September/October 2011

What is That Mysterious Booming Sound?


The residents of coastal North Carolina are occasionally treated to sequences of booming sounds of unknown origin. The sounds are often energetic enough to rattle windows and doors. A recent sequence occurred in early January 2011 during clear weather with no evidence of local thunder storms. Queries by a local reporter (Colin Hackman of the NBC affiliate WETC in Wilmington, North Carolina, personal communication 2011) seemed to eliminate common anthropogenic sources such as sonic booms or quarry blasts. So the commonly asked question, “What’s making these booming sounds?” remained (and remains) unanswered.

This phenomenon is hardly unique to North Carolina or to the modern Industrial Age. Residents in the vicinity of Lake Seneca in the Catskill Mountains of New York have long known similar booming sounds as “Seneca guns” (a term also common throughout the coastal region of the Carolinas). This name has been variously attributed to the section in Washington Irving’s short story “Rip Van Winkle” (1819) that describes the ghosts of Henry Hudson’s crew playing nine pins in the Catskill Mountains, or to the short story “The Lake Gun” by James Fenimore Cooper (1851). Elsewhere, such sounds are known by a variety of names including “mistpouffers” (fog belches) in coastal Belgium, “Bansal guns” in the Ganges delta and the Bay of Bengal, “brontidi” (thunder-like) in the Italian Apennines (Gold and Sorter 1979), and “yan” by the people of Harami in Shikoku, Japan.

Proposed explanations for natural booming sounds lacking an obvious proximal source are varied and imaginative. The more plausible include mud volcanoes and/or explosive venting of gas; tsunamis or large, storm-driven waves; meteors; booming sands; rock bursts; local earthquakes; and distant thunder. The latter are the best documented and best understood natural sources of booming sounds. Linking the sound to the source can be challenging for a variety of reasons. Under appropriate wind conditions and atmospheric thermal (density) profiles, for example, the low-frequency component of a boom can propagate as a guided wave for distances significantly beyond the visible range of the source.



Anecdotal reports of sounds associated with local earthquakes have a long history. Mallet (1862) relates descriptions of sounds accompanying the great (M ~ 6.9) Neapolitan earthquake of 1857 as “sudden explosive reports variously contemporaneous with rushing and rolling sounds.” Davison (1938) compiled descriptions of earwitness sounds accompanying small to moderate earthquakes in England from 1880 through 1916. Descriptions of the sounds in his catalog include the boom of a distant cannon or distant blasting, loads of falling stones, the blow of a sea wave on shore, the roll of a muffled distant drum, an immense covey of partridges on the wing, and more. A section of the Lawson report on the great San Francisco earthquake of 1906 entitled “Sounds Connected with the Earthquake” (Lawson 1908) includes earwitness descriptions of sounds accompanying the mainshock as ranging from “a rumbling, roaring sound,” “a heavy wind,” “a rushing noise,” and “an approaching train” to “a team crossing a bridge.” A significant number of earwitness descriptions of earthquake sounds cite the sound as preceding the felt shaking from earthquake by several seconds. Indeed, on page 288 of Elementary Seismology, Richter (1958) recounts the experience of seismologist Pierre St. Amand in the recording vault at the University of Alaska, Fairbanks, during a series of earthquakes in 1947 when he noted that audible sounds coincided with the first (P-wave) arrivals while felt shaking began with the S-wave arrivals.

Reports of low, rumbling sounds accompanying earthquakes heard and felt by U.S. Geological Survey (USGS) personnel installing seismic stations during the September 1975 Brawley swarm in the Imperial Valley, California, provided the opportunity to record both acoustic and seismic signals on the same time base (Hill et al. 1976). The results for three earthquakes with magnitudes ranging from M 2.0 to M 2.8 demonstrated that a 40–70-Hz acoustic signal began within 0.02 sec of the P-wave arrival at the station and gradually died out by the time the S-wave arrived some two seconds later—a result consistent with St. Amand’s observation in 1947. Calculation of the seismic-acoustic transmission coefficients confirmed that the seismic body waves from these earthquakes were capable of generating acoustic wave amplitudes within the threshold of human hearing in the 40–70-Hz frequency band. Sylvander et al. (2007) carried out a similar experiment and analysis for a series of small earthquakes (ML < 2.8) in the French Pyrenees in 2004 with similar results.

Whether small (M < 2.5), shallow earthquakes produce audible sounds and felt shaking depends on local site conditions including ambient noise levels. The experiments described above were carried out in the open air and away from cultural noise sources. Under such circumstances, it seems that the free surface acts as a giant woofer in response to the incident P-wave but remains below the threshold of felt shaking, while the slower S-wave produces perceptible shaking, at least for earthquakes in the M 2 .0 to 2 .8 range. Based on personal experience, it seems that even smaller earthquakes are capable of producing audible sounds with no perceptible shaking. While on the flank of Mammoth Mountain with Bill Ellsworth one day during the 1989 Mammoth Mountain earthquake swarm, we both heard muffled booming sounds but felt no shaking. On checking, we found that the earthquakes during that period were shallow (< 4 km deep) with magnitudes M < 2.0. This may explain reports by people living on the flanks of restless volcanoes of ominous booming sounds that both feed local legends and serve as an early warning of a possible impending eruption.

Rock bursts can be viewed as a class of small, near-surface earthquakes. They are capable of producing locally loud, explosive reports. Most rock bursts are associated with mining and quarry operations as the confining pressure of overburden is removed leading to the spontaneous, explosive release of stress stored in long-buried rock. Spontaneous rock bursts occasionally occur at depths of a few hundred meters in sheeted granitic or metamorphic terrains exposed by the retreating Pleistocene ice sheets (Monroe and Wicander 1992). Bill Ellsworth and Bernard Chouet describe feeling a perceptible jolt and hearing sharp, booming sounds from rock bursts associated with the development of columnar jointing in the 30-m-thick cooling crust of Kilauea Iki lava lake on Kilauea Volcano, Hawaii (Chouet 1979).



While conducting on-site interviews during their investigation of the 2004 M 9.1 Sumatra earthquake and tsunami, George Plafker, Lloyd Cluff, and Stuart Nishenko documented multiple accounts by widespread witnesses of loud, offshore booming sounds accompanying the main phase of the tsunami (Plafker, personal communication 2011). The number of reported booming sounds coincided closely with the two or three largest waves that impacted the coast at any given site. In follow-up interviews, Plafker learned that booming sounds are a familiar phenomenon among big-wave surfers during extreme waves, and that such sounds are also familiar to residents in the vicinity of Maverick’s in northern California, a world-famous site for big-wave surfing. Similar reports accompanied the 1896 and 1933 Sanriku M~8 earthquakes and tsunamis in Japan, both of which occurred at night (Shuto 1997). In a carefully researched novel, Wall of the Ocean, author Akira Yoshimura describes booming sounds accompanying the 1896 Sanriku tsunami:

About the same time [as the earthquake] the villagers were still celebrating without paying too much attention to the sudden change in the sea condition, but all of a sudden they heard big booms from off shore. Some thought that they were rumblings of thunder, but others thought that they were the booms of cannons firing. Some apparently thought that Russian battleships started firing. An individual who heard the booms at about 8:20 p.m. watched off shore, and saw lanternlike fire balls moving gradually from off shore toward the beach. It was described that the booming sounds and fire balls were produced by huge walls of water. (Translation from the Japanese by Hiroo Kanamori, personal communication 2011).

Yoshimura relates similar accounts of booms and lights witnessed during the 1933 earthquake and tsunami. This raises the possibility that the source of booming sounds heard in some coastal regions (e.g., the Seneca guns of the coastal Carolinas, the mistpouffers of coastal Belgium, or the Bansal guns around the Bay of Bengal) might be large waves generated by distant storms breaking well off shore (beyond barrier beaches or outer banks). The mechanisms and conditions under which big storm (or tsunami) waves generate booming sounds, however, remains unclear. One possibility is that the “fire balls” and booming sounds attending the 1896 Sanriku tsunami may be somehow related. Enomoto (1999) notes that of 17 large tsunamis documented in Japan from 684 to 1946, nine included descriptions of luminous phenomena. He suggests that, rather than bioluminescence excited by wave turbulence, this “tsunami lightning” may be associated with methane released from disrupted volumes of methane hydrate residing in offshore accretionary prisms. In any case, factors contributing to wave-generated booming sounds likely include the depth and local morphology of the sea floor, average inclination and stability of adjacent continental slopes, and, most importantly, the amplitudes and wave-lengths of the incoming waves.

Under proper circumstances, sand dunes are capable of producing a variety of lowlevel whispering, whistling, singing, humming, or squeaking sounds, and less commonly, loud booming sounds.


An implication of Enomoto’s (1999) paper is that both “tsunami lightning” and booming sounds may result from explosive ignition of methane gas released from methane hydrate beds disrupted by either the tsunamigenic earthquake or the tsunami itself rather than directly from turbulent wave action. A potential difficulty with this explanation is that bubble ascent rates are at least an order of magnitude smaller than gravity wave propagation speeds, implying a significant spatial-temporal separation between methane bubbles breaching the surface and tsunami waves breaking on shore. (Methane hydrate is stable at depths greater than 300 M and most deposits reside at depths of 500 M to several thousand meters.) Submarine landslides on continental margins are also capable of disrupting gas hydrate beds, thereby releasing methane with the potential for explosive ignition at the ocean surface. Astrophysicist Tomas Gold, along with his colleague Stephen Sorter, proposed a more general explanation for natural explosive sounds (which they label “brontides” after the Italian “brontidi”) involving the explosive release of high-pressure methane from deep within the Earth (Gold and Sorter 1979). This proposal stems from Gold’s theory of an abiogenic source of petroleum involving the inclusion of abundant hydrocarbons in the core and mantle during the early accretionary phase of the Earth’s formation. Merits of the abiogenic petroleum theory aside, onshore methane gas bursts in developed areas seem an unlikely explanation for booming sounds in the absence of eyewitness accounts or tell-tale signs such as craters, mud volcanoes, or maars. Active volcanoes commonly produce booming sounds associated with the explosive venting of volcanic gasses and eruptions (e.g., Johnson and Lees 2000). Of course active volcanoes are generally highly visible, noisy neighbors, so the source of any associated booming sounds is likely to be quite evident to the local population.


Under proper circumstances, sand dunes are capable of producing a variety of low-level whispering, whistling, singing, humming, or squeaking sounds, and less commonly, loud booming sounds (Sholtz et al. 1997; Lindsay et al. 1996). The so-called “booming sands” appear to be limited to large sand dunes with steep leeward faces in arid climates. The booming sounds produced by such dunes can grow to levels comparable to rumbling thunder and, under the right conditions, can be heard to distances of 10 km with durations as long as 15 minutes, and they can couple into seismic waves that produce locally perceptible shaking (Sholtz et al. 1997). To produce booming sounds evidently requires very low humidity and loosely packed, quasispherical sand grains with high surface smoothness, although details of the process by which the acoustic emissions are produced remain poorly understood. In their global survey, Lindsay et al. (1996) do not identify the Carolina coast as an area known for booming sands.


Meteoroids penetrating the upper atmosphere become meteors, which can produce sonic booms of varying intensity. Because of the time required for a sonic shock wave to reach the Earth’s surface from the upper atmosphere, the visible trace of the meteor has usually vanished before its sonic boom is heard. Thus, particularly during daylight hours, the source of the boom may go unnoticed. Of course in the less common case of a meteoroid that penetrates the atmosphere and strikes the Earth (a meteorite), the link between the shock wave and “fireball” can be rather obvious if not dramatic.


Determining the source of booming sounds becomes an exercise in the process of elimination beginning with a thorough search for common anthropogenic sources such as sonic booms, military exercises (of course the military can be reticent about some of its boom-producing exercises), construction or quarry blasting, etc. Data from a local seismic network coupled with an array of acoustic infrasound sensors would quickly reveal whether the sounds were generated by local earthquakes (or in volcanic regions, explosive venting of a neighboring volcano). An acoustic array would provide information on the direction and spectral character of atmosphere-borne sounds from remote sources. Local geologic settings will of course narrow the possibilities. North Carolina has no volcanoes, but it does have a significant volume of methane-hydrates in the deep sediments of the Carolina trough and substantial sand dunes in the outer banks. Earthquakes are rare in coastal North Carolina but relatively common in the Charleston area of South Carolina, the site of the 1886 M 7.6 Charleston earthquake. The Seneca Lake region in upper New York State is not large enough to support booming storm waves (or tsunamis) but the Catskills do support low-level earthquake activity. In the absence of evidence for earthquake-generated sounds, the challenge becomes correlating the occurrence of booming sounds with plausible sources such as regional thunder storms; large waves breaking well off shore driven by major, mid-ocean storms; explosive offshore methane bursts; meteors; or perhaps strong winds stimulating local sand dunes into a booming mode.   


I’m grateful to George Plafker, Hiroo Kanamori, and Bill Ellsworth for background information as well as suggestions on an early draft.


Chouet, B. (1979). Sources of seismic events in the cooling lava lake of Kilauea Iki, Hawaii. Journal of Geophysical Research 84, 2,315– 2,330.

Davidson, C. (1938), Earthquake sounds, Bulletin of the Seismological Society of America, 28, 147−161.

Enomoto, Y. (1999). Historical seismology for the next generation: On earthquake tsunami lightning in historical Japanese documents. Journal of Geography 108 (4), 433–439 (in Japanese with English abstract).

Gold, T., and S. Sorter (1979). Brontides: Natural explosive noises. Science 204, 371–375.

Hill, D. P., F. G. Fischer, K. M. Lahr, and J. M. Coakley (1976). Earthquake sounds generated by body-wave ground motion. Bulletin of the Seismological Society of America 66 (4), 1,159–1,172.

Johnson, J. B., and J. M. Lees (2000). Plugs and chugs—seismic and acoustic observations of degassing explosions at Karymsky, Russia, and Sangay, Ecuador. Journal of Volcanology and Geothermal Research 101, 67–82.

Lawson, A. C. (1908). The California Earthquake of April 18, 1906: Report of the State Earthquake Investigation Commission VI. Part 2. Washington, DC: Carnegie Institution of Washington.

Lindsay, J. F., D. R. Criswell, T. L. Criswell, and B. S. Criswell (1976). Sound-producing dune and beach sands. Geological Society of America Bulletin 87, 463–473.

Mallet, R. (1887). Great Neapolitan Earthquake of 1875: The First Principles of Observational Seismology. London: Royal Society of London, vol. 2, 87–294.

Monroe, J. S., and R. Wicander (1992). Physical Geology: Exploring the Earth. St. Paul, MN: West Publishing, 639 pp.

Richter, C. F. (1958). Elementary Seismology. San Francisco: W. H. Freeman, 768 pp.

Sholtz, P., M. Bretz, and F. Nori (1997). Sound-producing sand avalanches. Contemporary Physics 38 (5), 329–342.

Shuto, N. (1997). A natural warning of tsunami arrival, in Perspectives on Tsunami Hazard Reduction, ed. G. Hebenstreit, 157–173. Dordrecht: Kluwer Academic Publishers.

Sylvander, M., C. Ponsolles, S. Benahmed, and J.-F. Fels (2007). Seismoacoustic recordings of small earthquakes in the Pyrenees: Experimental results. Bulletin of the Seismological Society of America 97 (1B), 294–304.

David P. Hill Scientist Emeritus U.S. Geological Survey hill [at] usgs [dot] gov

<srled [at] seismosoc [dot] org>.


Posted: 18 August 2011