Ocean surface waves are the result of forces acting on the ocean. The characteristics of the waves depend on the controlling forces. Tidal waves are generated by the response to gravity of the Moon and Sun and are rather large-scale waves. Capillary waves are dominated by surface tension in the water. Where the Earth’s gravity is the major determining factor we have the so-called gravity waves. Wind-generated gravity waves are almost always present at sea. These waves are generated by winds somewhere on the ocean. They are also very relevant in climate processes since they play a role in the heat, energy, gases and particles exchange between the oceans and atmosphere. Further, gravity waves can be classified into wind sea and swell. Wind seas are waves that constantly experience the action from the winds. Swells, however, are waves that propagate away from the wind forcing area.

To estimate wind stress over the ocean is one of the most important issues in atmospheric and ocean modeling, including extratropical and tropical cyclones forecasting. In the most operational numerical models the momentum flux at the air-sea interface is parameterized by a nondimensional parameter called surface roughness or Charnock coefficient (z_ch) [1] . This formulation is used in the most atmospheric models, however over the sea, where the surface experiences constant changes, z_ch must consider the state of the sea [2] .

A direct dependence between surface roughness and the sea state is suggested in several papers [3] - [10] . The results of these works pointed that the increase of roughness length (z₀), a height in meters at which the wind speed becomes zero, occurs in the presence of young waves, while there is a low relationship between old waves and roughness length. [11] showed that roughness length computed as function of the developing sea state better represents the observed sea wave height (SWH). The SWH computed by the Charnock constant overestimates the observed values. This pattern is commonly observed in comparisons between observed and modeled SWH.

From observed and experimental data, [12] evaluated the role of the young waves on the air-sea momentum transfer. It was observed that the relationship between z₀ and the waves varies in specific conditions. In addition, it was noted that z₀ tends to diminish as the ratio between c_p and u_* (phase speed at the peak frequency and friction velocity, respectively) decreases. This ratio is a dependent relation between cause (winds) and effect (gravity waves) and is usually called wave age. The parameter wave age indicates the development state of the sea. When the nondimensional value of the wave age is less than 10 the sea is characterized by young waves [13] . The young waves are gravity waves in process of constant growing, once they are continually extracting momentum from the winds. By another way, old waves (wave age greater than 10) are gravity waves that are completely developed. In this case, there is either very weak or any momentum transfer between winds and waves, considering that the winds and waves propagate in the same direction. The term strong (weak) coupling is usually used when the sea is characterized by strong (weak) momentum transfer in the air-sea interface. Strong coupling generally occurs in the presence of young waves, when the winds act as a source of energy to the waves.

[8] investigated the effect of the surface waves on air-sea momentum exchange by combining ocean wave models and a wave boundary layer model. They performed several numerical experiments for constant winds from 10 to 45 m/s to investigate the effect of mature and growing seas on the air-sea momentum exchange. They observed that, for mature seas, the Charnock coefficient is estimated to be about 0.01 - 0.02 and the drag coefficient increases as wind speed increases. With growing seas, results for winds less than 30 m/s show that the drag coefficient is larger for young waves. For winds higher than 30 m/s, however, results show a different trend: very young waves yield less drag.

In this context, the present study evolves a combination of an ocean wave numerical model (WW3) and a very simple algorithm to provide some insight on the effect of the waves on the behavior of some surface variables, including: z₀, sea surface drag (C_D), wind stress (u_*), and wind velocity at 10 meters (U₁₀). These effects are evaluated in conditions of growing and mature sea. A brief outline of the WW3, the simplified algorithm, and the experimental design, used here is introduced in Section 2. Section 3 describes results of the experiments with constant winds from 15 to 45 m/s to investigate roughness length behavior in mature and growing sea conditions. The summary and conclusions are given in Section 4.

The WW3 runs for all time integration. It outputs SWH, mean wave length (MWL), wave mean period, mean wave direction and peak frequency [14] . The simplified algorithm, based on diagnostic equations, computes z₀, C_D, u_* and U₁₀ from two different manner. In the first, the algorithm uses the Charnock relation (R_BULK), which computes z₀ considering z_ch without dependence with waves. In the second case, the parameter wave age is included in the place of z_ch (R_WA). In this case, z_ch takes into account the sea state. The simplified algorithm uses the complete wave spectrum from the WW3 model to compute R_BULK and R_WA.

In this work, the effect of sea state on sea surface roughness length, drag coefficient, wind stress and wind velocity in 10 meters is evaluated. Two distinct cases were analyzed: mature and growing seas. Further, the results are divided into those which consider z_ch as a constant value of 0.0185 and those which use wave age in the place of z_ch.

Figure 1 shows sea wave height and mean wave length values for each experiment with uniform wind speedy. The values of sea wave height and mean wave length were obtained for a reference point near the north edge of the domain (not showed). In the first thirty hours of simulation, the wave height and the wave length show right ratio of development when compared with the 42 hours of spin up. This different behavior is due to the strong momentum transfer from the atmosphere to the ocean which occurs in the first hours of simulation [19] . Figure 1 shows that as the wind becomes strong both sea wave height (Figure 1(a)) and mean wave length (Figure 1(b)) increases. This behavior is observed before 24 hours of simulation. This occurs because sea extracts more energy from the atmosphere in the first hours of spin up. In this case the sea is in process of development. After 30 hours of spin up, the waves reaches their peak intensity (or the sea becomes in equilibrium) and no more growth occurs. In this case, the sea wave height is constant due to the fact that the energy gained by the wind equals to the energy loss by dissipative processes S_ds (Equation (1)).

Figure 2 shows the temporal variability (model time integration) of the wave age term for different wind speed experiments in the same grid point (reference point). When the waves are in process of development the sea is characterized by young waves (wave age less than 15). For mature sea cases (spin up > 30 hours), the sea is dominated by old waves. According to Figure 2 younger waves are related to the strongest winds, while older waves occur in cases of weakest winds. It is also observed that young waves are not produced or observed during weak wind conditions (wind velocity less than 25 m/s).

Figures 3(a)-(d) show scatter plot of z₀, C_D, and U₁₀ versus wave age for each experiment with uniform wind speed. At this time the sea is completely developed. For R_WA case (Figure 3(a)) two different conditions are observed: one with winds less than 30 m/s and other for stronger winds (wind velocity great than 30 m/s). In the first situation, as the waves become older z₀ decreases. The ratio of z₀ diminishing is more accentuated in cases of strong winds. In the second situation (wind velocity less than 30 m/s), different trends are noted. As the waves become older z₀ values keep invariant. This means that old waves (or mature sea) produce slight or any effect on z₀, as observed in several studies. Results from R_BULK case (Figure 3(b)) show that z₀ values are not modified by wave type. This occurs because z₀ in R_BULK case is kept constant and it does not suffer any modification as the sea or waves growth. In R_BULK case the parameter z₀ is just forced by wind speed. Because wind speed is it only forcing mechanism one can expected that z₀ values are large for experiments with strong winds.

Figure 3(c) shows the scatter plot between C_D and wave ages for R_WA case. It is noted that the behavior of C_D is similar to the observed behavior of z₀. For strong wind experiments sea surface drag decreases as the waves become older. In experiments with wind velocity less than 30 m/s, C_D suffers slight changes with the sea state. The relation between CD and wave age are more significant for experiments with strong winds. As young waves yields more drag it is expected that wind speed diminish. Expressive reduction of the wind velocity at 10 meters level under strong wind speed and young sea conditions is observed in Figure 3(d). As the winds become strong and the waves become older U₁₀ increases. The values of U₁₀ are not substantially modified with the sea state in cases of experiments with wind speed weaker than 30 m/s. As can be noted, young waves produce more drag and weak winds. However, in experiments with uniform wind speed lower than 25 m/s the relation between U₁₀ and wave ages weak until they become independent. Those results show that significant changes in the planetary boundary layer as well as momentum, heat and moisture fluxes can be expect by considering the sea state.

Figures 4(a)-(c) show the behavior of z₀, C_D and U₁₀ in the reference point for each experiment with constant

wind speed. Further, surface parameters are put in perspective for developing (06 hours) and mature (72 hours) sea conditions (R_WA). It is also showed the results from R_BULK case. Figure 4(a) shows that young waves yield high values of z₀, while old waves are associated to low values of z₀. Lowest values of z₀ are produced for cases without the sea state influence (R_BULK). More discrepancy between z₀ values are observed for experiments with strong winds. Results from mature sea conditions and R_BULK case show similar z₀ values for weak wind experiments (wind velocity less than 35 m/s). An important fact to note is that R_BULK case underestimates z₀ values in comparison with young and old waves (R_WA) for all experiments. This results are in agreement with numerical modeling studies, including complex coupled experiments with atmospheric and ocean wave models [5] [13] [19] [20] .

Figure 4(b) shows that young waves produce more drag (C_D) than old waves. Lower values of C_D are produced in R_BULK case. Differences between C_D values for mature and growing sea are more expressive in cases of strong wind conditions (wind velocity greater than 30 m/s). C_D values for mature sea conditions are similar to C_D values for R_BULK cases for weak wind experiments (wind velocity less than 30 m/s). It can be also noted that R_BULK case produces the lowest values of C_D for all experiments. This results are similar to those observed for z₀ (Figure 4(a)). It means that young waves yield more drag than old waves and drag is more accentuated for

strong wind conditions. As young waves yield more drag and high values of z₀, it can be expected that in conditions of developing sea the wind velocity, near surface, diminish.

Figure 4(c) shows that U₁₀ is lower at sea dominated by young waves than at developed sea. The wind velocity is reduced in developing sea because young waves produce more resistance (or drag) to the wind flow. According to [19] the reduction of wind velocity, under the influence of young waves, can produce less mass and moisture convergence into meteorological systems. It can diminish both the meteorological system intensity and the height of the waves. Further, the velocity of the considered meteorological phenomena (Hurricanes or extratropical systems) can experience a substantial reduction. At developed sea conditions the wind velocity experiences a less reduction. This occurs due the fact that the resistance to the wind displacement is low is this sea condition. This pattern is similar to conditions of R_BULK case, where sea is considered completely developed. U₁₀ behaves as in the cases of z₀ and C_D for experiments under strong wind conditions. However, under strong wind conditions young waves produces weak winds. Our results are in agreement with several works which have showed that when waves are considered to interact with the lower atmosphere they can produce significant impacts on wind field [5] [13] [19] [20] .

The effect of waves on sea surface roughness length, sea drag, and wind velocity at 10 meters has been investigated by combining the WW3 model with a simplified algorithm. The combined models estimate the behavior of z₀, C_D, and U₁₀ for particular sea state situations. To evaluate the sea state effect the wave age coupling term (c_p/u_*) was included in the algorithm. Several numerical experiments were carried out for constant winds ranging from 15 to 45 m/s. For each numerical experiment, z₀, C_D, and U₁₀ were computed in terms of mature and growing seas.

The results showed that there is a significant dependency between z₀ and the sea state. This relation is strong in cases of developing sea under higher wind speed conditions (wind speed > 30 m/s). This dependency is slight weak in experiments with weak winds (wind speed less than 30 m/s). In addition, it was observed that young waves are related to high values of z₀ while old waves are associated to low values of z₀. The behavior of C_D is very similar to those of z₀ values. The wind velocity at 10 meters shows an inverse trend with relation to z₀ and C_D patterns. As for instance, as the wave age increases, which usually occurs when the sea is reaching an equilibrium condition, U₁₀ also increases. It means that, when the sea is young U₁₀ must decrease because the sea is extremely rough. This pattern is consistent with earlier studies which point out that wind velocity near sea surface is reduced in regions dominated by young waves [5] [19] . This occurs because young waves yield more resistance to the wind displacement and this decreasing in the wind velocity produces significant changes in the heat and moisture fluxes at the air-sea interface.

To evaluate the dependence of z₀ on the sea state under mature and developing sea conditions, two cases were carried out. The first (R_BULK) considers z_ch constant in time, while the second one (R_WA) admits that z_ch changes according to the sea state. In R_BULK case z₀ and C_D values present just a slight increase with wind speed in all experiments. However, in the case of R_WA, z₀ and C_D present accentuated and expressive increase as the wind speed in the numerical experiments increases. Despite both z₀ and C_D obtain a high ratio of increase in the case of R_WA, important and notable differences between developing and mature seas are observed. At developing seas z₀ and C_D increase. In the case of mature sea z₀ and C_D values are lower than those in the developing sea case. The difference between developing and mature seas increases for experiments with strong winds. This behavior is also valid for the variable U₁₀. However, U₁₀ decreases more for developing sea conditions than for mature stage (R_WA). U₁₀ in R_BULK cases does not suffer any modification in all experiments. This is due to the fact that the sea state condition does not affect rigorously the flow passing by developing seas, as it occurs in R_WA cases.

The present results show important aspects when the sea state is included in the computation of sea surface roughness length. These aspects are related to the change of values of drag and wind velocity near surface, which would bring substantial effects on the life cycle of atmospheric system moving on young sea. Despite the numerical experiments showed that wave state affects the patterns of z₀, C_D and U₁₀, they are very limited. This limitation is due to the fact that in real conditions the winds will not blow and support constant wind speed too long. Issuing to bring more reality to the results, the second part of this work includes experiments with idealized tropical storms with different intensity and translation speeds.

José Augusto P.Veiga,Mônica R.Queiroz, (2015) Impact of the Waves on the Sea Surface Roughness under Uniform Wind Conditions: Idealized Cases for Uniform Winds (Part I). Atmospheric and Climate Sciences,05,317-325. doi: 10.4236/acs.2015.53024