J Oceanogr (2011) 67:359–363
DOI 10.1007/s10872-011-0063-y

SPECIAL SECTION: EDITORIAL

Regional Environmental Oceanography in the South
China Sea and Its Adjacent Areas (REO-SCS): I

Introduction to the special section on regional environmental
oceanography in the South China Sea and its adjacent areas(REO-SCS)
Jianyu Hu • Jiayi Pan • Xinyu Guo •Quanan Zheng

Published online: 9 August 2011Ó The Oceanographic Society of Japan and Springer 2011

1 Introduction

2 The South China Sea dynamics

The South China Sea (SCS) plays important roles in theinteractions between the Pacific and Indian Oceans andbetween the Asian continent and the oceans. In recent
years, oceanographers, especially those from surrounding
countries and regions, have carried out several government-supported projects in the SCS and have harvested
valuable in situ measurements, satellite data, and numericalmodeling results. In order to deliver these new results to
the regional environmental oceanography community, weorganize and edit a special section entitled ‘‘Regional
Environmental Oceanography in the South China Sea and
Its Adjacent Areas (REO-SCS)’’. We hope that this section
will contribute to the promotion of regional environmental
oceanography research and serve as a platform for thecommunity to exchange and share ideas and results. This
special section appears in two issues in Journal of
Oceanography (Nos. 4 and 5, Vol. 67).

The SCS is an important area connecting the tropical
Pacific Ocean with the Indian Ocean through the South
China Sea Throughflow (Fang et al. 2002; Qu et al. 2006a;
Wang et al. 2006; Tozuka et al. 2009). It is a semi-enclosed
marginal sea with a deep basin and broad shelves. As it isaffected by the seasonal solar radiation, monsoon, and thesurrounding continent and islands, the temperature in the
SCS has a significant seasonal variation. The sea surface
temperature (SST) ranges are 20–28, 26–28, 27–30, and
23–29°C in winter, spring, summer, and autumn, respectively. In winter, a typical Luzon cold eddy appears at depths
from 50 downward to 300 m to the west of Luzon Island(Yang and Liu 1998). It has a spatial scale of 300–400 km anda temperature difference of at least 3–4°C between the coldcore and its surroundings at 100 m depth. In summer, theVietnam cold eddy (spatial scale 200–300 km, temperature
difference 3–4°C) exists east off the Vietnamese coast (Guoet al. 2004; Su and Yuan 2005; Sun 2006).
The annual mean salinity in the SCS is about 34.0 psu(Su and Yuan 2005). The sea surface salinity is lower in thenorthern SCS, particularly in the sea area off the Pearl
River (the Zhujiang River) where the Pearl River plume
extends offshoreward and forms a strong salinity front. In
the SCS basin, the water is stratified in 4 layers of different
salinity: relatively low salinity surface water (thickness
50–100 m, S 33.50–34.50 psu), relatively high salinity
subsurface water (between 100 and 300 m, S [ 34.60 psu),
low salinity intermediate water (300–900 m, S \ 34.50 psu),
and high salinity deep water (1000–2500 m, S 34.50–
34.60 psu).
The circulation patterns in the SCS and its adjacentareas are very complicated (Hu et al. 2000, 2010; Su 2005;
Fang et al. 2005; Zheng et al. 2006a; Liu et al. 2008b; Isobe

J. Hu (&)
State Key Laboratory of Marine Environmental Science,
Xiamen University, Fujian 361005, Chinae-mail: hujy@xmu.edu.cn
J. PanInstitute of Space and Earth Information Science,
The Chinese University of Hong Kong, Shatin,
N.T., Hong Kong, China
X. GuoCenter for Marine Environmental Studies, Ehime University,
2-5 Bunkyo-Cho, Matsuyama 790-8577, Japan
Q. Zheng
Department of Atmospheric and Oceanic Science,
University of Maryland, College Park, MD 20742, USA

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2008). As a result of the monsoon–mountain interaction,
the seasonal pattern of the sea surface wind stress curl is
spatially non-uniform and therefore induces basin-scale
circulations and gyres together with very active mesoscaleeddies in the SCS (Wang et al. 2003). At the top layer, theSCS current is the Ekman drift influenced by local winds.
The upper layer mean circulation is cyclonic in winter with
one cyclonic eddy west of Luzon Island and anothersoutheast off Vietnam, but in summer it is anticyclonicwith an anticyclonic eddy southeast off Vietnam and acyclonic eddy east of Vietnam coast (Hu et al. 2000). In
addition, the SCS Warm Current (Guan and Fang 2006),
the Kuroshio intrusion into the SCS, and the multiple
mesoscale eddies are also incorporated into the generalseasonal circulation patterns.
The SCS upwelling studies are mainly concentrated in
the northern SCS and its northwestern continental shelf,
especially along the Guangdong coast and the eastern coastof Hainan Island (Gan et al. 2009; Jing et al. 2009; Su andPohlmann 2009). Wu and Li (2003) and Hu et al. (2003)
summarized more than 40 years of upwelling research in
the SCS and the Taiwan Strait, respectively. They concluded that the upwelling is a common phenomenon on thewhole continental shelf in the northern SCS and in the
Taiwan Strait in summer. One major dynamical factor
inducing such upwelling is the prevailing southwesterly
monsoon. Therefore, the summertime upwelling canappear along the northeastern coast of Hainan Island andalong the coasts of Fujian and Guangdong. The upwellingaround the Taiwan Bank is characterized by multi-cellstructure existing year-round with different features interms of chemistry and biology. Additionally, coastal
upwelling also occurs along the eastern coast of Vietnam insummer (Xie et al. 2003) and off the northwestern coast of
Luzon Island in winter (Shaw et al. 1996).

3 Research hotspots related to SCS regional
environmental oceanography
3.1 Hydrodynamics in the Luzon Strait
Being a strong western boundary current in the North
Pacific Ocean, the Kuroshio plays an important role in theseawater volume transport between the North Pacific
Ocean and the SCS. Previous investigations revealed that
the Kuroshio may intrude into the SCS through the Luzon
Strait in many ways (Caruso et al. 2006), such as a direct
branch (Qiu et al. 1985; Yuan et al. 2006), warm-core eddy
(Wang and Chern 1987), looping current (Li and Wu 1989;
Xue et al. 2004; Yuan et al. 2006; Sheu et al. 2010),
detached ring (Li et al. 1998; Yuan et al. 2006), extending
pattern (Hu et al. 2000), westward Rossby wave

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propagation (Hu et al. 2001; Wang et al. 2008), eddy
shedding process (Jia and Liu 2004; Jia et al. 2005), and as
ocean vortex trains (Zheng et al. 2008). Some researchers
also focused on the deep water overflow through the Luzon
Strait (Qu et al. 2006b) and the flow pattern in the intermediate layer of the Luzon Strait (Yuan et al. 2008; Xieet al. 2011a). The volume transport through the Luzon
Strait was estimated to range from 0.5 to 10 Sv (Wyrtki
1961; Metzger and Hurlburt 1996; Qu et al. 2000; Fanget al. 2005; Tian et al. 2006; Yang et al. 2010). However,the Kuroshio intrusion and the volume transport throughthe Luzon Straitremain disputed.
3.2 Near-inertial oscillation in the SCS
Near-inertial oscillation (NIO) is one of the significant
components affecting upper ocean dynamics, particularlyin the coastal oceans and continental shelves. The majormechanism for the NIO generation is believed to be sudden
rising of wind stress caused by typhoons or storms (orhurricanes as mentioned in some references). Several fieldobservations revealed strong near-inertial current in thewake of hurricanes (Shay and Elsberry 1987; Xie et al.
2009). Other mesoscale processes, such as eddies and loop
currents, may modify the NIO propagation and induce the
NIO frequency shift (Shay et al. 1998; Zhai et al. 2007;
Oey et al. 2008).
The SCS has usually experienced frequent typhoon andtropical storm events, averaging up to 15 occurrences per
year according to historical records. In addition, the SCS
has variable hydrographic structures and circulation patterns due to the alternating monsoonal winds. The topography, stratification, and background flow are supposed tohave significant influence on characteristics of the NIOs.
Chu et al. (2000) employed the Princeton Ocean Model tosimulate the response of upper SCS to tropical cyclone
Ernie in 1996, and the simulation indicated the existence of
the NIO-induced surface divergent currents. Zhang et al.
(2005) studied the NIO at the upper 450 m of the northern
SCS. Using the buoy or mooring observation data, Zhang
et al. (2007) and Zhu and Li (2007) reported a typhooninduced NIO in the deep basin SCS and the near-shore area
off Hainan Island, respectively.
McComas and Bretherton (1977) predicted that theparametric subharmonic instability (PSI) of internal tides
would lead to the generation of NIO waves. The SCS is
located between 2.5 and 23.5°N, i.e., crossing the criticallatitudes at which PSI of diurnal internal tides occurs(13.44°N for O1 tide and 14.52°N for K1 tide). Thus, the
PSI mechanism should be considered as an importantfactor for generating the NIO waves in the SCS. Recently,
Alford (2008) studied the NIO led by the PSI of the diurnal
tides in the eastern SCS. Xie et al. (2009) analyzed theIntroduction to the special section on (REO-SCS): I

influence of PSI on the NIO spectra using mooring acoustic
Doppler current profiler (ADCP) data measured in the SCS
deep basin. They also observed the PSI-induced nearinertial waves equatorward of the critical diurnal latitude in
the northeastern SCS from 75-day-long mooring current
measurements (Xie et al. 2011b).

361(Lin et al. 2009). Scatterometer data provide ocean surface
wind observations. SAR data are frequently utilized for thedetection of internal waves (Zheng et al. 2007), bathymetry(Zheng et al. 2006b), and oil spills.

4 The special section
3.3 Responses of SCS regional environment to globalchanges and El Niño events
Kienast et al. (2001) presented the alkenone SST records
for the tropical SCS that show an abrupt temperature
increase of at least 1°C at the end of the last glacial period.
Li et al. (2002) used TOPEX/POSEIDON satellite altimetry data to identify a general trend of sea level rising in the
SCS during 1993–1999. Liu et al. (2007) analyzed thelong-term variability of temperature and salinity in the SCS
and demonstrated that the seawater at the SCS intermediate
layer has become significantly fresher since the 1960s. Liuet al. (2009) reconstructed high resolution Sr/Ca-SST
sequences extracted from the modern massive Porites coralin the northern SCS and concluded that a general intensification trend existed in the summer upwelling from 1906
to 1993 with significant interannual and decadal variations,which is consistent with the global warming in the twentieth century and El Niño and Southern Oscillation. Cai
et al. (2011) studied spatial and temporal oscillation andlong-term variation of SST in the SCS and analyzed SST
interannual and long-term variations, which result from themeridional wind anomaly and zonal migration of the subtropical high over the western Pacific Ocean. Since ‘‘El
Niño Modoki’’ (Ashok et al. 2007; Ashok and Yamagata2009) was recently introduced, oceanographers are paying
more and more attention to the responses of the SCS to thisnew type of El Niño phenomenon (Chang et al. 2008).
3.4 Applications of satellite data to SCS regional
environmental oceanography
Data from satellite remote sensing, such as altimeters,
synthetic aperture radar (SAR), visible and infrared spectrometers, and microwave scatterometers, have been
widely used to study regional environmental oceanography
in the SCS and its adjacent areas (Liu et al. 2008a).
Satellite altimeter data have been employed to derive ocean
circulation, mesoscale eddies, tides, sea level variations,and waves. Satellite-derived SST and ocean color data areusually used to study upwelling, oceanic fronts, different
scales of variations in SST and chlorophyll a distributions,
local responses to the climate change, El Niño events, andtyphoons (Shang et al. 2008), to estimate the surface water
pCO2 and air–sea CO2 fluxes (Zhu et al. 2009), andto assess aerosol impact on the SCS biogeochemistry

The special section, as a whole package of closely related
papers including this introductory note, provides thereaders with a convenient way to share newly obtained
results and information on the regional environmental
oceanography in the SCS and its adjacent areas. Using insitu data, satellite data, and numerical modeling, contributors to this special section cover studies including the NIO
in the SCS, the interaction between nonlinear Rossby eddy
and Kuroshio in the Luzon Strait, currents and upwelling in
the northern SCS and the Taiwan Strait, water mass in the
Beibu Gulf, and satellite data applications for shallow
water depth retrieval, residual settlement detection, andSST and warm pool area variability in the SCS and its
adjacent areas.
Acknowledgments This work is funded by the Natural Science
Foundation of China through projects 40976013 and 40821063, theNational Basic Research Program of China through project
2009CB421208 (for Hu), partially supported by the US National
Science Foundation Program AGS-1061998 (for Zheng), and supported by a direct grant from the Chinese University of Hong Kong(for Pan). The editing of the special section is jointly supported by theState Key Laboratory of Marine Environmental Science of Xiamen
University (MELRS0942), the Institute of Space and Earth Information Science of the Chinese University of Hong Kong, and the Global
COE Program from the Japanese Ministry of Education, Culture,
Sports, Science and Technology (for Guo). We, the guest editors of
the special section, also thank the dedicated work of all the reviewers,
and appreciate the extensive and sustained efforts of Profs. Toshiro
Saino and Toshiyuki Hibiya, Editors-in-Chief of Journal of Oceanography, and Springer Japan. Without their perseverance and guidance, the special section would not be possible.

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