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Proceedings of 2013 IAHR Congress © 2013 Tsinghua University Press, Beijing

ABSTRACT: A two-dimensional tidal wave model for the Chinese marginal seas with high resolution is set up and the verification results demonstrate that it can well simulate the large domain. Based on this model, a series of numerical experiments are constructed to analyze the influence of local bathymetry and reclamation of the Jiangsu coast on the tidal wave system. According to the simulation results, the existence of the radial tidal current pattern have not been obviously influenced by the local bathymetry except the magnitude of the current velocity. However, it effects the tidal wave near the Jiangsu coast considerably. The reclamation affects the radial current field slightly, whereas the tidal wave near the southern Jiangsu coast is impacted significantly. Besides, further experiments by adding thin dam in the Southern Yellow Sea are studied and discussed. The results illustrate the existence of the tidal wave from the Northern Yellow Sea, which is important for the formation of the rotating tidal wave system in the Southern Yellow Sea.

KEY WORDS: Southern Yellow Sea, Jiangsu coast, Rotating tidal wave system, Tidal current, Delft3D. 1 INTRODUCTION

The Southern Yellow Sea (SYS) is a semi-enclosed shelf sea with the average water depth less than 45 m (Tang, 1989). China coast is located in the west and northwest part and Korean Peninsula is situated in the east part. It connects the East China Sea in the south and the Northern Yellow Sea (NYS) in the north. Its geographic location decides that there is a unique tidal wave system. In this region, the semi-diurnal tides are the dominant tidal constituents and there is a rotating tidal wave system near the Jiangsu coast.

Jiangsu coast, located in the east of the SYS, has the advantage of unique location and plenty of potential land resources. The radial sand ridge field is in the central Jiangsu coast and has become a hot issue in recent years due to its distinctive shape and complicated hydrodynamic conditions. It covers an area of 2×104 km2 and the water depth is less than 25 m (Zhang et al., 2009). Tide is the main hydrodynamic factor in this region (Zhu et al., 1998). Zhang et al. (1996) built a tidal wave numerical model for the Chinese marginal seas and analyzed the relationship between the radial sand ridges and the M2 tide. Ye (2012) used a two-dimensional tidal model for the Yellow Sea to simulate the hydrodynamic

Further Research on the Tidal Wave System in the Southern

Yellow Sea

Min Su

PhD student, Faculty of Civil Engineering and Geosciences, Delft University of Technology, Delft, 2600 GA, The Netherlands; College of Harbour, Coastal and Offshore Engineering, Hohai University, Nanjing 210098, China. Email: M.Su@tudelft.nl

Zhengbing Wang

Professor, Faculty of Civil Engineering and Geosciences, Delft University of Technology, Delft, 2600 GA The Netherlands; Deltares, Delft, 2600 MH, The Netherlands. E-mail: Zheng.Wang@deltares.nl

Changkuan Zhang

Professor, College of Harbour, Coastal and Offshore Engineering, Hohai University, Nanjing 210098, China. E-mail: ckzhang@hhu.edu.cn

Peng Yao

PhD student, Faculty of Civil Engineering and Geosciences, Delft University of Technology, Delft, 2600 GA, The Netherlands. Email: P.Yao@tudelft.nl

M.J.F. Stive

Professor, Faculty of Civil Engineering and Geosciences, Delft University of Technology, Delft, 2600 GA, The Netherlands.. Email: M.J.F.Stive@tudelft.nl

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and morphological evolution of the radial sand ridges. Zhang et al. (1998) summarized the dynamic mechanism of the evolution of the radial sand ridges to be “Tidal current-induced formation -- storm-induced change -- tidal current-induced recovery”.

The question whether the submarine topography generates the radial tidal current field or not has been a controversial problem for a long time. Zhu et al. (2001) built a two-dimensional tidal model to study the M2 tide in the radial sand ridges area, using a flat bottom and a shelving slope. It is demonstrated that the tidal current field is independent of the bottom topography and might exist before the radial sand ridges is formed. However, Ye (2012) argued that the radial tidal current field would disappear when the topography of the whole Yellow Sea is set to be a horizontal flat bed. Furthermore, he claimed that other mechanisms such as the waves and storms are more important for the formation of radial sand ridges. However, few researches pay attention to the change of the tidal wave when the local bathymetry is changed.

Jiangsu coast has abundant tidal flat, which account for ¼ of the resources in China (Tao et al., 2011). “The Developing Plan for Jiangsu Coastal Zone” was approved by the Chinese government in 2009 in order to have an integrated reclamation planning of this resource and it plans to have reclamation of 1800 km2 between 2010 and 2020. Some researches have analyzed the influence of the tidal flat reclamation project of Jiangsu coast, but most of them focus on one of the reclamation projects, such as the evolution of Tiaozini (Shen et al., 2000; Zhang, 2005) or the possibility of deep water port (Li et al., 2011). Tao et al. (2011) analyzed the influence of reclamation on the M2 tide, as well as the current velocity and tidal prism in the tidal inlets by a local model. While it is also important to understand the large-scale influence of the reclamation on the tidal wave system.

There are a few researches paying attention to the tidal wave system in the SYS. Shen (1993) considered the tidal wave system in the Yellow Sea by adding a thin dam in the central of Yellow Sea and dividing the domain into two parts. He gave the conclusion that the semi-diurnal tidal wave system in the Yellow Sea is the combination of two independent tidal wave systems. Besides, Lin (2000) insisted that the formation and characteristics of the tidal wave system in the Southern Yellow Sea were mainly depended on the surrounding coastline formed by the Shandong Peninsula and Jiangsu coast.

In this paper, a two-dimensional tidal wave numerical model of the Chinese marginal seas is set up first. Based on it, a series of sensitivity experiments are carried out to investigate the influence of local bathymetry and reclamation on the tidal wave and tidal current in the SYS. Then, a further research about the tidal wave system in the SYS is carried out in order to obtain a better understanding of the tidal wave system.

2 STUDY METHODS 2.1 Model Set Up

The tidal wave model is based on Delft3D modeling system (Deltares, 2012) and mainly focuses on the study of tide propagation in the Chinese marginal seas, especially the Jiangsu coast in the SYS (Su et al., 2013). The domain is shown in Figure 1 and the resolution of the grids is relatively high. In the region around the Jiangsu coast, it is about 0.7'×0.7' (Figure 2).

In the model, 13 tidal constituents are considered along the open boundary as the driving force. Meanwhile, 14 rivers such as the Huai River in the Jiangsu Province and the Yangtze River with the largest discharge, are included in this domain. Besides, this model takes the influence of tidal generating force into account. The simulation period is set to be two months (from August 1st to October 1st, 2006). The time step is 1 minute.

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118 120 122 124 126 128 130 25 30 35 40 Longitude (degree)  Lat it ude ( deg ree)  Ko rea n Pe n isula open boun dary 2  Open bound ary 1  Shand ong Pe ninsula Japanese archipelago

East China Sea Bohai Sea

Yellow Sea

Jiangsu Coast

N

Figure 1 The domain of the Chinese marginal seas Figure 2 The grid near the Jiangsu coast

2.2 Model Performance

There are 190 water level observation points and 14 current velocity observation stations in the whole domain for the verification (Figure 3). With respect to the SYS, there are 8 stations for the tidal currents verification and 6 points for the water level verification near the Jiangsu coast. Here we only take the points in the SYS as an example to show the model performance.

Figure 3 Distribution of the observation points in the domain

The detailed comparisons between calculated and observed harmonic constants of M2 tide constituent are listed in the Table 1. It is found that the model results are in good agreement with the observations. However, the relatively larger deviations in some points (for example, Lvsi port), which also happed in other researches (Ye, 2012), illustrate that the grids are still too coarse to simulate the hydrodynamic conditions accurately in such complex topography.

Furthermore, tidal velocities at 8 observation stations are verified, of which 4 stations are located in the middle of the sea and another 4 near the Jiangsu coast. Here we only take Lianqingshi Fishing Port in the central of the SYS and V1 station near the Jiangsu coast as an example to show the performance of the model. The verification data of the tidal current is the predicted values from the Tide Table and the field

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observations, respectively. The comparison results are shown in Figure 4. It can be seen that the calculated values (both the magnitudes and directions) are in a good agreement with the verification data. In general, this model is in good agreement with the observations and it can be used to simulate the tidal wave and tidal current in the SYS.

Table 1 The comparison of harmonic constant of M2 constituent with the observations (near Jiangsu coast)

Station

Position Observed Calculated

gc-go (°) hc/ho Longitude Latitude Amplitude

(ho) /m Phase (go) /° Amplitude (hc) /m Phase (gc) /° Lianyungang 119°27' 34°45' 1.70 310.16 1.45 309.56 -0.60 0.85 Yanwei 119°47' 34°29' 1.53 320.16 1.32 324.36 4.20 0.87 Sheyang estuary 120°30' 33°49' 0.90 58.16 0.92 53.67 -4.49 1.02 Yangkou port 120°56' 32°36' 2.54 137.16 2.28 143.73 6.57 0.90 Lvsi port 121°35' 32°08' 1.75 124.00 1.38 129.50 5.50 0.79 Lianxing 121°52' 31°41' 1.31 108.16 1.06 101.78 -6.38 0.81 0 0.5 1 0 100 200 300 400 27/08/2006 00:00 29/08/2006 00:00 31/08/2006 00:00 02/09/2006 00:00 04/09/2006 00:00 06/09/2006 00:00 Ve lo ci ty  m ag n it ude  (m /s ) Ve lo city  di re cti o n  (° ) Time Lianqingshi Fishing Port

Calculated value (direction) Predicted value (direction) Calculated value (magnitude) Predicted value (magnitude)

0 1 2 3 4 5 0 100 200 300 400 23/08/2006 00:00 24/08/2006 00:00 25/08/2006 00:00 26/08/2006 00:00 Ve lo ci ty  m ag n it ude  (m /s ) Ve lo city  di re cti o n  (° ) Time V1

Calculated value (direction) Measured value (direction) Calculated value (magnitude) Measured value (magnitude)

Figure 4 The verification of the tidal currents velocity in the Southern Yellow Sea

3 RESULTS AND DISCUSSION

3.1 Co-tidal charts and tidal current field

The tidal wave motions are usually illustrated by the co-tidal charts. The simulated co-tidal charts of 8 principle tide constituents by the model are compared with the co-tidal charts in the Marine Atlas of the Bohai Sea, Yellow Sea and East China Sea (Atlas of the Oceans Editorial Board, 1993), which show a good accordance in both the amplitude and the phase. Figure 5 is the co-tidal charts of M2 constituent simulated by the model. Furthermore, the tidal current ellipses of M2 constituent are generated according to the simulation results (Figure 6). It can be seen clearly that the radial tidal current field exists in the central Jiangsu coast and Jianggang is the focal point of the convergent and divergent currents. During the flood tide in the sand ridges, the tidal currents from the north, northeast and southeast propagate to the Jianggang. Whereas the tidal currents spread from Jianggang during ebb tide.

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Figure 5 The co-tidal charts of the M2 constituent

simulated by the model

Figure 6 The simulated tidal ellipses of M2

constituent in the Chinese marginal seas 3.2 Tidal wave system in the Southern Yellow Sea

There is a rotating tidal wave system and a distinctive radial tidal current field near the Jiangsu coast in the SYS. The formation of the radial tidal currents is considered to be the consequence of the encounter of tidal wave systems. In this section, the influence of local bathymetry and reclamation on the radial tidal currents and tidal wave system is discussed first. At last, 3 cases are designed to study the propagation of the tidal wave system in the SYS.

3.2.1 The influence of local bathymetry on the tidal wave and tidal current

The bathymetry of the radial sand ridges is complicated, with about 10 major ridges and 4 main tidal troughs. Most of the sand ridges are submerged and exposed periodically during tidal cycles. A series of numerical experiments are designed in order to examine the impact of local submarine topography of the Jiangsu coast on the radial tidal current field and the tidal wave system near it. In each case, we use a linear bathymetry and two flat bottom instead of the original topography near the Jiangsu coast, respectively, and leave the bathymetry of other place unchanged. The new bathymetry covers the Jiangsu coast and east part of the Yellow Sea (Figure 7). The water depth of two flat bottoms is about 15 m and 30 m, respectively.

Figure 7 The linear bathymetry of local Jiangsu coast Figure 8 Tidal ellipses of the M2 constituent for

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The simulated tidal ellipses of M2 constituent are shown in Figure 8 and Figure 9. It can be seen that the radial tidal current field still exists centered on the city of Jianggang in both the linear bathymetry and the flat bottom. The unique topography of radial sand ridges does not directly influence the local special flow pattern. The results are in accordance with the previous researches (Zhu and Chang, 2001). The difference among these experiments is the magnitude of the current velocity due to different water depth. In summary, these experiments demonstrate that the radial tidal current field off Jiangsu coast is independent of the local bathymetry. However, whether the radial tidal current exist before the radial sand ridges formed is still uncertain. One of the requirement for the formation of the sand ridges is that the tidal current velocity should have the values between 0.5 – 2.5 m/s (Off, 1963). Although the radial tidal currents exist in this region, the radial sand ridges could not be formed if the magnitude of the velocity is below a certain level.

Figure 9 Tidal ellipses of the M2 constituent of the experiment with flat bottom: 15 m (left) and 30 m (right)

According to our experiments, although the local bathymetry hardly influences the radial tidal current pattern, the tidal wave system is effected considerably. Here we only take the linear bathymetry as an example to illustrate the influence. Figure 10 displays the change of the co-phase lines and the amplitude of M2 tide. The 120° co-phase line near the radial sand ridges is disappeared. And the amplitudes in the radial sand ridges and Haizhou Bay are both decreased. Besides, the amplitude in the southern Jiangsu coast has a growth of 0.4 m. The differences are due to the change of the submarine topography, which influences the local bottom frication and causes the change of the tidal elevation in consequence.

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3.2.3 Reclamation of the radial sand ridges

Jiangsu coast has plenty of potential land resource. The radial sand ridges of the Jiangsu coast is one of the widest intertidal flats in China and the reclamation project is in process. In this section, the influence of the reclamation is analyzed, focusing on the change of hydrodynamic conditions. Figure 11 shows the new coastline after reclamation, in which the red dotted line represents the original coastline and the new boundary is shown by the black line.

Figure 11 The new coastline after the reclamation of the radial sand ridges

The comparisons of the co-tidal chart of M2 constituent with the original model are shown in Figure 12, which mostly focuses on the change of the tidal wave around the Jiangsu coast. In the chart of co-phase lines, the red line indicates the results of the original model and the blue dotted line indicates the resluts after reclamation. The phase-lag around the radial sand ridges becomes smaller in the experiment, which can be seen from the change of the 90° and 120° co-phase lines. That is to say, the tidal wave propagation around the radial sand ridges will be faster after reclamation, especially in the southern Jiangsu coast. But the 60° co-phase line near the Yangtze Estuary moves southward which indicate the slower propagation in that region. The change of local shoreline may cause the reflection and deformity of the tidal wave. Therefore, the amplitude near the southern Jiangsu coast increases greatly (Figure 12b).

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3.2.3 Further investigation of the tidal wave system in the Southern Yellow Sea

We proposed a tidal wave propagation mechanism in the Chinese marginal seas, which suggests that there exist a tidal wave coming from the NYS and propagating along the Shandong Peninsula into SYS (Su et. al, 2013). The combination of the tidal wave from the NYS and the reflected tidal wave of the Shandong Peninsula encounters the progressive tidal wave from the East China Sea, and the rotating tidal wave system in the SYS is formed (Figure 13). In this section, a further research about the tidal wave system will be conducted by adding thin dams with different length to prevent the water exchange.

The thin dam is built in the central of the SYS and begins from the head of the Shandong Peninsula towards southeast. Its direction is basically parallel with the Jiangsu coastline and Korean Peninsula. It divides the SYS into two parts and prevents the water exchange in the center of sea. In order to have a further research about the influence of this thin dam and the tidal wave system in the SYS, three thin dams with different length are implemented in the model respectively (Figure 14). The lengths of the thin dam in three cases are short, medium and long, respectively.

Figure 13 The schematic diagram of the tidal

wave propagation mechanism (from Su et al., 2013)

Figure 14 The sketch map about the location

and length of the thin dams in the cases

The co-tidal charts of these three cases are shown in Figure 15, Figure 16 and Figure 17, respectively. The co-phase lines in the west part of the SYS simulated by the case 2 are almost the same with results of the original model (Figure 18). However, the tidal wave in the same region simulated by the other two cases propagates slower than the original model. The results demonstrate that thin dams with different lengths effect the tidal wave system in the SYS considerably. So, it is not accurate to conclude that the tidal wave system in the Yellow Sea is the combination of the two independent tidal wave systems in the west and east part of the thin dam. Furthermore, the influence of the thin dams with different lengths can be explained by the tidal wave propagation mechanism suggested by Su et al. (2013).

In case 1, the thin dam is short and its influence on the tidal wave system is not obvious, because the tidal wave from the NYS can still propagates along it and come into the west part of the thin dam. But the propagation along the thin dam leads to the delayed propagation. Therefore, the tidal wave in the west part of the thin dam propagates slower than in the original model. However, the co-phase lines underneath the thin dam in the east part of the thin dam change slightly (Figure 15).

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Figure 15 The co-tidal chart of M2 constituent of

case 1 with short thin dam

Figure 16 The co-tidal chart of M2 constituent of

case 2 with medium thin dam

Figure 17 The co-tidal chart of M2 constituent of

case 3 with long thin dam

Figure 18 The comparison of co-phase lines between

the original model (red lines) and the case 2 (blue line) With regard to case 2, the situation is more complicated than case 1. The co-phase lines in the west part of the thin dam are primarily similar to the original results with little increase. However, the tidal wave in the east part propagates slower (Figure 18). These phenomena may be due to a larger percentage of tidal wave spreads into the west part of the thin dam and a smaller percentage propagates into the east part compared with the original model. It can also be obtained from the difference of the 90° and 120° co-phase lines in the south of the SYS (Figure 18). The west part of the 90° co-phase line moves to the northwest greatly, whereas the rest part of it hardly changes. Besides, through the change of 120° co-phase line, we can see the obvious differences on both sides. That is to say, with the propagation of the tidal wave, more and more tidal energy penetrate into the west part of the thin dam leaving much less energy to the east part. Also, the tidal wave from the NYS becomes weaker and may be not able to propagate along the thin dam into the west part. On the other hand, the direction of the tidal wave propagation is perpendicular to the co-phase lines, so if the thin dam is built perpendicularly to the

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co-phase lines of the original model, it would hardly effect the tidal wave propagation in the SYS. However, the angle formed by the thin dam and co-phase lines is not 90° in the case 2, and the percentage of tidal wave into two sides of the thin dam changes as a consequence. Therefore, the tidal wave propagation in the west part of the thin dam is not delayed as in case 1, but almost the same as in the original model or even much faster.

In case 3, the thin dam is so long that it can prevent almost the entire tidal wave from the NYS propagating into the west part of the thin dam. The tidal wave from the NYS encounters the progressive tidal wave from the East China Sea at the east part of the thin dam, forming a rotating tidal wave system in the east of SYS, which is in accordance with the tidal wave theory in the rectangular basin (Figure 17). From the co-amplitude map of case 3, it is clear that there exists a water level difference between the two sides of the thin dam. So, there is water exchange in the end of the thin dam from the west part to the east part, which may induce a tidal wave from west to the east. Thus, compared with case 2, the tidal wave in the west of the thin dam becomes smaller. In consequence, the co-phase lines in the west part in case 3 are behind that in case 2.

Furthermore, it can be concluded that the water exchange in central of SYS is important. Thus, although the tidal wave system in the SYS and the NYS is relatively independent, they indeed have a certain extent relationship. That is, the tidal wave from the NYS and this part of tidal wave is essential for the formation of the rotating tidal wave system in the SYS.

4 CONCLUSIONS

First, in this study, we set up a two-dimensional tidal wave model of the Chinese marginal seas with high resolution. From the analysis of the water level and current velocity, as well as the co-tidal charts of 8 principle tidal constituents, it is concluded that the tidal wave and tidal current can be well reproduced by this model, especially in the southern Yellow Sea near the Jiangsu coast.

Several sensitive experiments are designed and compared with original model. It is found that the radial tidal current pattern near Jiangsu coast is not sensitive to the local bathymetry, but the local bathymetry can affect the tidal wave system considerably. Moreover, the influence of reclamation is also taken into account. It does not bring great influence to the radial tidal current, but the amplitude of the vertical tide in the southern Jiangsu coast increases greatly.

Furthermore, three cases are carried out by adding thin dam in the central of the Southern Yellow Sea and the tidal wave propagation mechanism are studied and discussed in detail. The results illustrate that there exists a part of tidal wave from the Northern Yellow Sea which propagating along the Shandong peninsula to the Jiangsu coast. It is important for the formation of the rotating tidal wave system in the Southern Yellow Sea.

ACKNOWLEDGEMENT

The first author is financially supported by the China Scholarship Council. This work is supported by the 111 Project of the Ministry of Education and the State Administration of Foreign Experts Affairs, China (Grant No. B12032).

References

Atlas of the Oceans Editorial Board, 1993. Marine Atlas of the Bohai Sea, Yellow Sea and East China Sea (Hydrological). The Ocean Press, Beijing. (In Chinese)

Deltares, 2012. Delft3D-FLOW user manual.

Li, M.G., YANG, S., Han, X.J., 2011. On hydro-dynamic sediment problems in the development of deep water port in radial sandbanks. Port & Waterway Engineering, 4, 1-8. (In Chinese)

Lin, H., Lv, G.N., Song, Z.Y., 2000. Tide wave system in East China Sea and simulation of coastal process. The Science Press, Beijing. (In Chinese)

Off, T., 1963. Rhythmic linear sand bodies caused by tidal currents. Assoc. Petroleum Geologists Bull, 47 (2), 324–341.

Shen, Y.J., Huang, D.Y., Qian, C.C., 1993. Preliminary research on the formation of semi-diurnal tidal system in the Yellow Sea. Acta Oceanologica Sinica, 15, 16-24. (In Chinese)

Shen, Y.M., Chen, S.T., Liu, Y.X., 2000. The Study of Promoting Deposit Experimentation Project on Offshore Tide Sands in Jiangsu. Journal of Nanjing Normal University (Natural Science), 23, 120-124. (In Chinese)

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Su, M., Stive, M.J.F., Zhang, C.K., Yao, P., Chen, Y.P., Wang, Z.B., 2013. The tidal wave system in the Chinese marginal seas. In: The 7th International Conference on Coastal Dynamics. (Accepted)

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