Cách Hoạt động Đứt gãy: Lệch giương, Bình thường, và Đảo chiều

Strike-Slip Fault: Horizontal Motion

A Strike-Slip FaultA fault where blocks of rock move horizontally past each other. The San Andreas Fault and North Anatolian Fault are major strike-slip faults that produce destructive earthquakes. is characterized by predominantly horizontal relative motion along its plane. The two sides of the fault slide past each other laterally, with little or no vertical displacement at the surface. Geologists classify strike-slip faults as right-lateral (dextral) or left-lateral (sinistral) depending on the direction of apparent motion of the far block relative to the near block when viewed from above. Looking across the San Andreas Fault in California, the block on the far side appears to have moved to the right — making it a right-lateral fault. The North Anatolian Fault in Turkey is also right-lateral. The Alpine Fault in New Zealand is a complex structure with both strike-slip and reverse components. Strike-slip faults form at transform boundariesA plate boundary where two plates slide horizontally past each other. The San Andreas Fault in California is the most famous example of a transform boundary. where plates slide past each other, but they also occur within plate interiors where crustal blocks are rotating or escaping due to distant convergence.

Recognizing Strike-Slip Faults

In the field, strike-slip faults are identified by offset features: streams, ridges, or road cuts that have been displaced horizontally by accumulated slip. Paleoseismological trenches across such faults reveal offset layers of soil and sediment, allowing scientists to reconstruct the history of past ruptures and estimate Earthquake Recurrence IntervalThe average time between major earthquakes on a particular fault. Estimated from paleoseismology and historical records. The Cascadia subduction zone has a recurrence interval of ~500 years.s for major events.

Normal Fault: Extensional Forces

A Normal FaultA fault where the rock above the fault plane (hanging wall) moves downward relative to the rock below. Associated with extensional forces in rift zones and divergent boundaries. forms where the crust is being pulled apart — in extensional tectonic settings. The defining characteristic is that the hanging wall (the block above the fault plane) has moved down relative to the footwall (the block below). Normal faults typically dip at 50 to 70 degrees from horizontal. They occur at divergent plate boundariesA plate boundary where two plates move apart from each other, creating new crust as magma rises from the mantle. Mid-ocean ridges are the most common example. such as mid-ocean ridges and continental rift zones, where the crust is being stretched. The East African Rift System — which may eventually split the African continent — is lined with normal faults that generate moderate earthquakes as the crust is pulled apart. The Basin and Range Province in the western United States is another classic extensional environment, where the crust has been thinned and faulted into a series of tilted blocks producing the alternating mountain ranges and valleys of Nevada and Utah.

Normal Fault Earthquakes

Earthquake focal mechanisms on normal faults show a characteristic pattern of tension: the compressional axis is near-vertical and the tensional axis is near-horizontal. Normal fault earthquakes are typically shallower and less prone to generating large tsunamis than subduction events, though notable exceptions exist. The 2009 L'Aquila earthquake in Italy (Mw 6.3), which killed 309 people, was a normal faulting event. Poorly constructed unreinforced masonry buildings suffered catastrophic collapse in that event, highlighting the interaction between building vulnerabilityA mathematical function describing the probability of various damage states for a specific building type given a level of ground shaking. Essential for loss estimation models. and shaking intensity.

Reverse Fault: Compressional Forces

A Reverse (Thrust) FaultA fault where the hanging wall moves upward relative to the footwall, caused by compressional forces. Thrust faults at shallow angles are responsible for the largest earthquakes. is the compressional counterpart to a normal fault: the hanging wall moves up relative to the footwall, reflecting crustal shortening. Reverse faults dip at angles between 30 and 60 degrees. Thrust faults are a special case — low-angle reverse faults, often dipping less than 30 degrees. Reverse and thrust faults form at convergent plate boundariesA plate boundary where two plates move toward each other. Can produce subduction zones (ocean-continent), mountain building (continent-continent), or deep trenches (ocean-ocean). wherever the crust is being compressed. The Himalayan frontal thrust and the megathrust interfaces of subduction zones are all reverse or thrust faults. Reverse faulting earthquakes can be exceptionally destructive: the 1994 Northridge earthquake (Mw 6.7) on a blind thrust fault beneath the San Fernando Valley killed 57 people and caused $20 billion in damage.

Blind Thrust Fault: Hidden Dangers

A Blind Thrust FaultA thrust fault that does not reach the surface, making it invisible at ground level and harder to detect. The 1994 Northridge earthquake occurred on a blind thrust fault. is a reverse fault that does not break the surface. Its upper tip remains buried beneath overlying sediment or rock, leaving no surface fault trace to alert planners or seismologists to its existence. These hidden faults pose a particularly insidious hazard because they can only be inferred from subtle surface topography — broad anticlinal folds, uplifted terraces — and geophysical surveys. The 1983 Coalinga earthquake (Mw 6.5) and the 1994 Northridge earthquake in California were both caused by blind thrust faults. In the Los Angeles Basin, numerous blind thrust systems have been identified beneath the urban area using subsurface geology and seismic reflection surveys. The discovery of the Puente Hills Fault beneath downtown Los Angeles revealed a structure capable of producing a Mw 7.0–7.5 earthquake directly under one of the world's most densely populated urban centers.

Fault Creep vs Locked Faults

Not all faults rupture in discrete earthquakes. Fault creepThe slow, continuous movement along a fault without generating significant earthquakes. Some sections of the San Andreas Fault creep at 2-3 cm/year. refers to slow, continuous slip along a fault without producing significant seismic waves. Creeping faults release stress gradually and tend to generate fewer large earthquakes than locked faultsA section of a fault where friction prevents movement, causing stress to accumulate. When a locked fault finally ruptures, it can produce a major earthquake., but they can cause progressive damage to roads, buildings, and infrastructure that cross the fault. The central section of the San Andreas Fault near Parkfield creeps at approximately 25 millimeters per year. The Calaveras and Hayward faults in the San Francisco Bay Area also creep measurably, producing small earthquakes and slow deformation. In contrast, a Locked FaultA section of a fault where friction prevents movement, causing stress to accumulate. When a locked fault finally ruptures, it can produce a major earthquake. has zero or near-zero creep — all plate motion must eventually be accommodated by sudden slip in earthquakes. The contrast between creeping and locked behavior reflects differences in fault zone composition, temperature, and pore fluid pressure.

Slow Slip and Silent Earthquakes

Between fully locked and continuously creeping behavior, some fault segments undergo slow slip events — transient episodes of fault slip that release stress over days to weeks without generating felt earthquakes. These were first detected using GPS networks and are now monitored on subduction zones and major strike-slip faults worldwide. Slow slip events may interact with the locked zones of faults, transferring stress and potentially influencing the timing of future large earthquakes, though the relationship is complex and an active area of research.

Mapping Fault Lines Worldwide

Understanding which Fault LineThe trace of a fault on the Earth's surface, visible as a line or zone of broken rock. Active fault lines are mapped by geologists to assess earthquake hazard for nearby communities.s exist, where they are located, and how active they are is foundational to seismic hazard assessment. Fault mapping uses multiple techniques: geological field surveys that trace fault scarps and offset features; aerial and satellite imagery that reveals linear topographic features; subsurface geophysical surveys using seismic reflection and refraction; PaleoseismologyThe study of prehistoric earthquakes through geological evidence such as fault trenches, uplifted terraces, and tsunami deposits. Extends the earthquake record back thousands of years. trenching studies; and GPS GeodesyThe use of Global Positioning System receivers to measure tectonic plate motion and crustal deformation with millimeter precision. Reveals how strain accumulates on faults between earthquakes. measurements that detect surface deformation. National geological surveys — notably the USGS in the United States — compile fault databases that form the backbone of national hazard mapsA map showing the probability of earthquake shaking exceeding specified levels over a given time period. Used by engineers, planners, and insurers to assess earthquake risk.. Globally, the International Seismological Centre and the GEM Foundation maintain databases of active faults that support Seismic Risk AssessmentThe process of evaluating earthquake hazard, building vulnerability, and potential losses for a specific area or structure. Combines hazard maps, building inventory, and damage models. in earthquake-prone regions worldwide.