P-wave

A P-wave is one of the two main types of elastic body waves, called seismic waves in seismology. P-waves travel faster than other seismic waves and hence are the first signal from an earthquake to arrive at any affected location or at a seismograph. P-waves may be transmitted through gases, liquids, or solids.

Plane P-wave

Representation of the propagation of a P-wave on a 2D grid (empirical shape)

Nomenclature

The name P-wave can stand for either pressure wave (as it is formed from alternating compressions and rarefactions) or primary wave (as it has high velocity and is therefore the first wave to be recorded by a seismograph).[1]

Seismic waves in the Earth

Velocity of seismic waves in the Earth versus depth.[2] The negligible S-wave velocity in the outer core occurs because it is liquid, while in the solid inner core the S-wave velocity is non-zero.

Primary and secondary waves are body waves that travel within the Earth. The motion and behavior of both P-type and S-type in the Earth are monitored to probe the interior structure of the Earth. Discontinuities in velocity as a function of depth are indicative of changes in phase or composition. Differences in arrival times of waves originating in a seismic event like an earthquake as a result of waves taking different paths allow mapping of the Earth's inner structure.[3][4]

P-wave shadow zone

P-wave shadow zone (from USGS)

Almost all the information available on the structure of the Earth's deep interior is derived from observations of the travel times, reflections, refractions and phase transitions of seismic body waves, or normal modes. P-waves travel through the fluid layers of the Earth's interior, and yet they are refracted slightly when they pass through the transition between the semisolid mantle and the liquid outer core. As a result, there is a P-wave "shadow zone" between 103° and 142°[5] from the earthquake's focus, where the initial P-waves are not registered on seismometers. In contrast, S-waves do not travel through liquids.

As an earthquake warning

Advance earthquake warning is possible by detecting the nondestructive primary waves that travel more quickly through the Earth's crust than do the destructive secondary and Rayleigh waves.

The amount of advance warning depends on the delay between the arrival of the P-wave and other destructive waves, generally on the order of seconds up to about 60 to 90 seconds for deep, distant, large quakes such as the 2011 Tohoku earthquake. The effectiveness of advance warning depends on accurate detection of the P-waves and rejection of ground vibrations caused by local activity (such as trucks or construction). Earthquake early warning systems can be automated to allow for immediate safety actions, such as issuing alerts, stopping elevators at the nearest floors and switching off utilities.

Propagation

Velocity

In isotropic and homogeneous solids, a P-wave travels in a straight line longitudinal; thus, the particles in the solid vibrate along the axis of propagation (the direction of motion) of the wave energy. The velocity of P-waves in such a medium is given by

v_{p}={\sqrt {\frac {K+{\frac {4}{3}}\mu }{\rho }}}={\sqrt {\frac {\lambda +2\mu }{\rho }}}

where K is the bulk modulus (the modulus of incompressibility), $\mu$ is the shear modulus (modulus of rigidity, sometimes denoted as G and also called the second Lamé parameter), $\rho$ is the density of the material through which the wave propagates, and $\lambda$ is the first Lamé parameter.

In typical situations the interior of the Earth, the density ρ usually varies much less than K or μ, so the velocity is mostly "controlled" by these two parameters.

The elastic moduli P-wave modulus, $M$ , is defined so that $M=K+4\mu /3$ and thereby

v_{p}={\sqrt {M/\rho }}\

Typical values for P-wave velocity in earthquakes are in the range 5 to 8 km/s. The precise speed varies according to the region of the Earth's interior, from less than 6 km/s in the Earth's crust to 13.5 km/s in the lower mantle, and 11 km/s through the inner core.[6]

Velocity of Common Rock Types[7]
Rock Type	Velocity [m/s]	Velocity [ft/s]
Unconsolidated Sandstone	4600 - 5200	15000 - 17000
Consolidated Sandstone	5800	19000
Shale	1800 - 4900	6000 -16000
Limestone	5800 - 6400	19000 - 21000
Dolomite	6400 - 7300	21000 - 24000
Anhydrite	6100	20000
Granite	5800 - 6100	19000 - 20000
Gabbro	7200	23600

Geologist Francis Birch discovered a relationship between the velocity of P waves and the density of the material the waves are traveling in:

V_{p}=a({\bar {M}})+b\rho

which later became known as Birch's law.

gollark: Well, that breaks, what did you expect to happen?

gollark: Works fine.

gollark: Checking, hold on while I run a CC instance.

gollark: See: KEYBOARDS.

gollark: Stupid because ridiculously uselessly complex.

References

Milsom, J. (2003). Field Geophysics. The geological field guide series. 25. John Wiley and Sons. p. 232. ISBN 978-0-470-84347-5. Retrieved 2010-02-25.
GR Helffrich & BJ Wood (2002). "The Earth's Mantle" (PDF). Nature. 412 (2 August): 501–7. doi:10.1038/35087500. PMID 11484043.
Justin L Rubinstein, DR Shelly & WL Ellsworth (2009). "Non-volcanic tremor: A window into the roots of fault zones". In S. Cloetingh, Jorg Negendank (ed.). New Frontiers in Integrated Solid Earth Sciences. Springer. p. 287 ff. ISBN 978-90-481-2736-8. The analysis of seismic waves provides a direct high-resolution means for studying the internal structure of the Earth...
CMR Fowler (2005). "§4.1 Waves through the Earth". The solid earth: an introduction to global geophysics (2nd ed.). Cambridge University Press. p. 100. ISBN 978-0-521-58409-8. Seismology is the study of the passage of elastic waves through the Earth. It is arguably the most powerful method available for studying the structure of the interior of the Earth, especially the crust and mantle.
Lowrie, William. The Fundamentals of Geophysics. Cambridge University Press, 1997, p. 149.
Dziewonski, Adam M.; Anderson, Don L. (1981). "Preliminary reference Earth model". Physics of the Earth and Planetary Interiors. 25 (4): 297–356. Bibcode:1981PEPI...25..297D. doi:10.1016/0031-9201(81)90046-7.
"Acoustic Logging". epa.gov. 2011-12-12. Retrieved 2015-02-03.

"Photo Glossary of Earthquakes". U.S. Geological Survey". Archived from the original on February 27, 2009. Retrieved March 8, 2009.

External links

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[John-1] Milsom, J. (2003). Field Geophysics. The geological field guide series. 25. John Wiley and Sons. p. 232. ISBN 978-0-470-84347-5. Retrieved 2010-02-25.

[Helffrich-2] GR Helffrich & BJ Wood (2002). "The Earth's Mantle" (PDF). Nature. 412 (2 August): 501–7. doi:10.1038/35087500. PMID 11484043.

[Negendank-3] Justin L Rubinstein, DR Shelly & WL Ellsworth (2009). "Non-volcanic tremor: A window into the roots of fault zones". In S. Cloetingh, Jorg Negendank (ed.). New Frontiers in Integrated Solid Earth Sciences. Springer. p. 287 ff. ISBN 978-90-481-2736-8. The analysis of seismic waves provides a direct high-resolution means for studying the internal structure of the Earth...

[Fowler-4] CMR Fowler (2005). "§4.1 Waves through the Earth". The solid earth: an introduction to global geophysics (2nd ed.). Cambridge University Press. p. 100. ISBN 978-0-521-58409-8. Seismology is the study of the passage of elastic waves through the Earth. It is arguably the most powerful method available for studying the structure of the interior of the Earth, especially the crust and mantle.

[5] Lowrie, William. The Fundamentals of Geophysics. Cambridge University Press, 1997, p. 149.

[6] Dziewonski, Adam M.; Anderson, Don L. (1981). "Preliminary reference Earth model". Physics of the Earth and Planetary Interiors. 25 (4): 297–356. Bibcode:1981PEPI...25..297D. doi:10.1016/0031-9201(81)90046-7.

[7] "Acoustic Logging". epa.gov. 2011-12-12. Retrieved 2015-02-03.