Proceedings of 2013 IAHR Congress
© 2013 Tsinghua University Press, Beijing
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: [email protected]
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: [email protected]
Changkuan Zhang
Professor, College of Harbour, Coastal and Offshore Engineering, Hohai University, Nanjing 210098,
China. E-mail: [email protected]
Peng Yao
PhD student, Faculty of Civil Engineering and Geosciences, Delft University of Technology, Delft, 2600
GA, The Netherlands. Email: [email protected]
M.J.F. Stive
Professor, Faculty of Civil Engineering and Geosciences, Delft University of Technology, Delft, 2600 GA,
The Netherlands.. Email: [email protected]
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
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.
2
40
Bohai Sea
N
re a
Ko
la
isu
en
nP
P
ng
nd o
S ha
s ula
enin
35
b
en
op
Latitude (degree) 
Yellow Sea
2
ary
nd
ou

Jiangsu Coast
Japanese archipelago
30
East China Sea
Open bo
un
dary 1

25
118
120
122
124
126
Longitude (degree) 
128
130
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
3
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)
Lianyungang
Yanwei
Sheyang estuary
Yangkou port
Lvsi port
Lianxing
Longitude
Latitude
119°27'
119°47'
120°30'
120°56'
121°35'
121°52'
34°45'
34°29'
33°49'
32°36'
32°08'
31°41'
Calculated
Amplitude Phase
(hc) /m
(gc) /°
1.45
309.56
1.32
324.36
0.92
53.67
2.28
143.73
1.38
129.50
1.06
101.78
gc-go
(°)
hc/ho
-0.60
4.20
-4.49
6.57
5.50
-6.38
0.85
0.87
1.02
0.90
0.79
0.81
Lianqingshi Fishing Port
400
Velocity direction (°)
Observed
Amplitude Phase
(ho) /m
(go) /°
1.70
310.16
1.53
320.16
0.90
58.16
2.54
137.16
1.75
124.00
1.31
108.16
1
300
200
0.5
100
0
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
Velocity magnitude (m/s)
Position
Station
0
06/09/2006 00:00
Time
Predicted value (direction)
Velocity direction (°)
400
Calculated value (magnitude)
Predicted value (magnitude)
5
V1
4
300
3
200
2
100
1
0
23/08/2006 00:00
24/08/2006 00:00
Velocity magnitude (m/s)
Calculated value (direction)
0
26/08/2006 00:00
25/08/2006 00:00
Time
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.
4
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 8 Tidal ellipses of the M2 constituent for
the linear bathymetry
Figure 7 The linear bathymetry of local Jiangsu coast
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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.
Figure 10 The influence of linear Jiangsu bathymetry on the phase-lag (left) and amplitude (right)
6
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).
Figure 12 The influence of the reclamation on the phase-lag (a) and amplitude (b) near Jiangsu coast
7
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).
8
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
9
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).
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