1 Solar Radiation and Arguments for its Use
1.1 Solar Radiation
1.1.1 Solar Energy
The most important supplier of energy for the earth is the sun. The whole of life depends on the sunās energy. It is the starting point for the chemical and biological processes on our planet. At the same time it is the most environmentally friendly form of all energies, it can be used in many ways, and it is suitable for all social systems.
In the core of the sun a fusion process takes place in which pairs of hydrogen nuclei are fused into helium nuclei. The energy thus released is radiated into space in the form of electromagnetic radiation. As the sun is 148 million km from the earth, it radiates only a tiny fraction of its energy to the earth. In spite of this, the sun offers more energy in four hours than the human race uses in a whole year.
The age of the sun is estimated by astrophysicists to be about 5 billion years. With a total life expectation of 10 billion years the sun will be available as an energy source for another 5 billion years. Hence from our human perspective the sun offers an unlimited life.
Figure 1.1 The sun: basis of all life on earth
1.1.2 Astronomical and Meteorological Bases
On the outer edge of the earthās atmosphere the irradiated power of the sun is virtually constant. This irradiated power or radiation intensity falling on an area of one square metre is described as the solar constant. This constant is subject to small variations influenced both by changes in the sunās activity (sunspots) and by differences in the distance between the earth and the sun. These irregularities are mostly found in the ultraviolet range; they are less than 5%, and hence not significant in application of the solar constant for solar technology. The average value of the solar constant is given as I0 = 1.367 W/m2 (watts per square metre).
Even based on the astronomical facts alone, the amount of solar energy available on the earth is very variable. It depends not only on the geographical latitude, but also on the time of day and year at a given location. Because of the inclination of the earthās axis, the days in summer are longer than those in winter, and the sun reaches higher solar altitudes in the summer than in the winter period (Figure 1.2).
Figure 1.2. The sunās path at different times of the year at central European latitude (London, Berlin)
Irradiated Power, Irradiance, Heat Quantity
When we say that the sun has an irradiance, G, of for example 1000 W/m2, what is meant here is the capability of radiating a given irradiated power, Ļ (1000 W), onto a receiving surface of 1 m2 (10.76 ft2). The watt is the unit in which power can be measured. If this power is referred, as in this case, to a unit area, then it is called the irradiance.
When the sun shines with this power of 1000 W for 1 hour it has performed 1 kilowatt-hour of work (1 kWh) (Work = Power Ć Time).
If this energy were converted completely into heat, a heat quantity of 1 kWh would be produced.
Irradiated power, | Ļ(W) |
Irradiance, | G(W/m2) |
Heat quantity, | Q(Wh, kWh) |
Figure 1.3 shows the sequence over a day of the irradiation in London on a horizontal receiving surface of 1 m2 (10.76 ft2) for four selected cloudless days over the year. It is clear from the graph that the supply of solar radiation, even without the influence of the weather or clouds, varies by a factor of about ten between summer and winter in London. At lower latitudes this effect decreases in strength, but at higher latitudes it can be even more pronounced. In the southern hemisphere the winter has the highest irradiations, as shown in Figure 1.4, which shows the sequence over a day of the irradiation in Sydney on a horizontal receiving surface of 1 m2 on three average days over the year.
Figure 1.3. Daily courses and daily totals for irradiation in London
Figure 1.4. Irradiation on three different days in Sydney, Australia
Even when the sky is clear and cloudless part of the sunās radiation comes from other directions and not just directly from the sun. This proportion of the radiation, which reaches the eye of the observer through the scattering of air molecules and dust particles, is known as diffuse radiation, Gdif. Part of this is also due to radiation reflected at the earthās surface. The radiation from the sun that meets the earth without any change in direction is called direct radiation, Gdir. The sum of direct and diffuse radiation is known as global solar irradiance, GG (Figure 1.5).
Figure 1.5. Global solar irradiance and its components
Unless nothing else is given, this always refers to the irradiation onto a horizontal receiving surface.1
When the sun is vertically above a location the sunlight takes the shortest path through the atmosphere. However, if the sun is at a lower angle then the path through the atmosphere is longer. This causes increased absorption and scattering of the solar radiation and hence a lower radiation intensity. The air mass factor (AM) is a measure of the length of the path of the sunlight through the earthās atmosphere in terms of one atmosphere thickness. Using this definition, with the sun in the vertical position (elevation angle, Ī³S = 90Ā°), AM = 1 (AM = 1/sin Ī³S).
Figure 1.6 shows the respective highest levels of the sun on certain selected days in London and Berlin. The maximum elevation angle of the sun was achieved on 21 June with Ī³S = 60.8Ā°, and corresponded to an air mass of 1.15. On 22 December the maximum elevation angle of the sun was Ī³S = 14.1Ā°, corresponding to an air mass of 4. At lower latitudes, all elevation angles will increase: for example, at a latitude of 32Ā° (north or south), the highest elevation angle will be 80.8Ā° and the lowest angle will be 34.1Ā°.
Figure 1.6 Sunās level at midday within the course of a year in London and Berlin (latitude: 52Ā°N)
The sunās radiation in space, without the influence of the earthās atmosphere, is described as spectrum AM 0. As it passes through the earthās atmosphere, the radiation intensity is reduced by: