सुनामी जोखिम अनुमानक

Estimate tsunami risk based on earthquake parameters and your coastal proximity.

Assessment

भूकंप सुनामी कैसे उत्पन्न करते हैं

सुनामी समुद्री लहरें हैं जो पानी के अचानक बड़े पैमाने पर विस्थापन से उत्पन्न होती हैं, जो सबसे अधिक सबडक्शन जोन के साथ पनडुब्बी भूकंपों के कारण होती हैं। जब एक बड़े भूकंप के दौरान महासागरीय भूपर्पटी का एक भाग ऊपर उठता है या नीचे गिरता है, तो यह पानी की एक विशाल मात्रा को विस्थापित करता है जो दीर्घ-अवधि लहरों की एक श्रृंखला के रूप में बाहर की ओर फैलती है। गहरे समुद्र में, सुनामी लहरें 500–800 किमी/घंटा (जेट विमान के समान) की गति से केवल 30–60 सेमी की लहर ऊँचाई के साथ यात्रा करती हैं, जिससे वे लगभग ज्ञात नहीं हो पातीं। जैसे-जैसे लहरें उथले तटीय जल के पास पहुँचती हैं, वे धीमी हो जाती हैं और संकुचित होती हैं, जिससे लहर की ऊँचाई नाटकीय रूप से बढ़ जाती है — इस प्रक्रिया को शोलिंग कहते हैं — जो तट पर 10–30 मीटर या उससे अधिक तक पहुँच सकती है।

सभी भूकंप सुनामी उत्पन्न नहीं करते। प्रमुख कारक हैं: भूकंप पनडुब्बी (समुद्र के नीचे) होना चाहिए, उथला (आमतौर पर 70 किमी गहराई से कम), बड़ा (स्थानीय सुनामी के लिए सामान्यतः M7.0 या अधिक, क्षेत्रीय के लिए M7.5+), और समुद्र तल का महत्वपूर्ण ऊर्ध्वाधर विस्थापन शामिल होना चाहिए। स्ट्राइक-स्लिप भूकंप, जिनमें मुख्य रूप से क्षैतिज भ्रंश गति शामिल होती है, शायद ही कभी महत्वपूर्ण सुनामी उत्पन्न करते हैं। सबसे खतरनाक सुनामी स्रोत तंत्र सबडक्शन जोन मेगाथ्रस्ट पर थ्रस्ट फॉल्टिंग है, जैसा कि 2004 हिंद महासागर (M9.1), 2011 तोहोकू (M9.1), और 1960 चिली (M9.5) घटनाओं में देखा गया।

सुनामी विज्ञान में प्रमुख अवधारणाएँ

सुनामी चेतावनी का समय दूरी पर निर्भर करता है: निकट-क्षेत्र सुनामी 10–30 मिनट में आ सकती हैं, जबकि महासागर-पार सुनामी में घंटे लग सकते हैं — 2011 जापान सुनामी 22 घंटे बाद चिली पहुँची।
सुनामी भूकंप धीमी-टूट वाली घटनाओं का एक विशेष वर्ग है जो अपनी तीव्रता के सापेक्ष असमान रूप से बड़ी सुनामी उत्पन्न करते हैं, जो उन्हें निकटवर्ती तटों के लिए विशेष रूप से खतरनाक बनाता है।
रन-अप ऊँचाई — तट पर पानी द्वारा प्राप्त अधिकतम ऊर्ध्वाधर ऊँचाई — तटीय स्थलाकृति और बंदरगाह अनुनाद प्रभावों के कारण अपतटीय लहर ऊँचाई से बहुत अधिक हो सकती है।
प्रशांत सुनामी चेतावनी केंद्र (PTWC) और क्षेत्रीय चेतावनी केंद्र वास्तविक समय में सुनामी का पता लगाने और पुष्टि करने के लिए DART बॉय (गहरे-समुद्र दबाव संवेदक) का उपयोग करते हैं।

सामान्य उपयोग

यह समझना कि रिपोर्ट किए गए भूकंप में उसके मापदंडों के आधार पर सुनामी उत्पन्न करने की क्षमता है या नहीं।
भूकंप विशेषताओं और सुनामी उत्पत्ति के बीच संबंध की शैक्षिक खोज।
यात्रा या स्थानांतरण योजना के लिए सुनामी खतरे के प्रति तटीय जोखिम का आकलन।
सुनामी चेतावनी प्रणालियों और निकट-क्षेत्र घटनाओं के लिए तत्काल निकासी के महत्व के बारे में सीखना।

How to Use

1
Enter Earthquake Parameters
Input the earthquake magnitude, focal depth, and location. Tsunamis are most efficiently generated by shallow (< 50 km depth) thrust earthquakes with vertical fault displacement; the tool checks these criteria automatically.
2
Specify Your Coastal Location
Enter your coastal city or coordinates. The tool calculates your approximate distance from the source and identifies whether you are in a mapped tsunami inundation zone based on NOAA and national tsunami center data.
3
Read Your Risk Summary
Review the estimated wave arrival time, indicative wave height range, and evacuation tier. Treat all outputs as supplementary to official warnings from PTWC, NTHMP, or JMA, which must always take precedence.

About

Tsunami science sits at the intersection of seismology, physical oceanography, and coastal engineering. The word tsunami derives from the Japanese 津波 (tsu, harbor; nami, wave), reflecting Japan's millennia of devastating experience with these events. Despite their colloquial name 'tidal waves,' tsunamis have no connection to tidal forces; they are long-period gravity waves with wavelengths of 100–500 km in deep water and wave periods of 10–60 minutes, compared to wind-driven ocean waves with periods of seconds.

The physics of tsunami generation requires a mechanism that displaces a large volume of water vertically over a large area. Megathrust earthquakes accomplish this by the sudden elastic rebound of the overriding plate—the 2011 Tohoku earthquake caused the seafloor to rise by 5–8 meters over a 300 × 200 km area instantaneously, displacing an estimated 5 cubic kilometers of water. The resulting wave system propagates radially, with energy concentrated perpendicular to the fault strike. Directivity effects mean that the coast directly opposite the rupture typically receives the highest waves.

The Deep-ocean Assessment and Reporting of Tsunamis (DART) buoy network, operated primarily by NOAA, provides real-time sea-level measurements from the deep ocean floor. These buoys detect tsunami wave amplitudes of centimeters in the open ocean, enabling confirmation or cancellation of warnings within 15–30 minutes of a potentially tsunamigenic earthquake. Combined with coastal tide gauge networks and numerical propagation models, DART data allows warning centers to issue probabilistic wave height forecasts for coastal communities hours before wave arrival in distant-field scenarios. Local and regional tsunamis remain the most challenging problem in warning science because the lead times are measured in minutes.

FAQ

What earthquakes generate tsunamis?

Tsunamis are most commonly generated by shallow (< 50 km depth) submarine thrust earthquakes that produce significant vertical seafloor displacement, typically exceeding 1 meter over large areas. The key factors are: magnitude ≥ M7.5 (though some M7.0 events with favorable geometry have generated destructive tsunamis), a thrust (reverse) or oblique-thrust focal mechanism with a large vertical displacement component, shallow focal depth in the crust or uppermost mantle, and occurrence beneath ocean floor rather than continental crust. Strike-slip earthquakes—where motion is primarily horizontal, as on transform faults—rarely generate significant tsunamis. The 2018 Sulawesi earthquake was exceptional: a predominantly strike-slip event triggered localized submarine landslides that generated the devastating Palu Bay tsunami.

How fast do tsunamis travel and when do they arrive?

Tsunami propagation speed in open ocean is governed by the shallow-water wave formula: v = √(g × d), where g is gravitational acceleration and d is ocean depth. In the deep Pacific (average depth ~4,000 m), tsunamis travel at approximately 700–800 km/h—comparable to a commercial jet aircraft. As waves enter shallower coastal water, they slow dramatically (to 50–100 km/h near shore) while their amplitude increases through shoaling. This means a tsunami generated 4,000 km away arrives in about 5–6 hours in deep water, but can take 30–60 minutes to inundate a coast after entering shallow shelf waters. The Pacific Tsunami Warning Center (PTWC) issues initial bulletins within 3 minutes of detecting a significant seismic event.

How far inland can tsunami waves travel?

Tsunami inundation distance depends on wave height, coastal topography, and land elevation. The 2011 Tohoku tsunami waves reached heights of 40.5 m (at Miyako, Japan) and inundated up to 10 km inland across flat coastal plains, destroying the town of Rikuzentakata. In contrast, mountainous coastlines confine inundation to narrow strips. Maximum inundation run-up is generally defined as the highest elevation reached by wave water, measured as meters above mean sea level. NOAA and national emergency management agencies have mapped tsunami inundation zones for high-risk coastlines using numerical models calibrated against historical events. These maps define evacuation zones (A through E or Zone 1 through 3 depending on jurisdiction) for emergency planning.

Is a tsunami warning always issued after a large earthquake?

Warning centers issue tsunami warnings, advisories, and watches based on rapid seismic analysis within minutes of a significant event. PTWC monitors earthquakes globally and issues initial bulletins for any event M7.0+ in ocean basin settings within 3 minutes. However, the first message is often a 'tsunami information statement' that may not indicate confirmed wave generation—definitive warnings come after sea-level gauges and DART buoys confirm or deny wave propagation. Local tsunamis—generated by earthquakes within 50–100 km of shore—can arrive within 5–20 minutes, before official warnings are disseminated. In these cases, the natural warning is the shaking itself: the international standard guidance is that prolonged strong shaking near the coast (> 20 seconds) is itself a tsunami warning signal, and coastal residents should evacuate immediately without waiting for official messages.

Are there tsunamis caused by non-earthquake sources?

Tsunamis can be generated by submarine landslides, volcanic activity, meteorite impacts, and atmospheric pressure disturbances (meteotsunamis). Submarine landslides are the second most common cause: the 1958 Lituya Bay event in Alaska, triggered by an earthquake-induced rockslide, produced a 524-meter run-up—the tallest wave in recorded history. The 2022 Hunga Tonga-Hunga Ha'apai volcanic eruption generated an unusual meteotsunami-like pressure wave that propagated globally at the speed of sound in the atmosphere (~340 m/s), reaching Peru and Japan within hours. Volcanic island collapses—hypothesized for the Canary Islands—could theoretically generate Atlantic basin tsunamis, though the probability and magnitude of such events are debated in the scientific community.