Alat Perbandingan Gempa Bumi

Bandingkan dua gempa bumi secara berdampingan pada energi, kedalaman, magnitudo, radius terasa, dan dampaknya.

Analysis

Mengapa Membandingkan Magnitudo Gempa Bumi Penting

Karena magnitudo gempa bumi menggunakan skala logaritmik, perbedaan antara dua magnitudo jauh lebih besar daripada yang terlihat. Perbedaan magnitudo 1,0 berarti 31,6 kali lebih banyak energi; perbedaan 2,0 berarti ~1.000 kali; dan perbedaan 3,0 berarti ~31.600 kali lebih banyak energi.

Kedalaman menambahkan dimensi kritis lain pada perbandingan gempa bumi. Gempa dangkal M6,5 pada kedalaman 10 km dapat menyebabkan kerusakan yang jauh lebih banyak daripada gempa dalam M7,0 pada kedalaman 500 km, karena yang lebih dangkal memusatkan energi di dekat permukaan di mana orang dan struktur berada.

Memahami Skala Eksponensial

Setiap kenaikan 1,0 dalam magnitudo mewakili 31,6 kali lebih banyak energi; setiap kenaikan 2,0 mewakili sekitar 1.000 kali lebih banyak energi.
Radius terasa secara kasar berskala dengan magnitudo — gempa M7 dapat dirasakan 10 kali lebih jauh dari gempa M5.
Klasifikasi kedalaman: gempa dangkal (0–70 km), menengah (70–300 km), dan dalam (300–700 km) berperilaku sangat berbeda dalam hal pola kerusakan dan area terasa.
Perbandingan energi dalam ekuivalen TNT membantu menjembatani kesenjangan antara angka magnitudo abstrak dan potensi destruktif dunia nyata.

Kegunaan Umum

Membandingkan gempa bumi terbaru dengan peristiwa historis terkenal untuk mengontekstualisasikan tingkat keparahannya.
Mengajarkan siswa tentang skala logaritmik dengan menunjukkan perbedaan energi antara dua magnitudo.
Memahami bagaimana kedalaman mempengaruhi potensi destruktif relatif gempa bumi dengan magnitudo serupa.

How to Use

1
Select Two Earthquakes
Search the database for two earthquakes by name, date, location, or USGS event ID. Both recent and historical events going back to the 1900 USGS catalog are available.
2
Choose Comparison Metrics
Select which parameters to compare: magnitude, energy release, depth, felt radius, fatalities, economic losses, tectonic setting, and maximum recorded intensity (MMI).
3
Review Side-by-Side Analysis
Examine the comparison table and energy ratio chart. The tool calculates the factor-difference in energy release and annotates each metric with contextual notes from the seismological record.

About

Comparing earthquakes reveals the enormous range of Earth's seismic output and the complex interplay between source parameters and surface impacts. The global seismic record contains millions of cataloged events: roughly 500,000 detectable earthquakes occur each year, of which about 100,000 can be felt and approximately 100 cause damage. This frequency-magnitude distribution follows the Gutenberg-Richter relation, a remarkably consistent power law observed across tectonic environments: for every unit increase in magnitude, there are roughly 10 times fewer events. This means that while M3.0 earthquakes occur hundreds of times daily worldwide, M8.0 events occur about once per year.

The tectonic setting fundamentally shapes earthquake character. Subduction zone megathrust earthquakes—like the 1960 Chile M9.5 and 2011 Tohoku M9.1—produce extremely long rupture durations (200–500 seconds), generate transoceanic tsunamis, and have predominantly low-angle reverse focal mechanisms. Transform fault earthquakes like those on the San Andreas system produce strike-slip motion, shorter ruptures, and generally lower tsunami potential. Intracontinental thrust belt earthquakes (Himalaya, Zagros, Andes) are associated with crustal thickening and can be devastating due to their proximity to densely populated mountain valleys.

Historical earthquake comparisons must account for detection capability changes over time. Before the establishment of the World-Wide Standardized Seismograph Network (WWSSN) in the 1960s, the catalog is incomplete for smaller magnitudes and location accuracies are far lower. Modern moment tensor catalogs (CMT, maintained since 1976) provide standardized source parameters for systematic comparison. Digital broadband networks since the 1980s enable waveform-based analyses that extract fault geometry, stress drop, and directivity effects—parameters inaccessible from earlier analog records.

FAQ

How do scientists compare earthquakes scientifically?

Seismologists compare earthquakes across several independent dimensions. Magnitude (Mw) characterizes source size. Focal mechanism (strike-slip, normal, reverse/thrust) describes the geometry of fault motion and influences the radiation pattern of seismic energy. Focal depth stratifies events into crustal (< 70 km), intermediate (70–300 km), and deep (> 300 km). Stress drop—the change in shear stress across the fault during rupture—influences the high-frequency content of shaking and explains why some moderate earthquakes feel 'sharp' while larger ones feel 'rolling.' Comparing earthquakes rigorously requires examining all these parameters simultaneously, not magnitude alone.

Why do smaller earthquakes sometimes cause more damage?

Several factors cause smaller earthquakes to sometimes be more destructive than larger ones. Depth is paramount: a M6.0 at 5 km depth can cause far more surface damage than a M6.5 at 80 km. The resonance of seismic waves with building natural periods matters enormously—if dominant wave periods match building heights (typically 0.1 s per floor), resonance amplifies structural response. Local soil conditions can amplify ground motion by a factor of 5–10 at soft sediment sites. Building stock vulnerability is equally critical: a M5.6 in rural Afghanistan or Haiti, where building quality is poor, can kill thousands, while the same event in Japan with modern construction codes may cause no fatalities.

What makes a 'great' earthquake different from a major earthquake?

The Gutenberg-Richter magnitude classification defines great earthquakes as Mw ≥ 8.0 and major earthquakes as Mw 7.0–7.9. The distinction is not merely semantic: great earthquakes rupture fault lengths of 200+ km and durations exceeding 60 seconds, exciting long-period surface waves that circumnavigate the globe multiple times. Great earthquakes can generate tsunamis capable of crossing ocean basins, trigger volcanic unrest, and temporarily alter Earth's rotation rate and axial tilt by measurable amounts. The 2011 Tohoku earthquake shortened Earth's day by approximately 1.8 microseconds. Globally, about 13–17 major earthquakes (M7.0–7.9) and 1–2 great earthquakes (M ≥ 8.0) occur per year on average.

How do shallow and deep earthquakes compare in terms of damage?

Shallow earthquakes (< 20 km depth) typically cause far greater localized damage than deep events of the same magnitude because the energy has less rock to travel through before reaching the surface. The short travel path means less geometric spreading and less attenuation, resulting in higher peak ground accelerations. Deep earthquakes (> 300 km) rarely cause surface damage because by the time the waves reach the crust, they have spread over a much larger volume. A notable exception is the scenario of deep earthquakes beneath populated areas with resonant sediment basins: the 1994 Northridge earthquake (19 km) caused US$20 billion in losses while a similar-magnitude deep earthquake in the Tonga trench the same year caused none.

Are earthquake comparisons useful for predicting future events?

Comparing past earthquakes provides important inputs for probabilistic seismic hazard analysis (PSHA) but does not enable deterministic prediction of future events. The Gutenberg-Richter relation—an empirical power law relating earthquake frequency to magnitude—describes the statistical distribution of seismicity on a fault system. Characteristic earthquake models propose that specific fault segments repeatedly rupture in events of similar magnitude and recurrence interval, based on paleoseismic evidence from trenching. While these models constrain long-term hazard forecasts with 30–50 year horizons, the precise timing of individual earthquakes remains unpredictable beyond short-term windows (days to weeks) following large foreshock sequences.