# The Evaluation of Estoque Model 1990 in Land/Sea Breezes Occurrence over Northern Persian Gulf

Authors: S. Hassanzadeh; A. Sedaghatkerdar; M. Soyuf Jahromi
Journal: Advances in Meteorology
 (2011)

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## Abstract

This is a mesoscale modeling study of land/sea breeze in the vicinity of Bushehr, Iran which is on the coast of the Persian Gulf. Two days in September, 2002 are studied using the model presented in Estoque Model (1990) (hereafter referred to as EsM90). The EsM90 produces a realistic day-night wind field somewhat in agreement with observations provided by the Port and Shipping Organization of Iran. The study demonstrates that the model has a 3-hour delay predicting the time of the maximum of sea breeze, but accurately predicts when the end of the sea breeze occurs. Accurate estimates near mountains at the edge of the modeled region require a more complex simulation. The study shows that a reliable modeling of a complicated coastal environment like Bushehr not only depends on land/sea breezes but also on elevations and prevailing winds. This dependence is especially important when local thermal forcings are weak, for example, during late afternoon and at night.


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## Body

## 1. Introduction

The Sea Breeze is a common mesoscale phenomenon during the summer months in many coastal areas and has been observed and documented since ancient times [1]. A typical sea breeze may penetrate 50 km or more inland, though its strength depends on the terrain over which it travels. At night the temperature contrast between land and sea reverses and the air over the sea is warmer. This generates a land breeze that blow in the opposite direction to the sea breeze [2]. Sea breeze speed usually ranges between 6 and 10 m/s and from 3 to 5 m/s for a land breeze. The land breezes tend to be weaker than sea breezes. The on/off shore extend of the sea breeze is about 10–20 Km [3].A typical land/sea breeze circulation is seldom completely free of the effects regarding atmospheric factors and nonatmospheric factors. Of the atmospheric factors, the gradient of the prevailing wind [4–7], the stability [5, 7], the cloudiness and humidity [2, 7], and the season [5], and the nonatmospheric ones, the coriolis force and latitudes [8] and land surface characteristics are most important. Land surface characteristics may influence the sea breeze circulation in three main ways: the topography [9–15], the vegetation cover, and soil properties such as soil type and soil moisture [9, 16–18], and finally the coastline shape [19, 20]. Among all factors, the prevailing wind is much more important (e.g., [21]). They showed that the characteristics of the sea breeze circulation over southern and east-central Florida are sensitive to synoptic scale wind direction and speed.On the other hand, a variety of tools, including aircraft measurements [22], pilot balloons (e.g., [23]), satellite images (e.g., [24]) and Doppler radar (e.g., [25]), have been utilized to investigate the thermodynamic and kinematical characteristics and structures of the sea breeze. Laboratory studies (e.g., [26]) and analytical models (e.g., [27]) have contributed extensively to our present knowledge. The sea breeze has also been studied with the help of two-dimensional models (e.g., [4, 28, 29]) and three-dimensional numerical models [21].As studies developed, it is recognized that meteorological models are essential to understanding pollutant transport, and, therefore, there have been many studies of land/sea breezes to analysis the dispersion of pollutants (e.g., [30]). Moreover, sea breezes have long been known to modify water motion in coastal regions. In particular, Hyder et al. [31], Chen and Xie [32], O’Brien et al. [33], Craig [34, 35], and Rosenfeld [36] discussed the impact of sea breeze on diurnal currents in shelf seas. So, studying land/sea breezes can help understanding some features at coastal area. To continue this way, we have provided a numerical two-dimensional model to simulate land/sea breeze at a coastal area of the Persian Gulf.


## 2. Model Description

In this study, we use the Estoque’s Model 1990, (EsM90), which had been defined for a complex terrain. In this study we use the model in Estoque [28] (EsM90) which permits specifying a complex terrain. Although, more complex and accurate models have been developed for simulating terrain-induced mesoscale circulations, but as expected, complex models are generally more accurate than the simpler ones, but, the simpler model has the obvious advantage of requiring smaller computers for integrating the model equations. In addition, the EsM90 equations can incorporate the effect of nonuniformities in surface temperature, roughness, and terrain elevation to some extent.


### 2.1. Model Equations [28]

Primitive model equations use a terrain-following coordinate in the vertical (σ) and the usual coordinates, x and y. The vertical coordinate is defined as
(1)σ≡z-hD-h.
Here, z is the height of a point, h is the height of the terrain, and D is the top of the physical model. The primary equations of the model are the momentum equations, the thermodynamic energy equation, and hydrostatic equation. 								(2)∂u∂t=-u∂u∂x-v∂u∂y+fv-θ∂ϕ∂x-g∂h∂x-K1u-K2(u-uD)+∂∂x(Kx∂u∂x)+∂∂y(Ky∂u∂y)+(∂u∂t)s,∂v∂t=-u∂v∂x-v∂v∂y-fu-θ∂ϕ∂y-g∂h∂y-K1v-K2(v-vD)+∂∂x(Kx∂v∂x)+∂∂y(Ky∂v∂y)+(∂v∂t)s,∂θ∂t=-u∂θ∂x-v∂θ∂y+∂∂x(Kx∂θ∂x)+∂∂y(Ky∂θ∂y)+(∂θ∂t)R+(∂θ∂t)ω+(∂θ∂t)Q,
where u and v are the components of the velocity along x and y, θ is the potential temperature, f is the coriolis parameter, and g is gravity. The quantities uD and vD are the wind component at level D. The quantity ϕ is defined as follows:(3)ϕ=cP(PP0)K,
K=R/cP; R = gas constant for air; cP = specific heat at constant temperature; P0 = 1000 mb. The hydrostatic equation is
(4)∂ϕ∂σ=-gθ(D-h).
All the above model equations were written in height coordinate.In the two momentum equations, there are four physical processes which are parameterized, corresponding to the last five terms:(a)
surface or skin friction:K1u and K1v;(b)
momentum exchange between the surface and the upper level,D, K2(u-uD) and K2(v-vD);(c)
horizontal diffusion of momentum,(5)∂∂x(Kx∂u∂x)+∂∂y(Ky∂u∂y),∂∂x(Kx∂v∂x)+∂∂y(Ky∂v∂y);(d)
slope wind generation,∂u/∂t)s and   ∂v/∂t)s.The first item above,K1u and K1v, represents the tendency of ground friction to reduce the surface wind speed. The expression for the resistance coefficients, K1, is given by
(6)K1≡CD|V|(D-h),where|V|=(u2+v2)1/2,The drag coefficient, CD, depends on the thermal stability; the formula for CD, is presented later in the text. The 2nd item, K2(u-uD) and K2(v-vD), represents the vertical exchange of momentum between the surface and the layer above. This produces the surface wind maximum during the daytime due to vertical mixing. The expression for K2 is K2=CmVD(1-SRi)(1+Cnh/D)/D, where Cm, S, and Cn are empirical constants. The value of these constants and other constants are given in Section 2.4. The quantity Ri is Richardson number. Its formula is presented on a later page. At the 3rd item, horizontal diffusion of momentum, the Kx and Ky coefficients which are the eddy diffusion coefficients, vary horizontally according to the formulas,
(7)Kx=Ck(Δx)2[(∂u∂x)2+(∂v∂x)2]1/2,Ky=Ck(Δy)2[(∂u∂y)2+(∂v∂y)2]1/2.
These expressions are based on a previous formulation by Smagorinsky et al. [37]. The constant Ck, is an empirical quantity, while Δx and Δy are grid distances along the x- and the y-directions. The 4th item, slope wind generation, represents the physical process which generates upslope motions during the daytime and downslope motions at night. The expression for ∂u/∂t)s and ∂v/∂t)s is:
(8)(∂u∂t)s=CBg∂h∂x(θs-θ)θ,(∂v∂t)s=CBg∂h∂y(θs-θ)θ.
Here, CB, is an empirical constant while θs is the temperature of the ground surface.Additionally, there are also four physical processes in theθ equation:(a) horizontal diffusion of heat (the two terms involvingKx and Ky).(b) radiative temperature changes(∂θ/∂t)R. The expression for this term is based on the concept of Newtonian cooling. Thus, (∂θ/∂t)R=CR[0.9(Ts-T)+0.1(TD-T)]. Here, CR, is an empirical constant while T is temperature at surface anemometer level; Ts is ground surface temperature, and TD is temperature at Z=D.(c) temperature changes due to vertical motion,(∂θ/∂t)W, for example, cooling due to expansion when the motion is upward; the formula for this term is
(9)(∂θ∂t)W=-KTθD-θD-h(V⋅Δh)+KC(θD-θ)(∂u∂x+∂v∂y),
the first term on the right-hand side represents the effect of orographically forced vertical motion; the second term represents the effect of vertical motions associated with surface convergence over flat terrain; Here, KT and KC are empirical constants;(d) temperature changes to the sensible heat flux from the earth surface,(∂θ/∂t)Q. In order to estimate this quantity, we assume θ(x,y,σ,t)=θ̅(σ)+θ′(x,y,σ,t), where  θ̅(σ) is the vertical variation of the prevailing large-scale potential temperature. Furthermore, we note that, at a particular point (x,y) at any level, σ, (∂θ/∂t)Q,σ=(∂θ′/∂t)Q,σ. We now make the important assumption that the vertical distribution of the heating is approximated by
(10)(∂θ′∂t)Q,σ=(1-σ1-σa)n(∂θ′∂t)Q,a.Here the subscript,a, refers to values at surface anemometer level; the exponent, n, is an empirical constant. This assumption is based primarily on experience, similar to the power law for wind profiles. From here on, we will drop the subscript, a, from (∂θ′/∂t)Q,σ for the sake of simplicity in notation. Having done that, we will now attempt to express (∂θ′/∂t)Q in terms of the sensible heat flux, Q, from the earth surface. In order to do this, the first step that is done is to integrate the equation above from the surface to the top of the domain. Thus,
(11)∫01(∂θ′∂t)Q,σdσ=(∂θ′∂t)Q(1-σa)-n∫01(1-σ)ndσ.
Performing the integration and then solving for (∂θ′/∂t)Q, one gets
(12)(∂θ′∂t)Q=(1-σa)n(n+1)∫01(∂θ′∂t)Q,σdσ.
Note, however, that the integrand represents the total heating of air column due to sensible heat flux. Therefore, ∫(∂θ′/∂t)Q,σdσ=(Q/(D-h)).Combining this equation with the preceding one, one gets(13)(∂θ′∂t)Q=(n+1)(1-σa)D-hQ≈n+1D-hQ=(∂θ∂t)Q.
Finally, the heat flux (Q) must be expressed in terms of u, v, σ, and the surface temperature,θs. On the basis of the so-called bulk aerodynamic method, the formula is: Q=CD(u2+v2)1/2(θs-θ). The drag coefficient (CD) is, in turn, formulated in terms of Richardson number (Ri) and the roughness parameter (Z0), following a suggestion by Louis et al. [38]. The formula is(14)CD={CDN[1+15Ri(1+5Ri)1/2],Ri>0,CDN{1-15Ri[1+75CDN(-RiZa/Z0)1/2]},Ri≤0,CDN=[k0ln⁡(Za/Z0)]2,Ri≡Zag(θ/θs-1)(u2+v2).
Here, k0 is the Karman constant, Za is the height of the surface observations for wind and temperature. The quantity, CDN, is the customary value of the drag coefficient for neutral stratification.The last important aspect of the model formulation which will be discussed is determination of the geopotential of the surface anemometer level,ϕa. This is done by integrating the hydrostatic equation from the top of the model domain (σD) to the surface anemometer level (σa). In connection with the integration, one has to specify the vertical distribution of θ′. For this purpose, we make the same power law assumption which was made previously. Thus, θσ′=θa′[(1-σ)/(1-σs)]n. Again, we will drop the subscript, a, in θa (for simplicity of notation) with the understanding that θ refers to the surface anemometer level. We note further that: θσ=θσ′+θ̅(σ) with θσ′ given by the preceding formula. Substituting this in the hydrostatic equation, (4), and integrating, we get: ϕ≡ϕa=ϕD+g(D-h)[α-(βθ′)/(1-σa)n]; α≡∫σa1(1/θ(σ))dσ, and β≡∫σa1(1-σ)n/[θ(σ)]2dσ.We have now finished the formulation of the model. All these information about EsM90 equations, the relationships between quantities and parameters are derived from Estoque [28].


### 2.2. Model Spatial and Temporal Situation

We choose Bushehr, Iran and its surrounding area (Figure9) because of its particular coastal line, its two climatological stations, and its important nuclear power plant. The diurnal variations of wind characteristics in this area, especially near the coastal zone, are normally attributed to the land and sea breeze effects [39]. The topographic map was obtained from The Geographical Armed Force Organization of Iran. It is based on UTM. system by the scale of 1 : 500,000 at the WM, VM, WN, and VN sections of this system, between 28°15′–29°15′ E and 50°16′–51°15′ N. The Bushehr basin is an almost flat region but has a mountain range, the Mond Mountains, whose direction is southeast-northwest, (SE-NW). Consequently, this area may be significantly affected by up- and downslope winds. These up- and downslope winds are valley and mountain breezes, respectively.Considering Bushehr Climate was the next step. This region has a warm, humid climate, which is affected by the Mediterranean cyclones and the Sudanese lows in the winter, and summer lows in the summer. Wind rose (Figure1), which is provided from the Bushehr synoptic station, located at 28°59′ N and 50°50′ E, shows that the predominant wind is Northwesterly (Shamal wind). Since the prevailing wind can mask the land/sea breeze, the monthly data are required. Observational studies of land/sea breeze, which were provided by The Port and Shipping Organization of Iran, for some selected days of September, October, November, and December (2002) have been shown in Tables 1, 2, 3, and 4, respectively. The tables illustrate that September has the most mean land/sea breezes. Due to this reason, September was selected as an optimum month for modeling. According to meteorological data, 23 September 2002 was the best, because there was no prevailing wind before and after that day.Table 1
Characteristics of land/sea breezes at different days of September 2002.
DateStarting timeEnding timeDurations (Hour)Speed (m/s)Depth (m)Horizontal extent (km)11th1222114.84614812th1121114.33704313th1321095.66275614th1121113.93043916th1123133.32183317th1123131.31923118th1023143.524535Mean——11.73.828938Table 2
Characteristics of land/sea breezes at different days of October 2002.
DateStarting timeEnding timeDurations (Hour)Speed (m/s)Depth (m)Horizontal extent (km)2nd1321093.3218333rd1121113.6260368th1121113.11923112th1221103.72743728th1119092.209722Mean——103.220532Table 3
Characteristics of land/sea breezes at different days of November 2002.
DateStarting timeEnding timeDurations (Hour)Speed (m/s)Depth (m)Horizontal extent (km)4th1221106.68716610th1222114.33704316th1320085.96965917th1418053.93043920th1519054.438744Mean——7.85.050050Table 4
Characteristics of land/sea breezes at different days of December 2002.
DateStarting timeEnding timeDurations (Hour)Speed (m/s)Depth (m)Horizontal extent (km)19th1221104.43874420th1320081.8651825th1123134.94804927th1619046.27696228th1322105.152051Mean——094.540545Figure 1
The diurnal wind rose of the synoptic Bushehr station from 1970 to 1995. It is provided from 26-year Bushehr synoptic station data, located at 28°59′ E and 50°50′ N. It can easily be seen, the predominant wind is NW-SE wind (Shamal), adopted from Iran Meteorological Organization.Then, a rectangular grid with a horizontal 2.5 km grid spacing was used. The vertical domain was 2 km, since breeze could not go higher. (A typical sea breeze has a height of about 1 km. [2]).The evaluations,h, were determined as follows: suppose point, A, if it was on a contour line, its evaluation was that height of contour line (Figure 2). Otherwise, it was determined by linear interpolation between the nearest contour lines as in the following equation:
(15)hA=1000×AMMN+1200×ANMN.
The resulting topography is illustrated in Figure 3.Figure 2
Inputting elevations to the grid points at the model.Figure 3
The 3D of terrain which is designed by Surfer 8.


### 2.3. Initial and Boundary Conditions

Solving the EsM90 model requires specification of the initial conditions. We setu(x,y), v(x,y), θ(x,y), and P(x,y) to be the value of u, v, θ and P at the surface anemometer level at initial time, t=0.These variables are specified from observations, and so that the initial flow is geostrophically balanced. However, values corresponding to the prevailing flow at the surface anemometer were sometimes chosen. Figures4 and 5 show the 3-hour wind magnitudes and temperature on September 23, 2002 at Bushehr and its coastal station. As can be seen, for example,  |U⃗|=0.7 m/s, θ=27.4° (Bushehr) and  |U⃗|=2.2 m/s, θ=28.6° (Bushehr coastal station) at 0600 Local Time (LT). In addition, model requires the vertical values of θ corresponding to the large-scale flow; that is: θ(z)=θ¯(z); h≤z≤D or θ(σ)=θ¯(σ); 0≤σ≤1. On the basis  of Figure 5, θ(x,y)=26°C=299 K, and,  on  the basis of Figure 6, P(x,y)=1003 Pa. while the land surface temperature varies with time in this study, the water temperature is held fixed at 33°C because there is only a little diurnal variability (Figure 7). The 48-hour simulation starts at 0600 LT, 23 September 2002 and ends at 0600 LT on 25 September. The initial large-scale flow is assumed approximately zero (u(x,y)=v(x,y)=0.1 m/s). Recalling that Figure 4 indicates |U⃗|=0.7 and 2.2 m/s at 6 : 00 LT.Figure 4
The mean 3-hour diagram of the wind speed at September 2002. It shows the actual Bushehr wind conditions for that month. The data adopted from the Synoptic Bushehr Station lactated at 28°59′ E and 50°50′ N and the Coastal Bushehr Station lactated at 28°54′ E and 50°49′ N, Iran Meteorological Organization.Figure 5
The mean 3-hour diagram of the temperature at September 2002. This figure shows the actual Bushehr air temperature at that month for starting Initial Conditions. The data adopted from the Synoptic Bushehr Station lactated at 28°59′ E and 50°50′ N and the Coastal Bushehr Station lactated at 28°54′ E and 50°49′ N, Iran Meteorological Organization.Figure 6
The mean 3-hour diagram of the pressure at September 2002. It illustrates the actual Bushehr pressure at that month for initial conditions. The data adopted from the Synoptic Bushehr Station lactated at 28°59′ E and 50°50′ N and the Coastal Bushehr Station located at 28°54′ E and 50°49′ N, Iran Meteorological Organization.Figure 7
The mean 3-hour diagram of the buoy temperature over the sea surface at September 2002. It shows the Bushehr water temperature at that month. This figure helps us to select the best water temperature for initial conditions. The data adopted from the Synoptic Bushehr Station lactated at 28°59′ E and 50°50′ N and the Coastal Bushehr Station lactated at 28°54′ E and 50°49′ N, Iran Meteorological Organization.Reflective boundaries were applied at open boundaries. Thus for a general quantity,S, we have Sn=Sn-1, where Sn is the open boundary value and Sn-1 is its adjacent value at the model domain.  On the coastal boundaries, rigid-lid conditions were applied, that is: Sn=0. At inflow point, values were held fixed.  At outflow point, the values are being predicted by the model.The roughness parameter,Z0(x,y), is taken as 0.1 m for land and 1 × 104 m for water. Surface temperature, θs(x,y,t), is taken as 26°C = 299 K (due to Figure 5) for t=0, and for t>0, it is being predicted by the formula.


### 2.4. EsM90’s Scheme and Constants

We use the same differencing methods which are described at EsM90. Thus, the forward upstream difference technique of EsM90 is used here.The time step used here is 300 seconds and the 3-hour outputs were printed and analyzed.The initial values ofu, v, and θ were specified so as to be in geostrophic balance. Other parameters and model constants which were used, are Cm=6×10-2; S=0.5; Cn=35; Ck=1×10-4; CB=0.0; CR=3×10-5; KT=1.0; KC=0.05; n=0.01; Za=10 m.The model constant values are determined by numerical experiments in which the model equations were solved by using different values of a particular constant. Then, the particular constant values which gave the most realistic result were selected. The chosen values may not be the optimum ones to be used universally.


### 2.5. EsM90’s Algorithm and the Procedures of the Calculations

The numerical integrations are done by the following step-by-step procedure (See Figure8 for more details).(a)
Using the specified values ofθ and θ̅ at the surface anemometer level, compute the corresponding value of θ′.(b)
Compute the heat term,Q.(c)
Using the value ofθ′, compute ϕ.(d)
Compute the local tendency terms,∂u/∂t and ∂v/∂t.(e)
Using the computed values of∂u/∂t and ∂v/∂t, calculate new (forecast) values of u and v.(f)
Compute the temperature tendency,∂θ/∂t.(g)
Using this value of∂θ/∂t, calculate new (forecast) values of θ.(h)
Using the forecast values ofu, v and θ obtained in steps (e) and (g), repeat steps (a) to (g).Figure 8
Model algorithm.Figure 9
The simulation of wind velocity at 0900 LT on 23 September 2002.Continue this repetitive procedure until the sum of theΔt’s is equal to the desired range of the forecast.The EsM90 program was run on the domain, centered at Bushehr peninsula by a personal computer with Pentium (R)-4, CPU = 1.70 GHz, and RAM = 1 Giga Byte for 48 hours; then, eventually its result was illustrated by Surfer 8 software. The method which was used to make grid files was Kriging.


## 2.1. Model Equations [28]

Primitive model equations use a terrain-following coordinate in the vertical (σ) and the usual coordinates, x and y. The vertical coordinate is defined as
(1)σ≡z-hD-h.
Here, z is the height of a point, h is the height of the terrain, and D is the top of the physical model. The primary equations of the model are the momentum equations, the thermodynamic energy equation, and hydrostatic equation. 								(2)∂u∂t=-u∂u∂x-v∂u∂y+fv-θ∂ϕ∂x-g∂h∂x-K1u-K2(u-uD)+∂∂x(Kx∂u∂x)+∂∂y(Ky∂u∂y)+(∂u∂t)s,∂v∂t=-u∂v∂x-v∂v∂y-fu-θ∂ϕ∂y-g∂h∂y-K1v-K2(v-vD)+∂∂x(Kx∂v∂x)+∂∂y(Ky∂v∂y)+(∂v∂t)s,∂θ∂t=-u∂θ∂x-v∂θ∂y+∂∂x(Kx∂θ∂x)+∂∂y(Ky∂θ∂y)+(∂θ∂t)R+(∂θ∂t)ω+(∂θ∂t)Q,
where u and v are the components of the velocity along x and y, θ is the potential temperature, f is the coriolis parameter, and g is gravity. The quantities uD and vD are the wind component at level D. The quantity ϕ is defined as follows:(3)ϕ=cP(PP0)K,
K=R/cP; R = gas constant for air; cP = specific heat at constant temperature; P0 = 1000 mb. The hydrostatic equation is
(4)∂ϕ∂σ=-gθ(D-h).
All the above model equations were written in height coordinate.In the two momentum equations, there are four physical processes which are parameterized, corresponding to the last five terms:(a)
surface or skin friction:K1u and K1v;(b)
momentum exchange between the surface and the upper level,D, K2(u-uD) and K2(v-vD);(c)
horizontal diffusion of momentum,(5)∂∂x(Kx∂u∂x)+∂∂y(Ky∂u∂y),∂∂x(Kx∂v∂x)+∂∂y(Ky∂v∂y);(d)
slope wind generation,∂u/∂t)s and   ∂v/∂t)s.The first item above,K1u and K1v, represents the tendency of ground friction to reduce the surface wind speed. The expression for the resistance coefficients, K1, is given by
(6)K1≡CD|V|(D-h),where|V|=(u2+v2)1/2,The drag coefficient, CD, depends on the thermal stability; the formula for CD, is presented later in the text. The 2nd item, K2(u-uD) and K2(v-vD), represents the vertical exchange of momentum between the surface and the layer above. This produces the surface wind maximum during the daytime due to vertical mixing. The expression for K2 is K2=CmVD(1-SRi)(1+Cnh/D)/D, where Cm, S, and Cn are empirical constants. The value of these constants and other constants are given in Section 2.4. The quantity Ri is Richardson number. Its formula is presented on a later page. At the 3rd item, horizontal diffusion of momentum, the Kx and Ky coefficients which are the eddy diffusion coefficients, vary horizontally according to the formulas,
(7)Kx=Ck(Δx)2[(∂u∂x)2+(∂v∂x)2]1/2,Ky=Ck(Δy)2[(∂u∂y)2+(∂v∂y)2]1/2.
These expressions are based on a previous formulation by Smagorinsky et al. [37]. The constant Ck, is an empirical quantity, while Δx and Δy are grid distances along the x- and the y-directions. The 4th item, slope wind generation, represents the physical process which generates upslope motions during the daytime and downslope motions at night. The expression for ∂u/∂t)s and ∂v/∂t)s is:
(8)(∂u∂t)s=CBg∂h∂x(θs-θ)θ,(∂v∂t)s=CBg∂h∂y(θs-θ)θ.
Here, CB, is an empirical constant while θs is the temperature of the ground surface.Additionally, there are also four physical processes in theθ equation:(a) horizontal diffusion of heat (the two terms involvingKx and Ky).(b) radiative temperature changes(∂θ/∂t)R. The expression for this term is based on the concept of Newtonian cooling. Thus, (∂θ/∂t)R=CR[0.9(Ts-T)+0.1(TD-T)]. Here, CR, is an empirical constant while T is temperature at surface anemometer level; Ts is ground surface temperature, and TD is temperature at Z=D.(c) temperature changes due to vertical motion,(∂θ/∂t)W, for example, cooling due to expansion when the motion is upward; the formula for this term is
(9)(∂θ∂t)W=-KTθD-θD-h(V⋅Δh)+KC(θD-θ)(∂u∂x+∂v∂y),
the first term on the right-hand side represents the effect of orographically forced vertical motion; the second term represents the effect of vertical motions associated with surface convergence over flat terrain; Here, KT and KC are empirical constants;(d) temperature changes to the sensible heat flux from the earth surface,(∂θ/∂t)Q. In order to estimate this quantity, we assume θ(x,y,σ,t)=θ̅(σ)+θ′(x,y,σ,t), where  θ̅(σ) is the vertical variation of the prevailing large-scale potential temperature. Furthermore, we note that, at a particular point (x,y) at any level, σ, (∂θ/∂t)Q,σ=(∂θ′/∂t)Q,σ. We now make the important assumption that the vertical distribution of the heating is approximated by
(10)(∂θ′∂t)Q,σ=(1-σ1-σa)n(∂θ′∂t)Q,a.Here the subscript,a, refers to values at surface anemometer level; the exponent, n, is an empirical constant. This assumption is based primarily on experience, similar to the power law for wind profiles. From here on, we will drop the subscript, a, from (∂θ′/∂t)Q,σ for the sake of simplicity in notation. Having done that, we will now attempt to express (∂θ′/∂t)Q in terms of the sensible heat flux, Q, from the earth surface. In order to do this, the first step that is done is to integrate the equation above from the surface to the top of the domain. Thus,
(11)∫01(∂θ′∂t)Q,σdσ=(∂θ′∂t)Q(1-σa)-n∫01(1-σ)ndσ.
Performing the integration and then solving for (∂θ′/∂t)Q, one gets
(12)(∂θ′∂t)Q=(1-σa)n(n+1)∫01(∂θ′∂t)Q,σdσ.
Note, however, that the integrand represents the total heating of air column due to sensible heat flux. Therefore, ∫(∂θ′/∂t)Q,σdσ=(Q/(D-h)).Combining this equation with the preceding one, one gets(13)(∂θ′∂t)Q=(n+1)(1-σa)D-hQ≈n+1D-hQ=(∂θ∂t)Q.
Finally, the heat flux (Q) must be expressed in terms of u, v, σ, and the surface temperature,θs. On the basis of the so-called bulk aerodynamic method, the formula is: Q=CD(u2+v2)1/2(θs-θ). The drag coefficient (CD) is, in turn, formulated in terms of Richardson number (Ri) and the roughness parameter (Z0), following a suggestion by Louis et al. [38]. The formula is(14)CD={CDN[1+15Ri(1+5Ri)1/2],Ri>0,CDN{1-15Ri[1+75CDN(-RiZa/Z0)1/2]},Ri≤0,CDN=[k0ln⁡(Za/Z0)]2,Ri≡Zag(θ/θs-1)(u2+v2).
Here, k0 is the Karman constant, Za is the height of the surface observations for wind and temperature. The quantity, CDN, is the customary value of the drag coefficient for neutral stratification.The last important aspect of the model formulation which will be discussed is determination of the geopotential of the surface anemometer level,ϕa. This is done by integrating the hydrostatic equation from the top of the model domain (σD) to the surface anemometer level (σa). In connection with the integration, one has to specify the vertical distribution of θ′. For this purpose, we make the same power law assumption which was made previously. Thus, θσ′=θa′[(1-σ)/(1-σs)]n. Again, we will drop the subscript, a, in θa (for simplicity of notation) with the understanding that θ refers to the surface anemometer level. We note further that: θσ=θσ′+θ̅(σ) with θσ′ given by the preceding formula. Substituting this in the hydrostatic equation, (4), and integrating, we get: ϕ≡ϕa=ϕD+g(D-h)[α-(βθ′)/(1-σa)n]; α≡∫σa1(1/θ(σ))dσ, and β≡∫σa1(1-σ)n/[θ(σ)]2dσ.We have now finished the formulation of the model. All these information about EsM90 equations, the relationships between quantities and parameters are derived from Estoque [28].


## 2.2. Model Spatial and Temporal Situation

We choose Bushehr, Iran and its surrounding area (Figure9) because of its particular coastal line, its two climatological stations, and its important nuclear power plant. The diurnal variations of wind characteristics in this area, especially near the coastal zone, are normally attributed to the land and sea breeze effects [39]. The topographic map was obtained from The Geographical Armed Force Organization of Iran. It is based on UTM. system by the scale of 1 : 500,000 at the WM, VM, WN, and VN sections of this system, between 28°15′–29°15′ E and 50°16′–51°15′ N. The Bushehr basin is an almost flat region but has a mountain range, the Mond Mountains, whose direction is southeast-northwest, (SE-NW). Consequently, this area may be significantly affected by up- and downslope winds. These up- and downslope winds are valley and mountain breezes, respectively.Considering Bushehr Climate was the next step. This region has a warm, humid climate, which is affected by the Mediterranean cyclones and the Sudanese lows in the winter, and summer lows in the summer. Wind rose (Figure1), which is provided from the Bushehr synoptic station, located at 28°59′ N and 50°50′ E, shows that the predominant wind is Northwesterly (Shamal wind). Since the prevailing wind can mask the land/sea breeze, the monthly data are required. Observational studies of land/sea breeze, which were provided by The Port and Shipping Organization of Iran, for some selected days of September, October, November, and December (2002) have been shown in Tables 1, 2, 3, and 4, respectively. The tables illustrate that September has the most mean land/sea breezes. Due to this reason, September was selected as an optimum month for modeling. According to meteorological data, 23 September 2002 was the best, because there was no prevailing wind before and after that day.Table 1
Characteristics of land/sea breezes at different days of September 2002.
DateStarting timeEnding timeDurations (Hour)Speed (m/s)Depth (m)Horizontal extent (km)11th1222114.84614812th1121114.33704313th1321095.66275614th1121113.93043916th1123133.32183317th1123131.31923118th1023143.524535Mean——11.73.828938Table 2
Characteristics of land/sea breezes at different days of October 2002.
DateStarting timeEnding timeDurations (Hour)Speed (m/s)Depth (m)Horizontal extent (km)2nd1321093.3218333rd1121113.6260368th1121113.11923112th1221103.72743728th1119092.209722Mean——103.220532Table 3
Characteristics of land/sea breezes at different days of November 2002.
DateStarting timeEnding timeDurations (Hour)Speed (m/s)Depth (m)Horizontal extent (km)4th1221106.68716610th1222114.33704316th1320085.96965917th1418053.93043920th1519054.438744Mean——7.85.050050Table 4
Characteristics of land/sea breezes at different days of December 2002.
DateStarting timeEnding timeDurations (Hour)Speed (m/s)Depth (m)Horizontal extent (km)19th1221104.43874420th1320081.8651825th1123134.94804927th1619046.27696228th1322105.152051Mean——094.540545Figure 1
The diurnal wind rose of the synoptic Bushehr station from 1970 to 1995. It is provided from 26-year Bushehr synoptic station data, located at 28°59′ E and 50°50′ N. It can easily be seen, the predominant wind is NW-SE wind (Shamal), adopted from Iran Meteorological Organization.Then, a rectangular grid with a horizontal 2.5 km grid spacing was used. The vertical domain was 2 km, since breeze could not go higher. (A typical sea breeze has a height of about 1 km. [2]).The evaluations,h, were determined as follows: suppose point, A, if it was on a contour line, its evaluation was that height of contour line (Figure 2). Otherwise, it was determined by linear interpolation between the nearest contour lines as in the following equation:
(15)hA=1000×AMMN+1200×ANMN.
The resulting topography is illustrated in Figure 3.Figure 2
Inputting elevations to the grid points at the model.Figure 3
The 3D of terrain which is designed by Surfer 8.


## 2.3. Initial and Boundary Conditions

Solving the EsM90 model requires specification of the initial conditions. We setu(x,y), v(x,y), θ(x,y), and P(x,y) to be the value of u, v, θ and P at the surface anemometer level at initial time, t=0.These variables are specified from observations, and so that the initial flow is geostrophically balanced. However, values corresponding to the prevailing flow at the surface anemometer were sometimes chosen. Figures4 and 5 show the 3-hour wind magnitudes and temperature on September 23, 2002 at Bushehr and its coastal station. As can be seen, for example,  |U⃗|=0.7 m/s, θ=27.4° (Bushehr) and  |U⃗|=2.2 m/s, θ=28.6° (Bushehr coastal station) at 0600 Local Time (LT). In addition, model requires the vertical values of θ corresponding to the large-scale flow; that is: θ(z)=θ¯(z); h≤z≤D or θ(σ)=θ¯(σ); 0≤σ≤1. On the basis  of Figure 5, θ(x,y)=26°C=299 K, and,  on  the basis of Figure 6, P(x,y)=1003 Pa. while the land surface temperature varies with time in this study, the water temperature is held fixed at 33°C because there is only a little diurnal variability (Figure 7). The 48-hour simulation starts at 0600 LT, 23 September 2002 and ends at 0600 LT on 25 September. The initial large-scale flow is assumed approximately zero (u(x,y)=v(x,y)=0.1 m/s). Recalling that Figure 4 indicates |U⃗|=0.7 and 2.2 m/s at 6 : 00 LT.Figure 4
The mean 3-hour diagram of the wind speed at September 2002. It shows the actual Bushehr wind conditions for that month. The data adopted from the Synoptic Bushehr Station lactated at 28°59′ E and 50°50′ N and the Coastal Bushehr Station lactated at 28°54′ E and 50°49′ N, Iran Meteorological Organization.Figure 5
The mean 3-hour diagram of the temperature at September 2002. This figure shows the actual Bushehr air temperature at that month for starting Initial Conditions. The data adopted from the Synoptic Bushehr Station lactated at 28°59′ E and 50°50′ N and the Coastal Bushehr Station lactated at 28°54′ E and 50°49′ N, Iran Meteorological Organization.Figure 6
The mean 3-hour diagram of the pressure at September 2002. It illustrates the actual Bushehr pressure at that month for initial conditions. The data adopted from the Synoptic Bushehr Station lactated at 28°59′ E and 50°50′ N and the Coastal Bushehr Station located at 28°54′ E and 50°49′ N, Iran Meteorological Organization.Figure 7
The mean 3-hour diagram of the buoy temperature over the sea surface at September 2002. It shows the Bushehr water temperature at that month. This figure helps us to select the best water temperature for initial conditions. The data adopted from the Synoptic Bushehr Station lactated at 28°59′ E and 50°50′ N and the Coastal Bushehr Station lactated at 28°54′ E and 50°49′ N, Iran Meteorological Organization.Reflective boundaries were applied at open boundaries. Thus for a general quantity,S, we have Sn=Sn-1, where Sn is the open boundary value and Sn-1 is its adjacent value at the model domain.  On the coastal boundaries, rigid-lid conditions were applied, that is: Sn=0. At inflow point, values were held fixed.  At outflow point, the values are being predicted by the model.The roughness parameter,Z0(x,y), is taken as 0.1 m for land and 1 × 104 m for water. Surface temperature, θs(x,y,t), is taken as 26°C = 299 K (due to Figure 5) for t=0, and for t>0, it is being predicted by the formula.


## 2.4. EsM90’s Scheme and Constants

We use the same differencing methods which are described at EsM90. Thus, the forward upstream difference technique of EsM90 is used here.The time step used here is 300 seconds and the 3-hour outputs were printed and analyzed.The initial values ofu, v, and θ were specified so as to be in geostrophic balance. Other parameters and model constants which were used, are Cm=6×10-2; S=0.5; Cn=35; Ck=1×10-4; CB=0.0; CR=3×10-5; KT=1.0; KC=0.05; n=0.01; Za=10 m.The model constant values are determined by numerical experiments in which the model equations were solved by using different values of a particular constant. Then, the particular constant values which gave the most realistic result were selected. The chosen values may not be the optimum ones to be used universally.


## 2.5. EsM90’s Algorithm and the Procedures of the Calculations

The numerical integrations are done by the following step-by-step procedure (See Figure8 for more details).(a)
Using the specified values ofθ and θ̅ at the surface anemometer level, compute the corresponding value of θ′.(b)
Compute the heat term,Q.(c)
Using the value ofθ′, compute ϕ.(d)
Compute the local tendency terms,∂u/∂t and ∂v/∂t.(e)
Using the computed values of∂u/∂t and ∂v/∂t, calculate new (forecast) values of u and v.(f)
Compute the temperature tendency,∂θ/∂t.(g)
Using this value of∂θ/∂t, calculate new (forecast) values of θ.(h)
Using the forecast values ofu, v and θ obtained in steps (e) and (g), repeat steps (a) to (g).Figure 8
Model algorithm.Figure 9
The simulation of wind velocity at 0900 LT on 23 September 2002.Continue this repetitive procedure until the sum of theΔt’s is equal to the desired range of the forecast.The EsM90 program was run on the domain, centered at Bushehr peninsula by a personal computer with Pentium (R)-4, CPU = 1.70 GHz, and RAM = 1 Giga Byte for 48 hours; then, eventually its result was illustrated by Surfer 8 software. The method which was used to make grid files was Kriging.


## 3. Results and Discussion

This study has attempted to produce the land/sea breeze development over the Bushehr peninsula. This peninsula is fairly complicated in that there is a large embayment to the north and coastal mountain to the south.  Although this mountain is not very high (less than 400 m), the production of up-and downslope winds cannot be ignored. Figures6–21 illustrate the model’s wind vectors at the anemometer level. The tick lines in these figures are the coastlines and thin ones are terrain height (contouring interval 100 m). A velocity scale (in m/s), for each figure is provided. The two large solid circles locate the meteorological stations at Bushehr (24° N, 29° E) (denoted as Bush) and at the near Bushehr (22° N, 28° E) (denoted as Bushcoast). The large × demonstrates the location of the meteorological buoy station. The open stars locate three landmarks: Burnt Castle, Bulkhayre Ameri, and Salem Abad. The solid triangle denotes the peak of the Mond Mountains. The capital A is an authority point, (38, 11), on the eastern side of the Mond Mountains. This place is adopted to study the model ability to mix land/sea breezes and mountain/valley breezes.Figure 10
The simulation of wind velocity at 1200 LT on 23 September 2002.Figure 11
The simulation of wind velocity at 1500 LT on 23 September 2002.Figure 12
The simulation of wind velocity at 1800 LT on 23 September 2002.Figure 13
The simulation of wind velocity at 2100 LT on 23 September 2002.Figure 14
The simulation of wind velocity at 0000 LT on 24 September 2002.Figure 15
The simulation of wind velocity at 0300 LT on 24 September 2002.Figure 16
The simulation of wind velocity at 0600 LT on 24 September 2002.Figure 17
The simulation of wind velocity at 0900 LT on 24 September 2002.Figure 18
The simulation of wind velocity at 1200 LT on 24 September 2002.Figure 19
The simulation of wind velocity at 1500 LT on 24 September 2002.Figure 20
The simulation of wind velocity at 1800 LT on 24 September 2002.Figure 21
The simulation of wind velocity at 2100 LT on 24 September 2002.


### 3.1. Start Time and Duration of Breezes

The sea breeze starts at 0900 LT along coastal line (Figure9) and as sea breeze penetrates into land at 1200 and 1500 LT, upslope winds are also generated (Figures 10 and 11). By looking at Figure 12, we see that wind field is being reduced and at 2100 LT the surface wind is perfectly calm. The observations of the Port and Shipping Organization of Iran, (Table 1), show that 2100 LT ± 0100 is when the land/sea breezes end. So our study using the EsM90 model realistically predicts when the land/sea breezes end. At 0000 LT downslope winds start at Mond Mountain. Land breezes develop at 0300 LT (Figures 15 or 23) and 0600 LT (Figures 16 or 24) over the Persian Gulf and end at 0900 LT (Figure 17). Observational data shows that land breeze ends exactly at 0600 LT (Figure 4), while, this time land breeze model’s prediction exists and finishes at 0900 LT.By comparing the two days, it seems the sea breeze extends in to the afternoon.  The duration of the sea breeze on the first and second day is about 15 h and 12 h, respectively, (Figure25), while the observed duration is about 15 h (Figure 4). But in both days the sea breeze is finished at 2100 LT (Figure 26). The duration and end time are two important results of this simulation; observational studies similarly indicate it is about 11 to 13 hours at September (Table 1). Parvaresh et al. [39] showed during the 21-day period (15 July–4 August 2000), that sea breezes have finished at 2100 LT. Their data were recorded at the same buoy station indicated by × in our simulation figures [39]. The prediction duration of the land breeze is 9 h; however the observations of Bushehr Synoptic Station show no land breeze and Bushehr Coastal Station’s land breeze’s duration is just about 6 h. Thus the model’s predictions overpredict the duration of land breeze by about 3 h.


### 3.2. Intensity and Horizontal Extension

After starting model and by approaching noon, intensity increases so that it reaches a maximum of 9.3 m/s at 1200 LT on the 1st day (Figure10) or 7.3 m/s at 1500 LT on the 2nd day (Figure 19). Then, it decreases by the evening and disappeared at 2100 LT in both days (just small values at the back of the mountain). If we make 1800 LT an exception, it can be said that sea breeze velocity on the 1st day is stronger than the 2nd one, while land breeze is reversed. Maximum of land breeze speed is 5.2 m/s at 0000 LT, 5.7 m/s at 0300 LT, and 8.5 m/s at 0600 LT, all of them take place on the 2nd day. When the land breeze ends at 0900 LT, just a weak sea breeze with the maximum of 2.2 m/s is predicted.The predicted sea breeze at Bushehr meteorological station is less than the observed wind speed by 1 m/s on the average; the predicted land breeze is somewhat greater than the observation (Figures4 and 27). The maximum predicted sea breeze occurs at 1200 LT while the observed one is three hours later at 1500 LT (Figures 4 and 27), but at the 2nd day is exactly the same.Parvaresh et al. [39] showed that wind speed at 10 m above sea level (U10) varied between 0.34 and 10.38 m/s with a characteristic diurnal oscillation. They also resolved wind speed into two components, along and across the shore. Their results show that the wind speed associated with the land breeze is less than 6 m/s, but that of the sea/land breeze is greater [39]. Although the model simulates a different month and year than when the data were collected, and the observations (as noted in [39]) do not remove the prevailing wind effect from the reported land/sea breeze, the model results show the land breeze <6 m/s at the observations, which is in agreement with the observations.If we use Bush pint (24° N, 29° E or (24, 29)) as a reference, by 1200 LT on 23 September 2002 (Figure10), horizontal extension of sea breeze is about 20 km and doubled by 1500 LT. By 1500 LT on 24 September 2002 (Figure 19), it is about 20 km in land, whereas land breeze is at about 60 km at 0600 LT over the sea. Comparing these two days, 2nd day’s sea breeze shows a shorter horizontal penetration than the 1st one at the same times, while land breeze is opposite.Since, sea breeze start atu=v=0.1 m/s on the first day, these values are different on the next day, sea breeze, therefore, starts from the previous land breeze, and this delay to reproducing land/sea breezes influence, both the intensity and horizontal extension, to some extent.


### 3.3. The Effect of Coastal Topography

At 1200 LT and 1500 LT (Figures13 and 14), a convergence area can be seen over the Bushehr peninsula, and also near Burnt Castle, Bulkhayre Ameri and Salem Abad. Lyons et al. [40] and Nicholls et al. [41] have shown that thunderstorms frequently form near and ahead of sea breeze fronts; so cumulus clouds and thunderstorms are probable at the convergence zones. Convergence zones are not restricted to sea breezes. Two of them are generated at 0300 and 0600 LT over the Persian Gulf when land breezes developed perfectly over the sea.If we look carefully to the model prediction of breezes at 2100 LT, it can be recognized that the maximum velocity values (2.6 m/s on 23 September 2002 and 3.2 m/s on 24 September 2002) is returning to the values back of the mountain.One gets the impression from the model results (Figures9–24) that the land/sea breeze is less pronounced along the coast at the northern boundary, and that this breeze is quite pronounced along the southern coast in the region near Mond Mountain. The predicted winds at point A on the lee side of mount (Figure 29) show that the land/sea breeze is generally stronger there than at the Bushehr and Bushehr Coastal stations (Figures 27 and 28).Figure 22
The simulation of wind velocity at 0000 LT on 25 September 2002.Figure 23
The simulation of wind velocity at 0300 LT on 25 September 2002.Figure 24
The simulation of wind velocity at 0600 LT on 25 September 2002.Figure 25
Maximum of wind velocity which is predicted for 0600 LT on 23 September 2002 to 0600 LT on 25 September 2002.Figure 26
The wind velocity at point Buoy (22, 24) for two study day.Figure 27
The predicted wind velocity at point Bush (24, 29) for two study day.Figure 28
The predicted wind velocity at point Bushcoast (22, 28) for two study days.Figure 29
The predicted wind velocity at an authority point A (38, 11) for two study day.


## 3.1. Start Time and Duration of Breezes

The sea breeze starts at 0900 LT along coastal line (Figure9) and as sea breeze penetrates into land at 1200 and 1500 LT, upslope winds are also generated (Figures 10 and 11). By looking at Figure 12, we see that wind field is being reduced and at 2100 LT the surface wind is perfectly calm. The observations of the Port and Shipping Organization of Iran, (Table 1), show that 2100 LT ± 0100 is when the land/sea breezes end. So our study using the EsM90 model realistically predicts when the land/sea breezes end. At 0000 LT downslope winds start at Mond Mountain. Land breezes develop at 0300 LT (Figures 15 or 23) and 0600 LT (Figures 16 or 24) over the Persian Gulf and end at 0900 LT (Figure 17). Observational data shows that land breeze ends exactly at 0600 LT (Figure 4), while, this time land breeze model’s prediction exists and finishes at 0900 LT.By comparing the two days, it seems the sea breeze extends in to the afternoon.  The duration of the sea breeze on the first and second day is about 15 h and 12 h, respectively, (Figure25), while the observed duration is about 15 h (Figure 4). But in both days the sea breeze is finished at 2100 LT (Figure 26). The duration and end time are two important results of this simulation; observational studies similarly indicate it is about 11 to 13 hours at September (Table 1). Parvaresh et al. [39] showed during the 21-day period (15 July–4 August 2000), that sea breezes have finished at 2100 LT. Their data were recorded at the same buoy station indicated by × in our simulation figures [39]. The prediction duration of the land breeze is 9 h; however the observations of Bushehr Synoptic Station show no land breeze and Bushehr Coastal Station’s land breeze’s duration is just about 6 h. Thus the model’s predictions overpredict the duration of land breeze by about 3 h.


## 3.2. Intensity and Horizontal Extension

After starting model and by approaching noon, intensity increases so that it reaches a maximum of 9.3 m/s at 1200 LT on the 1st day (Figure10) or 7.3 m/s at 1500 LT on the 2nd day (Figure 19). Then, it decreases by the evening and disappeared at 2100 LT in both days (just small values at the back of the mountain). If we make 1800 LT an exception, it can be said that sea breeze velocity on the 1st day is stronger than the 2nd one, while land breeze is reversed. Maximum of land breeze speed is 5.2 m/s at 0000 LT, 5.7 m/s at 0300 LT, and 8.5 m/s at 0600 LT, all of them take place on the 2nd day. When the land breeze ends at 0900 LT, just a weak sea breeze with the maximum of 2.2 m/s is predicted.The predicted sea breeze at Bushehr meteorological station is less than the observed wind speed by 1 m/s on the average; the predicted land breeze is somewhat greater than the observation (Figures4 and 27). The maximum predicted sea breeze occurs at 1200 LT while the observed one is three hours later at 1500 LT (Figures 4 and 27), but at the 2nd day is exactly the same.Parvaresh et al. [39] showed that wind speed at 10 m above sea level (U10) varied between 0.34 and 10.38 m/s with a characteristic diurnal oscillation. They also resolved wind speed into two components, along and across the shore. Their results show that the wind speed associated with the land breeze is less than 6 m/s, but that of the sea/land breeze is greater [39]. Although the model simulates a different month and year than when the data were collected, and the observations (as noted in [39]) do not remove the prevailing wind effect from the reported land/sea breeze, the model results show the land breeze <6 m/s at the observations, which is in agreement with the observations.If we use Bush pint (24° N, 29° E or (24, 29)) as a reference, by 1200 LT on 23 September 2002 (Figure10), horizontal extension of sea breeze is about 20 km and doubled by 1500 LT. By 1500 LT on 24 September 2002 (Figure 19), it is about 20 km in land, whereas land breeze is at about 60 km at 0600 LT over the sea. Comparing these two days, 2nd day’s sea breeze shows a shorter horizontal penetration than the 1st one at the same times, while land breeze is opposite.Since, sea breeze start atu=v=0.1 m/s on the first day, these values are different on the next day, sea breeze, therefore, starts from the previous land breeze, and this delay to reproducing land/sea breezes influence, both the intensity and horizontal extension, to some extent.


## 3.3. The Effect of Coastal Topography

At 1200 LT and 1500 LT (Figures13 and 14), a convergence area can be seen over the Bushehr peninsula, and also near Burnt Castle, Bulkhayre Ameri and Salem Abad. Lyons et al. [40] and Nicholls et al. [41] have shown that thunderstorms frequently form near and ahead of sea breeze fronts; so cumulus clouds and thunderstorms are probable at the convergence zones. Convergence zones are not restricted to sea breezes. Two of them are generated at 0300 and 0600 LT over the Persian Gulf when land breezes developed perfectly over the sea.If we look carefully to the model prediction of breezes at 2100 LT, it can be recognized that the maximum velocity values (2.6 m/s on 23 September 2002 and 3.2 m/s on 24 September 2002) is returning to the values back of the mountain.One gets the impression from the model results (Figures9–24) that the land/sea breeze is less pronounced along the coast at the northern boundary, and that this breeze is quite pronounced along the southern coast in the region near Mond Mountain. The predicted winds at point A on the lee side of mount (Figure 29) show that the land/sea breeze is generally stronger there than at the Bushehr and Bushehr Coastal stations (Figures 27 and 28).Figure 22
The simulation of wind velocity at 0000 LT on 25 September 2002.Figure 23
The simulation of wind velocity at 0300 LT on 25 September 2002.Figure 24
The simulation of wind velocity at 0600 LT on 25 September 2002.Figure 25
Maximum of wind velocity which is predicted for 0600 LT on 23 September 2002 to 0600 LT on 25 September 2002.Figure 26
The wind velocity at point Buoy (22, 24) for two study day.Figure 27
The predicted wind velocity at point Bush (24, 29) for two study day.Figure 28
The predicted wind velocity at point Bushcoast (22, 28) for two study days.Figure 29
The predicted wind velocity at an authority point A (38, 11) for two study day.


## 4. Conclusion

In brief, the EsM90 on Bushehr has some defects to reduce enough as breeze goes far in land or sea. Furthermore, some deviations occur on the prediction of breeze duration, although it is much more powerful to bring a good simulation based on coastal shape and approximately real values (about 0–3 m/s difference). The model also combines land/sea breezes by mountain/valley breezes very well at the side near the coast but be defeated to produce separately mountain/valley breezes as can be seen at the back of Mond Mountain.The duration of the sea breeze on the first and second day is about 15 and 12 hours, respectively. The model predicts well the land breeze at the Bushehr coastal station.The land/sea breeze is less pronounced along the coast at the northern boundary, and that this breeze is quite pronounced along the southern coast in the region near Mond Mountain.In the end, a satisfied wind field is produced which can show up- and downslope winds in addition to land/sea breezes.



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*Source: 564237-2011-06-29.xml*