THE STUDY OF LONGITUDINAL AND LATITUDINAL VARIATION OF EQUATORIAL ELECTROJET SIGNATURE AT STATIONS WITHIN THE 96MM AND 210MM AFRICAN AND ASIAN SECTORS RESPECTIVELY UNDER QUIET CONDITION
Abstract
Two current systems created by electric current in the ionosphere are the solar quiet current () and Equatorial Electrojet (EEJ). The EEJ is what strengthens the horizontal magnetic field. This study is required to monitor the equatorial geomagnetic current, which impacts satellite and high frequency communication and creates atmospheric instabilities. The equatorial electrojet signature’s longitudinal and latitudinal change during quiet conditions at stations inside the 96° 210° African and Asian sectors, respectively, are shown in this paper. For this investigation, information from eleven observatories was used. The purpose of this study is to identify the longitudinal and latitudinal magnetic signatures on the EEJ at several African and Asian sectors under quiet conditions, as well as analyze the equatorial variation of the solar quiet () current. Determining the longitudinal and latitudinal geomagnetic field fluctuations during solar calm conditions along the 96° 210° is the goal of the investigation. Look into daily transient seasonal variation and monthly variance; Find out the causes of the longitudinal and latitudinal fluctuation of the EEJ under solar quiet conditions by measuring the strength of the EEJ at stations within the same longitudinal sectors of 96° 210°. The study made use of the horizontal () component of the geomagnetic field for the year 2008 from the Magnetic Data Acquisition System (MAGDAS) network. To determine silent days, the International silent Days (IQDs) were employed. The formula 0 = 12 (24 + 1), where 0 is the daily baseline, can be used to calculate the values of each geomagnetic element’s daily baseline. The hourly departure from midnight for a specific day was obtained by subtracting the daily baseline from the hourly values, where = 1 24 offers the measure of the hourly amplitude of the change of. The diurnal variation’s monthly average was discovered. By averaging the monthly means for Lloyd’s season, the seasonal variation of was discovered. Results showed that: Depending on how close or far (latitudinal difference) they are to the EEJ band (confined within 3°) where the EEJ current flows eastwards, the longitudinal and latitudinal variation in the varies in magnitude from one station to another within the same longitude; The maximum DAV and TIR EEJ longitudinal monthly variation, which occurs in September around the equinox, is 92. This greater electric current (equatorial electrojet) passing over DAV and TIR was indicated by the elevated amplitude at DAV and TIR compared to the other 9 sites. Thus, a wider electrojet over the stations may be the cause of the large magnitude. The magnitude of EEJ strength at stations within the same specified longitude differs, with the maximum EEJ strength at ILR being maximum with a value of 55 at about 1100 LT and the maximum EEJ strength at DAV being maximum with a value of 93 at about 1200LT, which is the highest for the specified year. The possible causes of the variation of EEJ are seen to be the ionospheric processes and physical structure such as wind. For all of the charts, the value peaks between 1000LT and 0200LT, and it varies with both longitude and latitude. In solstice months, where the buildup flank is steeper in the morning than in the evening, the EEJ value is seen to be higher than those of equinoctial months.
First Chapter Introduction
1.1 Background Information
The ratio of nitrogen to oxygen in the Earth’s atmosphere is around 78 to 21, with traces of water, argon, carbon dioxide, and other gases. An atmosphere rich in free oxygen, found nowhere else in the solar system, ultimately proved essential to one of the Earth’s other distinctive properties.
The air that envelops the Earth gets thinner the further it is from the surface. The air is so thin at 160 km above the Earth that satellites may move through it with no resistance. Even yet, the atmosphere can be detected up to 600 km above the surface.
1.1.1 Atmosphere of the Earth’s Classification
The lower atmosphere and the higher atmosphere are the two main divisions of the earth’s atmosphere. Depending on the latitude, the lower atmosphere rises from the earth’s surface to a height of 40 to 50 km. The meteorologists use the parameters of this area to forecast the atmospheric weather conditions. The upper atmosphere of the earth, or ionosphere, begins around 50 kilometers above the surface and reaches up to 600 kilometers. Due to the partially ionized plasma created by photo-ionization, which is electrically conducting in this region, the ionization level of the ionosphere varies. Both regular and irregular variations are possible. Based on temperature, the atmosphere can be split into layers. The troposphere, stratosphere, mesosphere, thermosphere, and exosphere are the five levels or zones that can be distinguished based on temperature nomenclature (Figure 1.1). It can be separated into the neutrosphere, ionosphere, and protonosphere depending on the degree of ionization.
Troposphere
All weather on Earth occurs in the troposphere, which is the lowest layer of the atmosphere (Figure 1.1). The tropopause, a layer of air that divides the troposphere from the stratosphere, and the Earth’s surface are what hold the troposphere together at its top and bottom, respectively. The troposphere, which makes up 75% of the mass of the atmosphere, is 16 km wider at the equator than it is in the poles. It is in this layer that weather change phenomena occur because water vapor plays a major role in regulating air temperature due to its (the troposphere layer’s) ability to absorb solar energy and thermal radiation from the planet’s surface. Temperature and water vapor content in the troposphere decrease rapidly with altitude and the troposphere contains 99% of the water vapor in the atmosphere. While some of the sunlight that enters the atmosphere is instantly reflected back to space, the majority of it passes through and is absorbed by the earth’s surface. The earth then emits this energy as long-wave radiation back into the atmosphere. The energy is absorbed by carbon dioxide and water molecules, which then release a large portion of it back toward the earth, preventing the average global temperature from altering significantly from year to year.
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