Category Archives: EuroSun2008-13

SOLIS Clear Sky Model

The SOLIS clear sky model [3] uses the radiative transfer model libRadtran [4] to calculate input parameters for a fitting function called the modified Lambert-Beer (MLB) relation. For this, only two radiative transfer calculations are needed for a given atmospheric state to get the irradiance for a full day. Since SOLIS can provide spectrally resolved irradiance data, it can be used for different applications. Beside improved information for the planning of solar energy systems, the calculation of photosynthetic active radiation, UV index, and illuminance is possible.

We use climatologies with monthly averages of AOD [5] and water vapour content [6] as input parameters for SOLIS and get the direct and global irradiance as output.

1.2. Direct model

We propose a new model [7] to calculate direct irradiance as a function of the clear sky index k* and the direct irradiance at clear sky conditions bciear. An appropriate clear sky model is the basis for this approach, see sec. 2.2.

For cloud events, described by k* < (1 — c(6)) (whith с(в) is a fit function), an exponentially rising parametrisation b(k*) for the direct irradiance was found empirically. It is given by

Подпись: (5)Подпись: (6)b(k*) = bdear k*P

with P as a fit parameter.

Situations where k* — 1 becomes smaller than c(6), are defined as clear sky situations and the parametrisation results in

b(k*) = bciear + (k*-1) a where a is a fit parameter.

If the clear sky index becomes greater than (1 + c(6)) we assume a special cloudy situation. In this case the global irradiance becomes more than Iciear in consequence of an increasing diffuse irradiance by reflection on clouds. The direct irradiance is then parameterised by

b(k*) = bdear / k*. (7)

Подпись: Fig. 3: Distribution of direct irradiance fraction once determined from satellite data and once evaluated from ground data versus the clearsky index.

In Fig. 3 the beam fraction as a function of clearsky index is given for satellite and ground derived values.

2. Analysis and results

Bidirectional reflectance and shadow into a pixel

The soil bidirectional reflectance can be expressed as (Rahman et al., 1993):

rs = r0 M Fhg H (3)

where r0 is an arbitrary parameter characterizing the intensity of the surface cover. The function H is characterised by a large reflection in the illuminating direction. M and FHG are the symmetric and asymmetric angular functions. The variation of this reflectance around the albedo can be greater than 0.1. In the specific case of oceans, the reflectance varies from zero to values greater than cloud reflectance, it also depends on wind speed (Lefevre et al. 2007). Thus, by considering the albedo instead of the bidirectional reflectance, one commits a significant error on irradiance reflected by the ground then backscattered by the atmosphere, thus contributing to the diffuse fraction of the SSI. This omission is very often made for operational reasons because of the lack of data describing the ground.

Very often, for operational reasons, the irradiance calculations are done under the assumption of a flat terrain inside the pixel. However, the cosine of the local incident angle 9 is:

cos9(P, a) = (cosracosScos^i + sinSsin^^cosP

+ cosracosSsin^icosasinP + sinracosSsinasinP — sinScos^icosasinP (4)

where a is the hour angle, S is the solar declination, ф is the latitude of the site, a and /3 correspond to the direction of the local slope, respectively in azimuth and tilt. Thus, the SSI of the pixel should be modified by the ratio:

R = Hpixelcos9(a(p),P(p))dp / cos9(0,0) (5)

2. Conclusion

We have quantified the influence of the different atmospheric properties on the SSI. Clouds (cloud optical thickness and type) are the most important variable for the SSI. They also exhibit high temporal (~ 30 m) and spatial (~ 10 min) variation (Rossow and Schiffer 1999). Aerosol loading and type, water vapour amount and atmospheric profile have a great influence on SSI, particularly in clear skies. Wald and Baleynaud (1999) demonstrate noticeable variation in atmospheric transmittance due to local pollution in cities at scale of 100 m. Ground albedo and its spectral variation have an important influence on diffuse part and spectral distribution of SSI. They exhibit very high spatial variation on a pixel basis and seasonal temporal variations. The influence of ozone amount is large in the ultraviolet range, but remains low on the integrated wavelength SSI.

Data availability of water vapour and aerosol loading is fairly low. We are expecting one value per day for a 50 km pixel. The error induced on the SSI depends on the variation of these parameters within the pixel. The clearer the sky, the greater the error. Comparisons of ground measurements of hourly means of SSI made at sites in Europe less than 50 km apart for clear skies show that the spatial variation in SSI, expressed as the relative root mean square difference, can be greater than 10 %.This result is in agreement with Perez et al. (1997) who stressed the large spatial variability of the SSI.

The influences of vertical position and geometrical thickness of clouds in the atmosphere are negligible. Thus, the solution of the RTM for a cloudy atmosphere is equivalent to the product of the irradiance obtained under a clear sky and the extinction coefficient due to the cloud. In particular, it means that the method Heliosat-4 may be composed of two distinct parts: the clear-sky part and the cloudy-sky part. In addition, given the fact that the cloud parameters may be known every % h and 3 km and the clear-sky parameters every day and 50 km, the adoption of the concept of "a model for the clear sky, another for other types of skies" saves time: the first model, which takes into account all other atmospheric parameters, focuses the bulk of computation resources.

The results of this work form the basis for the establishment of the method, called Heliosat-4, based on the exploitation of a RTM for the operational processing of satellite data to produce assessments of solar surface irradiance every 3 km and % h on Europe and Africa. The necessary inputs to Heliosat-4 have been identified; a gross assessment of the relative importance of their uncertainties on the final assessment has been obtained.

References

[1] Bernhard, G., Booth, C. R., Ehramjian, J. C., 2002. Comparison of measured and modeled spectral ultraviolet irradiance at Antarctic stations used to determine biases in total ozone data from various sources. In Ultraviolet Ground-and Space-based Measurements, Models, and Effects, edited by J. R. Slusser, J. R. Herman, and W. Gao, Proceedings of SPIE, Vol. 4482, 115-126.

[2] Cano D., Monget J. M., Albuisson M., Guillard H., Regas N., and Wald L., 1986, A method for the determination of the global solar radiation from meteorological satellite data. Solar Energy, 37, 31-39.

[3] Hammer, A., 2000. Anwendunsgspezifische Solarstrahlungsinformationen aus Meteosat-Daten. Dissertation, Carl von Ossietzky Universitat Oldenburg, Fachbereich Physik, Oldenburg, Germany.

[4] Ineichen, P., 2006. Comparison of eight clear sky broadband models against 16 independent data banks. Solar Energy, 80 (4), 468-478.

[5] Kato S., Ackerman T. P., Mather J. H., Clothiaux E. E., 1999. The k-distribution method and correlated-k approximation for shortwave radiative transfer model. Journal of Quantitative Spectroscopy & Radiative Transfer 62 (1999) 109-121.

[6] Kuhleman, R., Betcke, J., 1995. CloudS: A new parameterization of radiative transfer through clouds (summary of development and first validations). Heliosat-3 Reports, 21 p., http://www. heliosat3.de/documents/.

[7] Liou K. N., 1976. On the absorption, reflection and transmission of solar radiation in cloudy atmospheres. Journal of the Atmospheric Sciences vol.33 798-805.

[8] Liou K. N., 1980. An Introduction to Atmospheric Radiation. International Geophysics Series, volume 26, Academic Press, 392 p.

[9] Mayer B., Kylling A., 2005. Technical note: The libRadtran software package for radiative transfer calculations — description and examples of use. Atmospheric Chemistry and Physics, 5, 1855-1877.

[10] Mueller, R., Dagestad, K. F., Ineichen, P., Schroedter, M., Cros, S., Dumortier, D., Kuhlemann, R., Olseth, J. A., Piernavieja, G., Reise, C., Wald, L., Heinnemann, D., 2004. Rethinking satellite based solar irradiance modelling — The SOLIS clear sky module. Remote Sensing of Environment, 91 (2), 160-174.

[11] Perez R., Seals R., Zelenka A., 1997. Comparing satellite remote sensing and ground network measurements for the production of site/time specific irradiance data, Solar Energy, 60, 89-96.

[12] Perrin de Brichambaut C. et Vauge C., 1982. Le Gisement Solaire : Evaluation de la Ressource Energetique. Technique et Documentation, Librairie Lavoisier, Paris, France, 222 pages.

[13] Pinker R. T., Frouin R., Z. Li, 1995. A review of satellite methods to derive surface shortwave irradiance. Remote Sensing of Environment, 51 (1), 108-124.

[14] Rigollier, C., Lefevre, M., Wald, L., 2004. The method Heliosat-2 for deriving shortwave solar radiation from satellite images. Solar Energy, 77 (2), 159-169.

[15] Rossow W. B., Schiffer R. A., 1999. Advances in understanding clouds from ISCCP, B. Bulletin of the American Meteorological Society, 80, 2261-2287.

[16] Shettle E. P., 1989. Models of aerosols, clouds and precipitation for atmospheric propagation studies. In AGARD Conference Proceedings No. 454, Atmospheric propagation in the UV, visible, IR and mm-region and related system aspects.

[17] Stamnes, K., S.-C. Tsay, W. Wiscombe and K. Jayaweera, 1988. Numerically stable algorithm for discrete — ordinate-method radiative transfer in multiple scattering and emitting layered media. Applied Optics, 27,

2502.

[18] Vermote, E., Tanre, D., Deuze, J. L., Herman, M., Morcrette, J. J., 1997. Second simulation of the satellite signal in the solar spectrum (6S), 6S: An overview. IEEE Transactions on Geoscience and Remote Sensing, 35, 675-686.

[19] Wald L., Baleynaud J.-M., 1999. Observing air quality over the city of Nantes by means of Landsat thermal infrared data. International. Journal of Remote Sensing, 20, 5, 947-959.

Data transformation

In this study the generation of the variable which is going to be used to forecast future values of half daily solar global radiation is done taking into account gaussian and stationary properties needed in the time series to be used by predictive methods. This approach is based on “lost solar component” (Fig.

1.) defined previously.

Lost component time series presents higher variation in central months of the year due to higher solar radiation levels and bigger influence of cloudiness reflection and absorption on solar irradiance.

Elimination of the trend component is done differencing between successive time steps of lost component time series.

Подпись:W/m2 half day

image033

In the other side, synoptic predictions of future states of sky conditions by statistical post-processing models presents less uncertainty than direct output of global solar irradiance in numerical weather prediction models. The classification of sky conditions is done by national weather services in six levels Fig. 2. As sky condition variable wasn’t available directly from AEMet it has been simulated dividing measured solar radiation in six levels. Future variation of sky conditions is combined with the difference of lost component time series as input to predictive methods. Besides, pure statistical models have the advantage of limiting the upper error of prediction and improving predictions errors of persistence by making relations of patterns of past observations and future values. In the next sections, results of using and not using sky condition as input to neural network is shown.

Numerical weather prediction models

The NWP models are able to provide the solution for seven atmospheric parameters, by solving the momentum, mass and energy conservation equations related to the motion of air and water vapor in the atmosphere. These models are also able to estimate the cloud cover, and incoming solar radiation [11]. By the model GFS (Global Forecasting System) [12], numerical modeling are performed in a (0.5 x 0.5)° earth surface grid with sampling interval of 3h. In order to improve the performance of local forecasts, the data of the global model are assimilated by regional NWP models. By using the hydrostatic model ETA with grid resolution of (0.4 x 0.4)°, Guarnieri [13] obtained a RMSE of 43.9 % and 43.6 % for the daily total of incoming solar radiation, for two different sites in Brazil.

MM5 Setup

The spatial configuration of the MM5 used in this work consisted in five nested domains and twenty four unevenly spaced sigma levels. The domains has an horizontal resolution of 71, 27,9, 3 and 1 km, respectively. The results of the last domain, of 1km resolution, were finally evaluated. Two-ways nesting was used to feed the information between domains. Atmospheric initial and boundary conditions were extracted from the analysis produce by the NCEP. The physical parameterizations used in the simulation were: the GRELL scheme for the cumulus parameterization, the MRF for the planetary boundary layer, the MIXED PASHED for the explicit moisture, the FIVE-LAYER SOIL for the soil model and the RRTM for the radiation scheme. This configuration is maintained for all the integrations. Finally, a 24 hours spin-up period was used in each 72-hours integration.

The simulations were carried out for a set of days selected along the year 2005. Particularly, four sets (one for each season of the year) of three consecutive days with clear-sky conditions were selected, one for each season of the year. As highlighted earlier, the aim of this work is to evaluate the ability of the MM5 to estimate the solar radiation in a complex topography area. To this end, two simulations were carried out for each season of the year. In one of the simulations (called hereinafter T, Topography), the solar radiation were computed using the MM5 subroutines OROSHAW and LEVSLP. These subroutines allows taking into account the effect of the slope, angle and shadow cast caused by the topography on the solar radiation estimates at the earth surface. In the second simulation, these subroutines were not used and, therefore, the MM5 solar radiation estimates do not account for these topographic effects. We will call these simulations as Not Topography (NT).

The MM5 estimates were evaluated in terms of the Mean Error (ME) and the Root-Mean-Square Error (RMSE). The ME quantified the overall bias and detected if the model is producing overestimation or underestimation, while the RMSE accounts for the spread of the error distribution. Al error estimates are computed using hourly values along the whole simulated period.

3. Results and conclusions

Table 2 to 5 shows the evaluation results for, respectively, winter, spring, summer and autumn,. The results are just presented for three representative stations: stations 4, 5 and 11. These stations have a important slope and represent different aspects (stations 4 aspect east, stations 5 aspect west and station 11 aspect south) (Table 1). Evaluation results present the comparison of the MM5 estimates using (T) and not using (NT) the topographic parameterization against the measured horizontal solar radiation (H). For instance, the NT-H notation in Tables 2 to 5 stands for the evaluation of the MM5 estimates not using topographic parameterization against the global horizontal radiation measured values.

Overall, the MM5 shows considerable skills in estimating the solar radiation under clear-sky conditions along the whole year, even for this complex topography area under study. Particularly, the lowest RMSEs are found in summer (~20%) and the highest during winter (more than 30%). Additionally, from the analysis of the ME values, it could be concluded the existence of a general tendency to overestimation in winter, spring and summer and to underestimation in autumn.

Regarding the topographic parameterization, tables 2 to 5 shows and overall improvement in the estimates, although this improvement strongly depends on the season of the year and the topographic characteristics of the location under study. Regarding the season of the year and as can be expected, the most important improvement takes place in winter (Table 2). The relatively low sun elevation angles during this seasons makes the topographic influence on the solar radiation measured ant the surface more important. The use of the topographic parameterization improves the MM5 estimates, in terms of RMSE, ranging from 10% of improvement in station 11 to less than 5% in the stations 4 and 5. This difference can be explained by the fact of that the station 11 has south aspect, while the station 4 has a west aspect and station 5 an east aspect. Therefore the station 11 receives more radiation than the other two and the potential improvement is higher. For the rest of the seasons, the improvement in the estimates provides by the MM5 topographic parameterization are lower than for the winter. Particularly, in spring and autumn, Tables 3 and 5, the improvement in the estimates in terms of the RMSE ranges from 1% to 7%. Particularly, the most important improvement (7%) is found during autumn and for station 5. Similar results are found in terms of the ME. During summer (Table 4), and as can be expected, the improvements in the estimates provide by the topographic parameterization are modest. The only important improvement (4% in terms of RMSE) is found for station 5.

image010

RMSE (Wm-2) (%) ME (Wm-2) (%)

Station

NT

T

NT

T

4

120.1

(23.4)

113.7

(22.1)

-61.1 (-11.9)

-68.0

(-13.2)

5

125.5

(22.4)

102.1

(19)

-30.7

(-5.8)

-44.8

(-8.4)

11

92.3

(17.5)

90.8

(17.3)

-60.8

(-11.6)

-63.6

(-12.1)

Table 4. As in Table 2 but for summer.

 

RMSE (Wm-2) (%) ME (Wm-2) (%)

Station

NT

T

NT

T

4

117.8

(279)

100.8

(23.7)

25.0

(5.8)

27.0

(6.2)

5

150.8

(37.6)

122.7

(30.6)

CO CO

1.8

(0.4)

11

92.7

(21.2)

82.8

(18.9)

-29.6

(-6.8)

25.8

(5.9)

Table 5. As in Table 2 but for autumn.

 

REFERENCES

[1] G. A. Grell, J. Dudhia and D. R: Stauffer, (1994). A description of the fifth-generation Penn State/NCAR Mesoscale Model (MM5). Tech. Rep. NCAR/TN-398+STR, National Center for Atmospheric Research.

Analysis of the incoming solar radiation and other significant. parameters to estimate the solar resource at eight sites in Galicia (NW Spain)

Alberto Pettazzi, Jose Antonio Souto Gonzalez*

Department of Chemical Engineering, University of Santiago de Compostela, Lope Gomez de Marzoa St.,

Campus Sur. 15782 Santiago de Compostela, Spain
Corresponding author, ia. souto@,usc. es

Abstract

The evaluation of the solar resource in a region needs the characterization of different meteorological parameters. In this work, an analysis of global irradiation, clearness index and sunshine hours has been carried out in Galicia (NW Spain). Mean values of irradiation are compared with those derived from satellite images. The analysis is completed with the evaluation of other related parameters: precipitations, temperature and relative humidity. A complete characterization of the solar resource has been achieved in eight areas of Galicia. Results show high variability in the solar irradiation values, describing a more complex pattern than that derived from satellite observations. Evidences of the presence of local atmospheric phenomena, that overlap the diurnal evolution of solar radiation, drive to the conclusion that the distribution of the solar resource in this region cannot be explained without the consideration of climatologic and topographical features.

Keywords: solar resource, ground-satellite comparison

1. Introduction

The development of technologies for renewable energies is a priority target in the policy from different fields. Between the renewable energies, solar thermal and solar photovoltaic energies have a great potential in Spain and in Galicia too [1]. In Spain, the only official reference of the solar radiation climatology is the Atlas of Solar Radiation [2] that collects monthly means of sunshine hours and global irradiation between 1951 and 1983. Unfortunately, the low resolution of its results and their oldness may not represent a valid reference for estimating the solar resource in the present. Other works [3] applies satellite images to obtain solar maps for Spain, but they lack of homogeneous validation with ground measurements.

In Galicia, only an attempt was done, by Vazquez et al. [4]. Using the method Heliosat-2 [5], they collected in an atlas the results of monthly means of solar radiation from observations by satellite Meteosat-6. Nevertheless, the analysis covered a short period of time and the results obtained were only compared with the measurements proceeding from one station. Finally, no information about other relevant parameters was provided.

This work is focused on the evaluation of the solar resource in Galicia from the ground. Over a 5- years period, the surface meteorological parameters that affect the performance of thermal and photovoltaic systems are analysed, keeping in mind the peculiarities of the Galician region. To accomplish this task, global irradiation, sunshine hours and clearness index have been evaluated at

eight locations, using daily measurements. Mean values of global irradiation proceeding from the stations have been compared with those derived from satellite observations. The evaluation is completed with the analysis of the time series of complementary parameters, such as precipitation, temperature and relative humidity, in order to obtain the most complete information about solar resource at these locations.

. Locally linear prediction

The easiest nonlinear method of local prediction was developed by Lorenz [4] and called method of analogies. Let be xt a point within the d-dimensional phase space, the predicted value a time T later, xt+T, will belong to some kind of interpolation between known points xt1+T, …, xtr+T, where x;7, …, xtr are the nearest r points to xt. Farmer and Sidorowich [12] propose an enhanced method by making a least-squared fit of a local linear map of xt into xt+T. Doing T = 1, we can obtain the predicted value as x’t+1 = atxt + bt by minimising:

W = SI lx+i- atxt — bt |2 (1)

XtGNi

in regard to at and bt. Nt is the s-neighborhood of xt.

Подпись: E2 Подпись: < E2 > Подпись: <[xt - xt]2 > <[xt -< xt >]2 > Подпись: (2)

Casdagli [10] suggests to use these models as a test for nonlinearity prediction, obtaining the average forecast error given by:

where <•> is the arithmetic average. If E = 0 then the prediction is perfect, and if E = 1, the prediction is no better than a constant predictor in the time series average. If E is calculated for different s-values, occurring the optimum for large neighbourhood sizes, this will indicate that the data are better described by a linear stochastic process in this embedding space. On the other hand, an optimum at rather small sizes will point out the existence of a nonlinear equation of motion.

The average forecast error of local linear models is plotted as a function of the neighbourhood size s in Fig. 5. Note the high value of E and how the minimum value of E occurs at higher neighborhood sizes. This result is associated with stochastic processes.

image126

Fig. 5. Average forecast error of the local linear modelas a function of the neighborhood size fot the

differenced time series.

Solar Climate of Azores:. results of monitoring at Faial and Terceira islands

Ricardo Aguiar *, Antonio Rocha e Silva and Ricardo Coelho

INETI, Department of Renewable Energies
Lisbon, Portugal

* Tel: +351 210 924 602, E-Mail: ricardo. aguiar@ineti. pt

1. Introduction

The North Atlantic archipelago of Azores (Portugal) consists of nine islands, located about 1,500 km from mainland Europe. Currently the Azores has about 243,000 inhabitants, which depend heavily on imported fossil fuel for their energy supply. This is a concern for the regional Government and its Agency for Energy and Environment, ARENA, which naturally support energy efficiency and use of renewable energies. The Azores are rich in several renewable resources, and have even pioneered Portuguese exploitation of wind, wave, and high enthalpy geothermal energy for electricity generation. However, so far solar energy has not been a priority in the renewable energy panorama, probably because the Azores climate has been considered too cloudy. Nevertheless, this is true only in comparison with the Portuguese mainland, as the radiation levels are probably similar or even better than those of Northern Europe.

In this context ARENA is developing efforts for increasing the use of solar systems. A collaboration, partly financed by an INTERREG III B Project of the European Community, has been established with INETI, the Portuguese Public Laboratory for the area of Energy, to improve the solar climatology of the Azores. This climatology is indeed quite incomplete. It consists mainly on daily measurements for two sites only at the S. Miguel and Terceira islands. Some sunshine records are available from Campbell-Stokes heliographs. Satellite data exists but their quality is uncertain due to the small size of the islands and the shallow view angle.

2. Methods

A measuring campaign was established to gather data on solar radiation, having in mind the data needs for sizing solar thermal and photovoltaic systems in the first place, but also for thermal simulation of buildings. Four meteorological stations were equipped to measure horizontal global solar radiation, ambient temperature and relative humidity. Unfortunately the financial and human resources available did not allow for diffuse radiation sensors.

The first phase of the work addressed the two islands of the eastern group, Sta. Maria and S. Miguel. The current work describes preliminary results for the second phase of the work, which concerned two of the five islands of the central group, Faial and Terceira, see Figure 1 and Table 1. Other efforts are now addressing a third island of this central group, Graciosa.

image016

Figure 1 — Location of monitoring stations.

Station sites were selected according to criteria that included island coverage, representation of microclimatic conditions, safety and reliance of the stations, low horizon obstructions, and placement near populated areas, i. e. those with potential solar energy users. Typical vistas can be appreciated in Fig. 2.

The equipment installed includes Rotronic Hygroclip S3 thermohygrometers, Huksefulx LP 02 pyranometers and Campbell Scientific CR510 dataloggers. The pyranometers were calibrated by early 2005 against a secondary standard (Kipp & Zonnen CM 11) held by the Laboratory for Solar Collector Testing at the INETI Campus, Lisbon.

Tabela 1 — Station sites.

Island

Zone

Site

Longitude

(W)

Latitude (N)

height

(m)

Terceira

Angra

Basic School Padre Jeronimo Emilio Andrade

27° 12′ 52.0»

38° 39′ 21.9»

80

Terceira

Biscoitos

Basic School of Biscoitos

27° 15′ 58.0»

38° 47′ 35.4»

100

Faial

Horta

Secondary School Doutor Manuel de Arriaga

28° 37′ 39.6»

38° 31′ 50.4»

50

Faial

Cedros

Basic School

Prof. Constantino Magno Amaral Jdnior

28° 41′ 34.2»

38° 38′ 9.4»

50

image017

Fig. 2 — Typical mounting of instruments and vistas around the stations.

3. Results

Measurements started by November 2005 and still continue, but the work reports only on the results obtained up to October 2007 (thus about two years).

Figure 3 shows recorded data at Angra, for the year of 2006, as an example. For solar radiation, the extraterrestrial values and clear-sky estimates are also shown. Clear-sky estimates were obtained with the ESRA model (ESRA, 2000) assuming a value of 2 for the Linke turbidity for airmass 2, TLK(2). Figure 4. shows monthly data for the 4 stations.

It is remarked that sequences of clear sky days — and even single clear sky days — are rare situations. On the contrary there are numerous overcast days. The seasonality of radiation data is low compared with continental sites. This feature is especially visible when the clearness index data is analysed: most of the daily values remain in a narrow range of 0.4 to 0.5, complemented with lower values during the Winter and higher values during the Summer, so at the seasonal level, the oscillation is from 0.2 to 0.55 (Fig. 4).

Temperature series show the well known characteristics for relatively small islands, of low thermal amplitude at daily (see Fig. 5) and seasonal levels. Also relative humidity levels are, as expected, quite high and show little variability.

image018

image019

image020

Fig. 3 — Daily records of solar radiation (top, kWh/m2), ambient temperature (middle, °C), and

relative humidity (bottom, %)

In Figure 5 it can be appreciated that the daily mean profiles of hourly solar radiation are almost symmetrical in respect to solar noon. This is somewhat different from the pattern for continental stations. For the later, it is usual that the afternoon values are a bit smaller than the corresponding morning values, due to larger cloud sizes brought about by the accelerated temperature related convection.

image021image022

image023 Подпись: (2005-2007)

Monthly Global Horizontal Solar Radiation (kWh/m2)

Jan Feb Mar Apr May Jun Jul Aug Sep Oct Nov Dec

image025 image026 Подпись: 2005-2007

Monthly Clearness Index

Jan Feb Mar Apr May Jun Jul Aug Sep Oct Nov Dec

12

10

8

6

Fig. 5 — Typical mean daily profiles for 2 stations (May 2006-2007).

4. Climatology

Long term records of sunshine hours are available for some classic meteorological stations operated by the Portuguese Weather Services. It is possible to estimate long term solar radiation data using the well known relationships of relative sunshine and clearness index at the monthly scale.

As simultaneous radiation and sunshine data was not available throughout the Azores region, the usual Angstrom relationship is difficult to apply. The approach taken was instead the one proposed by Suehrcke (e. g. Suehrcke, 2000; Tiba et al., 2002)

Подпись: [1](<Gm> /<Gcm>)2 = <Sm> / <S()m>

where <> denotes long term averages, index m a monthly mean, G is global horizontal solar radiation, Gc the corresponding clear sky value, S is bright sunshine hours and S0 the daylength.

Подпись: Fig. 6 - Adjusting the Linke turbidity for the Angra site.

A clear sky must be implemented to use the method. Figure 6 illustrates the approach used to obtain a Linke turbidity to feed in the ERA model. Maxima for each Julian day where computed from the data and these where fitted by adjusting the Linke turbidity. For many days and the short monitoring period, only cloudy values where available, so the method is not fully objective in this conditions. Nevertheless an estimate of TLK(2)=4 was obtained. This is higher than for continental unpolluted stations, which typically display values around 3.

Using these turbidity estimates and the recorded sunshine data for 1951-80 (IM, 2003), the climatology obtained is the one presented in Table 2.

The differences of the estimated climatology to the short-term monitoring mean data are surprisingly small. The Suehrcke approach points to long term data a bit above the short-term monitoring 2005-2007. The main difference appears for June, and it seems quite possible that this was because of atypical weather at the region, in particular for the Summer 2005.

Table 2 — Solar radiation climatology at Angra do Heroismo estimated from sunhsine records.

Tlk(2)

<Sm>

(hours/month)

<Gm>

(kWh/m2.day)

Л

E

V

Estimated

2005-07

Estimated

2005-07

Jan

4

83

2.08

1.81

0.33

0.28

Feb

4

87

2.67

2.67

0.35

0.35

Mar

4

114

3.44

3.28

0.38

0.36

Apr

4

134

4.27

4.20

0.42

0.40

May

4

168

4.96

5.54

0.45

0.50

Jun

4

170

5.13

4.79

0.45

0.42

Jul

4

201

5.45

5.66

0.49

0.51

Aug

4

227

5.56

5.10

0.53

0.49

Sep

4

167

4.42

4.24

0.47

0.45

Oct

4

133

3.31

2.96

0.42

0.36

Nov

4

93

2.34

2.09

0.35

0.31

Dec

4

80

1.93

1.59

0.32

0.26

Year

3.80

3.66

0.41

0.39

5. Conclusions

Preliminary results of monitoring for 2005-2007 reveal that the climate at the four stations — and therefore at the two islands — is very similar. Daily thermal amplitude is low and relative humidity levels are high, features already expected taking into account the nearby ocean. Atmospheric turbidity apparently suffers from high levels of humidity and marine aerosols.

Some morning-afternoon asymmetry exists but it is small. The findings at the Azores islands suggest that most of the nebulosity there is related to macroscale eddies (the Azores Anticyclone in particular). This would also explain why the data at the northern and southern sites of the islands, and at various islands, are so similar. Indeed average yearly global horizontal irradiation at Terceira island was about 3.65 kWh/m2 per day, slightly less than for Faial island, 3.75 kWh/m2 per day.

Daily radiation sequences do not display long runs of overcast or sunny conditions, but frequent oscillations, reflected in low autocorrelation values of the detrended sequences. However, the most striking aspect is the small seasonality of the various parameters. This was expected for temperature and humidity due to the presence of the ocean and the small size of the islands, but is also true for solar radiation, especially when viewed from a clearness index perspective.

As a result of the monitoring, a clear sly model and a methodology to obtain long term climatic values could be obtained for these islands.

6. Further work

The meteorological records are now being processed to yield Reference Meteorological Years, with the objective of providing better meteorological data for the Portuguese governmental schemes supporting solar energy as well as for the Portuguese building regulation codes (subsidiary to the EU Directive on Energy Efficiency in Buildings). These require that both the summer thermal energy balance of buildings and a mandatory contribution of solar energy be computed through detailed numerical simulation with hourly data — currently obtained from stochastic models not yet tuned for these mid-Atlantic climates.

Acknowledgements — This work was partly supported by Project ERAMAC — Maximizagao da Penetragao das Energias Renovaveis e Utilizagao Racional da Energia nas Ilhas da Macaronesia, integrated in Programme INTERREG III-B, also supported by the Regional Government of Azores, and implemented by the Azores Regional Energy and Environment Agency, ARENA.

References

ESRA (2000). The European Solar Radiation Atlas. Scharmer, K. and J. Greif, Eds. ISBN 2-911762-21­5, 110 pp. Presses de l’Ecole des Mines de Paris, Chapter 3: Basics of Solar Radiation. J. Page and R. Aguiar.

IM (2003). Normais Climatologicas para 1961-90 publicadas pelo Institute de Meteorologia, obtidas via Projecto CLIMAAT, INTERREG_3B — Mac 2.3/A3.

Suehrcke, H. (2000) On the relationship betweeen duration of sunshine and solar radiation on the earth’s surface: Angstrom’s equation revisited, Solar Energy, 68, 5, 417-425.

Tiba, C., N. Fraidenraich e R. Aguiar (2002). Valor Acrescentado do Modelo de Suerhcke para a

Radiagao Global Mensal Avaliado com Dados Brasileiros. Actas do XI Congresso Iberico e VI Ibero Americano de Energia Solar, 29 Set. a 2 Out. 2002, Vilamoura. Edigao SPES, Lisboa.

Yearly Sum and Frequency distribution of DNI

The accuracy of the proposed method to derive DNI was evaluated for the year 2005 for six stations of the Spanish Meteorological Service INM, see table 1. The evaluation was performed for all hourly values with the sun above horizon.

Table 1: INM stations with measurements of direct normal irradiance DNI.

Id

Site

Latitude

Longitude

1

Santander

43.49°N

3.80°W

2

Oviedo

43.35°N

5.87°W

3

A Coruna

43.37°N

8.42°W

4

Valladolid

41.65°N

4.77°W

5

Murcia

38.00°N

1.17°W

6

Madrid

40.45°N

3.27°W

Special focus of the evaluation was on the accuracy of yearly sums and on the investigation of frequency distributions of the time series, as these are relevant for yield estimates. Beside this, the relative bias rBIAS and the relative root mean square error rRMSE are used for quantitative comparisons.

For hourly values an rRMSE of 14.7% for global irradiance and of 31% for direct normal irradiance was found for the Spanish stations. The rBIAS is 1.5% for global irradiance and 1.1% for direct irradiance respectively.

Figure 4 displays rBIAS and rRMSE of DNI for the Spanish stations. The rBIAS for one year and one station is equivalent to the relative deviation of the annual sum for one station. In addition the rBIAS for clear sky situations rBIASclearsky is provided. Hours are assigned as clear sky situations, if two criteria match: The clear sky index lies within 0.9<=k*< =1.1 and the variability of the cloud index in a small region of 3×5 pixel is small.

The comparison of rBIAS and rBIASciearsky illustrates the strong influence of the quality of the clear sky model and the atmospheric input parameters on the quality of the annual sums. The deviation of annual satellite derived irradiance sums from the respective ground measured sums between -2% and 8.5% for DNI.

In table 2 the accuracy information is given on different time scales which are relevant for solar energy applications. The deviation of annual satellite derived irradiance sums from the respective ground measured sums is between -2% and 4.5% for GHI and between -2% and 8.5% for DNI.

Table 2: Accuracy of satellite derived global horizontal irradiance GHI and direct normal irradiance DNI for

Подпись: Fig. 5: Frequency distribution of calculated and measured direct normal irradiance (left) and of global irradiance (right) for the 6 spanish stations.

different time scales.

GHI

DNI

hourly mean

335 W/m2

366 W/m:

rRMSE hourly

14.5%

31.1%

rRMSE daily

7.5%

18.5%

rRMSE monthly

3.6%

6.3%

rBIAS

1.5%

1.1%

For energy conversion systems with non-linear response to the irradiance input a correct representation of the frequency distribution is of special importance. Figure 5 displays the frequency distribution of calculated and measured DNI and GHI for the Spanish stations; a fairly good agreement is achieved.

3. Conclusion

We developed a method to derive direct normal irradiance from MSG data. The influence of clouds on the direct normal irradiance is derived from MSG data with high quality. The quality for clear skies is determined by the accuracy of the aerosol climatology.

4. Acknowledgements

Thanks are due to the Spanish Meteorological Service INM for the supply of ground data.

References

[1] Hammer A., Heinemann D., Hoyer C., Kuhlemann R., Lorenz E., Muller R., Beyer H. G. (2003): Solar energy assessment using remote sensing technologies. Remote Sensing of Environment, 86, 423-432.

[2] Fontoynont, M., Dumortier, D., Heinemann, D., Hammer, A., Olseth, J. A., Skartveit, A., Ineichen, P., Reise, C., Page, J., Roche, L., Beyer, H. G. and Wald, L.: 1998, ‘Satellight: A WWW Server Which Provides High Quality Daylight and Solar Radiation Data for Western and Central Europe’, Proceeding of the 9th Conference on Satellite Meteorology and Oceanography, Paris, France, 25.-29.05.1998, 434-437

[3] Muller, R. W., Dagestad, K. F., Ineichen, P., Schroedter, M., Cros, S., Dumortier, D., Kuhlemann, R., Olseth, J. A., Piernavieja, C., Reise, C., Wald, L., Heinemann, D. (2004): Rethinking satellite based solar irradiance modelling — The SOLIS clear-sky module. Remote Sensing of the Environment, Volume 91, Issue 2, 160-174

[4] Mayer, B. and Kylling, A. (2005): Technical Note: The libRadtran software package for radiative transfer calculations: Description and examples of use. Atmos. Chem. Phys., 5:1855-1877, 2005

[5] Kinne et al. (2005): An AeroCom Initial Assessment — Optical Properties in Aerosol Component Modules of Global Models. In: Atmospheric Chemistry and Physics Discussions, 5, 8285-8330.

[6] Kalnay, E. et al. (1996): The NMC/NCAR 40-year reanalysis project. Bull. Am. Meteorol. Soc. 77 (3), 437­472.

[7] Kemper A. (2007): Bestimmung der Diffusstrahlung unter Wolken aus Daten des Satelliten MSG. Diploma thesis, Oldenburg Unversity, Germany.

Comparison of meteorological data from different sources. for Bishkek city, Kyrgyzstan

Ruslan Botpaev[2]*, Alaibek Obozov1,

Janybek Orozaliev2, Christian Budig2, Klaus Vajen2,

1 Kyrgyz State Technical University, Department for Renewable Energies, Bishkek (Kyrgyzstan)
2 Kassel University, Institute of Thermal Energy Engineering, Kassel (Germany)
Corresponding Author, botpaev@inbox. ru

Abstract

Meteorological data from different sources (a local weather station, Meteonorm 5.1 and 6.0 as well as own measurements) have been compared with each other for Bishkek, Kyrgyzstan. It was identified that Bishkek city in Meteonorm 5.1 and 6.0 has wrong altitude (2111 m instead of 760 m), which leads to significantly lower ambient temperatures. Therefore, it is necessary to define Bishkek manually as a new site with the correct coordinates. In this case the ambient temperatures are in agreement with those measured by the weather station Frunze. Annual global solar irradiation from own measurements («1500 kWh/m2a) and weather station Frunze (1572 kWh/m2a) are in a good agreement, while its values from Meteonorm 5.1 and 6.0 are approx. 20% lower. Furthermore, monthly sums of global solar irradiation generated with Meteonorm 5.1 have an untypical trend in summer, having two local maximum points. This is inconsistent with irradiation data from other sources and with the sunshine duration in the relevant period. The data from Meteonorm should be proved on plausibility, particularly for sites or stations in developing countries.

1. Introduction

For designing and dimensioning of solar plants and prediction of solar gains it is important to have precise meteorological data, i. e. data of solar radiation, ambient temperatures and wind velocity. Meteorological data for different places can be taken from own measurements, reference books, weather stations or generated with special software (e. g. Meteonorm1).

For Bishkek, the capital of the Kyrgyz Republic in Central Asia, basically, three sources of meteorological data are available: a local weather station Frunze, a software Meteonorm (only versions 5.1 and 6.0 are considered in this study) and own measurement data (only radiation). Geographical coordinates of Bishkek are 74.5°E longitude, 42.8°N latitude (comparable with Rome) and 760 m altitude. The climate is strong continental (hot summer, cold winter, high number of sunny days).

The objective of this investigation is to compare these sources of meteorological data with each other regarding average annual ambient temperatures and solar radiation data.