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Journal articles on the topic 'Receiver functions'

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Published: 4 June 2021
Last updated: 31 January 2023

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1

Park, Jeffrey, and Vadim Levin. "Receiver functions from regionalPwaves." Geophysical Journal International 147, no. 1 (September 2001): 1–11. http://dx.doi.org/10.1046/j.1365-246x.2001.00523.x.

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2

Wu, Qingju, Yonghua Li, Ruiqing Zhang, and Rongsheng Zeng. "Receiver Functions from Autoregressive Deconvolution." Pure and Applied Geophysics 164, no. 11 (December 2007): 2175–92. http://dx.doi.org/10.1007/s00024-007-0269-5.

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3

Alghoniemy, Masoud. "Regularized MIMO Decoders." Journal of Communications Software and Systems 5, no. 4 (December 20, 2010): 149. http://dx.doi.org/10.24138/jcomss.v5i4.201.

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In the Multi Input Multi Output (MIMO) antenna system, it is known that the Linear Minimum Mean Squared Error (MMSE) receiver is equivalent to Tikhonov regularization.Given that, we develop a family of generalized receivers based on regularization with different penalty functions that penalize the received symbols outside the convex hull of the modulating constellation. For illustration purposes we consider two types of penalty functions, the deadzone and infinity norm penalty functions. The proposed decoders have low complexity and can be implemented efficiently using convex optimization algorithms. Simulation results show that the proposed receivers outperform the MMSE receiver by as high as 5-dB at low Signal to Noise Ratio (SNR).
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4

Lekić, Vedran, and Karen M. Fischer. "Interpreting spatially stacked Sp receiver functions." Geophysical Journal International 210, no. 2 (May 12, 2017): 874–86. http://dx.doi.org/10.1093/gji/ggx206.

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5

Svenningsen, L., and B. H. Jacobsen. "AbsoluteS-velocity estimation from receiver functions." Geophysical Journal International 170, no. 3 (September 2007): 1089–94. http://dx.doi.org/10.1111/j.1365-246x.2006.03505.x.

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6

Kumar, M. Ravi, and M. G. Bostock. "Extraction of absolutePvelocity from receiver functions." Geophysical Journal International 175, no. 2 (November 2008): 515–19. http://dx.doi.org/10.1111/j.1365-246x.2008.03963.x.

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7

van Manen, D., J. O. A. Robertsson, A. Curtis, R. Ferber, and H. Paulssen. "Shear wave statics using receiver functions." Geophysical Journal International 153, no. 3 (June 2003): F1—F5. http://dx.doi.org/10.1046/j.1365-246x.2003.01945.x.

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8

Galetti, Erica, and Andrew Curtis. "Generalised receiver functions and seismic interferometry." Tectonophysics 532-535 (April 2012): 1–26. http://dx.doi.org/10.1016/j.tecto.2011.12.004.

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9

Tang, Chi-Chia, Chau-Huei Chen, and Ta-Liang Teng. "Receiver Functions for Three-layer Media." Pure and Applied Geophysics 165, no. 7 (July 2008): 1249–62. http://dx.doi.org/10.1007/s00024-008-0355-3.

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10

Frazer, L. Neil, and Xinhua Sun. "New objective functions for waveform inversion." GEOPHYSICS 63, no. 1 (January 1998): 213–22. http://dx.doi.org/10.1190/1.1444315.

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Inversion is an organized search for parameter values that maximize or minimize an objective function, referred to here as a processor. This note derives three new seismic processors that require neither prior deconvolution nor knowledge of the source‐receiver wavelet. The most powerful of these is the fourwise processor, as it is applicable to data sets from multiple shots and receivers even when each shot has a different unknown signature and each receiver has a different unknown impulse response. Somewhat less powerful than the fourwise processor is the pairwise processor, which is applicable to a data set consisting of two or more traces with the same unknown wavelet but possibly different gains. When only one seismogram exists the partition processor can be used. The partition processor is also applicable when there is only one shot (receiver) and each receiver (shot) has a different signature. In fourwise and pairwise inversions the unknown wavelets may be arbitrarily long in time and need not be minimum phase. In partition inversion the wavelet is assumed to be shorter in time than the data trace itself but is not otherwise restricted. None of the methods requires assumptions about the Green’s function.
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11

Vinnik, L. P. "Receiver function seismology." Физика Земли, no. 1 (March 27, 2019): 16–27. http://dx.doi.org/10.31857/s0002-33372019116-27.

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The application results of the receiver function technique are briefly outlined. The topography of the main seismic boundaries in the mantle transition zone is evaluated with resolution of about 3 km in depth and about 200 km laterally. The maximal amplitudes of depth variations of the main boundaries reach tens of kilometers. The mantle transition zone thinning in the hot spots and the respective increase in temperature by ~100 °C is established. In several regions, two low-velocity layers are revealed in the mantle transition zone, one directly above the 410-km seismic discontinuity and another at a depth of 450 to 500 km. The origin of the first layer is associated with dehydration in the mantle plumes during olivine – walesite phase transformation. The increase in the S-wave velocity at the base of the second layer can explain the observations of the so-called 520-km boundary. The traditional approach to studying the structure of the crust and upper mantle is from surface waves. Receiver functions can provide higher resolution at the same depths when a combination of P- and S-wave receiver functions is used. This type of results was obtained for Fennoscandia, Kaapvaal craton, Indian shield, Central Tien Shan, Baikal rift zone, the Azores, Cape Verde Islands, and the western Mediterranean. S-receiver functions were used in the studies of the lunar crust. The joint P- and S-receiver function inversion provides robust estimates of the parameters of seismic boundaries including weak discontinuities such as the lithosphere – asthenosphere interface of cratons. The parameters determined from receiver functions include the P- to S-wave velocity ratio. In a few regions, a very high (> 2.0) velocity ratio is observed in the lower crust, probably indicating the presence of a fluid with high pore pressure. Receiver functions allow estimating the parameters of azimuthal anisotropy as a function of depth. The changes of the parameters with depth make it possible to distinguish the active anisotropy associated with recent deformations from the frozen anisotropy – the effect of the past tectonic processes.
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12

Espíndola, Victor Hugo, Luis Quintanar, and Juan Manuel Espíndola. "Crustal Structure beneath Mexico from Receiver Functions." Bulletin of the Seismological Society of America 107, no. 5 (September 25, 2017): 2427–42. http://dx.doi.org/10.1785/0120160152.

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13

Vinnik, Lev, Yangfan Deng, Grigoriy Kosarev, Sergey Oreshin, and Larissa Makeyeva. "Permian plume beneath Tarim from receiver functions." Solid Earth 9, no. 5 (October 22, 2018): 1179–85. http://dx.doi.org/10.5194/se-9-1179-2018.

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Abstract. Receiver functions for the central Tien Shan and northern Tarim in central Asia reveal a pronounced depression on the 410 km discontinuity beneath the Permian basalts in Tarim. The depression may be caused by elevated temperature. The striking spatial correlation between the anomaly of the MTZ and the Permian basalts suggests that both may be effects of the same plume. This relation can be reconciled with the possible motion of Tarim on the order of 1000 km by assuming that the mantle layer, which has moved coherently with the plate since the Permian, extends to a depth of 410 km or more. Alternatively, the lithosphere and underlying mantle are decoupled at a depth of ∼ 200 km, but a cumulative effect of the Tarim plate motion since the Permian is less by an order of magnitude. A similar explanation is applicable to the Siberian traps.
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14

Neal, Scott L., and Gary L. Pavlis. "ImagingP-to-Sconversions with multichannel receiver functions." Geophysical Research Letters 26, no. 16 (August 15, 1999): 2581–84. http://dx.doi.org/10.1029/1999gl900566.

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15

Wu, Qingju, Yonghua Li, Ruiqing Zhang, and Rongsheng Zeng. "Wavelet modelling of broad-band receiver functions." Geophysical Journal International 170, no. 2 (August 2007): 534–44. http://dx.doi.org/10.1111/j.1365-246x.2007.03467.x.

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16

Lodge, Alexandra, and George Helffrich. "Grid search inversion of teleseismic receiver functions." Geophysical Journal International 178, no. 1 (July 2009): 513–23. http://dx.doi.org/10.1111/j.1365-246x.2009.04176.x.

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17

Vinnik, L. P., S. I. Oreshin, S. Speziale, and M. Weber. "Mid-mantle layering from SKS receiver functions." Geophysical Research Letters 37, no. 24 (December 2010): n/a. http://dx.doi.org/10.1029/2010gl045323.

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18

Vinnik, Lev, Hugues Chenet, Jeannine Gagnepain-Beyneix, and Philippe Lognonne. "First seismic receiver functions on the Moon." Geophysical Research Letters 28, no. 15 (August 1, 2001): 3031–34. http://dx.doi.org/10.1029/2001gl012859.

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19

Kim, Seongryong, and Junkee Rhie. "Calculation of Station-Representative Isotropic Receiver Functions." Pure and Applied Geophysics 176, no. 6 (January 24, 2019): 2367–82. http://dx.doi.org/10.1007/s00024-019-02109-3.

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20

Kim, D., and V. Lekic. "Groundwater Variations From Autocorrelation and Receiver Functions." Geophysical Research Letters 46, no. 23 (December 3, 2019): 13722–29. http://dx.doi.org/10.1029/2019gl084719.

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21

Cho, T. "Removing Reverberation in Ice Sheets from Receiver Functions." Seismological Research Letters 82, no. 2 (March 1, 2011): 207–10. http://dx.doi.org/10.1785/gssrl.82.2.207.

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22

Park, J. "Receiver Functions from Multiple-Taper Spectral Correlation Estimates." Bulletin of the Seismological Society of America 90, no. 6 (December 1, 2000): 1507–20. http://dx.doi.org/10.1785/0119990122.

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23

Tauzin, Benoit, Thanh-Son Pham, and Hrvoje Tkalčić. "Receiver functions from seismic interferometry: a practical guide." Geophysical Journal International 217, no. 1 (January 9, 2019): 1–24. http://dx.doi.org/10.1093/gji/ggz002.

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24

Morais, I., L. Vinnik, G. Silveira, S. Kiselev, and L. Matias. "Mantle beneath the Gibraltar Arc from receiver functions." Geophysical Journal International 200, no. 2 (January 13, 2015): 1153–69. http://dx.doi.org/10.1093/gji/ggu456.

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25

Chai, C., C. J. Ammon, S. Anandakrishnan, C. Ramirez, and A. Nyblade. "Estimating subglacial structure using P-wave receiver functions." Geophysical Journal International 209, no. 2 (February 23, 2017): 1064–79. http://dx.doi.org/10.1093/gji/ggx075.

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26

Leahy, Garrett M., Rebecca L. Saltzer, and Jan Schmedes. "Imaging the shallow crust with teleseismic receiver functions." Geophysical Journal International 191, no. 2 (September 7, 2012): 627–36. http://dx.doi.org/10.1111/j.1365-246x.2012.05615.x.

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27

Kind, Rainer, Xiaohui Yuan, and Prakash Kumar. "Seismic receiver functions and the lithosphere–asthenosphere boundary." Tectonophysics 536-537 (April 2012): 25–43. http://dx.doi.org/10.1016/j.tecto.2012.03.005.

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28

Schulte-Pelkum, Vera, and Kevin H. Mahan. "Imaging Faults and Shear Zones Using Receiver Functions." Pure and Applied Geophysics 171, no. 11 (May 9, 2014): 2967–91. http://dx.doi.org/10.1007/s00024-014-0853-4.

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29

Lombardi, Denis, Jochen Braunmiller, Edi Kissling, and Domenico Giardini. "Alpine mantle transition zone imaged by receiver functions." Earth and Planetary Science Letters 278, no. 3-4 (February 2009): 163–74. http://dx.doi.org/10.1016/j.epsl.2008.11.029.

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30

Shao-Hua, QI, LIU Qi-Yuan, CHEN Jiu-Hui, and GUO Biao. "NOISE SUPPRESSION OF RECEIVER FUNCTIONS USING CURVELET TRANSFORM." Chinese Journal of Geophysics 59, no. 2 (March 2016): 125–38. http://dx.doi.org/10.1002/cjg2.20219.

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31

Bianchi, I., G. Bokelmann, and K. Shiomi. "Crustal anisotropy across northern Japan from receiver functions." Journal of Geophysical Research: Solid Earth 120, no. 7 (July 2015): 4998–5012. http://dx.doi.org/10.1002/2014jb011681.

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32

Frederiksen, A. W. "Transfer functions between teleseismic data components." Geophysical Journal International 221, no. 2 (February 17, 2020): 1248–63. http://dx.doi.org/10.1093/gji/ggaa085.

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SUMMARY Different data components of teleseismic waveforms are related by transfer functions that depend only on receiver-side structure. This is the common basis of a number of teleseismic techniques, including receiver functions and shear wave splitting analysis. Common trace misfits used in these analysis techniques are shown to be equivalent to band-limited comparisons of real and synthetic transfer functions. The data deconvolution used in receiver function analysis leads to reduced structural resolution compared to direct trace-based misfits such as cross-convolution, with direct transfer function modelling of a data trace having the particular advantage of a physically meaningful misfit. Having established that the intertrace transfer function contains all available structural information, the sensitivity of transfer functions to structure is examined for a series of teleseismic scenarios. Transfer functions for the teleseismic P coda show a strong sensitivity to shallow low-velocity structures such as sedimentary basins; the Sp precursors used in S receiver functions are less affected. Examination of transfer functions for shear wave splitting shows that response complexities occur at frequencies too high to be observable in teleseismic studies, and that the dominant control on the response is the splitting intensity.
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33

Bello, Mohammed, David G. Cornwell, Nicholas Rawlinson, Anya M. Reading, and Othaniel K. Likkason. "Crustal structure of southeast Australia from teleseismic receiver functions." Solid Earth 12, no. 2 (February 24, 2021): 463–81. http://dx.doi.org/10.5194/se-12-463-2021.

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Abstract. In an effort to improve our understanding of the seismic character of the crust beneath southeast Australia and how it relates to the tectonic evolution of the region, we analyse teleseismic earthquakes recorded by 24 temporary and 8 permanent broadband stations using the receiver function method. Due to the proximity of the temporary stations to Bass Strait, only 13 of these stations yielded usable receiver functions, whereas seven permanent stations produced receiver functions for subsequent analysis. Crustal thickness, bulk seismic velocity properties, and internal crustal structure of the southern Tasmanides – an assemblage of Palaeozoic accretionary orogens that occupy eastern Australia – are constrained by H–κ stacking and receiver function inversion, which point to the following: a ∼ 39.0 km thick crust; an intermediate–high Vp/Vs ratio (∼ 1.70–1.76), relative to ak135; and a broad (> 10 km) crust–mantle transition beneath the Lachlan Fold Belt. These results are interpreted to represent magmatic underplating of mafic materials at the base of the crust. a complex crustal structure beneath VanDieland, a putative Precambrian continental fragment embedded in the southernmost Tasmanides, that features strong variability in the crustal thickness (23–37 km) and Vp/Vs ratio (1.65–193), the latter of which likely represents compositional variability and the presence of melt. The complex origins of VanDieland, which comprises multiple continental ribbons, coupled with recent failed rifting and intraplate volcanism, likely contributes to these observations. stations located in the East Tasmania Terrane and eastern Bass Strait (ETT + EB) collectively indicate a crust of uniform thickness (31–32 km), which clearly distinguishes it from VanDieland to the west. Moho depths are also compared with the continent-wide AusMoho model in southeast Australia and are shown to be largely consistent, except in regions where AusMoho has few constraints (e.g. Flinders Island). A joint interpretation of the new results with ambient noise, teleseismic tomography, and teleseismic shear wave splitting anisotropy helps provide new insight into the way that the crust has been shaped by recent events, including failed rifting during the break-up of Australia and Antarctica and recent intraplate volcanism.
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34

Kumar, P., X. Yuan, R. Kind, and J. Mechie. "The lithosphere-asthenosphere boundary observed with USArray receiver functions." Solid Earth Discussions 4, no. 1 (January 6, 2012): 1–31. http://dx.doi.org/10.5194/sed-4-1-2012.

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Abstract. The dense deployment of seismic stations so far in the western half of the United States within the USArray project provides the opportunity to study in greater detail the structure of the lithosphere-asthenosphere system. We use the S receiver function technique for this purpose which has higher resolution than surface wave tomography, is sensitive to seismic discontinuities and has no problems with multiples like P receiver functions. Only two major discontinuities are observed in the entire area down to about 300 km depth. These are the crust-mantle boundary (Moho) and a negative boundary which we correlate with the lithosphere-asthenosphere boundary (LAB) since a low velocity zone is the classical definition of the seismic observation of the asthenosphere by Gutenberg (1926). Our S receiver function LAB is at a depth of 70–80 km in large parts of westernmost North America. East of the Rocky Mountains its depth is generally between 90 and 110 km. Regions with LAB depths down to about 140 km occur in a stretch from northern Texas over the Colorado Plateau to the Columbia Basalts. These observations agree well with tomography results in the westernmost USA and at the east coast. However, in the central cratonic part of the USA the tomography LAB is near 200 km depth. At this depth no discontinuity is seen in the S receiver functions. The negative signal near 100 km depth in the central part of the USA is interpreted by Yuan and Romanowicz (2010) or Lekic and Romanowicz (2011) as a recently discovered mid lithospheric discontinuity (MLD). A solution for the discrepancy between receiver function imaging and surface wave tomography is not yet obvious and requires more high resolution studies at other cratons before a general solution may be found. Our results agree well with petrophysical models of increased water content in the asthenosphere, which predict a sharp and shallow LAB also in continents (Mierdel et al., 2007).
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35

Yang, Xiaotao, Gary L. Pavlis, and Yinzhi Wang. "A Quality Control Method for TeleseismicP‐Wave Receiver Functions." Bulletin of the Seismological Society of America 106, no. 5 (July 19, 2016): 1948–62. http://dx.doi.org/10.1785/0120150347.

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36

Kumar, P., X. Yuan, R. Kind, and J. Mechie. "The lithosphere-asthenosphere boundary observed with USArray receiver functions." Solid Earth 3, no. 1 (May 24, 2012): 149–59. http://dx.doi.org/10.5194/se-3-149-2012.

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Abstract. The dense deployment of seismic stations so far in the western half of the United States within the USArray project provides the opportunity to study in greater detail the structure of the lithosphere-asthenosphere system. We use the S receiver function technique for this purpose, which has higher resolution than surface wave tomography, is sensitive to seismic discontinuities, and is free from multiples, unlike P receiver functions. Only two major discontinuities are observed in the entire area down to about 300 km depth. These are the crust-mantle boundary (Moho) and a negative boundary, which we correlate with the lithosphere-asthenosphere boundary (LAB), since a low velocity zone is the classical definition of the seismic observation of the asthenosphere by Gutenberg (1926). Our S receiver function LAB is at a depth of 70–80 km in large parts of westernmost North America. East of the Rocky Mountains, its depth is generally between 90 and 110 km. Regions with LAB depths down to about 140 km occur in a stretch from northern Texas, over the Colorado Plateau to the Columbia basalts. These observations agree well with tomography results in the westernmost USA and on the east coast. However, in the central cratonic part of the USA, the tomography LAB is near 200 km depth. At this depth no discontinuity is seen in the S receiver functions. The negative signal near 100 km depth in the central part of the USA is interpreted by Yuan and Romanowicz (2010) and Lekic and Romanowicz (2011) as a recently discovered mid-lithospheric discontinuity (MLD). A solution for the discrepancy between receiver function imaging and surface wave tomography is not yet obvious and requires more high resolution studies at other cratons before a general solution may be found. Our results agree well with petrophysical models of increased water content in the asthenosphere, which predict a sharp and shallow LAB also in continents (Mierdel et al., 2007).
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37

Bodin, T., M. Sambridge, H. Tkalčić, P. Arroucau, K. Gallagher, and N. Rawlinson. "Transdimensional inversion of receiver functions and surface wave dispersion." Journal of Geophysical Research: Solid Earth 117, B2 (February 2012): n/a. http://dx.doi.org/10.1029/2011jb008560.

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38

Goev, A. G., G. L. Kosarev, O. Yu Riznichenko, and I. A. Sanina. "Velocity Model of Western Volgo-Uralia from Receiver Functions." Izvestiya, Physics of the Solid Earth 54, no. 6 (November 2018): 949–63. http://dx.doi.org/10.1134/s1069351318060058.

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39

Kraft, Helene A., Hans Thybo, Lev P. Vinnik, and S. Oreshin. "Crustal Structure in Central‐Eastern Greenland From Receiver Functions." Journal of Geophysical Research: Solid Earth 124, no. 2 (February 2019): 1653–70. http://dx.doi.org/10.1029/2018jb015919.

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40

Farra, V., and L. Vinnik. "Upper mantle stratification by P and S receiver functions." Geophysical Journal International 141, no. 3 (June 1, 2000): 699–712. http://dx.doi.org/10.1046/j.1365-246x.2000.00118.x.

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41

Randall, G. E. "Efficient calculation of differential seismograms for lithospheric receiver functions." Geophysical Journal International 99, no. 3 (December 1989): 469–81. http://dx.doi.org/10.1111/j.1365-246x.1989.tb02033.x.

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42

Mandal, Prantik, and Koushik Biswas. "Teleseismic receiver functions modeling of the eastern Indian craton." Physics of the Earth and Planetary Interiors 258 (September 2016): 1–14. http://dx.doi.org/10.1016/j.pepi.2016.07.002.

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43

Bishop, J. W., J. M. Lees, C. B. Biryol, T. D. Mikesell, and L. Franco. "Examining the interior of Llaima Volcano with receiver functions." Journal of Volcanology and Geothermal Research 352 (February 2018): 1–9. http://dx.doi.org/10.1016/j.jvolgeores.2017.11.022.

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44

Wang, Hsiao-Lan, Lupei Zhu, and How-Wei Chen. "Moho depth variation in Taiwan from teleseismic receiver functions." Journal of Asian Earth Sciences 37, no. 3 (February 2010): 286–91. http://dx.doi.org/10.1016/j.jseaes.2009.08.015.

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45

Schneider, F. M., X. Yuan, B. Schurr, J. Mechie, C. Sippl, S. ‐K Kufner, L. Ratschbacher, et al. "The Crust in the Pamir: Insights From Receiver Functions." Journal of Geophysical Research: Solid Earth 124, no. 8 (August 2019): 9313–31. http://dx.doi.org/10.1029/2019jb017765.

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46

Singh, Satyan, and Roel Snieder. "Source-receiver Marchenko redatuming: Obtaining virtual receivers and virtual sources in the subsurface." GEOPHYSICS 82, no. 3 (May 1, 2017): Q13—Q21. http://dx.doi.org/10.1190/geo2016-0074.1.

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By solving the Marchenko equations, one can retrieve the Green’s function (Marchenko Green’s function) between a virtual receiver in the subsurface and points at the surface (no physical receiver is required at the virtual location). We extend the idea behind these equations to retrieve the Green’s function between any two points in the subsurface, i.e., between a virtual source and a virtual receiver (no physical source or physical receiver is required at either of these locations). This Green’s function is called the virtual Green’s function, and it includes all primary, internal, and free-surface multiples. Similar to the Marchenko Green’s function, this virtual Green’s function requires the reflection response at the surface (single-sided illumination) and an estimate of the first-arrival traveltime from the virtual locations to the surface. These Green’s functions can be used to image the interfaces from above and below.
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47

Nowack, Robert L., and Wang-Ping Chen. "Source-receiver reciprocity and empirical Green's functions from chemical blasts." Bulletin of the Seismological Society of America 89, no. 2 (April 1, 1999): 538–43. http://dx.doi.org/10.1785/bssa0890020538.

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Abstract We investigated source-receiver reciprocity in the context of empirical Green's functions (EGF) for chemical blasts. Theoretically, reciprocity holds between a purely explosive source and the divergence of the displacement field (dilation). Using a pair of large, delay-sequence mining blasts in southern Indiana, we carried out a pilot experiment in the field. Preliminary results show that reliable EGF can be obtained using reciprocity below a frequency threshold of about 2 Hz, where fine details in the source function are not critical. These results have applications for the characterization of seismic sources and wave propagation at local and regional distances using reciprocal geometries.
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48

Leahy, G. M., and J. A. Collins. "Improved Statistical Processing for Common-Conversion-Point Stacked Receiver Functions." Bulletin of the Seismological Society of America 99, no. 2A (April 1, 2009): 914–21. http://dx.doi.org/10.1785/0120080263.

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49

Priestley, Keith F., George Zandt, and George E. Randall. "Crustal structure in eastern Kazakh, U.S.S.R. from teleseismic receiver functions." Geophysical Research Letters 15, no. 6 (June 1988): 613–16. http://dx.doi.org/10.1029/gl015i006p00613.

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50

Sheetz, Kraig E., and John W. Schlue. "Inferences for the Socorro magma body from teleseismic receiver functions." Geophysical Research Letters 19, no. 18 (September 23, 1992): 1867–70. http://dx.doi.org/10.1029/92gl02137.

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