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A seismologist, who uses it to measure the strength of earthquakes.
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∙ 11y ago
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What device is used to record seismic waves?
Seismic waves are measured by seismographs, geophones, hydrophones and accelerometers.
What is the difference between reflection and refraction seismic methods?
Reflection and refraction seismology are both ways to study the structure of the Earth near the surface. Among other things, they are used to search for oil and gas deposits. Reflection seismology works like sonar. You send a sound pulse into the Earth. The sound pulse is probably most often made by setting off an array of small explosive charges, but it could be from trucks that balance on a plate and vibrate that plate to send a waveform into the ground, or for measuring soil layers near the surface it could even be done by pounding on a metal plate with a sledgehammer. The sound pulse goes down into the Earth. Each time it hits a rock layer, soil layer, or other object with different acoustical properties (sound speed and material density) than the one above, part of the energy reflects back toward the geophones, the sound detection devices, you have arranged across the surface. You can record these reflections. Making a few assumptions about sound speed in the subsurface and other matters, and after doing a lot of computer processing, you can build up a picture of the underground structure. Refraction seismology uses a sound pulse and a line of geophones extending away from it to the side. The sound pulse goes into the ground. Some of the energy gets refracted into each of the various rock or soil layers in the ground and moves through them horizontally, and some of the energy is always refracting out of those layers again and returning to the surface, where the geophones detect it. In general, deeper rock layers have higher sound velocities than shallower ones. Therefore at first the earliest signal to reach the geophones will be the direct wave through the surface layer, but at geophones further away a wave that goes down into the Earth, gets into a layer that has a faster sound velocity, and after a while returns to the surface will be the wave that reaches the geophones first. You can take the arrival times of different wave paths at your geophones and calculate out a structure of the rock and soil layers, with the thickness and sound velocity of each. Reflection seismology needs a lot of data processing, so it wasn't that popular until computer power increased enough to make it practical. In general refraction seismology is good for finding the general structure of an area, while reflection seismology is good at finding small details. They really work best when you use them together. The sound velocity data you can get from refraction seismology can be applied to the reflection seismology, and can make it more accurate than it would have been otherwise.
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Non-living thing that uses energy?
A light bulb uses energy. It uses electricity.
How 3D component geophones work?
Geophones are devices created using spring-mounted magnetic masses that move within a wire coil. This creates an electrical signal, which can be measured. Deviations of these signals, called 'seismic responses,' are used to analyze the structure of energy waves of the earth. Most geophones only use one portion of the energy wave being generated, but 3D competent geophones require the use of the full wave for a more accurate reading.
What device is used to record seismic waves?
Seismic waves are measured by seismographs, geophones, hydrophones and accelerometers.
How do geophones work?
Two magnets and a copper coil are located inside the geophone. The coil bounces around because of electromagnetism. Wires send info to the oscylloscope or whatever it is connected to. The Oscylloscope will show the geowaves.
Can you do 4D Seismic Survey in deep marine environment?
Yes. Streamer can be used but the feather makes it hard to repeat. The best way is to place geophones or hydrophones on the sea floor and shoot a dense shot grid.
What is the difference between reflection and refraction seismic methods?
Reflection and refraction seismology are both ways to study the structure of the Earth near the surface. Among other things, they are used to search for oil and gas deposits. Reflection seismology works like sonar. You send a sound pulse into the Earth. The sound pulse is probably most often made by setting off an array of small explosive charges, but it could be from trucks that balance on a plate and vibrate that plate to send a waveform into the ground, or for measuring soil layers near the surface it could even be done by pounding on a metal plate with a sledgehammer. The sound pulse goes down into the Earth. Each time it hits a rock layer, soil layer, or other object with different acoustical properties (sound speed and material density) than the one above, part of the energy reflects back toward the geophones, the sound detection devices, you have arranged across the surface. You can record these reflections. Making a few assumptions about sound speed in the subsurface and other matters, and after doing a lot of computer processing, you can build up a picture of the underground structure. Refraction seismology uses a sound pulse and a line of geophones extending away from it to the side. The sound pulse goes into the ground. Some of the energy gets refracted into each of the various rock or soil layers in the ground and moves through them horizontally, and some of the energy is always refracting out of those layers again and returning to the surface, where the geophones detect it. In general, deeper rock layers have higher sound velocities than shallower ones. Therefore at first the earliest signal to reach the geophones will be the direct wave through the surface layer, but at geophones further away a wave that goes down into the Earth, gets into a layer that has a faster sound velocity, and after a while returns to the surface will be the wave that reaches the geophones first. You can take the arrival times of different wave paths at your geophones and calculate out a structure of the rock and soil layers, with the thickness and sound velocity of each. Reflection seismology needs a lot of data processing, so it wasn't that popular until computer power increased enough to make it practical. In general refraction seismology is good for finding the general structure of an area, while reflection seismology is good at finding small details. They really work best when you use them together. The sound velocity data you can get from refraction seismology can be applied to the reflection seismology, and can make it more accurate than it would have been otherwise.
what is seismic refraction method is Seismic refraction method?
Reflection and refraction seismology are both ways to study the structure of the Earth near the surface. Among other things, they are used to search for oil and gas deposits. Reflection seismology works like sonar. You send a sound pulse into the Earth. The sound pulse is probably most often made by setting off an array of small explosive charges, but it could be from trucks that balance on a plate and vibrate that plate to send a waveform into the ground, or for measuring soil layers near the surface it could even be done by pounding on a metal plate with a sledgehammer. The sound pulse goes down into the Earth. Each time it hits a rock layer, soil layer, or other object with different acoustical properties (sound speed and material density) than the one above, part of the energy reflects back toward the geophones, the sound detection devices, you have arranged across the surface. You can record these reflections. Making a few assumptions about sound speed in the subsurface and other matters, and after doing a lot of computer processing, you can build up a picture of the underground structure. Refraction seismology uses a sound pulse and a line of geophones extending away from it to the side. The sound pulse goes into the ground. Some of the energy gets refracted into each of the various rock or soil layers in the ground and moves through them horizontally, and some of the energy is always refracting out of those layers again and returning to the surface, where the geophones detect it. In general, deeper rock layers have higher sound velocities than shallower ones. Therefore at first the earliest signal to reach the geophones will be the direct wave through the surface layer, but at geophones further away a wave that goes down into the Earth, gets into a layer that has a faster sound velocity, and after a while returns to the surface will be the wave that reaches the geophones first. You can take the arrival times of different wave paths at your geophones and calculate out a structure of the rock and soil layers, with the thickness and sound velocity of each. Reflection seismology needs a lot of data processing, so it wasn't that popular until computer power increased enough to make it practical. In general refraction seismology is good for finding the general structure of an area, while reflection seismology is good at finding small details. They really work best when you use them together. The sound velocity data you can get from refraction seismology can be applied to the reflection seismology, and can make it more accurate than it would have been otherwise.
What instrument measures seismic activity?
Geophone is the instrument used for measuring earth tremors!!!By the way, the term geophone derives from the Greek word "geo" meaning "earth" and "phone" meaning "sound".A geophone is a device which converts ground movement (displacement) into voltage, which may be recorded at a recording station. The deviation of this measured voltage from the base line is called the seismic response and is analyzed for structure of the earth.Geophones have historically been passive analog devices and typically comprise a spring-mounted magnetic mass moving within a wire coil to generate an electrical signal. Recent designs have been based on Microelectromechanical systems technology which generates an electrical response to ground motion through an active feedback circuit to maintain the position of a small piece of silicon.The response of a coil/magnet geophone is proportional to ground velocity, while microelectromechanical systems devices usually respond proportional to acceleration. Microelectromechanical systems have a much higher noise level (50 dB velocity higher) than geophones and can only be used in strong motion or active seismic applications.The frequency response of a geophone is that of a harmonic oscillator, fully determined by corner frequency (typically around 10 Hz) and damping (typically 0.707). Since the corner frequency is proportional to the inverse root of the moving mass, geophones with low corner frequencies (< 1 Hz) become impractical. It is possible to lower the corner frequency electronically, at the price of higher noise and cost.Although waves passing through the earth have a three-dimensional nature, geophones are normally constrained to respond to single dimension - usually the vertical. However, some applications require the full wave to be used and three-component or 3-C geophones are used. In analog devices, three moving coil elements are mounted in an orthogonal arrangement within a single case.The majority of geophones are used in reflection seismology to record the energy waves reflected by the subsurface geology. In this case the primary interest is in the vertical motion of the Earth's surface. However, not all the waves are upwards travelling. A strong, horizontally transmitted wave known as ground-roll also generates vertical motion that can obliterate the weaker vertical signals. By using large areal arrays tuned to the wavelength of the ground-roll the dominant noise signals can be attenuated and the weaker data signals reinforced.Analog geophones are very sensitive devices which can respond to very distant tremors. These small signals can be drowned by larger signals from local sources. It is possible though to recover the small signals caused by large but distant events by correlating signals from several geophones deployed in an array. Signals which are registered only at one or few geophones can be attributed to ll, local events and thus discarded. It can be assumed that small signals that register uniformly at all geophones in an array can be attributed to a distant and therefore significant event.The sensitivity of passive geophones is typically 30 Volts/(meter/second), so they are in general not a replacement for broadband seismometers.Conversely, some applications of geophones are interested only in very local events. A notable example is in the application of Remote Ground Sensors (RGS) incorporated in Unattended Ground Sensor (UGS) Systems. In such an application there is an area of interest which when penetrated a system operator is to be informed, perhaps by an alert which could be accompanied by supporting photographic data.seismograph
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