139736eo.pdf (20MB) - Japan Oceanographic Data Center

More documents

Recommendations

Info

Several two-dimensional models of tides in the Gulf already exist (for complete references,see EL-SABH, 1984; LE PROVOST, 1984). All of these models either have been used or are capableof predicting tidal currents as well as heights, but there is almost a complete absence of systematiccurrent surveys to measure tidal current in detail to provide empirical verification. IMCOS Marine(HIBBERT, 1980) claims to have developed a verified model to predict currents from tide heightpredictions applicable to any part of the Gulf.More recently, MURTY and EL-SABH (1985) studied the age of tides in the Gulf (the age oftides is a term used to denote the interval between the time of new or full moon and the time of the localspring tide). As can be seen in Figure 10, the age of the semi-diurnal tide in the Gulf varies between-35 to 76 hours, with the major variations occurring in areas where the semi-diurnal tide has anamphidromic point. Higher values are found in the shallow area between Bahrain and United ArabEmirates. On the other hand, all ages for the diurnal tide show negative values which vary between -4and -92 hours; the lower value is found in the southern part of the Strait of Hormuz while highervalues occur in the area where the amphidromic point for the diurnal tide occurs. In general, higherages occur in shallow areas and near the amphidromic points, associated with a major topographicfeature.RESIDUAL CIRCULATIONVery little information exists describing the residual current field in the Gulf, the most recenteffort are those by HUNTER (1984) and GALT et al. (1984). It has been known for a long time thatevaporation exceeds precipitation in the Gulf, and so the more saline dense water should sink and passout of the Strait of Hormuz, giving rise to a compensating surface flow of less dense water into theGulf. The effect of the Earth's rotation would deflect these flows to the right, giving a surface flowwest and northwest along the Iranian coast, and a deep flow to the southeast and east along the coastsof Saudi Arabia and the United Arab Emirates (the deep flow would be constrained further to theselatter coastlines adjacent to the shallow sea areas of high evaporation). This circulation patternundoubtedly is modified by forcing of wind and atmospheric pressure, but it generally has beensupported by observations of ship drift. Evidence for this anti-clockwise residual circulation in theGulf, driven predominantly by evaporation (giving rise to horizontal density and pressure gradients),has been described by several authors (see HUNTER, 1984, for details).The northwestern part of the Gulf is undoubtedly influenced by the freshwater inflow of theTigris, the Euphrates and the Karun (entering the Gulf via the Shatt Al-Arab). This inflow appears tobe deflected to the right by Coriolis force to form a river plume of width approximately 20 km, flowingalong the Iraqi coast into Kuwait waters (MATHEWS et al., 1979). Freshwater inflow has beenestimated by GRASSHOFF (1976) to vary between 5 and 100 km3 yr-1. A more realistic estimatemade by HARTMANN et al. (1971) of 37 km3 yr-l represents only about 9% water loss fromevaporation. Since precipitation is light in the region, consideration of the differential flow through theStrait of Hormuz is crucial to the water balance in the Gulf.On the basis of a geostrophic force balance across the Gulf and a frictional balance along theGulf, HUNTER (1982) indicated the circulation schematically by the diagram shown in Figure 11.Evaporation in the shallow areas of the southwestern and southern Gulf leads to a sinking of densewater that is deflected to the right by Coriolis force, to flow out at the bottom of the Strait of Hormuz.This flow is compensated by a surface inflow along the Iranian coast. This circulation will bemodified by the effect of surface wind stress, especially in shallow areas where the effect of densityforcing wil be small.GALT et al. (1984) numerically simulated the steady state surface circulation in the Gulf fromthe combined effects of wind forcing and excess of evaporation (Fig. 12). One major feature of thecirculation is a current moving to the southeast along the western shore. This first develops insouthern Kuwait and then moves south along Saudi Arabia, gaining strength as it moves. By the timeit reaches Bahrain, some of it moves south along the western shore of Bahrain, but most of the flow isbathymetrically steered to the south and east towards the northern tip of Qatar where some smallfraction of it rounds the Qatar coast and moves into the eastern basin of the Gulf. Some re-circulationnorth of Qatar also can be seen. The maximum speed associated with this current is about one-halfknot along the southern coast of Saudi Arabia and north of Bahrain and Qatar. A second major featureof the derived current pattern is coastal flow along the eastern shore or the southwestern coast of Iran.240
This current is weaker and narrower than the one along the Saudi Arabian coast. Throughout thecenter of the northwestem basin, there is a weak return flow that covers the deeper segments of theGulf. This continues towards the northwest where it approaches the shoreline and bifurcates aboutmidway down the Kuwait coast.It is clear that the circulation of the Arabian Gulf is complex and three-dimensional. The onlynumerical three-dimensional model of the overall residual currents in the region is by HUNTER(1983). The model was used to simulate the steady-state response of the Gulf to a specified densitydistribution and a wind stress. The prediction (Fig. 13) indicates a surface inflow of strength around10 cm s-1 along the Iranian coast, some evidence of river inflow at the northwestern end of the Gulf,and an outflow of water along the bottom from the coastal areas off Saudi Arabia, Qatar and the UnitedArab Emirates.The inflow of water from the Gulf of Oman, near the Iranian Coast, and conditions in theStrait of Hormuz have been observed by SONU (1979). In the Strait of Hormuz, the inflow wasestimated to occupy the top 30 m of the water column, a mixing layer in the middle 20 m and theoutflow at the bottom 30 m. This deep saline outflow of water from the Strait of Hormuz into the Gulfof Oman has been observed by several authors (e.g. BREWER and DYRSSEN, 1985; EMERY, 1956;HARTMANN et al., 1971; LEVEAU and SZEKIELDA, 1967). It appears that a tongue of salinewater flows out of the Strait of Hormuz at a depth of about 100 metres, sinks to about 200 metres inthe Gulf of Oman and finally sinks to about 500 metres in the South Arabian Sea.ACKNOWLEDGEMENTSWe thank Jocelyne Gagnon for typing the manuscript and Coralie Wallace for drafting thefigures. This study was supported in parts by grants from the Natural Science and EngineeringResearch Council, Canada, to M.I. El-Sabh.REFERENCESBREWER, P.G. and DYRSSEN, D. (1985). Chemical oceanography of the Persian Gulf. Progressin Oceanography, 4,41-55.EL-SABH, M.,I.(ed.) (1984). <strong>Oceanographic</strong> modelling of the Kuwait Action Plan (KAP) Region.UNESCO Reports in Marine Science, no. 28,79 p.EL-SABH, M.I. (1982). Numerical modelling of the Arabian Gulf. Report submitted to the Facultyof Marine Sciences. King Abdulaziz Univ., Jeddah, Saudi Arabia.EMERY, K. (1956). Sediments and water of Persian Gulf. Amer. Assoc. Petrol. Geol. Bull., 40,2354-2383.EVANS-ROBERT, D. (1979). Tides in the Persian Gulf. Consulting Engineer, June 1979.FARMER, A.S.D. and DOCKSEY, J.E. (1983). A bibliography of the marine and maritimeenvironment of the Arabian Gulf and Gulf of Oman. Kuwait Bull. Mar. Sci., no. 4, KuwaitInstitute for Scientific Research, Kuwait.GALT, J.A., PAYTON, D.L., TORGIMSON, G.M. and WATABAYASHI, G. (1984).Applications of trajectory analysis for the Nowruz Oil Spill. In: M.I. El-Sabh (ed.),<strong>Oceanographic</strong> Modelling of the Kuwait Action Plan Region, UNESCO Report in MarineSciences, no. 28, 55-66.GRASSHOFF, K. (1976). Review of hydrographic and productivity conditions in the Gulf region.In: Marine Sciences in the Gulf Area. UNESCO Technical Papers in Marine Science, 26,39-62.241
Page 1 and 2:
Intergovernmental Oceanographic Com
Page 3 and 4:
of the IOC Marine Pollution Monitor
Page 5:
PageMARGINAL SEASSTORM SURGES IN TH
Page 9 and 10:
Marine PollutionAt present, marine
Page 11 and 12:
THE INDIAN OCEAN --- AN ENVIRONMENT
Page 13 and 14:
The subtropical anticyclonic gyre i
Page 15 and 16:
GEOLOGICALBecause of its asymmetric
Page 17 and 18:
RADIOACTIVE AND THERMAL WASTESIn co
Page 19 and 20:
RESEARCH AND MONITORING ACTIVITIESM
Page 21 and 22:
2-5, Mn 3-7, Zn 8-31, Fe 35-94, Pb
Page 23 and 24:
Localized problems, both short-term
Page 25 and 26:
HOLEMAN, J.N. (1968). The sediment
Page 28 and 29:
UNEP/UNIDO (1982a). Industrial sour
Page 30 and 31:
0-5-24 -I I I I I I I I I 11--25- A
Page 32 and 33:
I*in '0( U N '0- '0 '0 N , p d'0I I
Page 34:
C'EO IIFigure 6. Observations of oi
Page 38 and 39:
Table 2.Ranges of Dissolved heavy m
Page 40 and 41:
d.2 W2n2 n z0U.IzIO N m mENmIYEE*Ed
Page 42 and 43:
Table 6. Population and related dat
Page 44 and 45:
PROBLEMS IN THE PHYSICAL OCEANOGRAP
Page 46:
B2: How does the Agulhas Current in
Page 50 and 51:
0Q0mbWbvx(U49
Page 52 and 53:
Figure 6 Average wind stress curl f
Page 54 and 55:
THE DESTRUCTION OF THE TETHYS AND P
Page 56 and 57:
part of the Seychelles-Mascarene bl
Page 58 and 59:
Much of the old Tethys seafloor has
Page 60 and 61:
when there was little or no movemen
Page 62 and 63:
scouring of the sediments by cold b
Page 64 and 65:
CANDE, S.C. and MUTTER, J.C. (1982)
Page 66:
SHACKLETON, N.J. and KENNETT, J.P.
Page 71 and 72:
0EYNz 10c2XaYWeKB20LuUz a5 cl300 10
Page 75:
CALCAREOUS FORAMINIFERANANNOFOSSIL
Page 79 and 80:
GEOLOGICAL-GEOPHYSICAL MAPPING OF T
Page 81 and 82:
The latest tectonic generalization
Page 83 and 84:
LE PICHON, X. and HEIRTZLER, J.R. (
Page 85 and 86:
AN EXAMINATION OF THE FACTORS THAT
Page 87 and 88:
is the specific volume anomaly. Po
Page 89 and 90:
circulation. At Nagappattinam, Madr
Page 91 and 92:
Table 1.MarmagaoCochin1969-781958-7
Page 93 and 94:
tFigure 2. An idealized coastal cur
Page 95 and 96:
STATION : BOMBAY~ J , F I M .- , A
Page 97 and 98:
STATION : COCHIN, J , F , M , A , M
Page 99 and 100:
3007STATION : MADRASI J I F , M I A
Page 101 and 102:
STATION : CALCUTTA, J l F , M , A ,
Page 103 and 104:
RED TIDE§ IN THE INDO-WEST PACIFIC
Page 105 and 106:
were observed as early as 1770 duri
Page 107 and 108:
diarrhetic shellfish poisoning (DSP
Page 109 and 110:
GACUTAN, R.Q., TABBU, M.Y., AUJERO,
Page 111 and 112:
Table 1.Clinical symptoms of variou
Page 113 and 114:
Table 3. Fish species implicated in
Page 115 and 116:
FIGURE CAPTIONSFigure la. Trichodes
Page 118 and 119:
(*14aEE15aHH15c120
Page 120 and 121:
MINERAL RESOURCES OF THE INDIAN OCE
Page 122 and 123:
tonnes of monazite. Similar deposit
Page 124 and 125:
Madagascar and the Red Sea. Within
Page 126 and 127:
South Australian Basin: (Figs. 10-1
Page 128 and 129:
Offshore placers are likely to occu
Page 130 and 131:
MILLIMAN, J.D. (1974). Marine Carbo
Page 132 and 133:
Thailand Tin 5560 (1980) NA 4.2 (19
Page 134 and 135:
Table 2. The range (in percent) of
Page 136 and 137:
Table 4. Chemical composition of po
Page 138 and 139:
141FIGURE - 1
Page 140 and 141:
~IT 73qw p' le' IS IFigure 4. Map s
Page 142 and 143:
@A5 3 9 93 3 s 3 m4P 8O C ' . .' ,
Page 144 and 145:
Figure 10. Map showng the abundance
Page 146 and 147:
Figure 14. Map showing the distribu
Page 148 and 149:
IFigure 17. Marine mineral explorat
Page 150 and 151:
central are corals to the integrity
Page 152 and 153:
Very little information is availabl
Page 154 and 155:
leaving little trace of their exist
Page 156 and 157:
REFERENCESAGASSIZ, A. (1903). The c
Page 158 and 159:
PILLAI, C.S.G. (1969b). Studies on
Page 160 and 161:
Table 1.Extent of damage to coral r
Page 162 and 163:
STATUS OF CRITICAL MARINE HABITATS
Page 164 and 165:
OCCURRENCEThe distribution of reefs
Page 166 and 167:
Mining of Reef RockMining of reef r
Page 168 and 169:
-resource. Their significance deriv
Page 170 and 171:
Coating of Aerial Roots by Fine Sed
Page 172 and 173:
associated with the roots (e.g. GOE
Page 174 and 175:
Temperature and SalinityThe effects
Page 176 and 177:
significant numbers in the Red Sea,
Page 178 and 179:
mersas are known to serve as nurser
Page 180 and 181:
BURCHARD, J.E. (1979). Coral fauna
Page 182 and 183: HIRTH, H.F., KLIKOFF, L.G. and HARP
Page 184 and 185: MacNAE, W. (1974). Mangrove forests
Page 186 and 187: RINKEVITCH, B. and LOYA, Y. (1977).
Page 188 and 189: WALKER, D.I. and ORMOND, R.F.G. (19
Page 190 and 191: DAMMING AND DIVERSION OF RIVERSIn d
Page 192 and 193: FUTURE STUDIESWhat can marine scien
Page 194 and 195: !0OD9 -8 Nc80,a,u-3(dcab(Dbrr)8brr)
Page 196 and 197: 0 0-0 00 O0O 0% LD d- m cu 0 0202
Page 198 and 199: STORM SURGES IN THE BAY OF BENGAL*T
Page 200 and 201: low pressure centres over the Bay i
Page 202 and 203: ACKNOWLEDGEMENTSThe writers wish to
Page 204 and 205: Table 1.Latitude and longitude of p
Page 207 and 208: 214
Page 209 and 210: 0Poa9nU0m0Yan-I2li7mYUVQk?401mc0mYm
Page 211 and 212: 0In218
Page 214 and 215: 221
Page 216 and 217: Table 3. Nomenclature used by India
Page 218 and 219: ANDHRAB A Y OFB E N G A L ,.16'LO 4
Page 220 and 221: INDIABAY OF-Point CalirnereLanka L-
Page 222 and 223: pressure in the South Pacific and l
Page 224 and 225: SWALLOW, J.C. (1983). Arabian Sea c
Page 226 and 227: 234
Page 228 and 229: 236
Page 230 and 231: scale wind phenomenon that occurs w
Page 234 and 235: HARTMANN, M., LANGE, H., SEIBOLD, E
Page 236 and 237: Y-Model Domaint=6hrs.b-250 0 59 Xw-
Page 238 and 239: UELEVATIONS (m) ai 18 HOURS L2:-+EL
Page 240 and 241: HARMONIC CONSTITUENT K,Figure 8. Ob
Page 242 and 243: Age of Semi-Diurnal Tide (hrs)28".+
Page 244 and 245: ! 5"BOTTOMFigure 13. Predicted mode
Page 246 and 247: OCEANOGRAPHIC CONDITIONS PELAGIC PR
Page 248 and 249: Low oxygen content in subsurface wa
Page 250 and 251: R/V Dr. F. Nansen trawl of 41 m hea
Page 252 and 253: thermocline temperature decreases s
Page 254 and 255: Nitrate - NitrogenSimilarly to phos
Page 256 and 257: The maximum standing stocks in the
Page 258 and 259: By April/May the demersal stocks ha
Page 260 and 261: in 6 months when spawning occurs. T
Page 262 and 263: REFERENCES3BANSE, K. (1968). Hydrog
Page 264 and 265: GILSON, H.C., (1937). The nitrogen
Page 266 and 267: ROYAL SOCIETY (1963). International
Page 268 and 269: APPENDIX:REGIONAL COOPERATIVE INVES
Page 270 and 271: 20 015 20 25FEBOC015 20 25 30 35M A
Page 272 and 273: W0-8w0-Inww[r3a+eW281
Page 274 and 275: B35 36 a7 XlO+ 35 36 a7- Mar--- Fob
Page 276 and 277: a, A
Page 278 and 279: ...... :'I. .. ,... .. 8.*.. ... ._
Page 280 and 281: ASTAT.Si -Si (OH14 in p M - d ~ n -
Page 282 and 283:
YU0IwYY->02(33-1 II 1amLyY>02(33amL
Page 284 and 285:
I I I I I10 Ic L0U0mI(dw -rlo u0w m
Page 286 and 287:
III I I I0. 1....w'3...-0U-J..,....
Page 288 and 289:
297
Page 290 and 291:
clearly is too low. Because of low
Page 292 and 293:
KARBE, L., THIEL, H., WEIKERT, H. a
Page 294 and 295:
50010001 scoOxygen (rnl/l)0I1I2I3I4
Page 296 and 297:
c1 oc50C10001500_j_///.///II:I? 0:3
Page 298 and 299:
THE RED SEAPHYSIOGRAPHYThe Red Sea
Page 300 and 301:
intensity of magnetization which co
Page 302 and 303:
1969; SEARLE and ROSS, 1975). This
Page 304 and 305:
y normal faulting. This is most int
Page 306 and 307:
South of 19"N, the McKENZIE pole no
Page 308 and 309:
BAUMANN, A., RICHTER, H. and SCHOEL
Page 310 and 311:
EYAL, M., EYAL, Y., BARTOV, Y. and
Page 312 and 313:
LEWIS, B.T.R. (1983). The process o
Page 314 and 315:
TARLING, D.H. and MITCHELL, J.G. (1
Page 316 and 317:
mC- 1000- 2000- 3000E0Figure 2.Sche
Page 318 and 319:
-20b-0,20wFigure 4. Seismicity and
Page 320 and 321:
kmaFigure 6. Summary of seismic ref
Page 322 and 323:
kQ)Um 5U0c04 3N 4COQ)k3M*rlk332
Page 324 and 325:
5 b'o w-Y EO'i Ii04!I 0I0I334
Page 326 and 327:
II,'{34/,'0SOMALIAND: N. DANAKILFig
Page 328 and 329:
spreadingvulcanismmblock faultingII
Page 330 and 331:
SUPERFICIAL SEDIMENTS OF NORTHERN R
Page 332 and 333:
normally sorted, with median diamet
Page 334 and 335:
EL-SAYED (1983) used the trace meta
Page 336 and 337:
BEHAIRY, AKA. (1983). Marine transg
Page 338 and 339:
SHUKRI, N.M. (1953). Bottom deposit
Page 340 and 341:
Table 2 Heavy metal concentrations
Page 342 and 343:
EGYPTEl-Morgan 1Bargan IBargan 2Yub
Page 344 and 345:
Figure 4. Distribution of minerals
Page 346 and 347:
ARAGONITEHIGH HG-CALCITEFigure 6. T
Page 348 and 349:
MARINE LIVING RESOURCES OF THE RED
Page 350 and 351:
This elevated productivity may resu
Page 352 and 353:
REVELLE (1981) mentioned that the p
Page 354 and 355:
FISHELSON, L. (1964). Observation o
show all

139736eo.pdf (20MB) - Japan Oceanographic Data Center

You also want an ePaper? Increase the reach of your titles

Delete template?

Save as template?