Strongest earthquakes in recorded history, ranked by magnitude

A magnitude 9.0 earthquake releases roughly 32 times more energy than a magnitude 8.0, and about 1,000 times more than a 7.0. That logarithmic math is why the small group of ruptures above magnitude 8.5 sits in a category of its own. The thousands of other damaging earthquakes logged since seismic networks began keeping score do not come close. The gap between an 8.5 and a 9.5 is not a matter of degree. It is a difference in the physical size of the fault that broke, the length of time the ground moved and the volume of seawater displaced.

The strongest earthquakes in recorded history were not always the deadliest. Death tolls depend on population density, construction standards, the time of day and whether the rupture pushed up a tsunami. A magnitude 8.7 in an uninhabited stretch of the North Pacific can pass with no confirmed fatalities. A far weaker quake beneath a crowded city can kill tens of thousands. Raw energy release and human loss are two separate measurements, and they rarely line up.

This list covers the instrumental era, generally from 1900 onward, because that is when seismic networks became capable of assigning reliable numbers. Earthquakes described in older historical records may have matched or exceeded these, but without seismographs there is no way to measure them. The magnitudes here come from the moment magnitude scale, which replaced the Richter scale for large events. It calculates energy release from the physical dimensions of the fault rupture and the amount of slip, rather than from shaking recorded at a single station.

One pattern runs through nearly every entry. These ruptures occurred along subduction zones, where one tectonic plate grinds beneath another. The boundary locks in place for decades or centuries, then releases the stored strain in a few minutes. Chile, Alaska, Sumatra, Japan and Kamchatka appear repeatedly for that reason. Knowing which boundaries have produced earthquakes this size is the clearest guide to where comparable events remain possible.

Illustration: Quartz

The magnitude 9.5 earthquake that struck near Valdivia in southern Chile on May 22, 1960, is the most powerful earthquake ever measured by seismic instruments. No recorded event since has matched its energy release.

The rupture tore along the Peru-Chile Trench for a stretch estimated at more than 500 miles, as the Nazca Plate slipped beneath the South American Plate. A fault break of that length is what separates the event from everything below it on the scale. Magnitude depends on rupture area and the amount of slip, and few plate boundaries on Earth hold enough continuous locked fault to produce a break this long.

The rupture pushed a tsunami across the entire Pacific basin. Waves struck the Chilean coast within minutes, then crossed deep water at roughly 500 miles per hour toward Hawaii, Japan and the Philippines. The first destructive waves reached Hilo, Hawaii, about 15 hours later, more than 6,000 miles from the source, and wrecked much of the downtown waterfront. Hilo rebuilt with open parkland along the bayfront instead of commercial blocks.

Casualty figures for the combined earthquake and tsunami vary by source, ranging from about 1,000 to as high as 6,000. The spread reflects how hard it was to count the dead in 1960. Communications were cut across a sparsely settled, heavily damaged stretch of south-central Chile, and some coastal villages were erased outright. Economic losses were severe, with housing, farmland, ports and rail links destroyed across several provinces.

Valdivia remains the benchmark against which every other large earthquake is measured, and it also sets a practical ceiling in seismic hazard modeling. Anything substantially larger would require a locked fault segment longer than any subduction zone known to store strain. That constraint is why 9.5 is often treated as close to the physical limit of crustal rupture.

Illustration: Quartz

The magnitude 9.2 earthquake that ruptured beneath Prince William Sound on March 27, 1964, is the second-strongest quake ever recorded and the largest measured in North America. It broke along the Aleutian megathrust, where the Pacific Plate is forced beneath the North American Plate. Many accounts call it the Good Friday earthquake, after the day it struck.

Ground motion continued for four to five minutes across parts of south-central Alaska. That is an extreme duration — most large quakes shake for well under a minute. The sustained motion liquefied unstable ground in Anchorage, roughly 75 miles from the epicenter. Landslides carried away whole blocks of housing in the Turnagain Heights neighborhood and collapsed part of the downtown commercial district.

Tsunamis caused most of the deaths. Waves generated by submarine landslides reached Alaskan fishing communities within minutes of the shaking. The ocean-crossing wave arrived at Crescent City on the northern California coast hours later and killed people there. The combined toll is generally put at about 131 — low for a rupture this size, and a consequence of how thinly populated the affected coastline was in 1964.

The earthquake rearranged the land itself. Surveys afterward found stretches of coast and seafloor lifted by more than 30 feet. Other areas dropped far enough to flood shoreline forests, leaving stands of dead trees in salt water. Geologist George Plafker mapped that pattern of uplift and subsidence. His work showed the rupture had occurred on a shallow-dipping thrust fault. That evidence helped confirm how subduction zones generate the largest earthquakes, at a time when plate tectonics was still being worked out.

The event reshaped warning systems and engineering practice. The U.S. opened a tsunami warning center at Palmer, Alaska, in 1967, after the 1964 waves hit nearby coastlines with no alert. Studies of how Anchorage's slopes and structures behaved during prolonged shaking informed later seismic design standards for soil stability and building performance.

Illustration: Quartz

A magnitude 9.1 earthquake ruptured the seafloor off the northwest coast of Sumatra on December 26, 2004, breaking more than 900 miles of fault and generating the deadliest tsunami in recorded history.

The fault that failed marks the boundary where the Indian Plate descends beneath the Burma microplate, part of the Sunda subduction system. The seafloor lifted along that entire length. The movement displaced an enormous column of water, which spread outward across the Indian Ocean in every direction.

Waves struck Indonesia's Aceh province within roughly 20 to 30 minutes, destroying whole coastal districts of Banda Aceh. Sri Lanka, southern India and the Thai resort coast were hit within one to two hours. Hours after that, the waves still carried enough force to kill people on the coasts of Somalia and Tanzania, thousands of miles from the epicenter.

The death toll is generally placed at about 230,000 people across 14 countries, with Indonesia accounting for the largest share by far. That figure remains an estimate rather than a count. Many victims were never recovered, and some affected communities had no complete population records to measure the loss against.

Wave height alone does not explain the scale of the disaster. The Indian Ocean had no tsunami warning network comparable to the system already running in the Pacific. Seismologists registered the earthquake quickly, but no mechanism existed to turn that detection into warnings for the coastal populations in the path of the water. Most people standing on the beaches did not know what the sudden retreat of the sea meant.

The Indian Ocean Tsunami Warning System was built in the aftermath, connecting seismic sensors, deep-ocean pressure gauges and national alert channels across the region.

The rupture also shifted enough of Earth's mass to shorten the length of a day by a fraction of a microsecond, according to analyses by geophysicists who modeled the event's seismic data.

Illustration: Quartz

Japan's magnitude 9.1 Tohoku earthquake struck off the Pacific coast of the country's northeast on March 11, 2011. It is the strongest earthquake ever recorded in Japan and ties for fourth-strongest worldwide. The rupture broke a megathrust offshore of the Tohoku region, where the Pacific Plate descends beneath the Okhotsk Plate.

The tsunami, not the ground motion, caused most of the deaths. Waves exceeded 130 feet at points along the Sanriku coast, where narrow inlets squeezed and amplified the surge. Seawalls built for smaller historical events were overtopped within minutes in towns including Kamaishi and Minamisanriku. The combined toll of dead and missing is generally placed between roughly 18,000 and 20,000, and the great majority of those losses came from the water rather than the shaking.

The waves also pushed the Fukushima Daiichi Nuclear Power Plant into crisis. Reactors shut down automatically when the shaking began, but flooding disabled the backup diesel generators that powered the cooling systems. Three reactor cores melted over the following days, releasing radioactive material and forcing more than 150,000 residents out of surrounding communities. It remains the most serious nuclear accident since Chernobyl in 1986. Decommissioning at the site is expected to take decades.

Japan rewrote much of its coastal defense and evacuation planning afterward. Seawall height requirements rose in many prefectures. Evacuation signage and designated vertical shelter buildings were expanded along the coast. Warning systems were adjusted to issue more conservative initial wave estimates rather than risk understating a threat.

The earthquake also changed seismic thinking in Japan and beyond. Hazard assessments had not anticipated a rupture of this size along the Japan Trench off Tohoku. That segment had been treated as one that released strain in smaller, more frequent quakes. The event forced a reassessment of how much strain a subduction zone can store and how much of a fault can give way at once.

Illustration: Quartz

A magnitude 9.0 earthquake ruptured the seafloor off the Kamchatka Peninsula in the Russian Far East on November 4, 1952, making it one of the five largest quakes in the instrumental record. The break ran along the Kuril-Kamchatka subduction zone, where the Pacific Plate descends beneath the Okhotsk Plate.

The rupture displaced enough water to send a tsunami across the whole Pacific basin. Waves reached the Hawaiian Islands about five hours later and wrecked property at Hilo on the Big Island, thousands of miles from the source. Japan, the Aleutian Islands and the west coast of North America also registered the waves, with less damage than Hawaii absorbed.

Closer to the epicenter, the Kamchatka coast and the northern Kuril Islands bore the worst of it. Severo-Kurilsk, a fishing town on Paramushir Island, was hit by waves that leveled much of the settlement. Soviet authorities did not publicize the losses, and the disaster went largely unreported outside the country for decades.

That silence is why the casualty and damage record for 1952 is thinner than for comparable earthquakes elsewhere. Kamchatka was a restricted military zone in the early Cold War, sparsely populated and closed to foreign observers. Figures cited today draw on Russian archival material released much later, and they differ between accounts.

The Hilo damage carried consequences well beyond Hawaii. The Pacific Tsunami Warning Center had been set up in 1949 after an earlier disaster, and the 1952 waves showed in practice what a distant rupture could do to coastlines half an ocean away. The event supported the case for expanding tide gauge and seismic monitoring across the basin.

Kamchatka keeps producing large earthquakes along the same plate boundary. A magnitude 8.8 rupture there in July 2025 triggered tsunami warnings around the Pacific. The 1952 earthquake remains the measure of what that stretch of the subduction zone can produce.

Illustration: Quartz

A magnitude 8.8 earthquake struck off Chile's Maule region at 3:34 a.m. local time on February 27, 2010. It ranks among the most powerful quakes measured anywhere in the past century.

The rupture broke a stretch of the Peru-Chile Trench that had been storing strain for well over a century. It is the same plate boundary that produced the magnitude 9.5 Valdivia earthquake in 1960, but a different segment of it.

Shaking spread across a wide section of the country and reached Santiago, roughly 200 miles from the epicenter. It lasted long enough to damage buildings, bridges and highways in several regions. Concepción, the large city nearest the rupture zone, absorbed some of the heaviest structural damage.

A tsunami arrived within minutes along the Chilean coast, hitting fishing towns and the Juan Fernández archipelago. Wave energy crossed the Pacific and registered in Hawaii and Japan, with far less force at that distance. The combined earthquake and tsunami death toll is generally put at about 525 people.

That figure is low relative to the energy released, and Chile's construction standards are a major reason. Codes were tightened substantially after the 1960 disaster. Most modern mid-rise and high-rise buildings in Santiago swayed through the shaking without collapsing. The structures that failed tended to be older masonry or adobe.

The tsunami warning system performed far less reliably. Chilean authorities underestimated the wave threat in the first minutes after the rupture, and alerts to parts of the coast were delayed and at one point withdrawn. Some coastal residents who had moved to high ground on their own were told they could go back.

Chile rebuilt its emergency management and tsunami alert procedures in the years that followed. The changes included clearer lines of authority between the navy's hydrographic and oceanographic service and the national civil protection agency. The earthquake also lifted parts of the Chilean coastline by several feet.

Illustration: Quartz

A magnitude 8.8 rupture broke the seafloor off the Ecuador-Colombia border on January 31, 1906, ranking it among the most powerful earthquakes on record. It tore along the boundary where the Nazca Plate slides beneath the South American Plate, the convergent margin that shapes the Pacific coast of both countries.

The rupture lifted the ocean floor and pushed a tsunami into the shoreline between Esmeraldas in Ecuador and Tumaco in Colombia. Low-lying coastal settlements there absorbed the worst of the damage. The waves were large enough to register far beyond the region, with arrivals reported along the coast of Japan and at San Francisco.

Death toll figures vary considerably, and the commonly cited range runs from about 500 to 1,500. Most of the reported deaths came from the tsunami rather than from collapsing buildings. That spread in the casualty estimates reflects how little systematic record-keeping existed along that stretch of coast in 1906.

The magnitude carries more uncertainty than the figures attached to later events. Seismographs of the period were sparse and inconsistent in design. They were not calibrated to capture the full motion of a rupture this large. The 8.8 estimate comes from later reanalysis — historical accounts of shaking and damage, recorded tsunami arrival times and wave heights, and geological evidence of how the coast moved. Seismologists treat the number as a sound working estimate rather than a precise instrumental reading.

What the event established about the fault still shapes hazard planning. The 1906 rupture showed that the Ecuador-Colombia segment of the subduction zone can fail across a long stretch at once, rather than only in smaller sections. Later quakes along the same margin confirmed that the boundary stays active. The magnitude 7.8 earthquake near Pedernales, Ecuador, in April 2016 killed more than 600 people and caused heavy damage in coastal provinces. Cities built along that shoreline since 1906 sit above a fault with a demonstrated record of very large ruptures.

Illustration: Quartz

On February 4, 1965, a magnitude 8.7 earthquake tore through the Aleutian subduction zone beneath the Rat Islands in western Alaska. No deaths were confirmed and structural damage stayed minor, making it one of the largest 20th-century quakes to pass with almost no human cost.

The rupture ran along the boundary where the Pacific Plate slides beneath the North American Plate. The Rat Islands sit far west along the arc, closer to Russia's Kamchatka Peninsula than to Anchorage. The group includes Amchitka and Kiska, neither of which had a permanent civilian population; military and research posts were the only occupied sites.

Isolation accounts for the low toll. The shaking spread across a broad stretch of ocean floor, but no cities, ports or dense coastal villages sat within reach of the heaviest ground motion. Reported damage was largely limited to cracked runways, ruptured fuel tanks and split building walls at nearby installations.

The quake sent a tsunami across the Pacific that registered on tide gauges in Hawaii and Japan. Wave heights at those distant shorelines stayed small next to the tsunamis thrown off by megathrust ruptures of comparable size. Run-up was higher along the Rat Islands themselves, consistent with a shallow offshore break that lifts a long panel of seafloor.

The date carried scientific weight. Standardized seismograph stations installed around the world in the early 1960s recorded the event in far greater detail than any earlier earthquake of that size. Plate tectonics was then still an idea under debate, and clean recordings from long oceanic arcs fed directly into that argument.

Seismology texts still cite the 1965 rupture to show that magnitude alone predicts little about casualties. An identical break under a populated coast would rank among the worst disasters ever documented. The Aleutian arc can still produce earthquakes of this size, which is why tsunami warning centers serving Hawaii and the U.S. West Coast monitor it continuously.

Illustration: Quartz

A magnitude 8.6 earthquake struck the border region between Assam, India, and Tibet on August 15, 1950. It ranks among the largest earthquakes ever recorded on land rather than beneath the ocean.

The rupture broke along the collision zone where the Indian Plate pushes into the Eurasian Plate — the same boundary that raised the Himalayas. That setting makes the event unusual among the planet's biggest measured quakes. Ruptures of this size usually occur offshore at subduction zones, where one plate slides under another at a shallow angle and can break across hundreds of miles of seafloor. Continental collision zones tend to produce shorter, more fragmented breaks, which is why a magnitude 8.6 on land stands apart in the seismic record.

The shaking tore loose large volumes of rock across steep Himalayan terrain. Landslides blocked river channels and created temporary natural dams. Those dams later failed and sent surges of water down valleys in Assam and southeastern Tibet. Much of the destruction arrived days and weeks after the ground stopped moving.

Death toll estimates range from roughly 1,500 to more than 4,000. A large share of those deaths came from landslides and the flooding that followed, not from collapsing buildings. The spread in the figures reflects how hard the region was to reach in 1950. Few roads existed, and word from affected villages took weeks to arrive. Full damage assessments remained incomplete for years.

The earthquake still shapes how seismologists read risk across the Himalayan arc. The Indian Plate continues to advance into Eurasia at roughly two inches per year, loading strain into faults that run the length of Nepal, northern India, Bhutan and Tibet. Several segments of that boundary have not produced a major rupture in centuries. The populations living along that boundary are far larger and more densely housed than in 1950, which would raise the human cost of a comparable rupture today.