Earth’s magnetic field is generated by an interaction between rotation in the planet’s core and electrical currents. The field then creates the magnetosphere, which acts sort of like a force field, protecting the planet from the brunt of the sun's solar wind. This field has both a North and South pole, which can be used for navigational purposes, and they are not static.
The field itself is not fixed either, and about every 450,000 years or so, the poles actually reverse. This puts the magnetic North where the South was, and vice versa. In this work, the earth magnetic intensity of Uli Community in Anambra State was determined using deflection magnetometer.
TABLE OF CONTENTS
TITLE PAGE
APPROVAL PAGE
DEDICATION
ACKNOWELDGEMENT
ABSTRCT
TABLE OF CONTENT
CHAPTER ONE
- INTRODUCTION
- AIM/OBJECTIVE OF STUDY
- SCOPE OF THE STUDY
- CAUSES THE EARTH'S MAGNETIC FIELD
CHAPTER TWO
LITERATURE REVIEW
2.0 LITERATURE REVIEW
2.1 REVIEW OF MAGNETIC POLES AND MAGNETIC DIPOLE
2.2 VARIATION OF MAGNETIC FIELD
2.3 MAGNETIC FIELD DETECTION
2.4 CHARACTERISTICS OF EARTH'S MAGNETIC FIELD
2.5 EARTH MAGNETIC COMPONENTS
CHAPTER THREE
3.0 METHODOLOGY
3.1 APPARATUS
3.2 THEORY
3.3 INTRUMENT WORKING PRINCIPLE
CHAPTER FOUR
4.1 RESULT AND DISCUSSION
CHAPTER FIVE
5.0 CONCLUSIONS AND REFERENCES
- CONCLUSIONS
- REFERENCES
CHAPTER ONE
1.0 INTRODUCTION
The Earth's magnetic field is generated in the fluid outer core by a self-exciting dynamo process. Electrical currents flowing in the slowly moving molten iron generate the magnetic field. In addition to sources in the Earth's core the magnetic field observable at the Earth's surface has sources in the crust and in the ionosphere and magnetosphere. The geomagnetic field varies on a range of scales and a description of these variations is now made, in the order low frequency to high frequency variations, in both the space and time domains. The final section describes how the Earth's magnetic field can be both a tool and a hazard to the modern world. First of all, however, methods of observing the magnetic field are described.
Earth's magnetic field, also known as the geomagnetic field, is the magnetic field that extends from the Earth's interior out into space, where it meets the solar wind, a stream of charged particles emanating from the Sun. Its magnitude at the Earth's surface ranges from 25 to 65 microteslas (0.25 to 0.65 gauss).[3] Roughly speaking it is the field of a magnetic dipole currently tilted at an angle of about 10 degrees with respect to Earth's rotational axis, as if there were a bar magnet placed at that angle at the center of the Earth. The North geomagnetic pole, located near Greenland in the northern hemisphere, is actually the south pole of the Earth's magnetic field, and the South geomagnetic pole is the north pole. Unlike a bar magnet, Earth's magnetic field changes over time because it is generated by a geodynamo.
While the North and South magnetic poles are usually located near the geographic poles, they can wander widely over geological time scales, but sufficiently slowly for ordinary compasses to remain useful for navigation. However, at irregular intervals averaging several hundred thousand years, the Earth's field reverses and the North and South Magnetic Poles relatively abruptly switch places. These reversals of the geomagnetic poles leave a record in rocks that are of value to paleomagnetists in calculating geomagnetic fields in the past. Such information in turn is helpful in studying the motions of continents and ocean floors in the process of plate tectonics.
The magnetosphere is the region above the ionosphere that is defined by the extent of the Earth's magnetic field in space. It extends several tens of thousands of kilometers into space, protecting the Earth from the charged particles of the solar wind and cosmic rays that would otherwise strip away the upper atmosphere, including the ozone layer that protects the Earth from harmful ultraviolet radiation.
This work focused on determining the magnetic field earth intensity. The magnetic field intensity at a point is the force experienced by a unit North Pole at that point. The tangent, which is drawn on the line of forces, gives the direction of magnetic field intensity. It measures in Telsa(T) or Gauss.
1.1 AIM/OBJECTIVE OF THE STUDY
To determine the magnetic dipole moment (m) of a bar magnet and horizontal intensity (BH) of earth’s magnetic field of Uli community (in anambra state) using a deflection magnetometer.
1.2 SCOPE OF THE STUDY
Earth is largely protected from the solar wind, a stream of energetic charged particles emanating from the Sun, by its magnetic field, which deflects most of the charged particles. Some of the charged particles from the solar wind are trapped in the Van Allen radiation belt. A smaller number of particles from the solar wind manage to travel, as though on an electromagnetic energy transmission line, to the Earth's upper atmosphere and ionosphere in the auroral zones. The only time the solar wind is observable on the Earth is when it is strong enough to produce phenomena such as the aurora and geomagnetic storms. Bright auroras strongly heat the ionosphere, causing its plasma to expand into the magnetosphere, increasing the size of the plasma geosphere, and causing escape of atmospheric matter into the solar wind. Geomagnetic storms result when the pressure of plasmas contained inside the magnetosphere is sufficiently large to inflate and thereby distort the geomagnetic field.
The solar wind is responsible for the overall shape of Earth's magnetosphere, and fluctuations in its speed, density, direction, and entrained magnetic field strongly affect Earth's local space environment. For example, the levels of ionizing radiation and radio interference can vary by factors of hundreds to thousands; and the shape and location of the magnetopause and bow shock wave upstream of it can change by several Earth radii, exposing geosynchronous satellites to the direct solar wind. These phenomena are collectively called space weather. The mechanism of atmospheric stripping is caused by gas being caught in bubbles of magnetic field, which are ripped off by solar winds.[3] Variations in the magnetic field strength have been correlated to rainfall variation within the tropics.[4]
Right at the heart of the Earth is a solid inner core, two thirds of the size of the Moon and composed primarily of iron. At a hellish 5,700°C, this iron is as hot as the Sun’s surface, but the crushing pressure caused by gravity prevents it from becoming liquid. Surrounding this is the outer core, a 2,000 km thick layer of iron, nickel, and small quantities of other metals. Lower pressure than the inner core means the metal here is fluid.
Differences in temperature, pressure and composition within the outer core cause convection currents in the molten metal as cool, dense matter sinks whilst warm, less dense matter rises. The Coriolis force, resulting from the Earth’s spin, also causes swirling whirlpools. This flow of liquid iron generates electric currents, which in turn produce magnetic fields. Charged metals passing through these fields go on to create electric currents of their own, and so the cycle continues. This self-sustaining loop is known as the geodynamo.
The spiralling caused by the Coriolis force means that separate magnetic fields created are roughly aligned in the same direction, their combined effect adding up to produce one vast magnetic field engulfing the planet.
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