# P-wave

This article is on the type of seismic wave. For the term used in electrocardiography, see P wave (electrocardiography). P-wave can also refer to a type of electronic wavefunction in atomic physics; see atomic orbital.
Plane P-wave
Representation of the propagation of a P-wave on a 2D grid (empirical shape)

P-waves are a type of elastic wave, and are one of the two main types of elastic body waves, called seismic waves in seismology, that travel through a continuum and are the first waves from an earthquake to arrive at a seismograph. The continuum is made up of gases (as sound waves), liquids, or solids, including the Earth. P-waves can be produced by earthquakes and recorded by seismographs. 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 the highest velocity and is therefore the first wave to be recorded.[1]

In isotropic and homogeneous solids, the mode of propagation of a P-wave is always longitudinal; thus, the particles in the solid vibrate along the axis of propagation (the direction of motion) of the wave energy.

## Velocity

The velocity of P-waves in a homogeneous isotropic medium is given by

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

Of these, density shows the least variation, so the velocity is mostly controlled by K and μ.

The elastic moduli P-wave modulus, , is defined so that and thereby

Typical values for P-wave velocity in earthquakes are in the range 5 to 8 km/s.[2] 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 km/s through the core.[3]

Velocity of Common Rock Types[4]
Rocktype 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:

which later became known as Birch's law.

## Seismic waves in the Earth

Velocity of seismic waves in the Earth versus depth.[5] 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.[6][7]

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°[8] from the earthquake's focus, where the initial P-waves are not registered on seismometers. In contrast, S-waves do not travel through liquids, rather, they are attenuated.

### As an earthquake warning

Earthquake advance warning is possible by detecting the non-destructive primary waves that travel more quickly through the Earth's crust than do the destructive secondary and Rayleigh waves, in the same way that lightning flashes reach our eyes before we hear the thunder during a storm. 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 60–90 seconds for deep, distant, large quakes such as Tokyo would have received before 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) as otherwise false-positive warnings will result. Earthquake Early Warning systems can be automated to allow for immediate safety actions such as issuing alerts, stopping elevators at the nearest floors or switching gas utilities off.

## References

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.
2. "Speed of Sound through the Earth". Hypertextbook.com. Retrieved 2011-12-14.
3. "Seismographs - Keeping Track of Earthquakes". Earthquake.usgs.gov. 2009-10-27. Retrieved 2011-12-14.
4. "Acoustic Logging". epa.gov. 2011-12-12. Retrieved 2015-02-03.
5. GR Helffrich & BJ Wood (2002). "The Earth's Mantle" (PDF). Nature. Macmillan Magazines. 412 (2 August): 501; Figure 1. doi:10.1038/35087500.
6. Justin L Rubinstein, DR Shelly & WL Ellsworth (2009). "Non-volcanic tremor: A window into the roots of fault zones". In S. Cloetingh, Jorg Negendank. New Frontiers in Integrated Solid Earth Sciences. Springer. p. 287 ff. ISBN 90-481-2736-X. The analysis of seismic waves provides a direct high-resolution means for studying the internal structure of the Earth...
7. 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 0-521-58409-4. 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.
8. Lowrie, William. The Fundamentals of Geophysics. Cambridge University Press, 1997, p. 149.