INFLUENCE OF METEOROLOGICAL AND RELATED FACTORS ON SURFACE OZONE PATTERN AT MAKKAH STATION

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INFLUENCE OF METEOROLOGICAL AND RELATED FACTORS ON SURFACE OZONE PATTERN AT

MAKKAH STATION A. K Al-khalaf

Department. of Meteorology

Faculty of Meteorology, Environment, and Arid Land Agriculture King Abdulaziz University, P. O. Box 80208, Jeddah 21413, Saudi Arabia

Abstract

Surface ozone concentration, nitrogen dioxides, and related meteorological factors in urban areas of central Makkah, Saudi Arabia, at the east of the Holly mosque in year 1998, is investigated and analyzed with time series through monthly and seasonally time scales. High O3 episodes occur most of the time during year, with a major peak in autumn and minimum in winter. Near-surface monthly ozone concentrations exceed 0.080 ppm for the time of the study in October 1998. Typically, they occur in episodes during fair weather conditions with high solar radiation, and high air temperature (above 35°C). The corresponding monthly NOx daytime mean at the site is 0.020 ppm to .060 ppm. It is suggested that most of the ozone peaks are due to regional scale photochemistry. Data from the site show increasing monthly values from 0.036 to 0.080 ppm, while slowly monthly moving ozone peak. A classification according to influencing parameters shows that ozone formation is enhanced by high Concentrations of NOx,

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frequently combined with high radiation. Also, low Concentrations of NOx

combined with high radiation indicates that NOx limited ozone formation regime. For diurnal variations, ozone shows a marked diurnal cycle with no ozone peaks occur after sunset or in the early morning, indicating regional scale photochemistry. In all, early fall or spring ozone peaks are caused by in-situ photochemical ozone formation rather than transport. The data shows that long-lasting high pressure conditions, in Central Makkah can promote considerable photochemical ozone formation on a regional scale.

Introduction

Ozone (O3) is a secondary pollutant, photochemically produced in the atmosphere from reactions involving a variety of volatile organic compounds (VOCs), composed mainly of nonmethane hydrocarbons, in the presence of sufficient sunlight and nitrogen oxides (NOx) such as nitric oxide (NO) and nitrogen dioxide (NO2). Nitrogen oxides (NOx) emitted from a variety of natural and anthropogenic sources (notably motor vehicles). O3 is the most important gas in the photochemistry of the atmosphere and is the primary constituent of photo oxidative smog. It can thus be considered an indicator of the overall burden of atmospheric oxidants. The emissions of precursors for O3 formation over most of world are sometimes sufficient to feed photochemical episodes and keep mean concentrations in spring and summer at levels potentially toxic for human and plant health. This means that O3 levels depend mainly on the meteorological situation (Beck et al. 1998).

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The rate of these photochemical reactions, as well as the subsequent transport and scavenging of ozone, depends greatly on meteorological conditions, which are naturally variable (eder et. al 1994). They applied two-stage clustering approach as part of an automated meteorological classification scheme designed to better explain the dependence of ozone on meteorology. Using an atmospheric chemical reaction mechanism applied to air parcels near the earth's surface, the sensitivities ozone (O3) formation rates are measured for changes in four meteorologically controlled parameters: temperature, sunlight intensity, water vapor mixing ratio, and isoprene concentration. Over a wide range of NOx and anthropogenic hydrocarbon concentrations, enhanced photolysis rates and elevated isoprene concentrations are calculated to be the most significant factors contributing to increased O3 production rates on warmer days (Chris et al 1994). These results suggest that the most uncertain yet important meteorological factor controlling regional-scale O3 formation is fractional cloudiness and its impact on photolysis rates

Meteorology affects the formation, transport, deposition and seasonal behavior of ozone. The meteorological conditions which help the formation of ozone are intense solar radiation, low wind speed, high temperature and a restricted boundary layer depth (Comrie and Yarnal 1992; Mckendry, 1994). Radiation and temperature drive the chemical reactions producing ozone, while boundary layer characteristics and the absence of wind are the factors which respectively lead to the build-up of precursors and limit their dispersion. Ozone concentrations are characterized by seasonal and diurnal variations. Day-to–day variations in

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O3 attributed to variations in the rate, type, and sources of pollutant emissions as well as to the state of the atmosphere (Oke 1987). O3 formation increases rapidly during springtime and decreases sharply in the second half of the summer. Its diurnal behavior during spring and summer is in accordance with sunshine and daily temperature. In midlatitude regions, meteorological variables that influence air quality are strongly modulated by the synoptic-scale circulation as displayed by the passage of fronts, cyclonic systems, and anticyclones. This has encouraged the application of synoptic climatology to the investigation of day-to-day variations in air quality.

Unexpected high near-surface ozone values have been observed in Makkah air pollution monitoring station in 1998 and gave rise to some concern. In the month of October, 1998, record high ozone peaks have been observed in Makkah. In this study possible causes for theses episodes are discussed. There is an ongoing discussion on what extent this ozone is of stratospheric origin or in-situ photochemical formed (Penkett and Bric, 1986; Janach 1989; Roelofs and lelieveld, 1997). Ozone peaks appear also in industrialized regions, mainly in Northern Central Europe (Scheel, 1997), but also in other parts of the world (Wakamatsu et al., 1998). There are mostly two possible causes for ozone peaks: in-situ photochemical formation from NOx and (VOC) or large scale transport of ozone loaded air from the upper troposphere or stratosphere. Geophysical Fluid Dynamics Laboratory global chemical transport model was applied to investigate the contribution of photochemistry to the winter-spring ozone maximum in the northern hemisphere (NH) midlatitude free troposphere (770-240 mbar;

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30°N-60°N). Free troposphere ozone mass slowly builds up in the winter and early spring, with net chemistry and transport playing comparable roles (Yienger, et. al, 1999).

In this study, Makkah air pollution monitoring station was investigated.

In line with previous studies, which were mainly concerned with the long- term behavior, such as trend and seasonal variations, ozone concentrations were studied as a function of season and month. The interest was to study the relationship between ozone and meteorological parameters in the presence of nitric oxides.

Methods and data

Surface ozone measurements have been performed at the station Point in central Makkah. The measurement station, which is part of the Institute of the custodian of the two Holly Mosques for Hajj research, is predominantly exposed to polluted air due to movement of cars and people around the Holly mosque. The surface observations station located in the central part of the city, at the east of the Holly mosque, (21.44ô N, 39.77ô E, elevation 230 m). The data included air temperature (ôC), Barometric pressure (mb), Relative humidity (%), rainfall, wind speed and direction, and solar radiation. The air quality data included ozone, nitric oxides, dust, and some other chemical elements. These data are recorded at hourly bases.

This work analyzes the variations in monthly and seasonally means of daily maximum 1-hr O3 concentrations, the corresponding values for nitrogen oxides (nitrous oxide + nitrogen dioxide), and meteorological

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parameters in the region located close to the Holly mosque in central Makkah, Saudi Arabia over one year period.

Results and Analyses

Monthly mean values of daytime (10:00-18:00) ozone concentration, Global radiation (W/m²), temperature (^oC), relative humidity (%), wind speed (m/s), and nitrogen oxides NOx at the station for January to December 1998 are shown in Figure 1a-f. As shown in the figure 1, the ozone time series in1998 does not indicate any significant increase except in the month of October. Monthly ozone concentration exceeded 0.08 ppm for the month of October. Figure 1a shows the monthly mean ozone concentrations at the station have a range between 0.036 ppm, in the month of January and a value of 0.083 ppm in the month of October. Ozone peaks above 0.050 ppm in February to August occurred of these months with high solar radiation, high air temperature, variable values of relative humidity, and low wind speed (Figure 1b-e). This dependence on meteorology indicates to photochemistry. However, in winter, ozone photochemistry is known to be limited because the solar radiation is low. In early spring, air masses are exposed to a rapidly increasing solar radiation, which alters the chemical conditions.

The ozone formation due to photochemistry can be described using this kind of classification. The monthly mean of the five highest values from 10:00 to 18:00 for each day has been considered for February to May. This value is considered to best reproduce local photochemical

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activity, while minimizing ozone by NO transport in the morning and night time. These day time ozone peaks were classified according to the daytime mean NOx concentration (10:00-18:00) and the mean global radiation form 10:00 to 18:00. This classification, for high radiation, is similar to the method proposed by Bronnimann (1999) to find out the sensitivity of ozone formation to NOx. He made the classification based on daily maximum and from January to April.

The results are shown in Figure 2 a-c for Makkah station. The X- axis gives the average daytime ozone peak of the period of spring (Feb to May) whereas the Y-axis gives the average daytime solar radiation for figure a, and nitrogen dioxides for figure 2b. For figure 2c, the X- axis is the average daytime NOx and the Y-axis gives the average daytime solar radiation. The categorization clearly distinguishes different ozone formation regimes. The highest ozone peaks occurred with high radiation and around 0.07 ppm. At low NOx, the values of ozone become larger due to the destruction of nitrogen dioxide by high solar radiation (Figures 2b and 2c).

Ozone formation is enhanced by high Concentrations of NOx, frequently combined with high radiation, where ozone construction due to the destruction of NO by solar radiation is the controlling procedure;

whereas formation of ozone is restricted by low solar radiation. Also, low Concentrations of NOx combined with high radiation indicates that NOx limited ozone formation regime. A general limitation for ozone peaks have to be estimated by considering the general situation of air masses and its change from season to another. Figure 3 a-c shows

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seasonal cycle for the same location for ozone, nitrogen dioxides and solar radiation respectively.

The seasonal ozone shows a unique pattern with a small increase values from winter to summer. Figure 3 shows seasonal mean values of daytime ozone concentration (10-18), solar radiation (10-18), and daytime nitrogen dioxides. The seasonal means of daily maximum 1-hr O3 concentrations exhibit less distinct seasonal variations, with the maxima in summer and autumn and a minimum in winter and spring.

The daytime solar radiation increases from spring to summer whereas nitrogen dioxides decrease during summer fall. (Chan el. al. 1997) analyzed Surface ozone (O3) and its precursors in rural and urban areas of Hong Kong through the seasonal, temporal, and spatial variation patterns. They found that the seasonal O3 shows a unique pattern with a major peak in autumn and a trough in summer.

(a) Ozone concentration

0 0.02 0.04 0.06 0.08 0.1

Jan Feb MarchApril May June July Aug Sep Oct Nov Dec Month

Ozone (ppm)

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(b) Global radiation (W/m²)

0 100 200 300 400 500 600 700 800

Jan Feb MarchApril May June July Aug Sep Oct Nov Dec month

solar radiation (w/m2)

(c) Temperature (^oC)

0 10 20 30 40 50

temperature (oc)

(d) Relative humidity (%),

0 10 20 30 40 50 60 70

relative humidity (%)

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(e) Wind speed (m/s)

0.00 0.25 0.50 0.75 1.00 1.25 1.50 1.75 2.00

wind speed (m/s)

(f) Nitrogen Dioxides (NOx)

0 0.01 0.02 0.03 0.04 0.05 0.06 0.07

Nitrogen Oxides (ppm)

Figure 1: Monthly mean values of daytime (10:00-18:00) (a) ozone concentration, (b) Global radiation (W/m²), (c) temperature (^oC), (d) relative humidity (%), (e) wind speed (m/s), and (f) Nitrogen Dioxides (NOx) at the station for January to December 1998

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Diurnal cycles of NOx and ozone

Diurnal ozone and NOx cycles were investigated for Makkah station (figure 4). The diurnal NOx values have maximum in the late morning.

The reason is most likely due to transport of emissions from land sources such as cars and other human activities. It is also influenced by a larger scale circulation system of winds from surrounding mountains.

Mean diurnal cycles of ozone concentration during the period show a strong increase from late morning to late afternoon. However, the mean diurnal cycles of ozone concentrations at different days show a clear maximum in mid-afternoon. The diurnal ozone cycles can be explained photo chemically by taking into account the large NOx concentrations, and high temperatures in Central Makkah. Photochemical processes are also indicated by diurnal cycles of NO2 and NO concentration. The ozone increase follows the NO_x increase with a few hours delay. Ozone may also be transported by the wind system. Since the diurnal cycles point to photochemical ozone formation, local or regional photochemical ozone formation rather than transport caused the ozone peaks.

Conclusions

A detailed analysis, which aimed to describe the ozone levels in terms of meteorological parameters and nitric dioxides, was carried out over monthly and seasonal time scales. The seasonal means ozone concentrations show less distinct seasonal variations, with the maxima in

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summer and autumn and a minimum in winter and spring. These increases in O3 are associated with the decline in ambient concentrations of nitrogen oxides. The seasonal mean of nitrogen oxides is in descending order follow the order of winter, spring, summer, and autumn. Meteorological parameters in autumn and winter indicate that the ground-level O3 tends to accumulate and trigger a high O3 episode on a warm day with sufficient sunlight and low wind in a high-pressure system, consistent with the low mixing heights in these two seasons.

The relationship between short-term concentrations variations of ozone and NOx was investigated for selected episodes. Elevated ozone concentrations most of the time and a maximum value fall are usually indicative of air masses enriched in precursors, which lead to the photochemical production of ozone. During the winter months, on the other hand, the ozone values tend to be minimum values due to minimum temperatures and minimum solar radiation.

High ozone values are common phenomenon in the area of the study because the location is exposure to different people activities such that emission of ozone precursors from motor vehicles and the complex topography within the area and movement of people around the Holly mosque. These factors have a local effect on the distribution of ozone and on the diurnal ozone pattern. The aged air masses associated with air pollutants emitted from the urban neighborhoods around the station, and under favorable meteorological conditions for photochemical ozone formation, the ozone levels reaches maximum in autumn. Different possible causes are discussed. Intrusions of stratospheric air and large-

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scale transport of ozone are probably of minor importance. Most of the peaks occurred during fair weather conditions and were probably due to photochemical production on regional scale. Therefore, meteorology and the climate system associated with tropical hot weather system are the governing factors for the temporal ozone pattern in Makkah. Moreover, the nitrogen dioxides concentrations played a dominant role in determining ozone levels.

(a) Ozone vs global radiation,

0 100 200 300 400 500 600 700 800 900

0 0.025 0.05 0.075 0.1 0.125 0.15 0.175 0.2 Ozone (ppm)

Solar radiation (w/m2)

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(b) Ozone vs daytime mean NOx

0.00 0.03 0.05 0.08 0.10 0.13 0.15 0.18 0.20

0 0.025 0.05 0.075 0.1 0.125 0.15 0.175 0.2 Ozone (ppm)

Nitrogen oxides (ppm)

(c) Global radiation, vs daytime mean NOx

0 100 200 300 400 500 600 700 800 900 1000

0 0.05 0.1 0.15 0.2

Nitrogen oxides (ppm) Solar radiation (w/m2)

Figure2. Daytime ozone peaks (mean highest values) from February to May 1998 as a function of the, (a) the global radiation, and (b) daytime mean NOx concentration at, and (c) daytime nitrogen oxides as a function of solar radiation at Makkah station.

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(a) solar radiation

0 100 200 300 400 500 600 700

w inter spring summer fall

season Solar radiation (Wm2)

(b) ozone concentration

0 0.01 0.02 0.03 0.04 0.05 0.06 0.07

season

Ozone concentration (ppm)

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(c) daytime nitrogen dioxides

0.000 0.005 0.010 0.015 0.020 0.025 0.030 0.035 0.040 0.045 0.050

season

nitrogen oxides (ppm)

Figure 3. Seasonal mean values of daytime (a) solar radiation (10- 18), (b) ozone concentration (10-18), and (c) daytime nitrogen dioxides

0.000 0.005 0.010 0.015 0.020 0.025 0.030 0.035 0.040

1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 17 18 19 20 21 22 23 24 Time (hour)

Concetrations (ppm)

O3 No

Figure 4. Diurnal cycles of ozone and nitrogen dioxides

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References

Beck, J.P., M. Krzyzanowski, B. Koffi. (1998). TroposphericOzone in EU - The consolidated report. EEA Topic report No 8/1998, European

Environment Agency, Copenhagen

Chan, L. Y., Chan, C. Y & Qin, Y. (1997) Surface Ozone Pattern in Hong Kong. Appl. Met. 37, 1153-1165

Chris J. W. & Yuan, H. (1994) Calculated Influence of Temperature- Related Factors on Ozone Formation Rates in the Lower Troposphere J.

Appl. Met. 34, 1056-1069

Comrie, A. C., & Yarnal, B. (1992) Relationships between synoptic-scale atmospheric circulation and ozone concentrations in metropolitan Pittsburgh, Pennsylvania. Atmos. Environ., 26B, 301-312

Eder, B. K., Davis, J. M. & Bloomfield, P. (1994) An automated

classification scheme desiged to better elucidate the dependence of ozone on meteorology. J. Appl. Met. 33, 1182-1199

Janach, W. E., (1989) Surface ozone: Trend details, seasonal variations, and interpretation, J. Geophys. Res. 94, 18289-18295.

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Mckendry, I. G. (1994) Synoptic circulation and summertime ground-level ozone concentrations at Vancouver, British Columbia. J. Appl. Met. 33, 627-641

Oke, T. R. (1987) Boundary layer climates, Second edition, Methuen, 435 pp

Penkett,S. A., and Brice, K. A., (1986) The spring maximum of photo- oxidants in the northern hemisphere, Nature 319, 655-657.

Roelofsm G. J. and Leliveld, J., (1997) Model study of the influence cross- tropopuase O3 transports on tropospheric O3 levels, Tellus 49B, 38-55.

Scheel, H.E. (1997) On the spatial distribution and seasonal variations of lower troposphere ozone over Europe, J. Atmos. Chem. 28, 11-28.

Wakamatsu, S., Uno, L., and Ohara, T., (1998) Springtime phototchemical air pollution in Osaka: Field observation. J. Appl. Met. 37, 1100-1106.

Yienger, J. J., Klonecki, A. A, Levy II, H., Moxim, W. J., & Carmichael, G. R. (1999) An evaluation of chemistry's role in the winter-spring ozone maximum found in the northern midlatitude free troposphere Journal of Geophysical Research, 104(D3), 3655-3667

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ﺮﺻﺎﻨﻋ ﺮﻴﺛﺄﺗ ﻟا

نوزوﻷا مﺎﻈﻧ ﻰﻠﻋ ﻪﻗﻼﻌﻟا تاذ ﻞﻣاﻮﻌﻟاو ﺲﻘﻄ

ضرﻷا ﺢﻄﺳ ﻰﻠﻋ ﻪﻣﺮﻜﻤﻟا ﺔﻜﻤﺑ ﻪﻌﻗاﻮﻟا ﻪﻄﺤﻤﻟا ﻦﻣ

ﻒﻠﺨﻟا ﻒﻠﺧ ﻦﻤﺣﺮﻟاﺪﺒﻋ

ﻪﻓﺎﺠﻟا ﻖﻃﺎﻨﻤﻟا ﺔﻋارزو ﻪﺌﻴﺒﻟاو دﺎﺻرﻷا ﺔﻴﻠآ –

ﺰﻳﺰﻌﻟاﺪﺒﻋ ﻚﻠﻤﻟا ﺔﻌﻣﺎﺟ

ص . ب . 80208 – ﻩﺪﺟ – 21413 – ﻪﻳدﻮﻌﺴﻟا ﻪﻴﺑﺮﻌﻟا ﻪﻜﻠﻤﻤﻟا

ﺺﻠﺨﺘﺴﻤﻟا

ارد ﻢﺗ ضرﻷا ﺢﻄﺳ ﻰﻠﻋ نوزوﻷا ﺰﻴآﺮﺗ ﺔﺳ ﻊﻣ

تاذ ﻪﻳﻮﺠﻟا ﻞﻣاﻮﻌﻟاو ﻦﻴﺟوﺮﺘﻨﻟا ﺪﻴﺳﺎآأ ﺔﻋﻮﻤﺠﻣ

ﻪﻗﻼﻌﻟا مﺎﻋ ﻲﻓ ﻒﻳﺮﺸﻟا ﻲﻜﻤﻟا مﺮﺤﻟا قﺮﺷ ﻪﻌﻗاﻮﻟا و ﻪﻣﺮﻜﻤﻟا ﺔﻜﻣ ﻲﻓ ﻪﻳﺰآﺮﻤﻟا ﻪﻘﻄﻨﻤﻟا ﻲﻓ 1998

ﻪﻴﻠﺼﻓو ﻪﻳﺮﻬﺷ ﻪﻴﻨﻣز ﻞﺳﻼﺳ لﻼﺧ ﻦﻣ تاﺮﻴﻐﺘﻟا ﺚﻴﺣ ﻦﻣ م .

أ ﻪﺳارﺪﻟا ﺖﺤﺿوأ ن

ﺰﻴآﺮﺗ

ﻪﻌﻔﺗﺮﻣ نوزوﻷا ﻲﻓ ﺎﻬﻤﻴﻗ ﻲﻧدأو ﻒﻳﺮﺨﻟا ﻞﺼﻓ ﻲﻓ ﺎﻬﻤﻴﻗ ﻰﻠﻋأ ﻰﻟإ ﻞﺼﺗ ﺚﻴﺣ ﻪﻨﺴﻟا مﺎﻳأ ﻢﻈﻌﻣ

ءﺎﺘﺸﻟا ﻞﺼﻓ .

نوزوﻷا ﻢﻴﻗ تزوﺎﺠﺗ 0.08

ﺮﻬﺷ لﻼﺧ ضرﻷا ﺢﻄﺳ ﻦﻣ بﺮﻘﻟﺎﺑ نﻮﻴﻠﻤﻟا ﻦﻣ ءﺰﺟ

مﺎﻌﻟا ﻦﻣ ﺮﺑﻮﺘآأ 1998

ﻪﺳارﺪﻟا ﻪﻴﻓ ﺖﻳﺮﺟأ يﺬﻟاو .

ءﺎﻨﺛأ ةدﺎﻋ ﺮهاﻮﻈﻟا ﻩﺬه ﻞﺜﻣ ثﺪﺤﺗ ﺔﻟﺎﺣ

ﻪﺒﺳﺎﻨﻤﻟا ءاﻮﺟﻷا رإ ﻊﻣ

ﺮﺒآا ﻰﻟإ ﻞﺼﺗ ﻢﻴﻘﻟ ءاﻮﻬﻟا ةراﺮﺣ ﺔﺟرد عﺎﻔﺗرإو ﻲﺴﻤﺸﻟا عﺎﻌﺷﻹا ﻢﻴﻗ عﺎﻔﺗ

ﻦﻣ 35 ﻪﻳﻮﺌﻣ ﻪﺟرد .

ﻲﻓ تاﺮﺘﻔﻟا ﻩﺬه ﻞﺜﻣ ﻲﻓ رﺎﻬﻨﻟا لﻼﺧ ﻦﻴﺟوﺮﺘﻨﻟا ﺪﻴﺳﺎآأ ﺔﻋﻮﻤﺠﻣ ﻢﻴﻗ ﺖﻠﺻو

ﻰﻟإ ﻊﻗﻮﻤﻟا ﺲﻔﻧ 0.060

نﻮﻴﻠﻤﻟا ﻦﻣ ءﺰﺟ .

ﺐﺒﺴﺑ ﻪﻌﻔﺗﺮﻤﻟا نوزوﻷا ﻢﻴﻗ ﻢﻈﻌﻣ نأ ضﺮﺘﻔﻤﻟا ﻦﻣ

ﻪﻴﺋﻮﻀﻟا ﻪﻴﺋﺎﻤﻴﻜﻟا تﻼﻋﺎﻔﺘﻟا ﺔﻴﻠﺤﻤﻟا

ﺚﻴﺣ تﺎﻧﺎﻴﺒﻟا ﺮﻴﺸﺗ ﻊﻗﻮﻤﻟا ﻦﻣ

نوزوﻷا ﻢﻴﻗ ﻲﻓ ﻩدﺎﻳﺰﻟا ﻮﺤﻧ

ﻪﻳﺮﻬﺸﻟا ﻰﻤﻈﻌﻟا ﻦﻣ

0.036 ﻰﻟإ 0.080 ﻂﻴﺴﺒﻟا ﺮﻴﻐﺘﻟا ﻰﻟإ تﺎﻧﺎﻴﺒﻟا ﺮﻴﺸﺗ ﺎﻤﻨﻴﺑ نﻮﻴﻠﻤﻟا ﻦﻣ ءﺰﺟ

ﻪﻨﺴﻟا رﻮﻬﺷ لﻼﺧ .

ﻋ ﻒﻴﻨﺼﺘﻟا ﺢﺿﻮﻳ ﺐﺒﺴﺑ ﺪﻳاﺰﺘﻳ نوزوﻷا نﻮﻜﺗ نﺈﺑ ﻩﺮﺛﺆﻤﻟا ﻞﻣاﻮﻌﻟا ﺐﺴﺣ ﻰﻠ

إ ﺎﻓﺎﻀﻣ ﻦﻴﺟوﺮﺘﻨﻟا ﺪﻴﺳﺎآأ ﺰﻴآﺮﺗ ﻲﻓ ﻩدﺎﻳﺰﻟا ﺰﻴآﺮﺘﻟا ﺎﻤﻨﻴﺑ ، ﻲﺴﻤﺸﻟا عﺎﻌﺷﻹا ﻦﻣ ﻪﻴﻟﺎﻋ ﺐﺴﻧ ﻪﻴﻟ

ﻞﻜﺸﺗ ﻢﻴﺠﺤﺗو ﺪﻳﺪﺤﺗ ﻰﻟإ يدﺆﺗ ﻪﻌﻔﺗﺮﻤﻟا عﺎﻌﺷﻹا ﺐﺴﻧ ﺮﻓﻮﺗ ﻊﻣ ﻦﻴﺟوﺮﺘﻨﻟا ﺪﻴﺳﺎآﻷ ﺾﻔﺨﻨﻤﻟا نوزوﻷا نﻮﻜﺗو .

ﻴﻟا ﺮﻴﻐﺘﻠﻟ ﺔﺒﺴﻨﻟﺎﺑ تﺎﻋﺎﺳ لﻼﺧ ﻪﺤﺿاو ﻪﻴﻣﻮﻳ ﻩرود ﻰﻟإ نوزوﻷا ﺮﻴﺸﻳ ، ﻲﻣﻮ

ﻰﻟإ ﻚﻟذ اﺮﻴﺸﻣ ﺮآﺎﺒﻟا حﺎﺒﺼﻟا ﻲﻓ وأ ﺲﻤﺸﻟا بوﺮﻏ ﺪﻌﺑ ءاﻮﺳ ﻪﻌﻔﺗﺮﻣ ﻢﻴﻗ ثوﺪﺣ نوﺪﺑ رﺎﻬﻨﻟا ﻪﻴﻠﺤﻤﻟا ﻪﻴﺋﻮﻀﻟا ﻪﻴﺋﺎﻤﻴﻜﻟا تﻼﻋﺎﻔﺘﻟا .

ﺔﻳاﺪﺑ ﻲﻓ ﻰﻤﻈﻌﻟا نوزوﻷا ﻢﻴﻗ نﻮﻜﺗ ﻲﻓ ﺐﺒﺴﻟا ﻊﺟﺮﻳ

ﻴﻜﻟا تﻼﻋﺎﻔﺘﻟا ﻰﻟإ ﻊﻴﺑﺮﻟا ﻲﻓ وأ ﻒﻳﺮﺨﻟا ﺐﺒﺴﺑ ﻚﻟذو نوزوﻷا لﺎﻘﺘﻧإ ﻦﻋ ﺎﺿﻮﻋ ﻪﻴﻠﺤﻤﻟا ﻪﻴﺋﺎﻤ

ىﺮﺧﻷا ﻪﻳﻮﺠﻟا ﻞﻣاﻮﻌﻟا ﻰﻟإ ﺔﻓﺎﺿإ ﻪﻳﺰآﺮﻤﻟا ﻪﻣﺮﻜﻤﻟا ﻪﻜﻣ ﺔﻘﻄﻨﻣ ﻰﻠﻋ ﺐﻟﺎﻐﻟا ﻊﻔﺗﺮﻤﻟا ﻂﻐﻀﻟا .