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Earthquakes in Maine
Henry N. Berry IV
Maine Geological Survey
|Table 1. Estimated return times for earthquakes of different magnitudes in Maine.|
|Return time (years)||24||52||138||363||955||2512|
|(±20 to 30%)|
Ebel (1984) also made similar estimates based just on the seismic activity for Maine recorded in that same time span, and arrived at slightly shorter return times for magnitude 5.0 or smaller, and slightly longer return times for magnitude 6.5 or greater earthquakes.
Earthquakes have been reported from all counties in Maine, thereby indicating some level of statewide exposure. The occurrence is not equally distributed, however, and both modern and historical records indicate somewhat higher activity in the eastern, central, and southwestern parts of the State (Figure 1).
The amount of direct physical damage from an earthquake depends on a combination of factors, including the earthquake intensity, the density of structures in proximity to the epicenter, stability during an earthquake of geologic materials beneath structures, and the construction features of structures exposed to seismic vibration. In general, earthquakes with magnitudes less than 5.0 (corresponding approximately to Modified Mercalli intensity VI) cause little or very localized damage (Johnston, 1995). The largest reported Maine earthquakes have caused some damage to property near the epicenter, such as damaging chimneys and breaking glass (Ebel, 1989).
Most Maine buildings were not constructed to withstand the lateral motion of a significant (magnitude 6 or higher) earthquake. In general, unreinforced brick and masonry structures are especially prone to earthquake damage. Coastal and lakefront structures built on water-saturated, unconsolidated material such as artificial fill, may be vulnerable to liquefaction in a severe earthquake. Liquefaction is a loss of cohesion between particles due to lubrication by water during vibration, causing a sudden loss of strength. Most death and injury during earthquakes results from people being struck or trapped by falling debris (NESEC, 1993). Other possible concerns in a severe earthquake emergency would be the disruption of infrastructure facilities, such as road access, gas and oil pipelines, and electricity and water supplies, and the disruption of emergency services such as police, firefighting, ambulance, and hospital services (Ludman and Coch, 1982).
Instrumental monitoring of seismicity in Maine began in 1975, marking the beginning of the modern record. Earthquake events prior to 1975 are considered part of the historical record. The record of earthquake activity prior to the mid-1800's is sparse and of uneven quality (Ebel, 1989). The history of earthquake events, therefore, is well known only for the very recent part of the geologic past. The record of 507 historical and modern earthquake events including dates, epicenter locations, and sizes has been compiled by the Maine Geological Survey for the years 1747 to 1992 and is available in an open-file map format (Johnston, 1995). These data show that a higher incidence of modern earthquake activity has occurred in areas with a higher incidence of historical activity (Figure 1). The areas of relatively higher seismic activity include the Passamaquoddy Bay area of eastern Washington County; the Dover-Foxcroft - Milo area of southern Piscataquis County; and southwestern Maine in general, particularly the Portland-Lewiston region of Androscoggin and Cumberland Counties. The boundaries of these areas of higher activity are not clearly defined, and minor earthquake activity has been scattered across most areas of the State (Figure 2).
The largest earthquakes recorded in Maine are from the historical record. For most of them the magnitude was not measured, so an estimated intensity is assigned on the basis of the reported effects. Relative intensity is measured by the Modified Mercalli scale in which intensities I, II, and III are not felt by most people; intensity IV (noticeable) causes dishes to rattle; intensity V (moderate) is felt by most people and may cause plaster or windows to crack; intensity VI (rather strong) may move heavy furniture and cause some chimney damage; intensity VII (strong) causes considerable damage to poor structures and slight to moderate damage to ordinary structures; and intensity VIII (very strong) causes considerable damage and partial collapse of ordinary buildings. The scale continues through intensities IX to XII, but no earthquakes of this size have ever been reported for the New England region.
|Table 2. Maine earthquakes from the historical record (1800-1975) with intensity VI or greater (from Ebel, 1989). Intensities given are the maximum values for each event using the Modified Mercalli scale.|
|1904||Eastport area||VII||Largest earthquake in Maine (Reid, 1911)|
|1869||Passamaquoddy Bay?||VI||Location of epicenter uncertain, may have been in Bay of Fundy or in Eastport area.|
|1973||Bowmantown Twp.||VI||magnitude 4.8|
The most significant Maine earthquakes in the modern record have not caused much damage, but have been widely felt throughout the State. These are listed in Table 3.
|Table 3. Significant Maine earthquakes from the modern record (1975-1992). Data are from the New England Seismic Network operated jointly by Weston Observatory of Boston College and MIT. Magnitudes listed (Mc) are based on the duration of earthquake coda waves. Intensity is the maximum Modified Mercalli intensity (Ebel, 1989).|
|Date (local time)||Place||Magnitude||Intensity|
|April 17, 1979||Bath||4.0||V|
|Jan. 19, 1984||Machias||3.8||IV|
|Dec. 28, 1988||Albion||4.0||IV|
|Sept. 15, 1994||Springfield||3.9||IV|
|Feb. 25, 1999||Winslow-China||3.7|
There have been some larger earthquakes with epicenters elsewhere in New England and neighboring Canada that have been felt in Maine. The most notable of these was the earthquake of November 18, 1755 with an epicenter offshore from Cape Ann, Massachusetts. This earthquake is estimated to have had magnitude 6.0 and affected Cape Ann with intensity VII and southern Maine with intensity VI. The Cape Ann earthquake was notable because it affected a populated area. The St. Lawrence Valley northeast of Quebec City is perhaps the most active area in northeastern North America, but has a low population density. Other significant earthquakes in the surrounding region that have affected Maine are listed in Table 4.
|Table 4. Some significant earthquakes in the area surrounding Maine. Magnitudes have been estimated for earthquakes that were not measured. Intensities listed are the maximum intensities, in the epicentral region. Intensities generally decrease with distance from the epicenter.|
|1755||Cape Ann, Massachusetts||6.0?||VIII||toppled chimneys in Boston|
|1925||La Malbaie, Quebec||6.4-6.6?||IX||90 miles from Quebec City. Damaged some types of stone and brick walls over 100 miles away (Hodgson, 1950).|
|1940||Ossipee, N.H. (2 events)||5.5, 5.5||VII||some chimneys in Augusta cracked|
|1982||Miramichi, New Brunswick||5.7||VII||felt across Maine|
|1988||Chicoutimi, Quebec||6.0||VIII||felt in New York City. Largest in eastern North America since 1935.|
|1997||Quebec City||5.1||VII||felt across Maine|
The Maine Geological Survey (MGS) routinely maps, interprets, and publishes basic bedrock, surficial, and marine geologic information for Maine. The MGS provides advisory and interpretive information on earthquakes for planning and regulatory agencies. After an eathquake event, the MGS collects information from people in the area through an earthquake questionnaire made available to the general public and to county emergency management agencies.
The New England Seismic Network, operated by the Weston Observatory of Boston College, maintains a network of seismic stations across New England that monitors, analyzes, and reports earthquake activity in Maine.
Anderson, Walter A., Borns, Harold W., Jr., Kelley, Joseph T., and Thompson, Woodrow B., 1989, Neotectonic activity in coastal Maine, in Anderson, Walter A., and Borns, Harold W., Jr. (editors), Neotectonics of Maine: Studies in seismicity, crustal warping, and sea-level change: Maine Geological Survey, p. 1-10.
Ebel, John E., 1984, Statistical aspects of New England seismicity from 1975 to 1983 and implications for past and future earthquakes: Seismological Society of America, Bulletin, v. 74, p. 1311-1330.
Ebel, John E., 1985, A study of seismicity and tectonics of New England: Report NUREG/CR-4353, Weston Observatory, Weston, Mass.
Ebel, John E., 1989, The seismicity of Maine, in Anderson, Walter A., and Borns, Harold W., Jr. (editors), Neotectonics of Maine: Studies in seismicity, crustal warping, and sea-level change: Maine Geological Survey, p. 219-228.
Hodgson, E.A., 1950, The Saint Lawrence earthquake, March 1, 1925: Publication of the Dominion Observatory, Ottawa, Ont., v. 7, no. 10, p. 364-436.
Johnston, Robert A., 1995,Earthquakes in Maine: August 1747 to January 1992: Maine Geological Survey, Open-file Map 95-2, scale 1:500,000.
Ludman, Allan, and Coch, Nicholas K., 1982, Physical geology: McGraw-Hill, New York.
NESEC, 1993, New England's next earthquake: videotape (running time 19:52), New England States Earthquake Consortium, Portsmouth, N.H.
Osberg, Philip H., Tull, James F., Robinson, Peter, Hon, Rudolph, and Butler, J. Robert, 1989, The Acadian orogen, in Hatcher, Robert D., Jr., Thomas, William A., and Viele, George W. (editors), The Appalachian-Ouachita orogen in the United States: The geology of North America, vol. F-2, Geological Society of America, p. 179-232.
Reid, H.F., 1911, The earthquake of southeastern Maine, March 21, 1904: Seismological Society of America, Bulletin, v. 1, p. 44-47.
Magnitude and Intensity
Last updated on July 20, 2006
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