中文字幕熟女人妻在线| 久久精品国产鲁丝片午夜精品| 91久久精品电影网| 免费人成视频x8x8入口观看| 国产午夜精品一二区理论片| 中文精品一卡2卡3卡4更新| 晚上一个人看的免费电影| 欧美精品一区二区大全| 两个人视频免费观看高清| 国产高清三级在线| 白带黄色成豆腐渣| 在线免费观看的www视频| 国产单亲对白刺激| 精品人妻偷拍中文字幕| 69av精品久久久久久| 午夜久久久久精精品| 日韩av不卡免费在线播放| 国产成人a∨麻豆精品| 国产在线精品亚洲第一网站| 黄片无遮挡物在线观看| 亚洲va在线va天堂va国产| 麻豆一二三区av精品| 26uuu在线亚洲综合色| 久久九九热精品免费| 精品少妇黑人巨大在线播放 | 日本欧美国产在线视频| 欧美激情久久久久久爽电影| 在线观看一区二区三区| 夜夜夜夜夜久久久久| 人体艺术视频欧美日本| 亚洲欧美日韩卡通动漫| 成人一区二区视频在线观看| 日韩中字成人| 麻豆成人午夜福利视频| 日韩,欧美,国产一区二区三区 | 熟女人妻精品中文字幕| 高清在线视频一区二区三区 | www.色视频.com| 丝袜美腿在线中文| 99久久人妻综合| 边亲边吃奶的免费视频| 久久韩国三级中文字幕| 国产精品99久久久久久久久| 婷婷亚洲欧美| 欧美又色又爽又黄视频| а√天堂www在线а√下载| 观看免费一级毛片| 精品不卡国产一区二区三区| 搡老妇女老女人老熟妇| 日韩大尺度精品在线看网址| 日韩欧美 国产精品| 18禁在线播放成人免费| 久久精品国产亚洲av天美| 日本黄大片高清| 成年女人永久免费观看视频| 如何舔出高潮| 欧美又色又爽又黄视频| 成人漫画全彩无遮挡| 国产日韩欧美在线精品| 久久久久久久久大av| 99久久精品国产国产毛片| 搞女人的毛片| 欧美性猛交黑人性爽| 中出人妻视频一区二区| 亚洲精品日韩在线中文字幕 | 亚洲欧美精品专区久久| 日本撒尿小便嘘嘘汇集6| 国产亚洲精品久久久久久毛片| 深爱激情五月婷婷| 日韩 亚洲 欧美在线| 婷婷亚洲欧美| 欧美又色又爽又黄视频| 美女xxoo啪啪120秒动态图| 国产大屁股一区二区在线视频| 久久久久久九九精品二区国产| 国产精品日韩av在线免费观看| 51国产日韩欧美| 亚洲欧美日韩东京热| 国产蜜桃级精品一区二区三区| 国产精品伦人一区二区| 国产极品天堂在线| 少妇人妻精品综合一区二区 | 午夜老司机福利剧场| 亚洲欧美日韩高清在线视频| 国产成年人精品一区二区| 国产精品久久电影中文字幕| 一区福利在线观看| 一级av片app| 久久欧美精品欧美久久欧美| 最近的中文字幕免费完整| 寂寞人妻少妇视频99o| 六月丁香七月| 国产白丝娇喘喷水9色精品| 欧美性感艳星| 国产欧美日韩精品一区二区| 搡女人真爽免费视频火全软件| 桃色一区二区三区在线观看| 天堂中文最新版在线下载 | 九草在线视频观看| 亚洲av熟女| 欧美+日韩+精品| 久久久久久久久大av| 亚洲精品456在线播放app| 久久精品91蜜桃| 天天躁日日操中文字幕| kizo精华| 听说在线观看完整版免费高清| 久久精品国产亚洲av天美| 亚洲精品亚洲一区二区| 禁无遮挡网站| 成人特级黄色片久久久久久久| 国产精品久久视频播放| 国语自产精品视频在线第100页| 日本av手机在线免费观看| 日韩在线高清观看一区二区三区| 九九热线精品视视频播放| 久久久久久久亚洲中文字幕| 一本—道久久a久久精品蜜桃钙片 精品乱码久久久久久99久播 | 日本与韩国留学比较| 免费观看的影片在线观看| 黄色配什么色好看| 少妇猛男粗大的猛烈进出视频 | 春色校园在线视频观看| 精品熟女少妇av免费看| 午夜老司机福利剧场| 看免费成人av毛片| 岛国在线免费视频观看| 搞女人的毛片| 日日干狠狠操夜夜爽| 国产探花极品一区二区| 在线观看美女被高潮喷水网站| 国产亚洲精品av在线| 亚洲国产欧美人成| 美女被艹到高潮喷水动态| 亚洲av.av天堂| 国产精品永久免费网站| 日日撸夜夜添| 久久久久久久亚洲中文字幕| 又粗又硬又长又爽又黄的视频 | www.色视频.com| 亚洲av不卡在线观看| 2022亚洲国产成人精品| 久久精品国产亚洲网站| 自拍偷自拍亚洲精品老妇| a级毛色黄片| 精品人妻偷拍中文字幕| 欧美成人a在线观看| 欧美人与善性xxx| 亚洲av一区综合| 成人午夜精彩视频在线观看| 色综合站精品国产| 欧美日本视频| 美女xxoo啪啪120秒动态图| 日韩欧美在线乱码| 久久精品综合一区二区三区| 免费一级毛片在线播放高清视频| 有码 亚洲区| 天堂网av新在线| 久久精品国产清高在天天线| 精品久久久噜噜| 国产精品免费一区二区三区在线| 又黄又爽又刺激的免费视频.| 久久久久久久久久黄片| 99热这里只有是精品50| 国产精品国产三级国产av玫瑰| 国产综合懂色| 全区人妻精品视频| 欧美一区二区亚洲| 人人妻人人看人人澡| 国产一区二区激情短视频| 国产伦精品一区二区三区四那| 又粗又硬又长又爽又黄的视频 | 久久久久久久久大av| 国产精品永久免费网站| 国产精品,欧美在线| 男女那种视频在线观看| 美女黄网站色视频| 99久久成人亚洲精品观看| 午夜a级毛片| 亚洲国产精品久久男人天堂| www.色视频.com| 亚洲不卡免费看| 12—13女人毛片做爰片一| 美女内射精品一级片tv| 国产成人一区二区在线| 亚洲电影在线观看av| 麻豆成人午夜福利视频| 女人被狂操c到高潮| 日韩av不卡免费在线播放| 久久人人爽人人爽人人片va| 亚洲久久久久久中文字幕| 日韩欧美精品v在线| 美女内射精品一级片tv| 久久久久免费精品人妻一区二区| 亚洲精品色激情综合| 国产v大片淫在线免费观看| 久久鲁丝午夜福利片| 免费看a级黄色片| 国产一区二区激情短视频| 国产精品久久久久久精品电影| 亚洲国产精品成人综合色| 小蜜桃在线观看免费完整版高清| 美女大奶头视频| 好男人在线观看高清免费视频| 国产精品99久久久久久久久| 久久久久久国产a免费观看| 国产亚洲av片在线观看秒播厂 | 青春草亚洲视频在线观看| 九九爱精品视频在线观看| 精品一区二区三区人妻视频| 在线观看美女被高潮喷水网站| 欧美最黄视频在线播放免费| 九九久久精品国产亚洲av麻豆| 精品人妻熟女av久视频| 一个人看的www免费观看视频| 亚洲国产欧美人成| 亚洲精品乱码久久久v下载方式| 2021天堂中文幕一二区在线观| av免费观看日本| 黄色日韩在线| 亚洲精品日韩av片在线观看| 男女视频在线观看网站免费| 国产伦理片在线播放av一区 | 国产成人精品婷婷| 午夜激情福利司机影院| 熟女电影av网| 一夜夜www| 91精品一卡2卡3卡4卡| 哪里可以看免费的av片| 日本三级黄在线观看| 亚洲精品成人久久久久久| 精品一区二区三区视频在线| 全区人妻精品视频| 日本av手机在线免费观看| 亚洲在久久综合| 亚洲五月天丁香| 日本黄大片高清| 人妻少妇偷人精品九色| 亚洲自拍偷在线| 高清毛片免费看| 五月玫瑰六月丁香| 亚洲人成网站在线观看播放| 国产精品女同一区二区软件| 欧美最新免费一区二区三区| 亚洲欧美日韩高清专用| 久久精品人妻少妇| 欧美3d第一页| 午夜a级毛片| 国产日韩欧美在线精品| 久久久久久大精品| 伦理电影大哥的女人| 国产亚洲精品久久久com| 欧美精品一区二区大全| 亚洲精品456在线播放app| 久久久久久久久大av| 亚洲欧美日韩高清在线视频| 免费看美女性在线毛片视频| 日本成人三级电影网站| 好男人在线观看高清免费视频| 一区二区三区高清视频在线| 久久久国产成人精品二区| 最新中文字幕久久久久| 亚洲人成网站在线播| 亚洲av男天堂| 午夜视频国产福利| 一级毛片久久久久久久久女| 在线观看免费视频日本深夜| 少妇人妻精品综合一区二区 | 麻豆精品久久久久久蜜桃| 精品国产三级普通话版| 成人美女网站在线观看视频| 美女xxoo啪啪120秒动态图| 人人妻人人澡人人爽人人夜夜 | 国产精品日韩av在线免费观看| 中国美白少妇内射xxxbb| 国产成人a∨麻豆精品| 我的老师免费观看完整版| 亚洲人与动物交配视频| av免费观看日本| 日本一本二区三区精品| 狂野欧美激情性xxxx在线观看| 亚洲欧美日韩东京热| videossex国产| 亚洲成人久久性| 国产一级毛片在线| 丰满人妻一区二区三区视频av| 日韩欧美在线乱码| 99国产精品一区二区蜜桃av| 国产免费一级a男人的天堂| 国产麻豆成人av免费视频| av免费观看日本| 亚洲av成人精品一区久久| 综合色av麻豆| 黄色配什么色好看| 麻豆国产av国片精品| av免费观看日本| 成人美女网站在线观看视频| 欧美日韩乱码在线| 天堂中文最新版在线下载 | 男人舔奶头视频| 亚洲人与动物交配视频| 精品久久久久久久久亚洲| 久久久精品大字幕| 听说在线观看完整版免费高清| 大香蕉久久网| 国产真实乱freesex| 中文欧美无线码| 中文字幕人妻熟人妻熟丝袜美| 日韩强制内射视频| 婷婷精品国产亚洲av| 99在线视频只有这里精品首页| 美女大奶头视频| 午夜精品一区二区三区免费看| 黄色视频,在线免费观看| 黄色日韩在线| 熟女人妻精品中文字幕| 欧美日韩精品成人综合77777| 成人综合一区亚洲| 69人妻影院| 欧美三级亚洲精品| 午夜激情欧美在线| 久久亚洲精品不卡| a级一级毛片免费在线观看| 狠狠狠狠99中文字幕| 欧美高清成人免费视频www| 一夜夜www| 人妻夜夜爽99麻豆av| 久久午夜亚洲精品久久| 深夜a级毛片| 最近最新中文字幕大全电影3| 国产成人福利小说| 一个人看视频在线观看www免费| 久久久色成人| 亚洲精品自拍成人| 精品久久久久久久久久久久久| 97在线视频观看| 黄色日韩在线| 欧美xxxx性猛交bbbb| 精品国产三级普通话版| 国产欧美日韩精品一区二区| 精品免费久久久久久久清纯| 国产精品一区二区性色av| 亚洲av不卡在线观看| 亚洲av免费在线观看| 亚洲成av人片在线播放无| 午夜福利在线观看吧| av在线观看视频网站免费| 十八禁国产超污无遮挡网站| 久久综合国产亚洲精品| 三级国产精品欧美在线观看| 干丝袜人妻中文字幕| 亚洲自偷自拍三级| www.av在线官网国产| 亚洲人与动物交配视频| 热99在线观看视频| 亚洲丝袜综合中文字幕| 精品久久久久久久末码| 久久欧美精品欧美久久欧美| 观看免费一级毛片| 一级毛片久久久久久久久女| 两个人的视频大全免费| 久久草成人影院| 亚洲精品粉嫩美女一区| av天堂中文字幕网| 狂野欧美白嫩少妇大欣赏| 草草在线视频免费看| 亚洲人成网站在线观看播放| 最近手机中文字幕大全| 精品人妻视频免费看| 国产精品电影一区二区三区| 国产精品久久视频播放| 91aial.com中文字幕在线观看| 99热精品在线国产| 91久久精品国产一区二区成人| 亚洲精品日韩在线中文字幕 | 欧美性猛交╳xxx乱大交人| 波野结衣二区三区在线| 欧美丝袜亚洲另类| 日本五十路高清| 乱码一卡2卡4卡精品| а√天堂www在线а√下载| 国产精品综合久久久久久久免费| 女的被弄到高潮叫床怎么办| 欧美性猛交黑人性爽| 亚洲av二区三区四区| 简卡轻食公司| 色综合亚洲欧美另类图片| 久久久久免费精品人妻一区二区| 男插女下体视频免费在线播放| av在线观看视频网站免费| 国产色婷婷99| 欧美在线一区亚洲| 国产av在哪里看| 99热精品在线国产| 毛片一级片免费看久久久久| 亚洲真实伦在线观看|