Numerical Simulation of Wind Distributions for Resource
Assessment in Southeastern Eritrea, East Africa
Bereket Lebassi
Department of Mechanical Engineering,
Santa Clara University,
500 El Camino Real, Santa Clara, CA 95053
andRobert Van Buskirk,
Environmental Energy Technologies Division
Lawrence Berkeley National Laboratory,
MS 90-4000, 1 Cyclotron Road, Berkeley, CA 94720

ABSTRACT
We present the results of a simulation study of the wind energy resources of Southeastern
Eritrea. In this study, we simulate the three dimensional wind fields during typical, steadyconditions of the Southern Red Sea southeast monsoon season. The simulations verify theexistence of a low level jet (LLJ) contained within the highly stratified marine layer over theSouthern Red Sea. The LLJ is cause by the channeling and acceleration of marine layer flow as
it passes throught the straight of Bab el Mandeb on its way from the Indian Ocean to the Eastern
Sahara. The LLJ extends from 12.5o N to 14.5o N latitude in the Southern Red Sea and has peakvelocities at 300 – 600 m elevation above the Red Sea. Sea-land breezes advect the high speed
flow of the LLJ onshore along a 200 km streatch of Southeastern Eritrean coastline, producing an
excellent wind energy resource that peaks daily at 3 PM. This resource is currently underdevelopment for both grid-connected and decentralized village wind energy applications.
Keywords: wind resource assessment, Africa wind resources, meteorological modeling
OUTLINE
1. Introduction
1.1 Previous Eritrean Wind Resources Studies
1.2 Simulation Case Selection and Synoptic Conditions
2. Mesoscale Simulation

2.1 Methodological Overview
2.2 Model Setup
2.3 Model Initialization and Input Data
3. Results
3.1 Model Validation
3.2 Wind Speed Maps
3.3 Lower Level Jet Vertical Structure
4. Conclusion

1. Introduction
Eritrea, an African country along the Red Sea coast, needs a rapidly growing supply of energy inorder to satisfy the increasing electricity demand of its people. In providing for the rapidly
expanding electricity needs of its population, Eritrea faces two major constraints: environmental
impacts, and cost. Wind energy holds the potential of providing a significant contribution to
Eritrea's electricity needs using a means that is both environmentally friendly and low cost
(Garbesi et al. 1996). Another major benefit of wind energy for Eritrea given the recent rise inoil prices is that it can help decrease the national reliance on the expensive, imported diesel fueland fuel oil that is currently used for electricity production.
An essential component of wind energy development is determining the geographic distributionof wind energy resources. This involves determining wind speeds to a high degree of accuracy.
The power density of the wind determines the amount of power that can be produced by a given
wind generator, and the power density is proportional the third power of the wind speed.
Therefore, a 10% increase in wind speed produces a 33% increase in wind power.

Figure 1: Map of the extreme southern Red Sea study area. Water is shown as blue or dark grey

while elevations are shown as shades of grey with darker colors corresponding to higher
elevations. The highest elevations are approximately 3000 m.
Eritrea is a country located in the eastern part of Africa, with one thousand kilometers ofcoastline along the southwestern shore of the Red Sea. Our research is focused on the southernpart of the Eritrean coast, which has been identified as the country’s best wind energy resource
region (EDOE report 2000). We show the southern extreme of the Red Sea in figure 1. At thesouthwestern boundary of the Red Sea is Southeastern Eritrea. Adjacent to the coast is a flatcoastal plain; while parallel to the coast and 5-50 km inland is a range of coastal hills that varyfrom 1000 to 2000 m in elevation. West of the meridian at 40 degrees east, we have the 2000
meter Eritrean highland plateau, which extends from the north to the south of the country. In thesoutheast, at the extreme southern end of the Red Sea lies the straight of Bab el Mandeb, which
is a constriction of about 35 km between Aden and Djibouti that connects the Red Sea and theIndian Ocean. The locations of the meteorological stations in the southern coast are also shownin figure 1 (Tio, Idi, Aseb, and Gahro).
The goal of this investigation is to increase knowledge of the distribution of wind energy
resources of Southeastern Eritrea through simulation of the the mesoscale meteorology of theregion. Some key questions regarding the Southeastern Eritrea wind energy resource include
following:•

Hills or Coastline: Are the wind resources better on the hills or in the sea?

•

Extent of Resources: How far along the coastline do excellent wind resources extend?

•

Vertical Wind Shear: How does wind power depend on altitude? And is it very
beneficial to have extremely tall wind turbines?

•

Best Wind Resources Location: Where are the highest performance wind energy
generation sites?

In the following sections, we review previous studies, describe the particular case that we
simulate, describe the simulation set-up and methodology, present simulation results, andconclude with implications for further wind energy resource studies.
1.1 Previous Eritrean Wind Resources Studies
Recent wind energy research and resource assessment activities in Eritrea are carried out by the
Energy Research and Training Center (ERTC) of the Minisitry of Energy and Mines in Eritrea
where both of the authors have previously worked and with which they actively collaborate. The
ERTC, is responsible for renewable energy technology in Eritrea and is active in studying
assessing and developing renewable energy resources in Eritrea while promoting the efficient useof all energy sources. Since the establishment of the ERTC in 1995, the activities have included
training, seminars, demonstration events , advisory and information services, and promoting thebenefits of renewable and sustainable energy technology.
The ERTC has a fairly comprehensive wind data collection system with 25 stations around thecountry and in particular in southern coastal area of Eritrea. A wind information system WIS
was developed and implemented at the ERTC. GIS and databases are also established in ERTC,

which enable the ERTC to quickly provide information on the wind resources at selected
locations. The result of the wind data analysis shows a high wind potential in and around Aseband in the regions to the south of Aseb, though average wind velocities appear to decrease, toward the north. Current wind energy assessments are being used for the identification andselection of suitable rural villages for wind stand alone and wind hybrid systems in the wind richpart of Eritrea. The data from ground-based monitoring is also used for the conceptual planningand economic assessment of a 750 kW wind park currently being implemented in Aseb.
In terms of methodology, revious research on wind energy resource assessment in Eritrea and thesurrounding area has relied primarily on collecting and analyzing ground station data on windspeeds, with some preliminary efforts at performing mesoscale simulations for the southeastern
coast. Some of the earliest studies (Mulugeta & Drake 1996) identified the Aseb area of Eritrea
as an area of high wind potential. Further general assessment studies (Van Buskirk et al. 1998,
Garbesi et al. 1996 and Rosen et al. 1999) provided more detail on the potential of thesoutheastern coast and central highland passes. In addition to meteorological data, these studies
examined ship-based meteorological measurements (Rosen 1998), and satellite scatterometry
data (Van Buskirk et al. 1999). More recent investigations (Habtetsion et al. 2002) haveanalyzed data from 25 recently installed meteorological stations. Consultant studies(Lehremeyer 2000) have performed simulations using the German mesoscale atmospheric model
KLIMM, KLIma Model Mainz (Climatic model Mainz) in an effort to extrapolate
meteorological station data to a wider geographic area. But these earlier simulations did not
capture well-known wind dynamics of the southern Red Sea area. Other consultant studies(Swedish Consulting (SWECO 2002) attempted to geographically extrapolate station data using
the Wind Atlas Analysis and Application Program (WAsP), but extrapolations based on landbased station data did not accurately forecast the wind speeds over the Red Sea that are indicatedby ship-based measurements.
The current investigation is needed because the studies that have been performed to date havenot provided consistent answers regarding the extent and features of the Southeastern Eritrea
wind energy resources that are important for an accurate and well-resolved resource assessment.
With respect to whether or not the best wind resources are in coastal waters or at the tops ofcoastal mountains, different studies and investigations have provides varying results.
Scatterometry and ship-based measurements (Van Buskirk et. al. 1999; Rosen 1998) indicate theexistence of a low level jet (LLJ) that appears to be centered in the middle of southern portion of
the Red Sea. Meanwhile WAsP calculations (SWECO 2002) indicate very high wind resourceson the tops of hills and mountains. Furthermore, unpublished investigations indicate that low
hills in the Aseb area can have wind speeds that are higher than the wind speeds in the nearby
coastal plains (Eritrean Department of Energy 1997)
With regards to the extent of the high resource areas, simulations, the examination of ship-based
meteorological measurements, station measurements and scateromettry data have provided
significantly different answers. The KLIMM mesoscale simulations forecast a very limited areaof high wind resources centered around Aseb Airport that did not extend far into the Red Sea
and, which covered an area of less than 50 km radius. The ship-based measurements werelargely limited to the main shipping lanes in the Red Sea and did not resolve the details of thewind speeds near the Eritrean coast. But these measurements did indicate 10 m annual averagewind speeds of up to 8 m s-1 extending from 12.7 to 14 degrees N latitude in the Red Sea (Rosen

1999). Scatterometry measurements appear to indicate 10 m annual average wind speeds ofslightly more than 6 m/s from about 13 to 14 degrees N latitude, but such measurements are
known to be inaccurate near coastlines. Meanwhile more recent meteorological ground station
measurements have indicated 10 m annual average wind speeds of approximately 7.1 m/s atalong the coast at Gahro (12.8 degrees N) and 6.7 m/s at Aseb Airport (13.06 degrees N), but anannual average wind speed of only 4.7 m/s at Idi (13.93 degrees N) and 4.5 m/s at Tio (14.68
degrees N). It is currently unknown how much variability there might be in the wind speeds
between the existing stations, or if there are some particular spots along the coast that have windspeeds higher than any of these stations.
And finally, because there is no vertical profile measurements of wind speeds in the high wind
portion of the Southern Red Sea, very little is known regarding the three dimensional structure of
the LLJ and its dynamics with local sea breezes and coastal topography.
In this study, we apply the Regional Atmospheric Modeling System (RAMS) in order to map
specific wind energy resources in Southeastern Eritrea during a typical 4-day period during thehigh wind season. We find that RAMS reproduces well-know distinct features of the Eritrean
wind meteorology much better than previous modeling efforts. We compare the results fromRAMS with available surface data on winds and wind climatology. Given a good match
between the model and available ground data, we use RAMS to produce wind speed maps for atypical high wind season day. Because annual wind power estimates are dominated by winds
during the high wind season and because the winds during this period follow a consistentmonsoonal pattern, we assume that the wind speed maps produced for a typical high wind period
will correlate with annual wind power resources for the area.
With respect to our four Southeastern Eritrea wind resource questions: (1) Are the windresources better on the hills or in the sea? (2) How far do excellent wind resources extend? (3)How does wind power depend on altitude? and (4) Where are the highest performance windenergy generation sites? We propose the following hypotheses: (1) Because the source of thehigh wind is a LLJ over the Red Sea, the highest wind locations will be coastal protrusions orhills that are closest to the center of the LLJ. (2) Approximately 200 kilometers of coastline fromthe Djibouti border north to Tio has very good wind resources except for bays and protectedareas. (3) Vertical wind shear will be strongest near the coastline whereas further inland there
will be a great variability of vertical wind shear due to topographic effects, and (4) the highest
performance wind energy generation sites will be coastal hills near Aseb Airport and Gahro
stations.
1.2 Simulation Case Selection and Synoptic Conditions
The winds along the Southeastern Eritrea coast are monsoonal in nature. From October to May,winds are largely from the southeast, while from June to September they are from the northwest.
Figure 2 shows a scatterplot of daily average wind power density vector for Aseb Airport. This
figure demonstrates that a large portion of the wind energy resource is provided under theconditions of the southeastern monsoon. Thus by characterizing the conditions of a typicalstrong southeastern monsoon we are likely to capture the meteorology that is most important forwind power production in this region.

2000

2

PV (watt/m )

1500

1000

500

0
-2000

-1500

-1000

-500

2

0

500

-500

PU (watt/m )Figure 2: Scatterplot of daily average wind power density vector for Aseb Airport, Eritrea. Windpower density vectors are calculated from hourly data at 10 m, assuming an air density of 1.2 kg
m-3
The simulation period selected for this study is February 8-12, 2002 where the dynamics of theregion is typically stable and consistent. The synoptic pattern changed very little, is characterized
by the south east monsoon at the surface and a stable high pressure system over the South Red
Sea at the 700 mb level (Flohn 1965). The stable, stationary high pressure produces a strongly
stratified marine layer over the Gulf of Aden and the Red Sea and a heat low over Western
Eritrea and Eastern Sudan. The strongly stratified, relatively cool marine layer provides a massof dense air that is channeled and constrained as it travels from the Gulf of Aden to the Red Sea,and ultimately into the heat low in Eastern Sudan.

We illustrate synoptic conditions infigures 3 and 4. The synoptic patternchanged very little over the Aseb bay
region during this simulation period.
The upper-level flow (700 mb) fields
were characterized by a steady, stablehigh pressure ridge which lingers overthe Red Sea, Eritrea, and the Gulf ofAden, and then drifts to the southeast
over Somalia and the Indian Ocean.
Westerly flow persists over thenorthern Red Sea and easterly flow isdominant over Ethiopia and Somalia.
Mid-latitude westerlies of 10-50 knots
extended from Sudan to Saudi Arabia
to the north, while from Ethiopia to
the Indian Ocean the equatorial
easterlies can be seen in the southernpart of the domain. The high pressure
ridge produces a very stable marine
layer and a heat low over Eastern
Eritrea and Sudan. These features
drive the planetary boundary layer
mesoscale flows that create theSouthern Red Sea LLJ.
At 0000 UTC 10 February 2002 (Fig.
3), 700 mb, the winds werecharacterized by an anticyclonic flow
centered at the southern Red Sea andcovering northwestern Sudan, thenorthern Red Sea and Yemen. Winds over the Southern Red Sea and Eritrean land-mass wereweak and variable since the area was under the influence of an anticyclonic circulation boundedby the mid-latitude westerlies to the north and the equatorial easterlies to the south. The peak of
the synoptic high pressure (5900 m) was located over the Yemeni plateau the Southern Red Sea
and Gulf of Aden.
Figure 3: Synoptic conditions over the study
area. A high pressure anti-cyclonic circulationis centered over Southeastern Eritrea at the
700 mb level.

The surface (1000 mb) synoptic map is shown in figure 4 for 0000 UTC 10 February
2002, a synoptic high pressure system of 1015 hPa developed over Saudi Arabia and the Indian
Ocean combined with a heat low of 1005 hPa west of the Ethiopian Plateau produces a generaleast to west surface level pressure gradient. This high pushes marine air through the strait of Bab
el Mandeb. Winds are generally flowing from the southwest all over the Red Sea speeds ranging
from 10 – 25 knots, the maximum being at Bab el Mandeb. Western Eritrea was characterizedby calm winds (2-5 knots). The anticyclonic circulation around the eastern Sahara high (to thewest of the illustrated domain) pushes northern Red Sea winds from the north and produces a
low level convergence along the northern Eritrean coast. From here, air is pulled inland througha break in the mountains at Port Sudan to Western Eritrea by the heat low in that region. Thiscreates a pattern that is characteristic of thewintertime steady monsoon circulation
pattern in the region (Flohn 1965).
2. Mesoscale Simulation
2.1 Methodological Overview
The Regional Atmospheric Modeling
System (RAMS) model (version 4.4) wasused to perform a simulation of the wind
patterns over the selected four-day period
in February 2002 for the Southeastern
Eritrean coast. As described above, thisperiod was chosen because February is
within the high wind season of theSouthern Red Sea region based on
observational studies. The particularperiod was selected because it showedsteady, consistent strong winds from thesoutheast that are typical for this period,and because steady conditions increase thepotential accuracy of the mesoscale
simulation. The simulated winds andtemperatures were validated by comparing
with the observations from ground-based
Figure 4: Synoptic conditions over the study
meteorological stations. The automaticarea. A general pressure gradient exists
stations at Aseb Airport and Gahro
between the Gulf of Aden and Western(Habtetsion et.al. 2002) were used for theEritrea due to a heat low over Easternmodel validation. Finally, the simulation
Sudan. Peak winds occur at Bab el Mandeb
results were analyzed to both characterize
where flows are channeled as they pass fromthe structure of the wind patterns and to
the Gulf of Aden to the Red Sea.
find the best sites for wind energy
production. Wind speed maps and verticle cross-sections of the Red Sea LLJ are produced forthis anlaysis.
2.2 Model Setup
Our RAMS simulations focused on an analysis of the coastal wind dynamics in order to locate
the best sites for wind power generation in Southeastern Eritrea. For this purpose, a nested-gridconfiguration of four grids was used in RAMS. The outer model domain was extended westward
to include Eritrea, parts of Sudan, and Ethiopia. Meanwhile, on the eastern side of the domain
the Red Sea, parts of Saudi Arabia and Yemen were included. Finer nested grids were usedapplied to the area of interest in order to obtain meteorological fields of high resolution (Fig. 5).
In order to select the most suitable nested grid configuration, several test simulations were
performed. The configuration that was finally been selected and applied for the selected periodsof simulation is the following:•

Grid 1: A coarse grid with a mesh of 50x60 points and 40 km horizontal grid increment.

•

Grid 2: A medium grid with a mesh 42x42 points and 10 km horizontal grid increment.

•

Grid 3: A small grid with a mesh 62x50 points and 2.5 km horizontal grid increment.

•

Grid 4: A fine grid with a mesh 42x42 points and 0.7 km horizontal grid increment

Figure 5: Boundaries of grids 2 – 4 used for the computational
domain of the numerical simulation.

Grids one, two and threewere centred at thedomain coordinate of
12.791o N and 43.071o E(Aseb city), while thecentre of grid four was
adjusted to slightly southof Aseb Airport toinclude the hills near
Aseb Airport.
Concerning the verticalstructure, the grids wereidentical. In detail, 50
vertical layers with afirst grid spacing of 40 m
and a grid stretch ratio of
1.12 have been used.
The vertical structure
was dense in the lower
levels, and became
increasingly coarse
toward the top of thedomain, which was at 30km.

2.3 Model Initialization and Input Data
The data available for validating and calibrating meteorological simulations in Eritrea consist of
ground station data, historical and current radiosonde data, satellite-based scatterometry data, andhistorical ship-based measurements in the Red Sea. Station data exists for 25 first and secondclass stations recently installed by the Eritrean Department of Energy (Habtetsion et al. 2002).
These stations measure temperature, wind, humidity, pressure, and solar radiation. Historical
radiosonde data measurements exist for Asmara, and for nearby stations at Addis Abeba, andKhamis Saudi Arabia. Recent radiosonde data exists for Abha and Jedda, Saudi Arabia(University of Wyoming web site). Historical ship-based measurements from the Red Sea are
available from the Comprehensive Oceanographic and Atmospheric Data Set (COADS). In
addition, satellite-based measurements of wind using radar scatterometry exist for the Red Sea
and Gulf of Aden areas.
At the large scale, the model simulation obtains boundary condition information and large scale

synoptic forcing information from data provided by the National Centers for Environmental
Predication (NCEP). The NCEP data is available at a frequency of once every six hours andincludes: temperature, pressure, wind speed, wind direction, and relative humidity data with aresolution of 2.5 x 2.5 degrees. The simulation model was initialized at 0000 UTC 08 February
2002 and was allowed to spin up for 12 hours.
3. Results
3.1 Model Validation
To have confidence in the model results, validation of model results against observations was
carried out. To gain insight into how well the model simulation depicted the thermal forcing of
the low-level flow, the model surface temperature and wind speed fields were compared tosurface observations. For the time period simulated, there are detailed meteorologicalmeasurements for only two stations located in the higher resolutions grids three and four: Aseband Gahro. Time series plots of surface temperature and wind speed for stations at Aseb Airportand Gahro were compared to model results and observations.
Differences between direct model output and observations can largely be explained by possible
errors in near-surface extrapolation of model parameters due to local, subgrid characteristics ofsurface roughness. In our comparisons, we compared the time series model results of the 10 m
wind speed at Aseb Airport and Gahro, and 2 m temperature at the Aseb Airport station.
When we compare model output with observations for the Aseb Airport station, there was aconsistent underestimate of the wind speed by the model output. Given the systematic
underestimation of wind speed, the surface roughness assumptions of the 10 m wind speed
estimate was reexamined. The model used a total roughness length of 0.05 m in the Aseb area,
which is a level desert. A review of typical roughness lengths for level desert indicated that aroughness parameter adjustment for the 10 m estimate was needed given the local roughness
characteristics of the meteorological station site. To make this adjustment, the log law (Jacobson
1999) was used and the roughness- length was set 0.0003 m (Jacobson 1999) for level desert.
The adjusted estimate of the 10 m wind speed vs. time was recalculated for Aseb Airport fromthe surface grid cell average wind speed and plotted in figure 6. The roughness-adjusted
estimate of 10m wind speed now shows a very good match with the observational data (Fig. 6).
For the Gahro station, similar discrepancies were observed between model results and theobservations, but the adjustment in the 10 m wind speed estimate was made in a slightly different
manner. The meteorological station at Gahro is located less than 10m from the water’s edge at alocation where the winds are onshore during the entire simulation period. The model grid did
not resolve these subgrid characteristics of the meteorological station site well. Thus theappropriate surface for the Gahro station is water, but at the model resolutions, RAMS shows
Gahro to be on land. Thus, the model wind speeds used to compare with observations are thoseat the next grid cell east of Gahro, which has water surface characteristics in the model. These
recalculated comparisons show approximately the same level agreement as seen for the Aseb
Airport comparison.

Figure 6: Wind speed comparison of adjusted model output and wind speed observations. Model
output is adjusted to compensate for local roughness characteristics of meteorological station.

Figure 7: Temperature comparison of adjusted model output and wind speed observations.
Model output is adjusted for local roughness characteristics of meteorological station.
Surface temperature comparisons of model and observation at Aseb Airport station were also
carried out. The model calculates the grid cell average temperature of the surface grid cell anduses a surface boundary layer equation to calculate the estimate of the 2 m temperature. Before
any roughness adjustment was done to the equation that estimates 2 m temperatures from thegrid cell average temperature, the model under-estimated the surface temperature by an averageof 2.5oC. After a roughness an adjustment was made to the equation for estimating 2 mtemperatures using the value of 0.0003 m appropriate for the level desert at Aseb Airport, thesurface temperature matched very well with the observations at the Aseb Airport station (Fig. 7).
3.2 Wind Speed Maps
Given that the model reliably reproduces daily wind patterns and temperatures with appropriate
roughness adjustments, and that RAMS is a well-test mesoscale simulation model, it is likely thatthe model may also reproduce many of the key physical and geographic features of the winds inthe area. In this section we illustrate the larger geographic features of the simulated wind fields
as a candidate forecast of the wind speed patterns that are likely to be found in the Southern Red
Sea during the southeastern monsoon season.
Figure 8 shows a 10 m average wind speed map for the south coast of Eritrea for the simulation
period generated from the RAMS model results. This map shows a zone of average wind speedsof 9 - 11 m s-1 at 10 m and 13 – 15 ms-1 at 60 m stretching from approximately 12.8 to 14.6
degrees north latitude over the Red Sea. Coastal wind speeds reached 7-10 m s-1 at 10 m and 10– 14 m s-1 at 60 m, while inland wind speeds were 4-7 m s-1 at 10 m and 5 – 13 m s-1 at 60 m .
Higher resolution maps of the average wind speed distribution of the area (grid 3), were also
analyzed to show more detailed wind speed structure of the region. Figures 9 shows the higher
resolution the wind speed distribution around Aseb and Gahro.

Figure 8: Average 10 m (above) and 60 m (below) wind speed for the simulation period for grid
2. Results how a strong LLJ of 9 – 11 ms-1 over the Southern Red Sea for 10 m, and an LLJ windspeed of 13 – 15 ms-1 at 60 m height.

Figure 9: Average 10 m (above) and 60 m (below) wind speed for the simulation period forgrid 3. Results how a strong LLJ of 9 – 11 ms-1 over the Southern Red Sea for 10 m, and an LLJ
wind speed of 12 – 14 ms-1 at 60 m height. Both images show peak wind speeds n the Bay of
Beylul and on the top of the 900 m hills west of Aseb

3.3 Lower Level Jet Vertical Structure
The "Eritrean Low Level Jet" is a relatively narrow wind stream along the East African Red Sea
Coast and is part of the larger South West Monsoon circulation pattern. A conceptual model ofthe LLJ that shows a horizontal slice across southern Red Sea is shown on figure 10. The LLJ isa strong, sustained low-level wind systems produced by the channeling of strongly stratified
marine air through the straight of Bab el Mandeb. This marine air is driven by a persistent east
to west surface synoptic pressure gradient produced by a heat low on the western side of theEthiopian Highlands in Eastern Sudan during the southeast Southern Red Sea monsoon.

Figure 10: Conceptual model for Southern Red Sea Low Level Jet (SRS LLJ). Daily solar
heating produces sea-land and upslope flow that draws the jet that is funnelled through Bab el
Mandeb down to lower altitudes and advects high speed Red Sea winds onshore.
To examine the structure of this LLJ over the Southern Red Sea, we examine wind speed crosssections at Aseb Airport from the simulation. In figure 11 we show XZ cross sections of the LLJ
at the latitude of Aseb Airport for midnight and noon UTC (3 AM and 3 PM local time
respectively) on the third day of the simulation, February 11, 2002. The jet is centered at about
600 m with a core speed of 25 m s-1 at 0000 UTC and there is a layer of relatively low winds atthe surface below the jet, especially over land. Downslope winds from the Yemeni side of the
Red Sea are flowing towards the jet which is proximate to the Eritrean coast. During 1200 UTC
11 February 2002, the sea breeze has fully developed on both sides of the coast resulting in
subsidence of the marine layer air mass in the middle of the Red Sea. As a result, the jet has
lowered to about 400 m strengthening the Eritrean coastal wind speeds and surface winds as thesea breeze and upslope winds mix the momentum contained in the core of LLJ throughout thebasin contained between the Eritrean coastal hills and Yemeni highlands . The wind speeds
ranged from 10-16 m s-1 at the Eritrean side of the coast and are more than 20 m s-1 at the coreof the LLJ.

Figure 11: X-Z cross section of wind speeds in the Southern Red Sea for 0000 UTC (above) and1200 UTC (below) February 11, 2002.

If we take our simulation results as indicative of mesoscale flows during the southeast monsoon
in the Southern Red Sea, then we find that there is a persistent, 200 – 300 kilometer long LLJ in
this region. The LLJ extends from Bab el Mandeb at 12.5 deg N to approximately 14.5 deg. N in
the Southern Red Sea and is normally strongest in the period between November to March whencore maximum speeds may reach up to 20-30 m s-1. The LLJ is modified by the diurnal sea/landbreeze dynamics of the region. The core is usually centered at an elevation of about 300-600 m,
where it occupies the higher end of the elevation during nighttime hours and the lower range ofthe elevation during mid-afternoon. This semi-permanent low-level wind, which is particularly
strong during the southeastern Southern Red Sea monsoon, is the key to the high wind speeds
and excellent wind energy resources of observed in Southeastern Eritrea.
4. Conclusion
In this study, we posed four questions regarding the wind energy resources of Southeastern
Eritrea that we attempted to answer through the simulation of a typical high wind period during
the Southern Red Sea southeastern monsoon season:(1) Are the wind resources better on the hills or in the sea?
(2) How far do excellent wind resources extend?
(3) How does wind power depend on altitude? and(4) Where are the highest performance wind energy generation sites?
Since our simulation was conducted over a relative short time span, it cannot provide a definitive
answer to these questions. But the simulation has revealed the three dimensional structure of theSouthern Red Sea southeast monsoon low level jet. These results imply a set of provisional
answers to our four wind resource questions:•Hills or Coastline: The best wind resources are in the center of the Southern Red Sea
LLJ at an elevation of 300 to 600 m above the eastern side of the Southern Red Sea along
the Eritrean coastline. Those topographic features that can potrude closest to the centerof this LLJ will be the locations with the best wind energy resources•

Extent of Resources: The SRS LLJ extends from Bab el Mandeb (at 12.5 deg N) to 14.5
deg N in the Southern Red Sea.

•

Vertical Wind Shear: Vertical wind shear is strongest near the coast in the afternoon, orover coastal hills and mountains when the core of the SRS LLJ is closest to the land or
sea surface.

•

Best Wind Resources Location: There appears to be two maxima in the wind speeds in
the SRS LLJ during the southeastern monsoon. One peak is near the Bay of Beylul andextends southwest toward a group of hills west of Aseb that rise to 900 m in elevation.
The second peak in coastal wind speeds appears to be an area of coastline approximately
30-50 km ESE of the Eritrean town of Idi. Both of these locations have not yet had theirwind speeds measured with a meteorological station.

RAMS appears to have successfully simulated the main characteristics of the distribution ofwind energy resources for Southeastern Eritrea. Further research shall test these simulation
results agains new meteorological measurements to determine if the characteristics anddistribution of wind speeds and wind energy resources have been accurately forecast by thisstudy.

Disclaimer
This document was prepared as an account of work sponsored by the United States Governmentand Distributed Generation Systems Inc (DISGEN). While this document is believed to containcorrect information, neither the United States Government nor any agency thereof, nor DISGEN,
nor The Regents of the University of California, nor any of their employees, makes any
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views and opinions of authors expressed herein do not necessarily state or reflect those of theUnited States Government or any agency thereof, or The Regents of the University of California.
Ernest Orlando Lawrence Berkeley National Laboratory is an equal opportunity employer.

REFERENCES
EDOE, 2000: Eritrean Department of Energy 2000 Report.
EDOE, 1997: Eritrean Department of Energy 1997 Report.
Flohn, H., 1965: Studies on the Meteorology of the tropical Africa. Bonner meteorol.
Abhandlugen., 5, 2-35.
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