Research in Marine Sciences Volume 5, Issue 3, 2020 Pages 764 - 770

Mass water transfer and water-level fluctuations in Farur Island, Persian Gulf

Mojtaba Zoljoodi1, Eram Ghazi2, and Reyhane Zoljoodi3, * 1Faculty member and assistant professor, Atmospheric science Meteorological Research Center (ASMERC), Tehran, Iran 2Marine Science and Technology, Science and Research, Islamic Azad University, Tehran, Iran 3Candidate of bachelor of university of Tehran, Faculty engineering of university of Tehran, Tehran, Iran

Received: 2020-06-02 Accepted: 2020-09-10

Abstract

In this paper, a theoretical model is presented for coastal flows where parameters such as water level fluctuation, current, and mass transfer on the shallow shores of Farur Island are discussed. Parameters used include uniform coastal area (constant depth), interval wave breaks, and the slope of the coast after constant depth and water depth during wave break. There are two very important fractions in this context: constant depth relative to the balance between pressure gradient, and tension induced by the wave associated with the current on the shallow coral reef. The average of water transfer obtained 0.277 Sverdrup which was more in the north and northeast of Farur Island and less in northwest and southwest parts. A mean sea level variation up to 77 cm was calculated. Regarding the different slops over the study area, the vertical shears around the Island have been considered. It is notable that the water level fluctuation and transfer have been calculated after changing the parameters to non-dimensional and in dimensional analysis frame, and also based on the results derived from previous studies. Keywords: Coral coast; Water transfer; Water fluctuation; Coastal currents; Wave.

*Corresponding Author’s Email: [email protected] Research in Marine Sciences 765

1. Introduction Khark, Kharku, Kish, Larak, Lavan, and Sirri. The Farur Island is one of the Iranian Islands The Persian Gulf is a semi-enclosed, sub- that is situated in west of Hurmoz strait with a tropical marginal sea surrounded by a very geographic position from 26.14 to 26.17 North dry land and is located in the subtropical degree and 54.30 to 56.55 East degree, in 66 km northwestThe Persian of Gulf the Indianis a semi-enclosed, Ocean. The sub-tropi Gulf is caland marginal 260 km sea away surround fromed Abu by aMusa very Islanddry land and very shallow with average depth of 35m. Its Bandar Abbas port, respectively. The location and is located in the subtropical northwest of the Indian Ocean. The Gulf is very shallow with water flows through the Strait of Hormuz in of Farur Island is shown in Figure 1. exchangingaverage depth water of with35m. theIts openwater ocean flows (Bowerthrough theThe Strait synoptic of Hormuz and climatological in exchanging stations water with show etthe al .,open 2000). ocean The (BowerGulf with et alhigh., 2000). evaporation The Gulf that with the high Farur evaporation Island is a warm rate 1.5-2region m/yr, with highis rate 1.5-2 m/yr, is among the saltiest water humidity and an average annual temperature of among the saltiest water environment in the world and freshwater inputs come from a few environment in the world and freshwater inputs 27°C. The wind currents in the Persian Gulf comerivers from that a flowfew riversfrom thatIran flow and Iraq,from Iranthat andhave littleapproach contribution the island compared from theto the south, extreme while Iraq,evaporation that have rates little in thecontribution Gulf. These compared conditions, common particularly winter the winds arid blowdesert fromclimate the and west. toextensive the extreme areas evaporation of shallow rateswater, in causethe Gulf. extr emeThe environments study of the Island’sfor coral winds growth, in two with times the of These conditions, particularly the arid desert different period’s shows the prevailing winds highest variations in salinity and temperatures in the world. Thus, coral reefs and climate and extensive areas of shallow water, (in terms of duration, number and intensity) causecommunities extreme inenvironments the Gulf generally for coral have growth, relatively from low westbiodiversity, to south and. theFurthermore, ability of coralsmarine withto survive the highest is probably variations due to their in salinity strong genetic and adaptabilitymeteorology (Symonds in the Persian et al., 1995). Gulf has been temperatures in the world. Thus, coral reefs conducted by Symonds et al. (1995) and the andThe communities Persian Gulf in is the home Gulf to generally many small have a nd resultslarge islands.demonstrated The mostits effects important on currents Iranian and relativelyIslands included low biodiversity, Abu Musa, and Greater the ability Tunb, of Lesserwaves Tunb, in the Hendurabi,area. Hengam, Hormuz, corals to survive is probably due to their strong Water level fluctuations in freshwater Khark, Kharku, Kish, Larak, Lavan, and Sirri. The Farur Island is one of the Iranian Islands genetic adaptability (Symonds et al., 1995). ecosystems enhance efficiency and influence Thethat Persian is situated Gulf in iswest home of Hurmozto many strait small with and a geographicthe timing position of other from biological 26.14 to events26.17 North among largedegree islands. and 54.30 The to most56.55 importantEast degree, Iranian in 66 kmfauna. and 260They km also away modify from Abuhabitat Musa availability, Island Islandsand Bandar included Abbas Abu port, Musa, respectively. Greater The Tunb, locat ionquality of Farur and Island complexity. is shown Thein Figure minor 1. changes Lesser Tunb, Hendurabi, Hengam, Hormuz, in water level can lead to large variations in a

Figure 1. Location of Farur Island, Persian Gulf.

The synoptic and climatological stations show that the Farur Island is a warm region with high humidity and an average annual temperature of 27C. The wind currents in the Persian Gulf approach the island from the south, while common winter winds blow from the west. The study of the Island's winds in two times of different period’s shows the prevailing winds (in terms of duration, number and intensity) from west to south. Furthermore, marine 734 766 Mass water transfer and water-level fluctuations in Farur Island, Persian Gulf... / 764 - 770

coastal area, depending on the morphology of 2. Material and method the system (Kolding and van Zwieten, 2006; Gownaris et al., 2017). Gownaris et al. (2018) In this study, different slopes in four directions discovered relationships between interannual (1) northwest, (2) northeast, (3) southeast, and seasonal water level fluctuations. Their and (4) southwest with different terms of results indicated that interannual water level topography in the Farur Island are considered. fluctuations are positively correlated with the In order to solve the differential equations, primary and overall production and they are the numerical solution method in MATLAB negatively correlated with food chain length, program and the explicit implicit method are fish diversity, and water transfer efficiency. used. The slope area in surf zone according to Li et al. (2011) used the Environmental Fluid its topography is calculated. While around the Dynamics Code (EFC) and a three-dimensional island there are four stations and each side is numerical model to study the impacts of water influenced by its topography and local slope, transfer on the transport of dissolved substances the effect of different parameters on the waves in the lake using the concept of water age. Model is considered. Therefore, at these points, there results showed that the effect of water transfer will be differences between breaking waves, on transport processes in the lake is intensely wave height and distance from shore. Two

influenced by hydrodynamic conditions parameters (water level fluctuation) and dw induced by inflow/outflow branches and wind. (water transfer) are calculated at each station. Wave setup over coral reefs has been explained The wave profile on the coast is shown in by Tait (1972) and Jensen (1991) and has been Figure2 and displays the state of water particles described using the concept of radiation stress are the result of a balance between two forces presented by Longuet-Higgins and Stewart of radial stress in the U direction and the force (1964). The gradient in the radiation stress over of gravity, which is the same as the equation the reef is balanced by an offshore pressure of motion. In the wave profile on the coast gradient analogous to the plane beach solution observed that the force of waves is greater on described by Longuet-Higgins and Stewart the surface and less on the floor for the reason (1964) and Bowen et al. (1968). that the impact of the wave on the shore creates

a reaction force (RX) on the wave. This force

Figure 2. Wave profile on the coast. (Bowen et al., 1968)

The wave profile on the coast is shown in Figure 2 and displays the state of water particles are the result of a balance between two forces of radial stress in the U direction and the force of gravity, which is the same as the equation of motion. In the wave profile on the coast observed that the force of waves is greater on the surface and less on the floor for the reason

that the impact of the wave on the shore creates a reaction force (RX) on the wave. This force affects the wave and the effect of the wave force decreases according to profile (Thornton and Kim, 1993). The Equations (1) and (2) that determine the state of a particle of water are due to the equilibrium of two forces, radial stress and pressure gradient.

(1)

�� 1 ���� �� �� ��� �� (2)

�� 1 ���� �� �� ���� � �� �� where, c is radial stress, b is the pressure, d is the depth of water in any location and is the

water level fluctuation. Effective parameters on the beach are shown in Figure 3. The bedσ and the beach equations in terms of parameters are given as follows (Equations 3 to 10).

736 Research in Marine Sciences 767

FigureFigure 3. 3. Effective Effective parameters parameters on on the the beach beach (Bowen (Bowen et et al al.,., 1968) 1968)

The surface of the coral reef is assumed to be uniform and depth of water increases with Figure 2. Wave profile on the coast. (Bowen et al., 1968)The surface of the coral reef is assumed to be uniform and depth of water increases with Figure 2. Wave profile on the coast. (Bowen et al., 1968) movementmovement towards towards the the sea sea (Bowen (Bowen et et al al.,., 1968) 1968)

The wave profile on the coast is shown in Figure 2 and displays the state of water particles (3) (3) The wave profile on the coast is shown in Figure 2 and displays the st ate of water particles are the result of a balance between two forces of radial stress in ��the U direction and the force ���� 11������ ���� are the result of a balance between two forces of radial�� stress�� in the�� U direction and the force of gravity, which is the same as the equation of motion.���� �� �� In ��the�� wave � � profile on the coast (4)(4) of gravity, which is the same as the equation of motion. In the wave profile on the coast observedFigure 3. Effectivethat the forceparameters of waves on the is beachgreater (Bowen on the et surface ald� .,= � 1968)(X- �� and X �) �less ����� on the floor for the reason (5) observed that the force of waves is greater on the d�surface = � (X- �� andX� r )r �less ����� on the floor for the reason (5) affectsthat the theimpact wave of andthe wave the effect on th e of shore the creates wave a reaction force (RX) on the wave. This force that the impact of the wave on the shore creates a reaction force�������� (R � �X) on the wave. This force (6) (6)(6) forceaffects decreases the wave according and the effectto profile of the (Thornton wave force decreases according to profile (Thornton The surface of the coral reef is assumed to be uniform�� �and depth of water increases with affects the wave and the effect of the wave force decreases�� � according�� to profile (Thornton and Kim, 1993). The Equations (1) and (2) that � �� � � ��� � ��� � andmovement Kim, 1993). towards The the Equations sea (Bowen (1) andet al (2)., 1968) that de�termine�� � � ���the state � ��� of �a particle of water are (7) (7)(7) determineand Kim, 1993). the state The of Equations a particle (1) of and water (2) arethat determine the state of a particle of water are due to the equilibrium of two forces, radial stress and pressure�� gradient. due to the equilibrium of two forces, radial �� ��� � ���� ��� due to the equilibrium of two forces, radial stress and� pressure� �� ��� gradient. (3) (8)(8) stress and pressure gradient . (8) (1) �� 11 �� �� 1 �� �� � � �� ����� (1) � � ��� � � �� ����� (9) ����1 �� �� � (1) 2 2 (4) (9) (9) �� �� �� ���1 ���� � � �� ������d ���� (2) (10)(10) ��d� = ���� (X- �� X� r) ��� ����� w (5) (2) (2)(10) �� � � �� � �� ����1 � �� ����� (6) where,�� c is radial stress, �� b is the pressure, d is ���� �� ����1 � �� ���� where,where,�� isis thethe slopeslope ofof thethe bottom;bottom; X,X, PositivelyPositively facingfacing thethe sea;sea; XXr,r , aa widthwidth wherewhere thethe ����� � �� thewhere,�� depth c���� isof radial water � �� stress, in�� any b locationis the pressure and is, dthe is thewhere, depth of is waterthe slope in any of the location bottom; and X, Positively is the where,� �� � c� is��� radial� ��� stress, � b is the pressure, d is the coraldepthcoral layeroflayer���� water isis uniform uniformin any location andand almostalmost and inclined;inclined; is the(7) D,D, thethe depthdepth ofof waterwater aboveabove thethe uniformuniform coralcoral waterwater levellevel fluctuation.fluctuation. EffectiveEffective parametersparameters on thefacing beach the ����are sea; shown X , a in width Figure where 3. The the bedcoral and layer � layer; d the depthr at which the wavesσ break; d, depth of water in any location; X = L, the thewater beach level are fluctuation. shown in EffectiveFigure 3. parametersThe bed and on theislayer; beachuniform d b,areb, the andshown depth almost in at Figure whichinclined; 3. the The D,waves bed the andbreak;depth d, depth of water in any location; X = L, the the��� beach� �� � ���equations in terms of parameters are given as follows (Equations 3 to 10). σ distance where the wave breaks; W, the (8)vertical velocity obtained by integrating with respect thethe beachbeach equationsequations inin terms of parameters are givenofdistance as water follows where above (Equations the the wave uniform 3breaks; to 10). coral W, layer;the vertical db, velocity obtained by integrating with respect given as1 follows� (Equations 3 to 10). the depth at which the waves break; d, depth Figure 3. Effective parameters on the beach (Bowen et toalto., depth; depth;1968) C Cr r=1, =1, friction friction factor; factor; and and W Wuu is is the the vertical vertical speed speed from from surface surface to to depth. depth. A � flat-bottom � �� ����� is assumed as the initial condition, of water in any location; X = L, the distance(9) 2 where it has a constant depth, the surface of the whereInIn order order the to towave obtain obtain breaks; the the nondimensionl nondimensionl W, the vertical solutions, solutions,velocity divide divide the the outer outer shore shore distance distance by by the the width width of of ������ (10) coralThe surface reef is uniform,of the coral and reef the is depth assumed of water to be uniformobtainedthethe breakwaterbreakwater andby integratingdepth zonezone of waterand andwith divide divide increasesrespect thethe to with depthdepth;depth byby thethe breakingbreaking pointpoint ofof thethe firstfirst wave.wave. ToTo increases with movement towards the sea. C =1, friction factor; and W is the vertical movement����� towards the sea (Bowen et al., 1968) r u (Bowen et�� al., 1968) speed from surface to depth. where,�� is the slope of the bottom; X, Positively facing the sea; Xr, a width where the In order to obtain the nondimensionl solutions,737737 coral layer is uniform and almost inclined;(3) D, the depth of water above the uniform coral (3) ���� divide the outer shore distance by the width layer;�� db,1 the�� ��depth�� at which the waves break; d,of dept theh breakwaterof water in zoneany location; and divide X = the L, depththe � � � distance �� �� where �� the � wave breaks; W, the vertical (4) velocityby the obtained breaking by point integrating of the with first respect (4) wave. 736 To dimensionless equations of sea-level to depth; Cr =1, friction factor; and Wu is the(5)736 vertical speed from surface to depth. d� = � (X- �� X � r ) � ����� fluctuations (Equations 11-14), it is (5) assumed In order to obtain the nondimensionl solutions, dividethat thethe coastouter toshore be smoothdistance and by thewith width the same of ���� � (6) the�� breakwater� � zone and divide the depth by the breaking point of the first wave. To � �� � � ��� � ��� � (7) � �� � � �� � ��� 737 (8)

1 � � � �� ����� 2 (9) ������ (10)

����� �� where,�� is the slope of the bottom; X, Positively facing the sea; Xr, a width where the coral layer���� is uniform and almost inclined; D, the depth of water above the uniform coral layer; db, the depth at which the waves break; d, depth of water in any location; X = L, the distance where the wave breaks; W, the vertical velocity obtained by integrating with respect

to depth; Cr =1, friction factor; and Wu is the vertical speed from surface to depth.

In order to obtain the nondimensionl solutions, divide the outer shore distance by the width of the breakwater zone and divide the depth by the breaking point of the first wave. To

737 dimensionless equations of sea-level fluctuations (Equations 11-14), it is assumed that the coast to be smooth and with the same slope of the failure zone (Mei and Liu, 1997).

(11) ∗ � � � (12) ��� � ∗ � � �Mass water transfer and water-level fluctuations in Farur Island, Persian Gulf... / 764 - 770 (13) 768ε �� ∗ dimensionlessdimensionless ε equationsequations ofof sea-levelsea-level fluctuatfluctuationsions (Equations(Equations 11-14),11-14), itit isis assumedassumed thatthat thethe � coast 3to be� smooth .and with the same slope of the failure zone (Mei and Liu, 1997). coastslope toof � bethe� smooth��� failure�� andzone��� with (Mei the and same Liu, slope 1997). of the failureIn this zoneresearch, (Mei theand effectsLiu, 1997). of shallow (14)waves 2 are ignored. ∗ � (11)(11) u � 3 � � (11) ∗∗ ��� ��� In this2 research,� �the effects of shallow waves are ignored.3. Results and Discussion �� �� � (12)(12) ��� ��� � (12) ∗ 3.∗ 3.�� Results and Discussion The results in four geographical locations of (1( �� �� � (13)(13) εε ��� northeast, (2) northwest, (3) southeast, and (4) ∗∗ (13) The results in εε four geographical locations of (1) southwestnortheast, in(2) Farurnorthwest, Island (3) are southeast, calculated and and �� � . 33 � � . represented in Table 1 in different stations, (4) southwest�� �������� in�� �Farur ������ Island are calculated and represented in Table 1 in different stations,(14)(14) 2 2 where the breaking wave zone is between ∗ (14) 2 3 where∗ the �breaking� wave zone is between 2×10 m2×10to 2×102m tom. 2×10 3m. uu �� � 33 � �� ���� ������ InIn thisthis22 research,research, �the�the effectseffects ofof shallowshallow waveswaves areare ignored.ignored.

Table 1. Calculated parameters on stations of 1, 2, 3, and 4. 3.3. 3.3. ResultsResults andand DiscussionDiscussion

TheThe resultsresults inin fourfour geographicalgeographical locationslocations ofof (1)(1) northeast,northeast,b (m ) (2)(2)L northwest, northwest,(m) D (m (3)(3) ) southeast,southeast, Xr (m) andand � �� � � (4)(4) southwestsouthwest inin FarurFarur IslandIsland��� areare calculatedcalculated� �� �andand� representedrepresented� inin TableTable 11 inin differentdifferent stations,stations, 2 3 wherewhere thethe Stationbreakingbreaking 1 wavewave 3.3×10 zonezone -3 isis betweenbetween0.56 2×102×100.2412mm toto 2×102×102.5 3m.m. 952 0.71 230

-3 Station 2 4.1×10 0.612 0.217 1.23 829 0.74 180 TableTable 1.1. CalculatedCalculated parametersparameters onon stationsstations ofof 1,1, 2,2, 3,3, andand 4.4. -3 Station 3 4.9×10 0.628 0.297 1.85 370 0.65 110

-3 b (m(m )) LL (m)(m) D D (m(m )) X Xr (m)(m) Station 4 2.6×10 0.718 0.216 b 1.43 1500 0.72 r410 �� ���� ��� � ��� ������ � ��� � �� �� -3-3 StationStation 11 3.3×10 3.3×10 0.560.56 0.2410.241 2.52.5 952952 0.710.71 230230 Table 2. Value of σ*, d*, w*, and σ, dw around the Farur island Furthermore, different parameters of σ*, d*, w*, and σ, dw are calculated and represented in 4.1×10-3-3 0.612 0.217 1.23 0.74 StationStation 22 Station4.1×10 1 0.612 Station 20.217 1.23Station 3829 829 0.74Station 4180180 Table 2 around the Farur island. 0.9 -3-3 0.7 0.7 0.7 StationStation 33 4.9×104.9×10 0.6280.628 0.2970.297 1.85 1.85 370370 0.650.65 110110 ∗ � 0.1 0.18 0.16 0.17 2.6×10-3-3 0.718 0.216 1.43 0.72 ∗ Station∗Station 44 2.6×10 0.718 0.216738 1.43 15001500 0.72 410410 � �� 0.69 0.91 0.64 0.87

The mean� value of fluctuation is 0.77 m Furthermore,Furthermore, differentdifferent parametersparameters ofof σσ*,*, d*,d*, w*,w*, andand σσ,, dwdw areare calculatedcalculated andand representedrepresented inin dw 0.23 0.29 0.47 0.12 TableTable 22 aroundaround thethe FarurFarur island.island. The mean value of water transfer is 0.277 sv

738738 In the calculations, it was assumed that the wave breaking depth is the same as the water depth on the Farur coral reef, and water level fluctuation in the dimensionless mode is as small as possible. As shown in Figure 4 a diagram of sea-level fluctuations and water transport along the coral reef, when the calculated water transfer shows the lowest, the value

of nondimensionl Parameter A=Xr/L is also will be minimized. It means that the water transfer will be reduced in the southeastern and northeastern regions of the Farur Island and the region with more depth of water will not change significantly.

Figure 4. a) The diagram of sea-level fluctuations, b) Water transport along the coral reef

In the coastal areas of Farur, when the parameter B is minimized, calculated fluctuations tend to be one and water transfer move to the minimum value and when the water arrives in the coastal area the water level fluctuation will increase and when it reaches to the centre, the water transfer will be the lowest and tends to zero. When the nondimensionl parameter B=

739 Table 2. Value of σ*, d*, w*, and σ, dw around the Farur island

Station 1 Station 2 Station 3 Station 4

0.9 0.7 0.7 0.7 ∗ � 0.1 0.18 0.16 0.17 ∗ ∗ � �� 0.69 0.91 0.64 0.87

The mean� value of fluctuation is 0.77 m

dw 0.23 0.29 0.47 0.12

The mean value of water transfer is 0.277 sv

In the calculations, it was assumed that the wave breaking depth is the same as the water depth on the Farur coral reef, and water level fluctuation in the dimensionless mode is as small as possible. As shown in Figure 4 a diagram of sea-level fluctuations and water transport along the coral reef, when the calculated water transfer shows the lowest, the value of nondimensionl Parameter A=Xr/L is also will be minimized. It means that the water transfer will be reduced in the southeastern and northeastern regions of the Farur Island and Research in Marine Sciences 769 the region with more depth of water will not change significantly.

Figure 4. a) The diagram of sea-level fluctuations, b) Water transport along the coral reef

Furthermore,In the coastal different areas of Farur, parameters when ofthe σ*,parame d*, ter breakingB is minimized, wave point calculated and the fluctuations calculated tend water w*,to beand one σ, dandw are water calculated transfer and move represented to the minimum in level value fluctuation and when is alsothe watergreater arrives than the in thevalues Table 2 around the Farur island. and the calculated water transfer to the lowest coastal area the water level fluctuation will increase and when it reaches to the centre, the In the calculations, it was assumed that the value. Due to the prevailing west and northwest wavewater breaking transfer depthwill be is thethe lowestsame asand the tends water to zero.winds When on the the shores nondimensionl of Farur Island, parameter the highest B= depth on the Farur coral reef, and water level water mass transfer is seen on the west and 739 fluctuation in the dimensionless mode is as northwest coasts. Moreover, most of the water small as possible. As shown in Figure 4 a level changes are observed in these coasts. diagram of sea-level fluctuations and water Therefore, there is more movement and mixing transport along the coral reef, when the in the water column on the southwestern coast calculated water transfer shows the lowest, the of Farur Islands. Environmental conditions on value of nondimensionl Parameter A=Xr/L is the north to southeast coast of Faruar Island also will be minimized. It means that the water are more stable. Farur Island coral colonies are transfer will be reduced in the southeastern and more concentrated in these areas. Farur coral northeastern regions of the Farur Island and reefs due to its location in areas with unfavorable the region with more depth of water will not environmental conditions for growth and life, change significantly. such as shallow depths, extreme temperature In the coastal areas of Farur, when the parameter fluctuations from 12 °C in winter to more than B is minimized, calculated fluctuations tend to 40 °C in summer, high sea level variations and be one and water transfer move to the minimum oil tanker traffic, they are under ecological stress value and when the water arrives in the coastal and are on the verge of enduring their ecology. area the water level fluctuation will increase and According to the results of Pour Sheikhi et al. when it reaches to the centre, the water transfer (2015), the maximum wave height before the will be the lowest and tends to zero. When breaking point was about 0.71 m and the depth the nondimensionl parameter B= D/db (water at the breaking point was about 91.0 m in coasts transfer) increases, it means that the width of of Farur Island. According to the assumptions the shore is considered equal to the depth of the of this study, the results are well consistent. 770 Mass water transfer and water-level fluctuations in Farur Island, Persian Gulf... / 764 - 770

Conclusion desert lake. Ecohydrology, 10: e1769. Gownaris, N.J., Rountos, K.J., Kaufman, L., In this study, the results of the analysis two Kolding, J., Lwiza, K.M., Pikitch, E.K. 2018. nondimensionl Parameter A=Xr/L and B= D/ Water level fluctuations and the ecosystem db illustrate water level fluctuation and water functioning of lakes. Journal of Great Lakes transfer in the Farur Island. These parameters Research, 44(6):1154-63. estimate that the Minimum and maximum Jensen, O. 1991. Waves on coral reefs. In amount of water transfer are in the southeast Coastal Zone ‘91’ Proceedings of the and northeast and the northwest and southwest, Seventh Symposium on Coastal and Ocean respectively. The average of water transfer Management. Long Beach, California. obtained 0.277 Sverdrup, which was more in the American Society of Civil Engineers. New north and northeast of Farur Island and less in the York. pp. 2668-2680. northwest and southwest parts. A mean sea level Kolding, J., and van Zwieten, PM. 2006. Improving variation up to 77cm was calculated. Regarding productivity in tropical lakes and reservoirs. the different slops over the study area, the vertical Li, Y., Acharya, K., and Yu, Z. 2011. Modeling shears around the Island have been considered. impacts of Yangtze River water transfer on By reason of the north and northwest dominant water ages in Lake Taihu, China. Ecological winds on the shores of Farur Island, the highest Engineering, 37(2): 325-334. water mass transfer is observable on the west Longuet-Higgins, M., and Stewart, R.W. 1964. and northwest coasts. Furthermore, most of the Radiation stresses in water waves; a physical water level variations are seen in these coasts. discussion, with applications. Deep Sea, Thus, there is more movement and mixing in 11:529-562. the water column on the northwestern coast of Mei, C., and Liu, P. 1977. Effects of topography Farur Islands. Environmental conditions on the on the circulation in and near the surf-zone– north to the southeast coast of Faruar Island are Linear theory. Estuarine and Coastal Marine more stable, so the Farur Island coral colonies Science, 5:25–37. are more concentrated in these areas. Pour Sheikhi, H., Ashtari Larki, A., and Najjarpour, M.A. 2015. Qualitative References Comparison of Wind Wave Data at the Farur Coasts. Journal of Hydrophysics, 2(1):13-23. Bowen, A., Inman, DL., and Simmons, VP. Symonds, G., Kerry, P. Black, and Young, Ian 1968. Wave set-down and setup. Journal of R. 1995. Wave- driven flow over shallow Geophysical Research, 73(8): 2569–2577. reefs. Journal of geophysical Research, Bower, A., Hunt, HD., and Price, J.F. 2000. 100(C2): 2639-2648. Character and dynamics of the Red Sea and Tait, R. 1972.Wave setup on coral reefs. Journal Persian Gulf outflow. Journal of Geophysical of Geophysical Research, 77: 2207-2211. Research, 105(C3): 6387–6414. Thornton, E., and Kim, C. 1993. Longshore Gownaris, N., Pikitch, E., Aller, J., Kaufman, L., current wave height modulation at tidal Kolding, J., Lwiza, K., and et al. 2017. Fisheries frequency inside the surf zone. Journal of and water level fluctuations in the world’s largest Geophysical Research, 98(16):509-519.