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60-831: First suspected from mapping of gravitational anomalies in 1965 and an uplifted marine terrace at Restoration Point (foreground in picture above), the Seattle Fault's existence and likely hazard were definitively established by a set of five reports published in Science in 1992. These reports looked at the timing of abrupt uplift and subsidence around Restoration Point and Alki Point (distant right side of picture), tsunami deposits on Puget Sound, turbidity in lake paleosediments, rock avalanches, and multiple landslides around Lake Washington, and determined that all these happened about 1,100 years ago (between 923 and 924 CE , and most likely due to an earthquake of magnitude 7 or greater on

120-419: A shore (wave-cut/abrasion-) platform through the process of abrasion . A relative change of the sea level leads to regressions or transgressions and eventually forms another terrace (marine-cut terrace) at a different altitude, while notches in the cliff face indicate short stillstands. It is believed that the terrace gradient increases with tidal range and decreases with rock resistance. In addition,

180-512: A 4 to 7 km (2.5 to 4.3 miles) wide zone of complex faulting, with three or more main south-dipping thrust faults . Most of the faulting is "blind" (not reaching the surface), and generally difficult to locate because of heavy vegetation or development. Three principal strands have been identified, their location determined by high-resolution seismic reflection and aeromagnetic surveys. The northernmost strand lies nearly along Interstate 90 and then under Lake Sammamish . The central section of

240-459: A continuum from wave notches formed in quiet conditions at sea level to surf notches formed in more turbulent conditions and as much as 2 m (6.6 ft) above sea level. As stated above, there was at least one higher sea level during the Holocene, so that some notches may not contain a tectonic component in their formation. Fault scarp A fault scarp is a small step-like offset of

300-402: A mean uplift rate or the calculation of eustatic level at a particular time if the uplift is known. In order to estimate vertical uplift, the eustatic position of the considered paleo sea levels relative to the present one must be known as precisely as possible. Current chronology relies principally on relative dating based on geomorphologic criteria, but in all cases the shoreline angle of

360-458: A paleo-sea level. The platform of a marine terrace usually has a gradient between 1°–5° depending on the former tidal range with, commonly, a linear to concave profile. The width is quite variable, reaching up to 1,000 metres (3,300 ft), and seems to differ between the northern and southern hemispheres . The cliff faces that delimit the platform can vary in steepness depending on the relative roles of marine and subaerial processes. At

420-634: A rare exception can be seen at Mee Kwa Mooks Park south of Alki Point . This is the site of the West Seattle Fault ; the prominent rise there is due to uplift on the north side of the fault. The Seattle Fault (and the related Tacoma Fault) is not the only source of earthquake hazard in the Puget Lowland. Other faults in the near surface continental crust, such as the South Whidbey Island Fault (near Everett), and

480-585: A tsunami would also inundate the industrial areas on Commencement Bay 30 miles south (Tacoma) and low-lying areas on the Puyallup River delta. There is also concern that a severe or prolonged event could cause failure of the Duwamish or Puyallup River deltas, where the main port facilities for Seattle and Tacoma are located (Harbor Island and Commencement Bay). Marine terrace A raised beach , coastal terrace, or perched coastline

540-446: A very triangular shape. This formation is known as a triangular facet ; however, this landform is not limited to fault scarps. Fault scarps may vary in size from a few centimeters to many meters. Fault-line scarps are typically formed due to the differential erosion of weaker rocks along a fault. Such erosion, occurring over long time periods, may shift a physical cliff far from the actual fault location, which may be buried beneath

600-446: A wide variety of soils with complex histories and different ages. In protected areas, allochthonous sandy parent materials from tsunami deposits may be found. Common soil types found on marine terraces include planosols and solonetz . It is now widely thought that marine terraces are formed during the separated highstands of interglacial stages correlated to marine isotope stages (MIS). The formation of marine terraces

660-453: Is a rather fast process. A deeper transgression of cliffs into the shoreline may completely destroy previous terraces; but older terraces might be decayed or covered by deposits, colluvia or alluvial fans . Erosion and backwearing of slopes caused by incisive streams play another important role in this degradation process. The total displacement of the shoreline relative to the age of the associated interglacial stage allows calculation of

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720-473: Is a relatively flat, horizontal or gently inclined surface of marine origin, mostly an old abrasion platform which has been lifted out of the sphere of wave activity (sometimes called "tread"). Thus, it lies above or under the current sea level , depending on the time of its formation. It is bounded by a steeper ascending slope on the landward side and a steeper descending slope on the seaward side (sometimes called "riser"). Due to its generally flat shape, it

780-529: Is about the time that the strike-slip movement on the north-striking Straight Creek Fault to the east ceased, due to the intrusions of plutons . It appears that when the Straight Creek Fault became stuck the north–south compressive force that it had accommodated by strike-slip motion was transferred to the crust of the Puget Lowland, which subsequently folded and faulted, and the various blocks jammed over one another. Other scarps associated with

840-403: Is an ongoing debate about the roles of wave erosion and weathering in the formation of shore platforms. Reef flats or uplifted coral reefs are another kind of marine terrace found in intertropical regions. They are a result of biological activity, shoreline advance and accumulation of reef materials. While a terrace sequence can date back hundreds of thousands of years, its degradation

900-498: Is applied. This includes stereoscopic aerial photographic interpretation (ca. 1 : 10,000 – 25,000 ), on-site inspections with topographic maps (ca. 1 : 10,000) and analysis of eroded and accumulated material. Moreover, the exact altitude can be determined with an aneroid barometer or preferably with a levelling instrument mounted on a tripod. It should be measured with the accuracy of 1 cm (0.39 in) and at about every 50–100 metres (160–330 ft), depending on

960-435: Is believed to be the only instance in the past 7,000 years of the type that causes a regional uplift. The other type is more localized and shallower (and therefore more damaging); at least four such events are believed to have occurred in the past 3,000 years on the west end of the fault. (The history of the central and eastern segments is not known.) Calculations based on fault length and paleoseismological studies show that

1020-693: Is concern that such an earthquake on the Seattle Fault would devastate unreinforced masonry (URM) buildings , of which the City of Seattle is estimated to have around a thousand, concentrated in Capitol Hill , Pioneer Square , and the International District . Other recent work indicates that the Seattle Fault can generate two types of earthquakes; both pose "considerable hazard" to the Seattle metropolitan region. The A.D. 900–930 earthquake

1080-458: Is controlled by changes in environmental conditions and by tectonic activity during recent geological times . Changes in climatic conditions have led to eustatic sea-level oscillations and isostatic movements of the Earth's crust , especially with the changes between glacial and interglacial periods. Processes of eustasy lead to glacioeustatic sea level fluctuations due to changes of

1140-400: Is often used for anthropogenic structures such as settlements and infrastructure . A raised beach is an emergent coastal landform . Raised beaches and marine terraces are beaches or wave-cut platforms raised above the shoreline by a relative fall in the sea level . Around the world, a combination of tectonic coastal uplift and Quaternary sea-level fluctuations has resulted in

1200-654: Is the structural boundary where 50–60 million years old (early Tertiary ) basalt of the Crescent Formation on the south has been uplifted – the Seattle Uplift – and is tipping into the Seattle Basin, where the Tertiary bedrock is buried under at least 7 km (4.3 miles) of relatively softer, lighter sedimentary strata of the younger Blakeley and Blakely Harbor formations. This has resulted in

1260-616: The Cape Chignecto Provincial Park . Other important sites include various coasts of New Zealand , e.g. Turakirae Head near Wellington being one of the world's best and most thoroughly studied examples. Also along the Cook Strait in New Zealand , there is a well-defined sequence of uplifted marine terraces from the late Quaternary at Tongue Point. It features a well preserved lower terrace from

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1320-605: The San Andreas Fault . Hans Jenny famously researched the pygmy forests of the Mendocino and Sonoma county marine terraces. The marine terrace's "ecological staircase" of Salt Point State Park is also bound by the San Andreas Fault. Along the coasts of South America marine terraces are present, where the highest ones are situated where plate margins lie above subducted oceanic ridges and

1380-1042: The South China Sea coast, on west-facing Atlantic coasts, such as Donegal Bay , County Cork and County Kerry in Ireland ; Bude , Widemouth Bay , Crackington Haven , Tintagel , Perranporth and St Ives in Cornwall , the Vale of Glamorgan , Gower Peninsula , Pembrokeshire and Cardigan Bay in Wales , Jura and the Isle of Arran in Scotland , Finistère in Brittany and Galicia in Northern Spain and at Squally Point in Eatonville, Nova Scotia within

1440-516: The coast . Older terraces are covered by marine and/or alluvial or colluvial materials while the uppermost terrace levels usually are less well preserved. While marine terraces in areas of relatively rapid uplift rates (> 1 mm/year) can often be correlated to individual interglacial periods or stages, those in areas of slower uplift rates may have a polycyclic origin with stages of returning sea levels following periods of exposure to weathering . Marine terraces can be covered by

1500-400: The isostatic uplift . When eustasy was the main factor for the formation of marine terraces, derived sea level fluctuations can indicate former climate changes . This conclusion has to be treated with care, as isostatic adjustments and tectonic activities can be extensively overcompensated by a eustatic sea level rise. Thus, in areas of both eustatic and isostatic or tectonic influences,

1560-747: The topography . In remote areas, the techniques of photogrammetry and tacheometry can be applied. Different methods for dating and correlation of marine terraces can be used and combined. The morphostratigraphic approach focuses especially in regions of marine regression on the altitude as the most important criterion to distinguish coastlines of different ages. Moreover, individual marine terraces can be correlated based on their size and continuity. Also, paleo-soils as well as glacial , fluvial , eolian and periglacial landforms and sediments may be used to find correlations between terraces. On New Zealand's North Island , for instance, tephra and loess were used to date and correlate marine terraces. At

1620-420: The Seattle Fault can generate a very damaging magnitude 7.0 earthquake. In addition to extensive damage to unreinforced structures and structures built on fill (such as much of Seattle's Pioneer Square area, the industrial area, and the waterfront), computer modeling has shown that such earthquakes could cause a tsunami of about 2 m (6 feet 7 inches) high on Elliott Bay . The modeling shows that such

1680-537: The Seattle Fault. Although the 923-924 CE earthquake was over a thousand years ago, local traditional stories have preserved an association of a powerful supernatural spirit – a'yahos, noted for shaking, rushes of water, and landsliding – with five locales along the trace of the Seattle Fault, including a "spirit boulder" called Psai-Yah-hus near the Fauntleroy ferry dock in West Seattle. The Seattle Fault

1740-465: The Seattle Uplift as a sheet of rock that is being forced up a ramp. Subsequent work suggests that the structure of the Seattle Fault may vary from east to west, with both models being applicable in different sections. A later model has part of the north-thrusting sheet forming a wedge between the sedimentary formations of the Seattle Basin and the underlying bedrock. The Seattle Fault is believed to date from about 40 million years ago (late Eocene ). This

1800-546: The Seattle fault have been identified by LIDAR -based mapping; trenching has generally shown the faulting to be more complex than was first realized. Many of the details of the Seattle Fault, including recurrence rate, remain to be resolved. A study of sediments in Lake Washington found evidence of seven large (M > 7) earthquakes in the last 3,500 years. Surface scarps due to faulting are rarely observed in this area (due to topography, vegetation, and urbanization);

1860-591: The Seattle–Tacoma area, whereas a magnitude 9 subduction event would damage only around 87 bridges in all of Western Washington. The same study also found that with failure of just six bridges (the minimum damage for a Benioff M 6.5 event) there could be at least $ 3 billion lost in business revenue alone. Subsequent retrofitting by the Washington Department of Transportation and the City of Seattle would likely reduce damage to key bridges. But there

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1920-473: The accumulation of ice sheets have depressed the land so that when the ice sheets melts the land readjusts with time thus raising the height of the beaches (glacio-isostatic rebound) and in places where co-seismic uplift occur. In the latter case, the terrace are not correlated with sea level highstand even if co-seismic terrace are known only for the Holocene. For exact interpretations of the morphology, extensive datings, surveying and mapping of marine terraces

1980-399: The arrival of terrestrial cosmogenic nuclides method, and particularly through the use of Be and Al cosmogenic isotopes produced on site. These isotopes record the duration of surface exposure to cosmic rays . This exposure age reflects the age of abandonment of a marine terrace by the sea. In order to calculate the eustatic sea level for each dated terrace, it is assumed that

2040-473: The case of Pakistan's coastal cliffs. The height of the scarp formation tends to be defined in terms of the vertical displacement along the fault. Active scarp faults may reflect rapid tectonic displacement and can be caused by any type of fault including strike-slip faults . Vertical displacement of ten meters may occur in fault scarps in volcanic bedrock, but is usually the result of multiple episodic movements of 5 to 10 meters per tectonic event. Due to

2100-560: The course of the relative sea level curve can be complicated. Hence, most of today's marine terrace sequences were formed by a combination of tectonic coastal uplift and Quaternary sea level fluctuations. Jerky tectonic uplifts can also lead to marked terrace steps while smooth relative sea level changes may not result in obvious terraces, and their formations are often not referred to as marine terraces. Marine terraces often result from marine erosion along rocky coastlines in temperate regions due to wave attack and sediment carried in

2160-520: The direct dating of marine terraces and their related materials. The most common method is C radiocarbon dating , which has been used, for example, on the North Island of New Zealand to date several marine terraces. It utilizes terrestrial biogenic materials in coastal sediments , such as mollusc shells , by analyzing the C isotope . In some cases, however, dating based on the Th / U ratio

2220-460: The dramatic uplift along the fault, which exposes its surface, the fault scarp is very prone to erosion. This is especially true if the material being uplifted consists of unconsolidated sediment. Weathering, mass wasting, and water runoff can soon wear down these bluffs, sometimes resulting in V-shaped valleys along runoff channels. Adjacent V-shaped valley formations give the remaining fault spurs

2280-404: The eustatic sea-level position corresponding to at least one marine terrace is known and that the uplift rate has remained essentially constant in each section. Marine terraces play an important role in the research on tectonics and earthquakes . They may show patterns and rates of tectonic uplift and thus may be used to estimate the tectonic activity in a certain region. In some cases

2340-465: The exposed secondary landforms can be correlated with known seismic events such as the 1855 Wairarapa earthquake on the Wairarapa Fault near Wellington , New Zealand which produced a 2.7-metre (8 ft 10 in) uplift. This figure can be estimated from the vertical offset between raised shorelines in the area. Furthermore, with the knowledge of eustatic sea level fluctuations,

2400-495: The fault zone – where it crosses the apparent location of the Olympic–Wallowa Lineament – shows marked variation in the location of the strands and of the underlying structure, but the nature and significance of this is not understood. The fault extends for approximately 70 km (43 miles) from near Fall City on the east, where it appears to be terminated by the South Whidbey Island Fault , to Hood Canal on

2460-417: The formation of marine terrace sequences, most of which were formed during separate interglacial highstands that can be correlated to marine isotope stages (MIS). A marine terrace commonly retains a shoreline angle or inner edge, the slope inflection between the marine abrasion platform and the associated paleo sea-cliff. The shoreline angle represents the maximum shoreline of a transgression and therefore

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2520-633: The formation process. This way can be assessed, whether there were changes in sea level or whether tectonic activities took place. Raised beaches are found in a wide variety of coast and geodynamical background such as subduction on the Pacific coasts of South and North America , passive margin of the Atlantic coast of South America, collision context on the Pacific coast of Kamchatka, Papua New Guinea , New Zealand , Japan , passive margin of

2580-593: The ground surface in which one side of a fault has shifted vertically in relation to the other. The topographic expression of fault scarps results from the differential erosion of rocks of contrasting resistance and the displacement of land surface by movement along the fault. Differential movement and erosion may occur either along older inactive geologic faults, or recent active faults . Fault scarps often involve zones of highly fractured rock and discontinuities of hard and weak consistencies of rock. Bluffs can form from upthrown blocks and can be very steep, as in

2640-539: The highest and most rapid rates of uplift occur. At Cape Laundi, Sumba Island , Indonesia an ancient patch reef can be found at 475 m (1,558 ft) above sea level as part of a sequence of coral reef terraces with eleven terraces being wider than 100 m (330 ft). The coral marine terraces at Huon Peninsula , New Guinea , which extend over 80 km (50 mi) and rise over 600 m (2,000 ft) above present sea level are currently on UNESCO 's tentative list for world heritage sites under

2700-503: The intersection of the former shore (wave-cut/abrasion-) platform and the rising cliff face the platform commonly retains a shoreline angle or inner edge (notch) that indicates the location of the shoreline at the time of maximum sea ingression and therefore a paleo- sea level . Sub-horizontal platforms usually terminate in a low tide cliff, and it is believed that the occurrence of these platforms depends on tidal activity. Marine terraces can extend for several tens of kilometers parallel to

2760-599: The last interglacial , a widely eroded higher terrace from the penultimate interglacial and another still higher terrace, which is nearly completely decayed. Furthermore, on New Zealand's North Island at the eastern Bay of Plenty , a sequence of seven marine terraces has been studied. Along many coasts of mainland and islands around the Pacific , marine terraces are typical coastal features. An especially prominent marine terraced coastline can be found north of Santa Cruz , near Davenport , California , where terraces probably have been raised by repeated slip earthquakes on

2820-401: The magnitude 9 1700 Cascadia earthquake , where the entire Cascadia subduction zone , from Cape Mendocino to Vancouver Island , slips. But the Seattle and Tacoma faults are probably the most serious earthquake threat to the populous Seattle–Tacoma area. A 2002 study of bridge vulnerability estimated that a magnitude 7 earthquake on the Seattle Fault would damage approximately 80 bridges in

2880-584: The marine terraces is associated with numerical ages. The best-represented terrace worldwide is the one correlated to the last interglacial maximum ( MIS 5e ). Age of MISS 5e is arbitrarily fixed to range from 130 to 116 ka but is demonstrated to range from 134 to 113 ka in Hawaii and Barbados with a peak from 128 to 116 ka on tectonically stable coastlines. Older marine terraces well represented in worldwide sequences are those related to MIS 9 (~303–339 ka) and 11 (~362–423 ka). Compilations show that sea level

2940-618: The name Houn Terraces - Stairway to the Past. Other considerable examples include marine terraces rising up to 360 m (1,180 ft) on some Philippine Islands and along the Mediterranean Coast of North Africa , especially in Tunisia , rising up to 400 m (1,300 ft). Uplift can also be registered through tidal notch sequences. Notches are often portrayed as lying at sea level; however notch types actually form

3000-473: The relationship between terrace width and the strength of the rock is inverse, and higher rates of uplift and subsidence as well as a higher slope of the hinterland increases the number of terraces formed during a certain time. Furthermore, shore platforms are formed by denudation and marine-built terraces arise from accumulations of materials removed by shore erosion . Thus, a marine terrace can be formed by both erosion and accumulation. However, there

3060-572: The sediment sequence might make this analysis difficult. The biostratigraphic approach uses remains of organisms which can indicate the age of a marine terrace. For that, often mollusc shells , foraminifera or pollen are used. Especially Mollusca can show specific properties depending on their depth of sedimentation . Thus, they can be used to estimate former water depths. Marine terraces are often correlated to marine oxygen isotopic stages (MIS) and can also be roughly dated using their stratigraphic position. There are various methods for

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3120-401: The speed of isostatic uplift can be estimated and eventually the change of relative sea levels for certain regions can be reconstructed. Thus, marine terraces also provide information for the research on climate change and trends in future sea level changes. When analyzing the morphology of marine terraces, it must be considered, that both eustasy and isostasy can have an influence on

3180-526: The terminus advance of former glaciers marine terraces can be correlated by their size, as their width decreases with age due to the slowly thawing glaciers along the coastline. The lithostratigraphic approach uses typical sequences of sediment and rock strata to prove sea level fluctuations on the basis of an alternation of terrestrial and marine sediments or littoral and shallow marine sediments. Those strata show typical layers of transgressive and regressive patterns. However, an unconformity in

3240-531: The uplift of continental crusts along with their shorelines. Today, the process of glacial isostatic adjustment mainly applies to Pleistocene glaciated areas. In Scandinavia , for instance, the present rate of uplift reaches up to 10 millimetres (0.39 in)/year. In general, eustatic marine terraces were formed during separate sea level highstands of interglacial stages and can be correlated to marine oxygen isotopic stages (MIS) . Glacioisostatic marine terraces were mainly created during stillstands of

3300-425: The water volume in the oceans, and hence to regressions and transgressions of the shoreline. At times of maximum glacial extent during the last glacial period , the sea level was about 100 metres (330 ft) lower compared to today. Eustatic sea level changes can also be caused by changes in the void volume of the oceans, either through sedimento-eustasy or tectono-eustasy. Processes of isostasy involve

3360-406: The waves. Erosion also takes place in connection with weathering and cavitation . The speed of erosion is highly dependent on the shoreline material (hardness of rock ), the bathymetry , and the bedrock properties and can be between only a few millimeters per year for granitic rocks and more than 10 metres (33 ft) per year for volcanic ejecta . The retreat of the sea cliff generates

3420-571: The west (not shown on the map). However, boundaries defining the western termination zone is currently unclear (see Puget Sound faults#Question of western termination ). It is the northern edge of the Seattle Uplift, of which the Tacoma Fault is the southern edge. One model has the Seattle and Tacoma faults converging at depth to form a wedge, which is being popped up by approximately north–south oriented compression that ultimately derives from plate tectonics. Another model (see diagram) interprets

3480-504: The yet to be studied Olympia Fault (near Olympia), though historically quiescent, are suspected of generating earthquakes of around magnitude 7. Others, such as the 2001 Nisqually earthquake , originate about 50 to 60 km (31 to 37 miles) below Puget Sound in the Benioff zone of the subducting Juan de Fuca plate ; being so deep their energy is dissipated. And there are the infrequent but very powerful great subduction events, such as

3540-523: Was 3 ± 3 meters higher during MIS 5e, MIS 9 and 11 than during the present one and −1 ± 1 m to the present one during MIS 7 . Consequently, MIS 7 (~180-240 ka) marine terraces are less pronounced and sometimes absent. When the elevations of these terraces are higher than the uncertainties in paleo-eustatic sea level mentioned for the Holocene and Late Pleistocene , these uncertainties have no effect on overall interpretation. Sequence can also occur where

3600-584: Was applied, in case detrital contamination or low uranium concentrations made finding a high resolution dating difficult. In a study in southern Italy paleomagnetism was used to carry out paleomagnetic datings and luminescence dating (OSL) was used in different studies on the San Andreas Fault and on the Quaternary Eupcheon Fault in South Korea . In the last decade, the dating of marine terraces has been enhanced since

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