Figure
1.
Typical SAR ISW Images obtained from Sentinel-1 (a–c) and GF-3 (d–f).
| Citation: | Muping Zhou, Changlin Chen, Yunwei Yan, Wenhu Liu. Influence of two inlets of the Luzon overflow on the deep circulation in the northern South China Sea[J]. Acta Oceanologica Sinica, 2020, 39(11): 13-20. doi: 10.1007/s13131-020-1621-1
|
The Malacca Strait with 1 080 km long is the most important energy transport route. Due that the internal solitary waves (ISWs) have great influence on the navigation of ships and submarines, especially, Malacca Strait is the area where the ISWs occur frequently, it is necessary to study the characteristics of the ISWs in Malacca Strait.
It is well known that ISWs phenomenon shows strong randomness, and its amplitude, propagation velocity and wavelength are greatly affected by hydrology and other external environment (Fang and Du, 2005; Li et al., 2013; Alford et al., 2010; Cai and Xie, 2010; Huang et al., 2007; Hyder et al., 2005; Lai et al., 2010). The research of ISWs based on SAR image usually includes the following two aspects. One is to study the temporal and spatial distribution of ISWs. For example, in 2000, Hsu et al. (2000) studied the distribution of ISWs in the South China Sea based on 5-year satellite remote sensing images. Using satellite SAR data from July to October 2007, Kozlov et al. (2015) studied the characteristics of short-period ISWs in the Kara Sea. Filonov et al. (2014) studied the spatial distribution of ISWs of Todos Santos by means of the combination of real measurement and remote sensing. Another one is the imaging mechanism of ISWs on SAR image and the inversion of ISWs parameters. For example, in 2013, Liu et al. (2013) calculated the nonlinear phase velocity of the ISWs in the South China Sea using multi-source remote sensing data, and found that the velocity of the ISWs was greatly affected by the depth of water. In 2016, combined with nonlinear Schrodinger (NLS) equation, our team obtained the inversion model of SAR ISWs parameters, and the inversion results are close to the measured data (Zhang et al., 2016). With the increasing number of satellites in orbit, the understanding of ISWs by multi-source remote sensing becomes to be more and more comprehensive (Jackson, 2007; Schuler et al., 2003).
In a word, there is no research on the ISWs in Malacca Strait up to date. In this paper, ISWs in Malacca Strait are investigated from the spatial distribution of the waves, the velocity and amplitude of the ISWs, and so on, which will provide valuable scientific references for maritime navigation and marine engineering.
The Malacca Strait is located in the region of 0°–6°N and 97°–104°E. In order to observe and analyze the characteristics of ISWs in the Malacca Strait, Sentinel-1 SAR data from June 2015 to December 2016 and GF-3 data from April 2018 to March 2019 are collected. Because of the limitation of SAR orbital period, we obtain 20 Sentinel-1 images and 24 GF-3 images in total, and 344 ISW packets and ISWs are collected.
It can be seen from Fig. 1 that the ISWs in the Malacca Strait mainly appear in the form of wave packets and single solitary waves. Though the direction of ISWs propagation seems to be very complex, however, it always tends to propagate towards the shore.
Furtherly, according to the position and the crest length of the leading wave in the ISW packets in 45 SAR images, the spatial distribution of the wave and the length distribution of the leading wave crest in the Malacca Strait are obtained, which are shown in Fig. 2 and Fig. 3, respectively. As shown in Fig. 2, in region A, the depth of water in this area is about 50–100 m, and the largest wave packets is observed, accompany with a relatively long crest length of the leading wave. In the middle of the Malacca Strait (region B), the water depth is about 20–50 m, the ISW propagates in the form of wave packets and single solitary waves, and the crest length of the leading wave becomes shorter. In the southeast of the Malacca Strait (region C), the water depth is relatively shallow, with the shallowest part of only 4 m, and the ISW is mostly in the form of wave packets and single solitary waves, with the shortest crest length of the leading wave, but it is noticing that the ISWs is broken seriously, and the direction of the ISWs is also relatively messy.
By observed from satellite images, it can be found that there are three to seven ISWs on average in the Malacca Strait, with a maximum of 12 ISWs. The maximum (minimum) crest length of the wave packet is about 39 km (1.5 km) in the Fig. 2, and the crest length of the leading wave becomes to be shorter and shorter towards the southeast. Totally, 344 crest length of the leading wave are observed, in which 35 lines are more than 20 km in length, and most of them are located in the northwest region. In addition, most crest length of the leading wave less than 20 km are located in the regions B and C, and the number of crest length of the leading wave from 4 km to 14 km is about 273 crest lines, which accounts for the vast majority of total lines.
In addition, the occurrence of ISWs has a great relationship with seasons. Figure 4 shows the distribution of ISWs in different seasons. The largest number of ISWs observed from remote sensing images occurred from January to march, and the smallest from October to December. Most of the ISWs observed in SAR images from April to September occurred in region C.
The inversion of the ISWs parameters greatly depends on the two layer stratification. Temperature, salt and density data of the studied area are selected from the annual average data of World Ocean Atlas (2013), and hierarchical information is obtained by calculating the vertical distribution. The calculated temperature, salinity, density and buoyancy frequency curve are showed in Fig. 5. The water depth corresponding to the inflection point of buoyancy frequency in Fig. 5d is the upper water depth, about 25 m. The density corresponding to the upper water depth is found in the density curve, and the upper and lower average densities are calculated as 1 019.9 kg/m3 and 1 020.9 kg/m3 respectively.
Because of the balance between nonlinear effect and dispersion effect, the ISWs can be stable and spread over long distance.
The ISWs propagation equation adopts NLS equation. Combined with the SAR imaging mechanism of the ISWs, the amplitude inversion model of the ISWs based on the SAR image is established (NLS equation) (Zhang et al., 2016).
| $$\left\{ \begin{split} & D = 1.76l,\qquad \alpha \beta > 0\\ & D = 1.32l,\qquad \alpha \beta < 0 \end{split} \right.,$$ | (1) |
| $$\left\{ \begin{split} & {A_0} = \frac{{1.76}}{D}\sqrt {\left| {\frac{{2\alpha }}{\beta }} \right|},\qquad \alpha \beta > 0\\ & {A_0} = \frac{{1.32}}{D}\sqrt {\left| {\frac{{2\alpha }}{\beta }} \right|},\qquad \alpha \beta < 0 \end{split} \right.,$$ | (2) |
where A0 is the amplitude of the ISWs,
Then we apply the NLS amplitude inversion model to the previous 45 SAR images, and extract the distance D between the brightest spot and the darkest spot and hydrological parameters from each SAR image. The amplitude A0 of ISWs can be obtained from Eq. (2). We calculate the amplitude of ISWs happened in the Malacca Strait with water depth greater than 30 m.
By extracting the characteristic parameters of ISWs in the Malacca Strait, the amplitude distribution is obtained, as shown in Fig. 6. In region A, the maximum amplitude obtained by NLS amplitude inversion model is 23.9 m, which is located at the water depth of 78 m, and the average amplitude of ISWs in this area is about 18.4 m. The maximum amplitude in region B calculated by NLS amplitude inversion model is 17.9 m, the minimum amplitude is 4.7 m, and the average amplitude of ISWs is about 10.9 m. The water depth in region C is shallow. The maximum and minimum amplitude calculated by NLS amplitude inversion model are 14.1 m and 4.7 m respectively, and the average amplitude is 9.6 m. In addition, we also analyze the amplitude of the one ISW. Figure 7 is a SAR image from March 14, 2016, we extracted the parameter and calculated the amplitude of ISWs. Each red dot in Fig. 7 is the extraction position of the ISWs parameter, combined with the local depth of water, the relationship between amplitude and depth of water is shown in Fig. 8. From Fig. 8, it can be found that even in the same ISW, the amplitude of ISWs is different, and the amplitude distribution is linearly related to the water depth. Figures 4 and 8 show that in Malacca Strait, with the decrease of water depth, the amplitude decreases. This may be due to the increase of the nonlinear effect of ISWs with the shallow water depth, which leads to the breakage of ISWs.
ISWs in the Malacca Strait can be divided into two types: single solitary waves and solitary wave packets. Therefore, we use NLS equation to derive the group velocity of solitary wave packets and KdV equation to obtain the phase velocity of single solitary waves.
The group velocity formula derived from the NLS equation (Zhang et al., 2015) is
| $${c_g} = \frac{{\rm d\omega }}{{\rm dk}} = \frac{\omega }{{2k}}\left[ {1 + \frac{{2k{h_2}}}{{ {\rm {sh}}(2k{h_2})}}} \right] ,$$ | (3) |
where k is the wave number, h2 is the depth of the lower layer, and
The phase velocity formula obtained by KdV equation (Zheng et al., 2001) is
| $$c = {\left[ {\frac{{g({\rho _2} - {\rho _1}){h_1}{h_2}}}{{{\rho _2}{h_1} + {\rho _1}{h_2}}}} \right]^{1/2}} + \frac{{\alpha {A_0}}}{3}, $$ | (4) |
where hl and h2 are the thickness of the upper and lower layers, respectively, and their water densities are
The propagation velocity of ISWs is affected by many factors, such as water depth, stratification. The two-dimensional water depth distribution map of Malacca Strait has been given in Fig. 2. It can be seen that the depth of the water in the south is the shallower, and the deeper is to the northwest. The distribution characteristics of the group velocity and the phase velocity in Malacca Strait are analyzed. Figure 9 shows the group velocity distribution of ISWs in Malacca Strait calculated by using the group velocity formula derived from the NLS equation. Figure 10 shows the distribution of phase velocity calculated by KdV equation.
As can be seen from Fig. 9, the group velocity of the wave packets reduced from 0.4 m/s to 0.12 m/s and the phase velocity of ISWs in Fig. 10 decreases from 0.6 m/s to 0.26 m/s. In general, the group velocity and phase velocity of ISWs in Malacca Strait are related to the topography.
Based on the Sentinel-1 and GF-3 SAR data, totally 45 SAR images in Malacca Strait are obtained, and the characteristic parameters of the ISWs in Malacca Strait are studied. The distribution of ISWs and crest length of the leading waves in Malacca Strait are statistically analyzed. It is found that ISWs are present in most of Malacca Strait, and the ISWs appear in the form of wave packets and single solitary waves. Furthermore, the direction of ISWs propagation is more complex, but the ISWs always tends to propagate towards the shore. The crest length of the leading wave is the longest in the northwest.
In addition, the group velocity and amplitude distributions of the area are calculated based on the high-order completely NLS equation inversion model. The phase velocity is obtained by KdV equation. The group velocity and phase velocity of ISWs are closely related to water depth and stratification. From northwest to southeast, with the water depth becoming shallow, the group velocity and phase velocity of ISWs becomes smaller. The group velocity distribution is between 0.12 m/s and 0.40 m/s, the phase velocity distribution is between 0.26 m/s and 0.6 m/s, and the amplitude of the ISWs is in the range of 4.7–23.9 m. The general trend of the amplitude and velocity is decreasing, which indicates that with the depth of water decreases, the nonlinearity increases, leading to the breakup of ISWs.
| [1] |
Carnes M R. 2009. Description and Evaluation of GDEM-V3.0. Naval Research Laboratory (NRL) Report NRL/MR/7330-09-9165. Washington, DC: Naval Research Laboratory
|
| [2] |
Chang Y T, Hsu W L, Tai J H, et al. 2010. Cold deep water in the South China Sea. Journal of Oceanography, 66(2): 183–190. doi: 10.1007/s10872-010-0016-x
|
| [3] |
Döös K, Kjellsson J, Jönsson B. 2013. TRACMASS—A Lagrangian trajectory model. In: Soomere T, Quak E, eds. Preventive Methods for Coastal Protection. Heidelberg: Springer, 225–249
|
| [4] |
Garabato A C N, Polzin K L, King B A, et al. 2004. Widespread intense turbulent mixing in the southern ocean. Science, 303(5655): 210–213. doi: 10.1126/science.1090929
|
| [5] |
Godin G. 1966. Daily mean sea level and short-period seiches. International Hydrographic Review, 43(2): 75–89
|
| [6] |
Heywood K J, Garabato A C, Stevens D P. 2002. High mixing rates in the abyssal Southern Ocean. Nature, 415(6875): 1011–1014. doi: 10.1038/4151011a
|
| [7] |
Kunze E, Sanford T B. 1996. Abyssal mixing: Where it is not. Journal of Physical Oceanography, 26(10): 2286–2296. doi: 10.1175/1520-0485(1996)026<2286:AMWIIN>2.0.CO;2
|
| [8] |
Lan Jian, Wang Yu, Cui Fengjuan, et al. 2015. Seasonal variation in the South China Sea deep circulation. Journal of Geophysical Research: Oceans, 120(3): 1682–1690. doi: 10.1002/2014JC010413
|
| [9] |
Lan Jian, Zhang Ningning, Wang Yu. 2013. On the dynamics of the South China Sea deep circulation. Journal of Geophysical Research: Oceans, 118(3): 1206–1210. doi: 10.1002/jgrc.20104
|
| [10] |
Ledwell J R, Montgomery E T, Polzin K L, et al. 2000. Evidence for enhanced mixing over rough topography in the abyssal ocean. Nature, 403(6766): 179–182. doi: 10.1038/35003164
|
| [11] |
Li Li, Qu Tangdong. 2006. Thermohaline circulation in the deep South China Sea basin inferred from oxygen distributions. Journal of Geophysical Research, 111: C05017
|
| [12] |
Liu C T, Liu R J. 1988. The deep current in the Bashi Channel. Acta Oceanographica Taiwanica, 20: 107–116
|
| [13] |
Liu Zhifei, Stattegger K. 2014. South China Sea fluvial sediments: An introduction. Journal of Asian Earth Sciences, 79: 507–508. doi: 10.1016/j.jseaes.2013.11.003
|
| [14] |
Mauritzen C, Polzin K L, McCartney M S, et al. 2002. Evidence in hydrography and density fine structure for enhanced vertical mixing over the Mid-Atlantic Ridge in the western Atlantic. Journal of Geophysical Research, 107(C10): 3147. doi: 10.1029/2001JC001114
|
| [15] |
Qu Tangdong. 2002. Evidence for water exchange between the South China Sea and the Pacific Ocean through the Luzon Strait. Acta Oceanologica Sinica, 21(2): 175–185
|
| [16] |
Qu Tangdong, Girton J B, Whitehead J A. 2006. Deepwater overflow through Luzon Strait. Journal of Geophysical Research: Oceans, 111: C01002
|
| [17] |
Shao Lei, Li Xuejie, Geng Jianhua, et al. 2007. Deep water bottom current deposition in the northern South China Sea. Science in China Series D: Earth Sciences, 50(7): 1060–1066. doi: 10.1007/s11430-007-0015-y
|
| [18] |
Shu Yeqiang, Xue Huijie, Wang Dongxiao, et al. 2014. Meridional overturning circulation in the South China Sea envisioned from the high-resolution global reanalysis data GLBa0.08. Journal of Geophysical Research: Oceans, 119(5): 3012–3028. doi: 10.1002/2013JC009583
|
| [19] |
Shu Yeqiang, Xue Huijie, Wang Dongxiao, et al. 2016. Persistent and energetic bottom-trapped topographic Rossby waves observed in the southern South China Sea. Scientific Reports, 6: 24338. doi: 10.1038/srep24338
|
| [20] |
Speer K, Tziperman E, Feliks Y. 1993. Topography and grounding in a simple bottom layer model. Journal of Geophysical Research, 98(C5): 8547–8558. doi: 10.1029/92JC03018
|
| [21] |
St Laurent L, Garrett C. 2002. The role of internal tides in mixing the deep ocean. Journal of Physical Oceanography, 32(10): 2882–2899. doi: 10.1175/1520-0485(2002)032<2882:TROITI>2.0.CO;2
|
| [22] |
Stommel H, Arons A B. 1959–1960a. On the abyssal circulation of the World Ocean-I. Stationary planetary flow patterns on a sphere. Deep Sea Research, 6: 140–154. doi: 10.1016/0146-6313(59)90065-6
|
| [23] |
Stommel H, Arons A B. 1959–1960b. On the abyssal circulation of the World Ocean-II. An idealized model of the circulation pattern and amplitude in oceanic basins. Deep Sea Research, 6: 217–233. doi: 10.1016/0146-6313(59)90075-9
|
| [24] |
Stommel H, Arons A B, Faller A J. 1958. Some examples of stationary planetary flow patterns in bounded basins. Tellus, 10(2): 179–187. doi: 10.3402/tellusa.v10i2.9238
|
| [25] |
Tian Jiwei, Qu Tangdong. 2012. Advances in research on the deep South China Sea circulation. Chinese Science Bulletin, 57(24): 3115–3120. doi: 10.1007/s11434-012-5269-x
|
| [26] |
Tian Jiwei, Yang Qiangxuan, Liang Xinfeng, et al. 2006. Observation of Luzon Strait transport. Geophysical Research Letters, 33(19): L19607. doi: 10.1029/2006GL026272
|
| [27] |
Tian Jiwei, Yang Qingxuan, Zhao Wei. 2009. Enhanced Diapycnal Mixing in the South China Sea. Journal of Physical Oceanography, 39(12): 3191. doi: 10.1175/2009JPO3899.1
|
| [28] |
Wang Aimei, Du Yan, Peng Shiqiu, et al. 2018. Deep water characteristics and circulation in the South China Sea. Deep Sea Research Part I: Oceanographic Research Papers, 134: 55–63. doi: 10.1016/j.dsr.2018.02.003
|
| [29] |
Wang Dongxiao, Wang Qiang, Cai Shuqun, et al. 2019. Advances in research of the mid-deep South China Sea circulation. Science China Earth Sciences, 62(12): 1992–2004. doi: 10.1007/s11430-019-9546-3
|
| [30] |
Wang Dongxiao, Xiao Jingen, Shu Yeqiang, et al. 2016. Progress on deep circulation and meridional overturning circulation in the South China Sea. Science China Earth Sciences, 59(9): 1827–1833. doi: 10.1007/s11430-016-5324-6
|
| [31] |
Wang Guihua, Xie Shangping, Qu Tangdong, et al. 2011. Deep South China Sea circulation. Geophysical Research Letters, 38(5): L05601
|
| [32] |
Wang J. 1986. Observation of abyssal flows in the northern South China Sea. Acta Oceanographica Taiwanica, 16: 36–45
|
| [33] |
Wyrtki K. 1961. Physical oceanography of the Southeast Asian waters. In: NAGA Report Volume 2, Scientific Results of Marine Investigations of the South China Sea and the Gulf of Thailand. San Diego, California: Scripps Institution of Oceanography
|
| [34] |
Yang Jiayan. 2005. The arctic and subarctic ocean flux of potential vorticity and the arctic ocean circulation. Journal of Physical Oceanography, 35(12): 2387–2407. doi: 10.1175/JPO2819.1
|
| [35] |
Yang Jiayan, Price J F. 2000. Water-mass formation and potential vorticity balance in an abyssal ocean circulation. Journal of Marine Research, 58(5): 789–808. doi: 10.1357/002224000321358918
|
| [36] |
Yang Qingxuan, Zhao Wei, Liang Xinfeng, et al. 2016. Three-dimensional distribution of turbulent mixing in the South China Sea. Journal of Physical Oceanography, 46(3): 769–788. doi: 10.1175/JPO-D-14-0220.1
|
| [37] |
Ye Ruijie, Zhou Chun, Zhao Wei, et al. 2019. Variability in the deep overflow through the Heng-Chun Ridge of the Luzon Strait. Journal of Physical Oceanography, 49(3): 811–825. doi: 10.1175/JPO-D-18-0113.1
|
| [38] |
Zhang Yanwei, Liu Zhifei, Zhao Yulong, et al. 2014. Mesoscale eddies transport deep-sea sediments. Scientific Reports, 4(1): 5937
|
| [39] |
Zhang Zhiwei, Zhao Wei, Tian Jiwei, et al. 2015. Spatial structure and temporal variability of the zonal flow in the Luzon Strait. Journal of Geophysical Research: Oceans, 120(2): 759–776. doi: 10.1002/2014JC010308
|
| [40] |
Zhao Wei, Zhou Chun, Tian Jiwei, et al. 2014. Deep water circulation in the Luzon Strait. Journal of Geophysical Research: Oceans, 119(2): 790–804. doi: 10.1002/2013JC009587
|
| [41] |
Zheng Hongbo, Yan Pin. 2012. Deep-water bottom current research in the Northern South China Sea. Marine Georesources and Geotechnology, 30(2): 122–129. doi: 10.1080/1064119X.2011.586015
|
| [42] |
Zhou Chun, Zhao Wei, Tian Jiwei, et al. 2014. Variability of the deep-water overflow in the Luzon Strait. Journal of Physical Oceanography, 44(11): 2972–2986. doi: 10.1175/JPO-D-14-0113.1
|
| [43] |
Zhou Chun, Zhao Wei, Tian Jiwei, et al. 2017. Deep western boundary current in the South China Sea. Scientific Reports, 7(1): 9303. doi: 10.1038/s41598-017-09436-2
|
Figures(9) / Tables(1)
Supported by:
Beijing Renhe Information Technology Co. Ltd
SUSANTO R Dwi, WEI Zexun, ADI Rameyo T, FAN Bin, LI Shujiang, FANG Guohong. Observations of the Karimata Strait througflow from December 2007 to November 2008[J]. Acta Oceanologica Sinica, 2013, 32(5): 1-6. doi: 10.1007/s13131-013-0307-3
DownLoad:
