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= Receiver function = |
= Receiver function = |
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The '''receiver function''' technique is a way to image the [[structure of the Earth]] and its internal boundaries by using the information from [[teleseism]]ic [[earthquake]]s recorded at a three-component [[seismograph]]. |
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A teleseismic [[P-wave]] will generate P |
A teleseismic [[P-wave]] will generate P-to-S conversions at boundaries, such as the [[Mohorovičić discontinuity|Moho]] (crust-mantle boundary), beneath the seismograph. The difference in travel time between the generated [[S-wave]] and P-wave contains information about the depth to the boundary and about the P- and S-wave velocities. If further reverberations are included more detailed structure can be resolved.<ref>{{Cite journal|last=Vinnik|first=L.P.|date=1977-9|title=Detection of waves converted from P to SV in the mantle|url=http://linkinghub.elsevier.com/retrieve/pii/0031920177900085|journal=Physics of the Earth and Planetary Interiors|language=en|volume=15|issue=1|pages=39–45|doi=10.1016/0031-9201(77)90008-5}}</ref> This is done by [[deconvolution]] of the incoming vertical and longitudinal components of the seismogram which removes the common part of the components - namely, the source and travel path information.<ref>{{Cite journal|last=Frederiksen|first=A. W.|last2=Bostock|first2=M. G.|date=2000-05-01|title=Modelling teleseismic waves in dipping anisotropic structures|url=https://academic.oup.com/gji/article-lookup/doi/10.1046/j.1365-246x.2000.00090.x|journal=Geophysical Journal International|language=en|volume=141|issue=2|pages=401–412|doi=10.1046/j.1365-246x.2000.00090.x|issn=0956-540X}}</ref> The resulting waveform is the receiver function. |
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Similarly, a teleseismic [[S-wave]] will generate an S |
Similarly, a teleseismic [[S-wave]] will generate an S-to-P conversion beneath the seismic station. |
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== Method == |
== Method == |
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[[File:Receiver Function Incident Wave.svg|thumb|300x300px|Incident P and S wave phases for a receiver function.]] |
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As a P wave in the mantle pass upwards through the Moho, it is |
As a P wave in the mantle pass upwards through the Moho, it is partially converted into an S wave. Both the P-wave and S wave (known at Ps) is picked up by the seismometer on the Earth's surface, and can be used to analyze discontinuities within the Earth. In addition to these P and Ps waves, additional phases are created by multiple reflections. These phases include: ''PpPmp PpSmp, PpPms'', and ''PpSms, as well as PsPmp, PsSmp, PsPms and PsSms''. (See [[Seismic wave#Notation|seismic phase notation]] for more info). The phases for which the last "leg" is a P-wave (P, Ps, Smp, etc.) are dominantly recorded on the vertical component of the seismograph, whereas the phases for which the last "leg" is an S-wave (Ps, Pp, Sms, etc.) are dominantly recorded on the horizontal component.<ref name=":2" /> |
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The primary method for creating a receiver function is based on analyzing the product of waves that pass from the mantle through the Moho boundary. |
The primary method for creating a receiver function is based on analyzing the product of waves that pass from the mantle through the Moho boundary. The large compositional differences between the crust and the mantle cause large differences in seismic waves as they pass through the discontinuity.<ref name=":0">{{Cite journal|last=Wiemer|first=S.|last2=Agostinetti|first2=N. Piana|last3=Kissling|first3=E.|last4=Bianchi|first4=I.|last5=Spada|first5=M.|date=2013-08-01|title=Combining controlled-source seismology and receiver function information to derive 3-D Moho topography for Italy|url=https://academic.oup.com/gji/article/194/2/1050/600668|journal=Geophysical Journal International|language=en|volume=194|issue=2|pages=1050–1068|doi=10.1093/gji/ggt148|issn=0956-540X}}</ref> Receiver functions use [[Snell's law]] refraction of P waves and converted S waves to estimate the depth of the Moho. They are only generated clearly if the [[Central angle|central angle]] (angle subtended at the center of the Earth) between the seismic event and the seismograph station is between 30 and 80 degrees (between about 3300 and 8900 km separation).<ref name=":2" /> The method is also most effective when the seismic event causing the waves occurs significantly below the Moho, which is important to avoid surface interference.<ref name=":2">{{Cite journal|last=Langston|first=Charles A.|last2=Burdick|first2=L. J.|date=1977-06-01|title=Modeling crustal structure through the use of converted phases in teleseismic body-wave forms|url=https://pubs.geoscienceworld.org/ssa/bssa/article-abstract/67/3/677/117706/modeling-crustal-structure-through-the-use-of|journal=Bulletin of the Seismological Society of America|language=en|volume=67|issue=3|pages=677–691|issn=0037-1106}}</ref> |
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| ⚫ | |||
| ⚫ | Over time, several seismic events can occur in the same geographic area, with each event causing a corresponding vertical waveform and horizontal waveform. Once several observations have been collected, the waveforms can be summed together for the vertical component and for the horizontal component. The summed seismogram reduces random noise and makes it easier to see a pattern in the data. By visual inspection, or more commonly by deconvolution of the two waveforms, it is possible to identify each of the relevant phases of the P wave conversions. With the timing of the phases, it is then possible to model the seismic velocities within the crust and the Moho depth beneath the seismic station.<ref name=":2" /> |
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=== Stacking === |
=== Stacking === |
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Where there are many adjacent seismograph stations, it is possible to "stack" receiver function data across seismograph stations to build a 2D or even 3D model of the depth of the Moho.<ref name=":3">{{Cite journal|last=Rondenay|first=Stéphane|date=2009-10-01|title=Upper Mantle Imaging with Array Recordings of Converted and Scattered Teleseismic Waves|url=https://doi.org/10.1007/s10712-009-9071-5|journal=Surveys in Geophysics|language=en|volume=30|issue=4|pages=377–405|doi=10.1007/s10712-009-9071-5|issn=1573-0956}}</ref> This is possible because each station can determine the depth of the Moho at its own location (essentially a 1D measurement). Data from multiple individual data points from adjacent stations can be grouped together and plotted side by side to create a unified graph of the Moho depth over a given area.<ref name=":3" /> |
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TODO: Add a diagram of an incident wave hitting the Moho |
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== Applications == |
== Applications == |
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Receiver functions |
Receiver functions contain detailed information on the average seismic velocities within the crust and on the depth of the Moho at a specific location. This data alone can be useful in obtaining information about a specific location.<ref name=":2" /> But when receiver function data from one seismic station is combined with data from many other stations, it is possible to build a detailed map of the Moho depth and of seismic velocity across a large geographic area. |
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This data can be used for a variety of purposes. It can be used to note variations in the depth of the crust. Receiver functions have been used, for example, to discover depressions in the Moho below mountains in southwest Japan.<ref name=":1">{{Cite journal|last=Yamauchi|first=Makiko|last2=Hirahara|first2=Kazuro|last3=Shibutani|first3=Takuo|date=2003-01-01|title=High resolution receiver function imaging of the seismic velocity discontinuities in the crust and the uppermost mantle beneath southwest Japan|url=https://doi.org/10.1186/BF03352463|journal=Earth, Planets and Space|volume=55|pages=BF03352463|doi=10.1186/BF03352463|issn=1880-5981}}</ref> This data can also be used to better understand [[Earthquake|earthquakes]] that cause natural disasters.<ref name=":1" /> Additionally, maps of seismic velocities and crustal |
This data can be used for a variety of purposes. It can be used to note variations in the depth of the crust. Receiver functions have been used, for example, to discover depressions in the Moho below mountains in southwest Japan.<ref name=":1">{{Cite journal|last=Yamauchi|first=Makiko|last2=Hirahara|first2=Kazuro|last3=Shibutani|first3=Takuo|date=2003-01-01|title=High resolution receiver function imaging of the seismic velocity discontinuities in the crust and the uppermost mantle beneath southwest Japan|url=https://doi.org/10.1186/BF03352463|journal=Earth, Planets and Space|volume=55|pages=BF03352463|doi=10.1186/BF03352463|issn=1880-5981}}</ref> This data can also be used to better understand [[Earthquake|earthquakes]] that cause natural disasters.<ref name=":1" /> Additionally, maps of seismic velocities and crustal thickness are useful as baseline data for additional seismological studies.<ref name=":0" /> |
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Data from receiver functions can also be used in conjunction with data, such as data from controlled source seismology |
Data from receiver functions can also be used in conjunction with data, such as data from controlled source seismology to provide higher resolution 3D maps of the Earth's crust.<ref name=":0" /> |
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==References== |
==References== |
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<br /> |
<br /> |
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Latest revision as of 08:23, 15 March 2019
Article to improve: Receiver function.
 | This is a user sandbox of Jreinstr. You can use it for testing or practicing edits. This is not the sandbox where you should draft your assigned article for a dashboard.wikiedu.org course. To find the right sandbox for your assignment, visit your Dashboard course page and follow the Sandbox Draft link for your assigned article in the My Articles section. |
Receiver function
[edit]The receiver function technique is a way to image the structure of the Earth and its internal boundaries by using the information from teleseismic earthquakes recorded at a three-component seismograph.
A teleseismic P-wave will generate P-to-S conversions at boundaries, such as the Moho (crust-mantle boundary), beneath the seismograph. The difference in travel time between the generated S-wave and P-wave contains information about the depth to the boundary and about the P- and S-wave velocities. If further reverberations are included more detailed structure can be resolved.[1] This is done by deconvolution of the incoming vertical and longitudinal components of the seismogram which removes the common part of the components - namely, the source and travel path information.[2] The resulting waveform is the receiver function.
Similarly, a teleseismic S-wave will generate an S-to-P conversion beneath the seismic station.
Method
[edit]
As a P wave in the mantle pass upwards through the Moho, it is partially converted into an S wave. Both the P-wave and S wave (known at Ps) is picked up by the seismometer on the Earth's surface, and can be used to analyze discontinuities within the Earth. In addition to these P and Ps waves, additional phases are created by multiple reflections. These phases include: PpPmp PpSmp, PpPms, and PpSms, as well as PsPmp, PsSmp, PsPms and PsSms. (See seismic phase notation for more info). The phases for which the last "leg" is a P-wave (P, Ps, Smp, etc.) are dominantly recorded on the vertical component of the seismograph, whereas the phases for which the last "leg" is an S-wave (Ps, Pp, Sms, etc.) are dominantly recorded on the horizontal component.[3]
The primary method for creating a receiver function is based on analyzing the product of waves that pass from the mantle through the Moho boundary. The large compositional differences between the crust and the mantle cause large differences in seismic waves as they pass through the discontinuity.[4] Receiver functions use Snell's law refraction of P waves and converted S waves to estimate the depth of the Moho. They are only generated clearly if the central angle (angle subtended at the center of the Earth) between the seismic event and the seismograph station is between 30 and 80 degrees (between about 3300 and 8900 km separation).[3] The method is also most effective when the seismic event causing the waves occurs significantly below the Moho, which is important to avoid surface interference.[3]
Over time, several seismic events can occur in the same geographic area, with each event causing a corresponding vertical waveform and horizontal waveform. Once several observations have been collected, the waveforms can be summed together for the vertical component and for the horizontal component. The summed seismogram reduces random noise and makes it easier to see a pattern in the data. By visual inspection, or more commonly by deconvolution of the two waveforms, it is possible to identify each of the relevant phases of the P wave conversions. With the timing of the phases, it is then possible to model the seismic velocities within the crust and the Moho depth beneath the seismic station.[3]
Stacking
[edit]Where there are many adjacent seismograph stations, it is possible to "stack" receiver function data across seismograph stations to build a 2D or even 3D model of the depth of the Moho.[5] This is possible because each station can determine the depth of the Moho at its own location (essentially a 1D measurement). Data from multiple individual data points from adjacent stations can be grouped together and plotted side by side to create a unified graph of the Moho depth over a given area.[5]
Applications
[edit]Receiver functions contain detailed information on the average seismic velocities within the crust and on the depth of the Moho at a specific location. This data alone can be useful in obtaining information about a specific location.[3] But when receiver function data from one seismic station is combined with data from many other stations, it is possible to build a detailed map of the Moho depth and of seismic velocity across a large geographic area.
This data can be used for a variety of purposes. It can be used to note variations in the depth of the crust. Receiver functions have been used, for example, to discover depressions in the Moho below mountains in southwest Japan.[6] This data can also be used to better understand earthquakes that cause natural disasters.[6] Additionally, maps of seismic velocities and crustal thickness are useful as baseline data for additional seismological studies.[4]
Data from receiver functions can also be used in conjunction with data, such as data from controlled source seismology to provide higher resolution 3D maps of the Earth's crust.[4]
References
[edit]
- ^ Vinnik, L.P. (1977-9). "Detection of waves converted from P to SV in the mantle". Physics of the Earth and Planetary Interiors. 15 (1): 39–45. doi:10.1016/0031-9201(77)90008-5.
{{cite journal}}: Check date values in:|date=(help) - ^ Frederiksen, A. W.; Bostock, M. G. (2000-05-01). "Modelling teleseismic waves in dipping anisotropic structures". Geophysical Journal International. 141 (2): 401–412. doi:10.1046/j.1365-246x.2000.00090.x. ISSN 0956-540X.
{{cite journal}}: CS1 maint: unflagged free DOI (link) - ^ a b c d e Langston, Charles A.; Burdick, L. J. (1977-06-01). "Modeling crustal structure through the use of converted phases in teleseismic body-wave forms". Bulletin of the Seismological Society of America. 67 (3): 677–691. ISSN 0037-1106.
- ^ a b c Wiemer, S.; Agostinetti, N. Piana; Kissling, E.; Bianchi, I.; Spada, M. (2013-08-01). "Combining controlled-source seismology and receiver function information to derive 3-D Moho topography for Italy". Geophysical Journal International. 194 (2): 1050–1068. doi:10.1093/gji/ggt148. ISSN 0956-540X.
{{cite journal}}: CS1 maint: unflagged free DOI (link) - ^ a b Rondenay, Stéphane (2009-10-01). "Upper Mantle Imaging with Array Recordings of Converted and Scattered Teleseismic Waves". Surveys in Geophysics. 30 (4): 377–405. doi:10.1007/s10712-009-9071-5. ISSN 1573-0956.
- ^ a b Yamauchi, Makiko; Hirahara, Kazuro; Shibutani, Takuo (2003-01-01). "High resolution receiver function imaging of the seismic velocity discontinuities in the crust and the uppermost mantle beneath southwest Japan". Earth, Planets and Space. 55: BF03352463. doi:10.1186/BF03352463. ISSN 1880-5981.
{{cite journal}}: CS1 maint: unflagged free DOI (link)