Formation and Movement of the ESIW as Modeled by MICOM

Journal of Oceanography, Vol. 55, pp. 369 to 382. 1999

369Copyright The Oceanographic Society of Japan.

Keywords:⋅ JES circulation,⋅ESIW,⋅MICOM,⋅numerical model-ing.

Formation and Movement of the ESIW as Modeled by MICOM

KUK JIN KIM and YOUNG HO SEUNG

Department of Oceanography, Inha University, Yonghyun-dong 253, Nam-gu, Inchon, Korea

(Received 20 September 1998; in revised form 27 November 1998; accepted 10 December 1998)

The presence of the minimum salinity and oxygen-rich East Sea Intermediate Water(ESIW) off Korean coast has raised many questions about its origin and movement. Thisstudy attempts to answer these questions in the context of numerical model. For this, theMiami Isopycnic Coordinate Ocean Model is used with surface and inflow boundaryconditions based on available data. Model results show that the ESIW forms mostdistinctly off Vladivostok, where the center of doming structure is observed, and movessouthward along Korean coast forming a large cyclonic gyre around the doming. Therenewed ESIW has the character of minimum potential vorticity common to usual modewaters. These results are compatible with various indications made in previous obser-vational and theoretical studies. However, it is not known whether the doming structureis a result of convection or the latter is favored by the former.

σθ = 27.25 (Kim and Chung, 1984; Kim et al., 1991). Thepresence of oxygen-rich ESDIW indicates that it also isrenewed by deep winter mixing as well as the ESIW. Theseobservations indicate that the ESDIW is the lowest limit ofpresent deep convective mixing because they show a transi-tion from bottom water formation to deep/intermediatewater formation during these thirty years. For reference, thedeep mixed water column found in the northwestern part ofthe basin (Seung and Yoon, 1995a) in early 1982 under arelatively severe winter condition had density range of about27.30 < σθ < 27.31. Furthermore, water mass analyses basedon historical data by Senjyu and Sudo (1993 , 1994) showthat upper portion of the JSPW, equivalent to the layerbetween the ESIW and the ESDIW with density range27.31 < σθ < 27.34, is also formed near the same location bywinter mixing. Their studies indicate that the renewed watermass circulates cyclonically around the basin. Recent obser-vations (Isobe and Isoda, 1997) show more clearly thecyclonic circulation of fresh water in the Western JapanBasin. These studies along with the study by Shin et al. (1998)indicate that the ESIW has minimum potential vorticity. Onthe other hand, application of the ventilation theory (Seung,1997) suggests that these water masses subduct beneath thepolar front, intrude southward along the western boundaryand then return to the north through the basin interiorcompleting the large-scale cyclonic circulation. The degreeof southward intrusion depends on the intensity of positivewind stress curl.

Most of the numerical models applied to the East Seaare of the Bryan-Cox type (Bryan, 1969; Cox, 1984), framedin the cartesian coordinates in the vertical, upon which theprimitive equations for the fluid motion are discretised. As

1. IntroductionA warm surface water is carried by the Tsushima

Current (TC) which enters the Japan/East Sea (JES) throughthe Korea/Tsushima Strait (K/T, see Fig. 1). A part of it,named the Nearshore Branch (NB), flows along Japanesecoast due to the topographic control (Yoon, 1982b) and therest flows northward along Korean coast, forming the EastKorean Warm Current (EKWC). The EKWC is known toseparate from the coast near 38°N, then moves eastwardtoward the Tsugaru (TG) and Soya (SO) Straits, where itleaves the JES. North of the warm current region, a coldcurrent called the North Korean Cold Current (NKCC) orthe Liman Current (LC) flows southward along the westernboundary and meets with the EKWC where the EKWCseparates from the coast. The separation of the EKWC andthe formation of the NKCC may be controlled by the windstress curl and the buoyancy flux (Seung, 1992). All theseschematic features of surface circulation are mostly con-firmed by numerical models (Yoon, 1982a, b; Seung andKim, 1993; Seung and Yoon, 1995b; Kim, 1996).

Most of the JES basin is filled with a very deep, coldand nearly homogeneous water, traditionally called theJapan Sea Proper Water (JSPW). Recent CREAMS obser-vations (Kim et al., 1996; Kim and Kim, 1996) have, how-ever, revealed that this water mass is not really homoge-neous, containing a low-salinity and high-oxygen wateraround the density σθ = 27.345 (depth 1000–2000 m), whichthey named as the East Sea Deep Intermediate Water(ESDIW) in distinction from the upper intermediate waterknown as the East Sea Intermediate Water (ESIW) which isalso relatively fresh and oxygen-rich but found in the layersshallower than 500 m off Korean coast around the density

370 K. J. Kim and Y. H. Seung

Fig. 1. Model domain with bottom topography. Thick arrowsmean inflow and outflows. Line A coincides with the PM lineof Maizuru Marine Observatory, Japan Meteorological Agency,line B is along 37.5°N. Abbreviations are as follows: K/Tmeans Korea/Tsushima Strait, TG Tsugaru Strait, SO SoyaStrait, VL Vladivostok, WJB Western Japan Basin, EJBEastern Japan Basin, YB Yamato Basin and UB UlleungBasin.

Fig. 2. Initial setting of layers. Approximate positions of theESIW and ESDIW are marked.

shown by Roberts et al. (1996), the advantages of theisopycnic coordinate models over those using cartesianvertical coordinate arise essentially from the facts thatmixing of fluid is largely isopycnic, that the formers cancope with any depth without the need of transforming it ontoa discrete set of depths, that they allow outcropping ofisopycnals and that the analysis of model results is done onthe isopycnal surface. These facts render the isopycnicmodels suitable for studying the processes associated withthe deep/intermediate water formation as considered here. Apreliminary study using the isopycnic coordinate model hasalready been done (Seung and Kim, 1997) in relativelycoarse-grid resolution, in which the residence time of renewalis estimated.

The primary aim of this study is to clarify the questionsassociated with the existence of the ESIW in the context ofnumerical experiment. Although there are some indicationsthat this water is formed in the northwestern part of the basinand circulates cyclonically around the basin, detailed for-mation process and circulation pattern are not yet known.Fortunately, these works are more enabled by the recentdevelopment of isopycnic models (e.g., Bleck et al., 1992)mentioned above. In the following contents, the model isfirst described, then model results are discussed and finally,a concluding remarks are given.

2. ModelThe model is the same as that used by Bleck et al. (1992)

except that inflow and outflow through open boundaries areimplemented. The model allows the free surface and usesthe mixed layer of Kraus and Turner (1967) type with thedissipation parameterized according to Gaspar (1988). Thedeepening of mixed layer by surface cooling, which will beshown later, is largely due to this mixed layer dynamicsalthough there is also mass flux by vertical diapycnal diffusionbetween layers. For further details about thermo-dynamicfoundation of the model, refer to Bleck et al. (1989). Themodel advances the barotropic and baroclinic solutionsusing the split-explicit scheme. The eddy viscosity used inisopycnal mixing of momentum depends on the horizontalshear, which is about 1,000 m2/sec in this model. To handlethe advection of sharp discontinuity of density interfaces,special schemes such as the Flux Corrected Transport(Zalesak, 1979) and the Multidimensional Positive DefiniteAdvection Transport Algorithm (Smolarkiewicz, 1983, 1984)are employed. For more details about the model, the readeris referred to Bleck et al. (1992).

The model domain (Fig. 1) is divided into horizontalgrid of 0.2° by 0.2° in latitude and longitude. Vertically, itconsists of 10 layers as shown in Fig. 2. The first layer(initial depth 50 m) is the mixed layer which can havevariable temperature, salinity and depth. Densities and ini-tial depths of the remaining layers are determined based on

Formation of the ESIW 371

the CREAMS results (c.f., Kim and Kim, 1996) which aremostly obtained in summer in the Japan Basin. Since theseobservations represent the northern part of the basin, thedensity of the Tsushima Current Water (TCW), representedpartly by the mixed and the second layers, is taken slightlylarger. However, this fact will not affect significantly thebehavior of the underlying ESIW. Later, the model run isstarted from the summer condition. The temperature, salinityand layer depth of the mixed layer are determined by themixed layer dynamics implemented in the model in responseto the imposed surface conditions. In each layer below themixed layer, the salinity and layer thickness are updated.The temperature is automatically determined using theequation of state from the updated salinity and the fixeddensity. For the layers representing the ESIW and the layersbelow, the salinity change is mostly due to the winterconvective mixing and in lesser degree to diapycnal diffu-sion.

At the surface, wind stresses provided by Na et al. (1992)are applied. To impose the buoyancy forcing at the surface,the mixed layer temperature and salinity are relaxed to thesurface temperature and salinity of the climatology providedby JODC (1978), the same one used by Seung and Kim(1993). In imposing the surface temperature and salinity, thesimple Newtonian restoring formulation is used with thedamping coefficient of time scale fifteen days. Althoughone can obtain the similar patterns of horizontal circulationindependently of the value of damping coefficient, the depthof convective mixing is quite sensitive to the latter. Thus thedamping coefficient is determined such that the convectivemixing does not reach beyond the level of ESDIW, inaccordance with the CREAMS observations.

At the inflow (Korea/Tsushima Strait) and outflowopenings (Tsugaru and Soya Straits), the depths are soshallow that they consist only of the mixed layer and thesecond layer which represents the core of TCW. A volumetransport of 2.0 Sv is imposed through these layers. Of this,1.5 Sv flows out through the Tsugaru Strait and 0.5 Svthrough the Soya Strait. Currents are assumed barotropic atthe inflow and outflow openings. At the inflow opening, themixed layer temperature, salinity and depth, assumed uni-form along the boundary, are also prescribed. They arededuced from the observed hydrography (NFRDA, 1986)by assuming that the temperature and salinity of the inflowingsecond layer water are fixed at (11.73°C, 34.4 psu), whichmay characterize the core of the TCW, while the heat andsalt within the whole water column remain unchanged. Theresulting mixed layer temperature and salinity at the inflowopening have a seasonal fluctuation ranging from about14°C in February to about 27°C in August for temperatureand from about 32.3 psu in August to about 34.6 psu in Aprilfor salinity. At the outflow openings, the temperature, salin-ity and layer thickness are taken the same as those at theadjacent interior points.

3. ResultsThe model was run for thirty years. Time series plots of

the volume in each layer (Fig. 3) show quite distinctivesignals of seasonal variations. It is characterized by increaseof mixed layer volume in winter and corresponding decreasein layers below, indicating the winter convective mixing.The seasonal variation is seen only slightly in layer 8 (thelayer representing the ESDIW) and is absent in layers 9 and10. Time serieses of kinetic energy (Fig. 4) also show theseasonal variation although they are more complicated.There are long-term trends superimposed on these seasonalvariations, by which the upper 5 layers become slightlythicker than they are at the initial state. The long-term trendsof kinetic energy are less significant than those for the totalvolume. Because of the long-term trend, the model cannotbe thought to be thermally equilibrated at year 30. However,these long-term trends are not considered to affect much theseasonal fluctuation which is our main interest. The modelis run for extra one year and the corresponding results are thebasis of following descriptions.

Current patterns in the mixed layer (Fig. 5) show fourmajor surface currents: the NB flowing along Japanesecoast, the EKWC flowing northward along Korean coast,the current along the polar front extending offshore fromKorean coast, and the NKCC (or LC) flowing southwardalong Russian/Korean coast. These results are similar toprevious model results in that the NKCC and the EKWCstrengthen, respectively, in winter and summer. As in Seungand Yoon (1995b), there is no overshooting of the EKWC.The NB looks more organized in winter rather than insummer contrary to what observations (e.g., Lee et al., 1997)indicate.

Before presenting details about the third and fourthlayers, currents in deeper layers are shown here for thepurpose of comparison. Lie et al. (1989) performed a long-term current measurement off Korean coast near 37.7°Nfrom August 26 to November 7 at depths 620 m and 790 mwhich approximately fall in the fifth layer in the model after30 years of run. It shows an average southward current withmagnitude 3 cm/sec, which can be compared with the modelresults shown in Fig. 6(b). Nitani (1972) and Ohwada andTanioka (1971) estimated dynamic topographies of 1200–1500 db surfaces, which indicate a cyclonic circulationwithin the Eastern Japan Basin both in winter and summer.In July and October, they show an anti-cyclonic circulationwithin the Yamato Basin. On the other hand, Takematsu etal. (1997) carried out long-term current measurements indeep layers of the Japan Basin. They show highly fluctuatingcurrents with magnitude on the order of 10 cm/sec especiallyin winter and spring. At one place (his station M6) where notopographic irregularity exists a current compatible with theLC is observed. Model results show a strong cycloniccirculation of order 10 cm/sec in winter (Fig. 6(c)) in theJapan Basin compatible with the former observational re-


Fig. 3. Time series plots of the volume for each layer.


Fig. 4. Time series plots of the kinetic energy for each layer.


sults and partly with the latter ones. In the Yamato Basin,current appears to be anti-cyclonic in both winter andsummer compatible with the former results. In general,however, the modeled bottom currents are weaker thanthose observed, which is common to all previous models.

The distributions of salinity, layer thickness and

Montgomery potential (defined by gz + pα where g is thegravity constant, z is the vertical coordinate, p is the pressureand α is the specific volume) are shown for layer 3 (Fig. 7)and layer 4 (Fig. 8). Due to the space limit, only those ofFebruary and August are presented. Prior to describing thewater mass renewal, we briefly compare the circulation

Fig. 5. Currents in the mixed layer at three months interval.


obtained in the model with some available observations.The cyclonic circulation pattern in the northwest is quitecompatible with previous estimations (Senjyu and Sudo,1994) and especially the recent CREAMS measurements(Isobe and Isoda, 1997). The southwestern current alongJapanese coast flowing in opposite direction to the surfacecurrent has usually been obtained in previous models. Al-

though the second layer is most affected by convectivemixing, it is largely diluted by the advecting TCW. Thus thethird layer is most influenced by the surface fresh waterduring the convective mixing. The climatology indicatesthat the fresh water flows southward along the Russian coastfrom the Tartarsky Strait as discussed by Seung and Yoon(1995a). In February, large part of the third layer in the

Fig. 6. Currents in the fifth and ninth layers each in February and August.


central northern region disappears by an encroachment ofthe mixed layer (Figs. 7(a) and 7(b)). However, it is near41.5°N, 131.5°E off Vladivostok where the encroachmentbegins first (in January) and disappears last (in March),although not shown here. This place is thus believed to be

the place of most intense convective mixing as observationsindicate (Seung and Yoon, 1995a). A local minimum layerthickness is usually found at this place (e.g., Fig. 7(d)),which is later found to be associated with a doming struc-ture. One may think that the doming favors the initiation of

Fig. 7. Distributions of salinity and Montgomery potential in the third layer (left panels) in February and August. Corresponding layerthicknesses are shown in the right panels. Montgomery potential is contoured from –17500 at interval 500. The areas with smalldark squares in the north denote the vanishing of layer.


convection. The distribution of Montgomery potential indi-cates that the refreshed water intrudes southward alongKorean coast down to the continental slope off Korean coastwhere the ESIW was first observed by Kim and Chung(1984). It then progressively separates from the coast form-ing a cyclonic circulation elongated in the direction parallelto Russian coastline. The center of cyclonic circulation

approximately coincides with the minimum layer thickness(Figs. 7(c) and 7(d)) and thus with the doming. The otherhalf of the basin to the southeast is in anti-cyclonic circula-tion and not significantly refreshed (Figs. 7(a) and 7(c)).Similar observations are made for fourth layer (Fig. 8) butwith lesser degree of intensity. Though not shown here, thefourth layer also vanishes in early March with much smaller

Fig. 8. Same as Fig. 7 except for the fourth layer. Montgomery potential is contoured from –18000 at interval 500.


horizontal extent slightly east of the place where the mostintense convection is observed in the third layer.

For some moving patches of refreshed water, localsalinity (S in psu) minimum coincides with local thicknessmaximum (H), showing the character of minimum potentialvorticity common to usual mode waters: for example, around

40.5°N, 129.5°E with 33.81 < S < 33.91 and H > 100 m, alongKorean coast south of 39°N with 33.91 < S < 33.93 and H >100 m (Figs. 7(a) and 7(b)), and around 38–41°N, 128–131°E with 33.91 < S < 33.93 and H > 100 m (Figs. 7(c) and7(d)). In the fourth layer, this character is less clear probablybecause advection is weaker relative to diffusion. However,

Fig. 10. Same as Fig. 9 except for the fourth layer.

Fig. 9. Space-time diagram of salinity and layer thickness along the line C (see Fig. 1 for location) for the third layer. Dotted arrowsdenote advection of fresh and low-potential vorticity water.


some signatures are seen around 40.2°N, 130.2°E with34.01 < S < 34.02 and H > 300 m (Figs. 8(a) and 8(b)) andalong Russian coast east of 130°E with 34.02 < S < 34.03 andH > 250 m (Figs. 8(c) and 8(d)). The movement of lowsalinity and low potential vorticity water is further clarifiedby drawing a time-space diagram of salinity and layerthickness along the presumed flow path. The southwardmovement along Korean coast is seen in winter for the thirdlayer (Figs. 9(a) and 9(b)), and further north in winter and

spring for the fourth layer (Figs. 10(a) and 10(b)). It seemsthat the southward advection velocity is smaller in the fourthlayer than in the third layer. Offshore movement is also clearin the third layer, for example near 37.5°N in winter andspring (Figs. 11(a) and 11(b)), although it is not quite clearin the fourth layer probably because of weak advectioncompared with diffusion.

The vertical salinity section along the line A (Fig. 12)shows a doming of isopycnals around 41.6°N and southward

Fig. 12. Vertical section of salinity (in psu) and layer thickness along the line A (see Fig. 1 for location) in February and August. Solidand dotted lines are, respectively, layer interfaces and salinity contours. The lowest layer is the eighth layer. For comparison withobservations, station numbers are marked along the upper abscissa.

Fig. 11. Same as Fig. 9 except for along the line B (see Fig. 1 for location).


Fig. 13. Vertical salinity distribution along the PM line, same as the line A, observed by Maizuru Marine Observatory (1975, 1976).The station numbers along the upper abscissa are the same as in Fig. 12.

Fig. 14. Same as Fig. 12 except for the line B. The lowest layer is the seventh layer.

penetration of the fresh water, considered as the ESIW,along the third and fourth layers. Due to the doming of lowerlayers, the upper layers become thinner than they are other-wise. The general pattern is quite comparable with observa-tions (c.f., Fig. 13) although the depth of the ESIW in themodel is slightly deeper than in observations. The doming ismore prominent and more fresh water appears in August.The fresh water is supplied from the coast to the oppositeside of the dome by advection, consistently with the resultsshown in Figs. 7 and 8 and observations (Isobe and Isoda,1997). Though not shown here, the mixed layer deepening

reaches maximum down to about 900 m around March 5completely destroying the doming structure. This event,however, lasts only for a few days and there is a rapidrestoration. The vertical sections along the line B (Fig. 14)also show the offshore penetration of the ESIW along thethird and fourth layers. Although the distributions of theESIW do not exactly coincide between the model andobservation (Fig. 15), they show a common feature that thefresh water develops in the coastal area in December andleaves much of its place to the TCW in May.


4. Concluding RemarksThe ESIW found off Korean coast is richer in oxygen

content and fresher than the similar one found furthereastward. However, the two types have long been consid-ered the same except that the latter has lost its originalcharacter by mixing with surrounding waters during thecourse of advection. This view is partly supported by Senjyuand Sudo (1994) and more recently by Isobe and Isoda(1997). One of the major achievements of this study is thatthis view is confirmed numerically. According to the model,the ESIW is carried southward along Korean coast in agree-ment with the ventilation theory (Seung, 1997). This south-ward moving ESIW progressively separates from the coastforming a large cyclonic gyre elongated in the northeast-southwest direction. There is an indication that the mostdistinct formation area of the ESIW is probably offVladivostok, confirming the suggestion by Senjyu and Sudo(1994) and Seung and Yoon (1995a). This place also ap-proximately coincides with the centers of both the cyclonicgyre and the doming mentioned earlier. The freshening ofthe ESIW is due to the vertical mixing with surface freshwater coming from the north along Russian coast, as indi-cated by the distribution of surface salinity (JODC, 1978).One can deduce that the doming of isopycnals usually foundoff Vladivostok favors the initiation of vertical mixing. Thisdoming may be related with the cyclonic gyre. However, itis not known how this gyre, and thus the doming, is generated.The distribution of wind stress curl does not indicate that itis solely due to the wind forcing. It may be possible that theconvective mixing itself is the cause of the doming. Thefreshened ESIW moves in patches showing the character ofminimum potential vorticity common to usual mode waters,

confirming the previous observations. The distributions ofthe ESIW in the vertical sections appear comparable withobserved ones.

Despite these successes, there remains some problemsto be resolved. The seasonal change of the Nearshore Branchappears different from that obtained by geometric coordi-nate models. In this respect, an inter-comparison studyamong different models may be necessary. The deep currentsare somewhat different from observations, which is gener-ally common feature to all numerical models. To improvethis drawback, a fundamental examination of the interactionbetween the current and bottom topography and its imple-mentation to the model scheme may be needed, such as theone considered by Holloway (1995). The long-term thermo-haline trend is also one of unresolved problems in oceanmodeling. The slight mismatch in depth of the ESIW betweenthe model and observations may be improved by attemptingdifferent initial states and by applying more correct surfaceboundary conditions. Above all, the convective mixinggreatly depends on the surface heat flux and evaporationrendering it critical to this kind of modeling, especiallywhen it concerns the deep water formation rather thanintermediate water formation.

AcknowledgementsThis study is supported partly by NON DIRECTED

RESEARCH FUND, Korea Research Foundation (1995–1998), by KOSEF research grant 981-0405-018-2, by BasicScience Research Institute Program, Ministry of Education(1997) and partly by Center for Ocean Circulation andCycles (1998). The authors thank Prof. K. Kim of SeoulNational University for providing CREAMS data.

Fig. 15. Vertical salinity distributions along the line B observed by Kim et al. (1991) in December and May. The station numbers alongthe upper abscissa are the same as in Fig. 14.


National Fisheries Research and Development Agency (1986):Mean Oceanographic Charts of the Adjacent Seas of Korea.Pusan, Korea. 186 pp.

Nitani, H. (1972): On the deep and bottom waters in the Japan Sea.p. 151–201. In Research in Hydrography and Oceanography,ed. by D. Shoji, Hydrographic Department of Japan MaritimeSafety Agency, Tokyo.

Ohwada, M. and K. Tanioka (1971): Currents and distribution ofwater masses in the Japan Sea. p. 51–72. Report study on theJapan Sea, Tokyo.

Roberts, M., R. Marsh, A. L. New and R. A. Wood (1996): Anintercomparison of a Bryan-Cox type ocean model and anIsopycnic ocean model. Part I: The subpolar gyre and high-latitude processes. J. Phys. Oceanogr., 26, 1495–1527.

Senjyu, T. and H. Sudo (1993): Water characteristics and circu-lation of the upper portion of the Japan Sea Proper Water. J.Mar. Sys., 4, 349–362.

Senjyu, T. and H. Sudo (1994): The Upper Portion of the JapanSea Proper Water; Its source and circulation as deduced fromisopycnal analysis. J. Oceanogr., 50, 663–690.

Seung, Y. H. (1992): A simple model for separation of EastKorean Warm Current and formation of North Korean ColdCurrent. J. Oceanol. Soc. Korea, 27, 189–196.

Seung, Y. H. (1997): Application of the ventilation theory to theEast Sea. J. Korean Soc. Oceanogr., 32, 8–16.

Seung, Y. H. and J.-H. Yoon (1995a): Some features of winterconvection in the Japan Sea. J. Oceanogr., 51, 61–73.

Seung, Y. H. and J.-H. Yoon (1995b): Robust diagnostic model-ing of the Japan Sea circulation. J. Oceanogr., 51, 421–440.

Seung, Y. H. and K. Kim (1993): A numerical modeling of theEast Sea circulation. J. Oceanol. Soc. Korea, 28, 292–304.

Seung, Y. H. and K. J. Kim (1997): Estimation of the residencetime for renewal of the East Sea Intermediate Water usingMICOM. J. Korean Soc. Oceanogr., 32, 17–27.

Shin, C. W., S. K. Byun, C. S. Kim and Y. H. Seung (1998):Southward intrusion of the East Sea Intermediate Water intothe Ulleung Basin: observations in 1992 and 1993. J. KoreanSoc. Oceanogr., 33 (in press).

Smolarkiewicz, P. K. (1983): A simple positive definite advectionscheme with small implicit diffusion. Mon. Wea. Rev., 111,479–486.

Smolarkiewicz, P. K. (1984): A fully multidimensional positivedefinite advective transport algorithm with small implicitdiffusion. J. Comput. Phys., 54, 325–362.

Takematsu, M., Z. Nagano, A. G. Ostrovskii and T. Kita (1997):Seasonal deep current in the Sea of Japan. p. 25–30. Pro-ceedings of International Symposium on CREAMS, Fukuoka,Japan.

Yoon, J.-H. (1982a): Numerical experiment on the circulation inthe Japan Sea, Part I: Formation of the East Korean WarmCurrent. J. Oceanogr. Soc. Japan, 38, 43–51.

Yoon, J.-H. (1982b): Numerical experiment on the circulation inthe Japan Sea, Part III: Mechanism of the Nearshore Branch ofthe Tsushima Current. J. Oceanogr. Soc. Japan, 38, 125–130.

Zalesak, S. T. (1979): Fully multidimensional flux-correctedtransport algorithms for fluids. J. Comput. Phys., 31, 335–362.

ReferencesBleck, R., H. P. Hanson, D. Hu and E. B. Kraus (1989): Mixed

layer-thermocline interaction in a three-dimensional isopyc-nic coordinate model. J. Phys. Oceanogr., 19, 1417–1439.

Bleck, R., C. Rooth, D. Hu and L. T. Smith (1992): Salinity-driventhermocline transients in a wind- and thermohaline-forcedisopycnic coordinate model of the North Atlantic. J. Phys.Oceanogr., 22, 1486–1505.

Bryan, K. (1969): A numerical method for the study of thecirculation of the world ocean. J. Comput. Phys., 4, 347–376.

Cox, M. D. (1984): A primitive equation, three-dimensionalmodel of the ocean. Tech. Rep. No. 1, Ocean Group, GFDL,Princeton, NJ, 143 pp.

Gaspar, P. (1988): Modeling the seasonal cycle of the upperocean. J. Phys. Oceanogr., 18, 161–180.

Holloway, G. (1995): Dynamics of circulation of the Japan Sea. J.Mar. Res., 53, 539–569.

Isobe, A. and Y. Isoda (1997): Circulation in the Japan Basin, thenorthern part of the Japan Sea. J. Oceanogr., 53, 373–381.

Japan Oceanographic Data Center (1978): Marine EnvironmentalAtlas: Adjacent seas of Japan (monthly), Japan HydrographicAssociation.

Kim, C. H. (1996): A numerical experiment study on the circula-tion of the Japan Sea (East Sea). Ph.D. Thesis, Kyushu Univ.,151 pp.

Kim, C. H., H.-J. Lie and K. S. Chu (1991): On the IntermediateWater in the southwestern East Sea (Sea of Japan). p. 129–141. In Oceanography of Asian Marginal Seas, ed. by K.Takano, Elsevier, Amsterdam.

Kim, K. and J. Y. Chung (1984): On the salinity-minimum anddissolved oxygen-maximum layer in the East Sea (Sea ofJapan). p. 55–65. In Ocean Hydrodynamics of the Japan andEast China Seas, ed. by T. Ichiye, Elsevier, Amsterdam.

Kim, K., K. R. Kim, Y. G. Kim, Y. K. Cho, J. Y. Chung, B. H.Choi, S. K. Byun, G. H. Hong, M. Takematsu, J.-H. Yoon, Y.Volkov and M. Danchenkov (1996): New findings fromCREAMS observations: Water masses and eddies in the EastSea. J. Korean Soc. Oceanogr., 31, 155–163.

Kim, K. R. and K. Kim (1996): What is happening in the East Sea(Japan Sea)?: Recent chemical observations during CREAMS93–96. J. Korean Soc. Oceanogr., 31, 164–172.

Kraus, E. B. and J. S. Turner (1967): A one-dimensional model ofthe seasonal thermocline. Part II: the general theory and itsconsequences. Tellus, 19, 98–105.

Lee, D. K., J. C. Lee, S. R. Lee and H.-J. Lie (1997): A circulationstudy of the East Sea using satellite-tracked drifters.1: Tsushima Current. J. Korean Fish. Soc., 30, 1021–1032.

Lie, H.-J., M. S. Suk and C. H. Kim (1989): Observations ofsoutheastward deep currents off the east coast of Korea. J.Oceanol. Soc. Korea, 24, 63–68.

Maizuru Marine Observatory (1975) Oceanographic Prompt Re-ports. Supplement for No. 283.

Maizuru Marine Observatory (1976) Oceanographic Prompt Re-ports. Supplement for No. 290.

Na, J. Y., J. W. Seo and S. K. Han (1992): Monthly-mean seasurface winds over the adjacent seas of the Korea Peninsular.J. Oceanol. Soc. Korea, 27, 1–10.

Documents

Formation and Movement of the ESIW as Modeled by MICOM