<span>Coulomb's law describes the magnitude of the electrostatic force between two electric charges.
The Coulomb's law formula is:
<span>F = Ke * q1 * q2 / r2</span>
Where:
q1: Charge of object 1
q2: Charge of object 2
r: Distance between the two objects
F: Force between the two objects. A positive force implies a repulsive interaction, while a negative force implies an attractive interaction
Ke = Coulomb Constant, 8.9875517873681764 * 109 N.m2.C<span>-2
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Coulomb's Law Examples:
What is the magnitude of the force between two protons which are 1.6E10-6 meters apart?
The charge of 1 proton is +1e (+1.602E-19 C).
F = 8.9875517873681764 * 109 * 1.602E-19 * 1.602E-19 / (1.6E-6 * 1.6 E-6) = 9 * 10-17 N
Source- http://www.endmemo.com/physics/coulomb.php
f = k (q^1)(q^2)/r^2
both sides by r^2 Multiply
fr^2/r^2 = kq^3/r^2
both sides by r^2 divide
f = kq^3/r^2
Answer:
f = kq^3/r^2
Hope this helps!!!!
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The frequency of the waves are 0,5
This is because the frequency of the wave is calculated by dividing the speed by the wavelength.
Answer
As the angle of incidence increases in Figure 2.8, a point is finally reached where the refracted ray does not emerge at the second layer but lie along the interface. This particular angle of incidence at which the angle of refraction is 90° and the refracted ray lies along the interface is known as the critical angle. At and beyond the critical angle, there is no transmitted ray and therefore a very high reflected ray will be recorded .
Therefore,
sinθisin90=Vp1Vp2
But, sin 90 = 1.
At critical angle,
sinθcritical=Vp1Vp2
A critical refracted wave travels along the interface between layers and is refracted back into the upper layer at the critical angle. The waves refracted back into the upper layer are called head waves or first-break refractions because at certain distances from a source, they are the first arriving energy. Recorded first-break refraction is shown in Figure 2.10.
Note that these first-break refractions can give us important information about the shallow velocities on land seismic data.
Note also that seismic data are acquired in such a way that reflections from horizons of interest are in the pre-critical region, even at the farthest offset in the data.
In reality, part of the seismic energy arriving at an interface is transmitted and refracted, and another part of the energy is reflected at that same interface. Given that there are many reflectors in the subsurface, there will be many paths from source to receiver, each of them with a different travel time. The proportion of energy reflected depends on the material properties of the two bounding layers and on the angle of incidence
