Sheeted Clastic Dikes in the Megaflood Region

Sheeted Clastic Dikes in the Megaflood Region, Washington, Oregon and Idaho

Skye W. Cooley

Mission Valley, MT

Abstract

Clastic dikes in the Channeled Scablands of Washington, Oregon, and Idaho are vertically-sheeted wedges filled with silt, sand, and gravel sourced from above. For this study, I mapped the distribution of dikes throughout a 30,000 km2 region and collected width and sheet count measurements on several thousand dikes at hundreds of sites between Priest River, ID and The Dalles, OR. All of the dikes observed exhibit identical characteristics and occur entirely within the margins of Ice Age floodways. The dikes are sediment-filled hydraulic fractures that grew incrementally in width and length during discrete, repeated loading events during the Pleistocene, but not before or since. I interpret them as 'flood injectites' triggered by loads imposed by glacial megafloods coursing through the landscape and inundating side valleys. An injectite interpretation is supported by numerous lines of evidence including taper direction, sources of the fill material, occurrence within floodways, and clear crosscutting relationships with dated flood deposits, non-flood deposits, paleosols, and various bedrock units. The dikes are not larger or more numerous near Quaternary faults of the Yakima Fold Belt. Widespread liquefaction was not observed in the study area, though more than a dozen faults capable of generating earthquakes in excess of M 6.0 cross it. Instead, the controls on diking appear closely tied to grainsize, stratigraphic thickness, and landscape position. The largest dikes cluster where silty slackwater sequences are thickest and where floodwaters were deepest. Dikes in the Channeled Scablands are not feeder conduits to sand blows or seismites of any kind, rather they are small-scale sand injectites formed during cataclysmic terrestrial floods. Analogous wedge-shaped dikes with sheeted fills are found in marine turbidite, subaqueous landslide, subglacial, debris flow, and lahar settings, where rapid and repeated overloading of silty-sandy substrates also occurs.

Keywords: clastic dike, sand dike, sand injectite, hydraulic fracture, Channeled Scablands, Missoula floods, megafloods, Columbia Basin, Cordilleran Ice Sheet, Touchet Beds

Definition

The term "clastic dike" describes tabular bodies of sediment that crosscut bedding, including features formed by liquefaction (Fuller, 1912; Obermeier, 1998), forceful injection in deep sea fans and subglacial settings (Jenkins, 1930; Kruger, 1938; Anderson, 1944; Haff, 1944; Lupher, 1944; Newcomb, 1962; Fryxell and others, 1965; Potter and Pettijohn, 1977), passive infilling of open cracks (Newsom, 1903; Collins, 1925; Dobie, 1926; Fackler, 1941; Shrock, 1948), intrusion involving release of CO2-charged volatiles (Diller, 1890; Vitanage, 1894; Harms, 1958; Gonzales and Koch, 2017), freeze-thaw action in permafrost (Alwin and Scott, 1970), subaqueous slumping (Baker, 1973), and other processes (Brown and Brown, 1962; Fecht and others, 1999). 

Previous Work on the Clastic Dikes

The earliest reports on clastic dikes date to the 1800s (Strangways, 1821; Murchison, 1827; Darwin, 1834; Diller, 1890; Cross, 1894; Case, 1895). The first mention of clastic dikes in the Pacific Northwest appears in Dana (1849), in Eastern Washington with Jenkins (1925), and later in articles on the Channeled Scablands (Bretz, 1928-29; Baker, 1973; Waitt, 1985; Smith, 1993; Atwater, 1986). Detailed descriptions of dikes in scabland deposits are relatively few (Jenkins, 1925; Lupher, 1944; Black, 1979; Woodward-Clyde Associates, 1981) and reports containing more than a handful of measurements are rare (Alwin and Scott, 1970; Cooley and others, 1996; Neill and others, 1997; Ward and others, 2006). Otherwise detailed stratigraphic reports on Missoula flood deposits at classic localities inexplicably omit the dikes from stratigraphic columns, despite their ubiquity (Waitt, 1985; Smith, 1988a,b; Lindsey and others, 1996; Benito and O'Connor, 2003; Sweeney and others, 2017). Numerous authors have speculated on the origin of clastic dikes in the Touchet Beds, but few have provided maps, measurements, or models to support their assertions (Flint, 1938; Newcomb, 1962; Bingham and Grolier, 1966; Jones and Deacon, 1966; Beaulieu, 1974; Carson and others, 1978; Shaw and others, 1999; Pritchard and Cebula, 2016; Reidel  and others, 2021). Recent experiments involving bubble trains by Howard and Pritchard (2020) mark a refreshing divergence from this trend.

World's first article. Strangways (1821) is the world's first publication on clastic dikes. In his sketch of a shoreline exposure near St. Petersburg, Russia, yellow clay veins descend from a gravel-capped bed into a thick blue clay below. The dikes form a polygonal network as they criss-cross the gently-sloping beach.

Jenkins was first to describe clastic dikes the Channeled Scablands. Field geologist Olaf P. Jenkins in 1923 examines a large clastic dike in a gravel pit near Lowden, WA. The caption reads, "Clastic dikes in Touchet Beds and dust dune between Touchet and Walla Walla". The dike is sourced in light-colored slackwater sediments that overlie darker flood-laid sands. Source: Washington Geological Survey Archives (No. 00604).

Proposed Origins

Five origins for clastic dikes in the Channeled Scablands have been proposed: Earthquakes (Jenkins, 1925), ground ice (Lupher, 1944; Alwin and Scott, 1970; Black, 1979), slumping/lateral spreading (Brown and Brown, 1962; Baker, 1973; Cooley and others, 1996), desiccation (Grolier and Bingham, 1978), and hydraulic fracture (Pogue, 1998). A dubious sixth, “multigenetic” (Black, 1979; Fecht and others, 1999), suggests the dikes formed by a combination of processes. Cooley (2015) provides a concise summary of the arguments for and against each hypothesis. See Footnote 16.

This Study

I searched for clastic dikes in unconsolidated sediments, partially-lithified sediments, and flood-scoured bedrock exposed along roads, streams, and rail lines throughout the Channeled Scablands between Priest River, ID and The Dalles, OR. Long foot traverses were made through sections exposed in valleys of the Columbia, Snake, Yakima, Spokane, Walla Walla, Sanpoil, Touchet, Tucannon, Umatilla Rivers, and those of tributary creeks. Thick sections of non-flood sediments at Saddle Mountains, Smyrna Bench, Frenchman Hills, White Bluffs, and Palouse Hills were also carefully surveyed. I measured the widths of >3000 dikes at >300 exposures and recorded the number of sheets in >1000 dikes. Field work was conducted between 1995 and 2025. The dikes observed varied in width and length, but were otherwise identical and were found only within the Pleistocene floodway (scabland tracts, backflooded valleys). Fine grained, non-flood sediments beyond floodway margins contain no dikes. The sheeted, wedge-shaped structures appear to have formed by the same mechanism during the Pleistocene and not before or since. This article updates previous reports (Cooley and others, 1996; Cooley, 1996, 2008, 2014, 2015, 2020). The photos and figures included here are mine unless otherwise credited.

Study sites. Locations where sheeted dikes were measured are black dots. White dots are searched locations where no dikes were found. Most of the white dots lie just outside the floodway, shown in gray. The Cordilleran Ice Sheet terminus is shown in blue. Glacial Lake Columbia, mostly north of the ice sheet margin, is shown filled to its 600m-elevation shoreline. Exposures containing dikes are more numerous in the southern part of the study area, where many streams form good outcrops. Good exposures are few between Moses Coulee and Cheney, where loose, patchy gravels lie atop scoured bedrock. The few dikes observed north of the Channeled Scablands occur in sandy outwash and some flood-laid beds. Gravels and Palouse Loess within the floodway generally contain few dikes unless interfingered with or overlain by Touchet Beds. No dikes cut loess anywhere above the local maximum stage for flooding. No dikes were found east of Priest River, ID (Glacial Lake Missoula basin), east of Lewiston, ID (Snake River Valley), west of White Swan, WA (Yakima River Valley), south of Cecil, OR (Willow Creek Valley), north of Hunters, WA (Columbia River Valley), north of Bridge Creek, WA (Sanpoil River Valley), or north of Omak, WA (Okanogan River Valley). The Willamette, Wenatchee, and Methow Valleys were not part of this study. Two red dots near Ellensburg identify isolated, unsheeted dikes of Tertiary age in terraces mapped by Porter (1976) and Waitt (1979).

A typical Touchet-type dike. A vertically-sheeted clastic dike intrudes silty-sandy late Pleistocene megaflood rhythmites (Touchet Beds) at Smith Hollow Rd in the Tucannon Valley, WA. Wall-parallel sheeting is the product of crack-and-fill cycles accompanied by leakoff and skin wall formation. The dikes were filled from the top in discrete pulses.

Dike-sill-dike geometry. Dikes follow least-resistance pathways through the material that hosts them. The dike shown here cuts vertically across silty, low-permeability layers (tan) and parallels bedding where coarser-grained and higher-permeability (gray). The orientation of fill bands flips between vertical in the dike segments and horizontal in the sill segments. Geometry of the entire dike, mostly out-of-plane, is a wedge-shaped, branching structure with blade-like lateral pinchouts (i.e., KGD hydraulic fracture model). The fracture controlled fluid flow in vertical portions while porosity controlled flow in horizontal portions. Vertical and horizontal resistance were nearly equal during diking, though the maximum principle stress was vertical. Hellsgate Recreation Area near Lewiston, ID.

Stratified fills. The sediment within fill bands is commonly stratified with concave-up to planar bedding consistent with top-down infilling. Evidence for lateral flow along strike is present. Repose angles range from flat to greater than 55 degrees, indicating the material was a slurry when it entered the fracture.

Fill bands. This dike contains more than 40 sheets (fill bands). A few distinctive band-pairs, once whole, but now separated by slightly later injections, can be matched up.

Zoomed in. Sheeted fills in detail. Both images are approximately 15cm wide.

More than a Touchet Bed story. The dikes intrude flood deposits, older partially-lithified sediments, and bedrock. Here, a sheeted dike filled with sediment sourced from an overlying bed cuts reworked basaltic colluvium derived from a nearby scree slope. The angular material was swept a short distance downstream by a Missoula flood. Location is near Alderdale, WA.

Huge dikes formed where slackwater lakes were deepest. Very large dikes with widths exceeding a meter often contain >100 fill bands and are most common in the southern part of the Lake Lewis basin, where rhythmite stacks are thickest and slackwater lakes deepest. The dike shown here strikes obliquely to the bladed cutface. Foster Wells Rd-Hwy 395 intersection north of Pasco, WA.

Touchet Beds in Burlingame Canyon. About 40 slackwater beds are exposed at this classic Walla Walla Valley locality near Gardena, WA (Waitt, 1980, 1985; Moody, 1987; Clague and others, 2003). The size, completeness, and accessibility of the Burlingame Canyon exposure is unique in the Scablands region, though other sizable outcrops exist elsewhere in the scablands, including many beyond the margin of Lake Lewis (~380 m elevation contour). Outcrops elsewhere reveal a wider sedimentological diversity than rhythmites in Walla Walla Valley. Touchet-equivalent rhythmite sections are found at Latah Creek, Lacrosse, Cecil, Portland, Salem, and other locations where slackwater lakes formed behind local bedrock constrictions. Photo: Washington Geological Survey Archives (1978, No. 3455). See Footnote 5.

Liquefaction Dikes vs. Sheeted Injectites

Clastic dikes are sediment-filled fractures found worldwide in rocks and sediments from the Precambrian to the Holocene. Most are sand-filled structures formed by liquefaction and the rapid, upward escape of groundwater triggered by strong seismic shaking. Strong shaking, typically above magnitude 6.0, elevates pore fluid pressures in wet, unconsolidated beds in the shallow subsurface, causing silty and sandy material to mobilize and vent to the surface, often forming sand blows and boils (Obermeier, 1998). Earthquakes capable of liquefying sediments are not uncommon in areas near plate boundaries and most clastic dikes described in the literature are upward-pinching structures that contain unstratified to crudely-stratified sandy fills sourced from below. Many are feeder dikes to sand blows (or would be if they had reached the surface) that contain sediment remobilized from beds deposited long before the triggering earthquake.

The clastic dikes described here are different. They are slender, vertically-sheeted, wedge-shaped structures that were filled from the top. They are sediment-filled hydraulic fractures propagated downward into a variety of sedimentary and bedrock substrates. They resemble downsized versions of sand injectites described in submarine turbidite-fan systems (Jolly and Lonergan, 2002; Hurst et al., 2011 Appendix A; Cobain and others, 2016), subglacial settings (von Brunn and Talbot, 1986; Broster, 1991; Larsen and Mangerud, 1992; Dreimanis and Rappol, 1997; LeHeron and Etienne, 2005), sandy lahars (Herriott and others, 2014), and other settings where rapid overloading and hydraulic fracture occur.

Reinjection and the development of sheeting in dikes. Growth of sheeted, or composite, dikes through reinjection is illustrated in a figure by LeHeron and Etienne (2005) revised slightly by me. Since each individual sheet (dikelet) tapers downward, the composite dike to which they belong will also taper downward. A dike containing multiple dikelets injected from above will never achieve an upward-tapering form.

Dikes and flute casts. (A) A typical sheeted clastic dike in Touchet Beds (slackwater rhythmites) containing a range of grainsizes. Light-colored silt partitions (skin walls) separate sheets from one another. This example contains ~12 sheets and is filled with silty, sandy sediment resembling the host material. Location is Umatilla Basin at Cecil, OR (slackwater Lake Condon). (B) A gravel-filled dike intruding a gravelly eddy bar deposit is truncated at its top by a younger floodbed. Its fill reflects the host formation and is crudely sheeted with less prominent skin walls, reflecting a lack of fines in the gravel. Dikes in coarse-grained deposits are often stubby (lower length-to-width ratios) than dikes in fine-grained sediments. Location is near Exit 147 off I-84 at the mouth of Willow Creek. (C) Examples of flute casts that decorate the interior faces of skin walls. Upward-pointing noses are a clear directional indicator of filling from above. Flood-transported sediment entered a fracture from the top. Quarter for scale. Location is Walla Walla Valley, WA (slackwater Lake Lewis). (D) A dike with ~10 sheets is filled with a mix of sandy flood sediment and quartzite cobbles liberated from the underlying Ellensburg Fm. Hoe is 28 cm long. Location is Emerald Road near Granger, WA (slackwater Lake Lewis).

Size and Shape of Dikes

The wedge-shaped dikes, most numerous in the Touchet Beds, intrude a dozen other geologic units. Most dikes measure <15 cm wide and contain fewer than a dozen sheets. Large dikes contain >100 fill bands, exceed 2 m in width, and penetrate to depths >50 m. Dikes in silt-sand rhythmites are long and slender (H >> W), while those in coarse, laminated sand or gravel are few in number, crudely sheeted, and stubby. Dikes that penetrate bedrock (Columbia River Basalt) are slender. The average width of a sheet is around 1 cm. The widest sheet that I have observed was 30 cm. Preliminary calculations on data collected from several thousand dikes suggest there may be a length-to-width ratio limit of ~40 for most Touchet-type dikes. Most dikes are sediment-filled tensile fractures (Mode I joints) that tend to branch as they pinch out. Shear plays only a minor role in their formation. In three dimensions, the dikes resemble blade-shaped hydraulic fractures with curved fronts (i.e., PKN fracture model for fluid-driven fractures (Perkins and Kern, 1961; Nordgren, 1972; Belin and Carey, 1997; Rahman and Rahman, 2010).

Fill Materials

Sedimentology of dike fills closely resembles the composition of Touchet Beds and, to a lesser extent, the local bedrock. Fills typically contain a mix of quartz-plagioclase-muscovite grains (Touchet Beds, Palouse loess) with a component of basalt (CRB). Along the margins of the Channeled Scablands, dike fills contain material reworked from Ellensburg Fm/Ringold Fm/Dalles Group or gruss. Gravel-filled dikes are relatively uncommon, buy where found contain basaltic clasts or a mix of basalt and quartzite. Near Walla Walla, nearly all dikes are filled with  Touchet Bed sediment. At Granger, WA, near the western margin of the Scablands, dikes are filled with a mix of Touchet Bed sediment and quartzite gravel derived from the Ellensburg Fm (Snipes Mountain Conglomerate). At West Foster Creek near the northern margin, dikes contain gruss shed from deeply-weathered granites of the Okanogan Highlands (Colville Batholith).

Sheeting and Growth

The dikes are conspicuously sheeted structures that grew in pulses (crack-and-fill). Vertical sheeting developed as dikes widened and lengthened, while coherent "stacks" of sediment within sheets record discrete increments of infilling as the crack tip advanced. Three types of dikes occur in the study area: Single-fill, compound, and composite (Hayashi, 1966). Single-fill dikes contain a single body of sediment between two skin walls, consistent with a fracture that opened and filled once. Compound dikes contain two or more sheets with skin walls between. Multiple fractures opened and filled during a single diking event. Composite dikes contain multiple sheets injected during more than one diking event (reinjection). In composite dikes, new sediment is introduced into an older dike of any type during several successive events separated in time. New sets of sheets are sourced from different horizons and commonly have distinctive characteristics. Contrasts in grain size may be evidence of a variable and changing sediment source during single diking events and changes in the nature of the sediment available to new dikes over time.

Growth in stages. Sheeted dikes grow sheet by sheet as illustrated above. New sheets intrude alongside older ones (B parallels A) or split older ones (C2 splits B). The example dike, photo at left, contains 7 sheets formed in 4 widening stages (crack and fill pulses). Growth stages: A = 1 sheet, B = 1 sheet, C = 3 sheets, D = 2 sheets. Except in dikes with very few bands, the number of fill bands is always greater than the number of injections that split one band into two.

Stacks inside sheets record incremental fracture growth. I measured the thickness of 20 coherent packages of sediment, or "stacks", in a few dikes exposed in a roadcut at Touchet, WA. Each stack constitutes a portion of a sheet, therefore each sheet is composed of many stacks. Planar or cup-shaped silt partitions separate each stack from those above and below. Abrupt changes in grainsize and bedding angle commonly occurs at the bounding partitions. Stacks are interpreted as discrete pulses of sediment entering a fracture and represent increments of fracture lengthening (crack tip advance). The height of most stacks measured less than a meter, but one example exceeded 3 m. Stack height appears random below about 2m. Stacks taller than 2m were few and most were located high in the exposure, out of reach.

Descend and branch. Sheeted dikes cut downward (per descendum) through sandy Missoula Flood deposits at Latah Creek west of Spokane, WA. Small downward-pinching spurs mimic the form of the larger dike.

Arris and aperture. A dike is a sediment-filled fracture with a 3D shape loosely resembling an axe blade. Hydraulic fractures have a width (aperture), a volume, and a curved, irregular leading edge (arris). They thin in the directions they propagate (downward and outward). The shape of a dike's cross section changes depending on where the section is placed or where a dike intersects the plane of an outcrop (a natural section plane). The figure above shows a typical sediment-filled hydraulic fracture (clastic dike) that tapers both vertically and horizontally. Its 2D cross section appears to taper downward if sliced at Plane C, upward if sliced at at Plane B, and both upward and downward if sliced at at Plane A. The apparent taper direction (inferred propagation direction) can vary depending on where a dike intersects a particular cutface.

Pleistocene dikes in older sandstone. Energetic flooding down the Columbia Gorge incised deep, v-shaped gullies into fluvial sandstone of the Chenoweth Fm (Dalles Group) and filled them with gravel. Floodwaters at this site near The Dalles filled the lower 7 km of Chenoweth Creek valley to an elevation of 340 m (O'Connor and others, 2020). The gravel-filled, parallel-sided dike shown here exits the bottom of a flood-cut, gravel-filled gully and tapers downward below the road grade. The dike is filled with the same material that fills the gully. Hundreds of flood-deposited boulders mantle the bench-like surface above the roadcut. Chenoweth Creek Valley, OR.

Truncation and reinjection. Two episodes of injection, separated in time, are preserved in this composite dike. The first cuts Bed A. The second cuts Bed B and Bed A. The younger dike B merges with the older A, following the path A established. The dike is truncated twice at bedding contacts. This geometry is impossible with upward fluid escape (i.e., earthquake recurrence). Downward diking repeats with flooding.

Low-angle and bedding-parallel faults offset dikes. A sheeted dike (red) is offset by a set of small normal faults (yellow), some parallel to bedding (blue). Faulting appears to be the result of slumping well after all beds were deposited (R1-R5) and dike was in place. Last Chance Rd near the Whitman Mission.

Polygonal Networks

Burned fields and bladed cutslopes expose polygonal dike networks in plan view (Silver and Pogue, 2002). Horizontal exposures reveal intertwining and crosscutting relationships between intersecting dikes. Well-developed polygonal networks containing many wide dikes occur in sandy benches lining backflooded valleys and certain flood-cut coulees. I have observed no relationship between polygonal networks of dikes and columnar jointing in the underlying basalt; bedrock joints do not translate into the overlying sediments. Dike polygons are recognized iin several different types of bedrock.

Silt Skins

Thin silt partitions (skin walls) comprise the outer walls of dikes and separate internal sheets from one another. Silt skins form when pore water migrates out of the fill, through the fracture wall, and into the drier surrounding material. Drainage directly to the formation appears to be the primary way dikes dewater. Dikes that penetrate impermeable bedrock such as basalt lack outer skins, but contain inner ones, indicating pore water moves laterally into adjacent sheets, possibly remaining there for a time before draining to the formation. Silt rapidly coats the fracture, thickening  into a continuous layer as more and more fines are screened against the wall. Skin thickness is typically 1–10 mm, sufficient to form an effective seal. Skin wall building and crack sealing begins immediately after sediment enters the fracture and appears to progress quickly. Concrete slurry walls used in heavy construction (i.e., trench-type building foundations) form in much the same way as skin walls in clastic dikes.

Flute Casts on Skin Walls

Upward-pointing flute casts ornament the faces of skin walls. They unambiguously indicate sediment entered the fractures from the top. The fluting is not sparse or subtle; the forms are obvious and present in nearly all dikes.

Leak-off Halos

"Leakoff halos" are firmer and discolored zones that extend a few centimeters beyond the outer skin walls of some dikes. Like skin walls, leakoff halos are a product of dewatering. They consist of fines that were not screened at the dike wall.

Lumpkins

"Lumpkins" are bulbous forms on the exterior walls of some dikes. They are convexities formed by leakoff. Leakoff indicates the host sediment during diking was ice-free and drier than fracture-filling slurries (i.e., vadose zone).

Rip-up Fragments in Fills

Fragments of older fills, chips of skin walls, and host material comprise dike fills. In places where dikes cut white tephras such as the Mount St. Helens Set S tephra, traces of ash are sometimes visible in the fill.

Fluted walls. Flute casts with upward-pointing noses decorate the interior silt walls of Touchet-type clastic dikes. Flutes are unambiguous directional indicators. Sediment entered from the top. Identical fluting is present in nearly all dikes throughout the study area. Quarter for scale.

Diking and leakoff. A fluid-driven fracture (hydraulic fracture) propagates by the advance of the crack tip. Tip advance in a clastic dike is jumpy and growth incremental. Fluid pressure is generated at the ground surface during megafloods, similar to a shut-in well bore in gas reservoir fracking. As pressure in a fracture rises, its aperture widens and is immediately filled by a slurry of pressurized sediment (proppant). Leakoff beings immediately, forming silty skin walls. Repeated fracturing, filling, and dewatering creates the conspicuous vertically-sheeted fills. Figure modified from Phillips and others (2013).

Leakoff halo. Fining and cementation is apparent just beyond the margin of some dikes. This leakoff halo is evidence of diffusion of pore water and fines out of the fill and through the dike wall during injection and for a short time after. While fines migrate during diking, cementation is diagenetic and occurs later. Hwy 24 near crest of Yakima Ridge.

Leak-off lumpkins. The outer surface of a dike's outer skin wall is decorated with with bulbous structures formed as the fill dewaters. These "lumpkins" look very much like tiny load casts, but are formed by the outward diffusion of pore water into the drier surrounding sediment. Walla Walla Valley.

Lumpkins aplenty. Leak-off creates bulbous forms on the outer walls of some dikes. Hwy 397 west of Finley, WA.

Lumpkin-o-rama. Bulbous forms on thin silt walls are easily damaged despite a soft brush. White Bluffs, WA.

Stress Orientation Determines Dike Taper Direction

Most of the dikes are vertical to nearly vertical structures that typically crosscut bedding at high angles. Sills are relatively few and most commonly branch off from larger vertical dikes. Sills tend to pinch out within a few meters. Overall, dike/sill shape is consistent with a maximum principle stress (O1) oriented vertically (vertical load). Fractures appear to have opened perpendicular to the load in tension without much shear (i.e., joints not faults). Dikes strike randomly and form polygonal networks when viewed from above, consistent with nearly equal intermediate and minimum principle stresses (O2, O3) oriented horizontally. Equal horizontal stresses also explains why dikes so often twist about their vertical axis (change strike with depth). Stairstepping, branched, and en echelon forms hint at a stress field changing from tension to shear at different depths during propagation. Shear may become more apparent and perhaps the dominant mode of deformation as dikes grow beyond some threshold length and propagation begins to slow. Since most in this study are composite dikes that increased in number, length, and width over time, dike spacing (fracture spacing) must have decreased as network density increased.

Dikes in Faulted Flood Deposits

Small normal faults in the Touchet Beds do not appear to be a primary control on diking. The faults, typically with offsets <1 m, are not numerous and, where present, are both followed by dikes and cut by them. Most dikes cut cleanly through unconsolidated sediments and appear to pioneer new paths independent of obvious faults or joints. Indeed, evidence of shear is quite modest in most Touchet Bed outcrops. At certain locations such as Touchet River Road, larger listric faults with meter-scale offsets obviously redirect dike paths, but fault control is generally contained within the outcrop. Thrust faults are uncommon in scabland deposits and their influence on diking is even less clear. Slip along bedding planes, very common in slackwater sections, is often difficult to see. Stairstepping dikes offset by sets of small, low-angle faults provide clearer indication that bed-parallel slip has occurred.

Dikes near Mapped Faults

Eastern Washington is cut by many sizeable thrust faults of the Yakima Fold Belt and other structures such as the the Hite Fault. Sheeted dikes are known to intrude folded and faulted basalt flows and lithified interbeds at Umapine, Touchet, Rattlesnake Hills, Horse Heaven Hills, Alder Ridge, Gable Mountain, Cecil, and elsewhere. The association of active faults and clastic dikes would appear important. In fact, many suggest a causative link between the faults and the dikes exists (Camp and others, 2017, Fig. 50; Reidel and others, 2021, Fig 8.). However, my own traverses through the sections of post-CRB sediments preserved atop fault-bounded ridges of the Yakima Folds have revealed far fewer and far smaller dikes than sections located in benches and flat-floored basins located far away from mapped faults. For example, no sheeted dikes were identified in a traverse of the remnant Plio-Pleistocene section preserved along the Saddle Mountain crest (45 km-long traverse). A complete traverse of thrust and normal fault-bounded Smyrna Bench (20 km) with its numerous gully exposures also revealed few dikes, none large. A traverse of the White Bluffs along strike of the Gable Mountain fault (25 km) revealed relatively few dikes, all sourced in flood deposits. Few dikes were found in the numerous cuts and quarries through the same section at Frenchman Hills and neighboring Royal Slope. No dikes occur in fine-grained sediments spectacularly cut by the Arlington-Shutler Butte Fault, exposed along I-84 west of Arlington, OR (more info HERE). Plio-Pleistocene sediments exposed in shoreline bluffs at the USBOR Lind Coulee fault trenching site (West and Shaffer, 1988) are all but devoid of dikes. In fact, all dikes I observed fell below highstand trimlines of the Missoula floods (~366 m near TriCities and higher to the north) despite abundant sandy loess and alluvium in upland areas.

Distribution

Sheeted dikes are not isolated features; they number in the hundreds of thousands if not millions and are distributed throughout an area exceeding 30,000 km2. Great distances separate outcrops containing dikes with identical characteristics. For example, sites near Kettle Falls, WA and Salem, OR are separated by more than 500 km. The dikes are not found above the local elevation of maximum flooding (~366m in south-central Washington and higher to the north), nor in unconsolidated sediments beyond the margins of Ice Age floodways. No dikes are known in Palouse Loess outside of flood coulees. Identical dikes occur in close proximity to mapped Quaternary faults (i.e., Wallula fault zone) and distances >150 km from them. They are largest, most abundant, and best-exposed in thick sections of silty slackwater rhythmites.

Age

Field relationships constrain the timing of dike injection to between ~1.8 Ma to ~14 ka, the period coinciding with ice sheet growth and scabland flooding (Easterbrook, 1994; Baker and others, 2016; Waitt and others, 2016). While an important set of cemented dikes associated with "ancient" flooding exists, most dikes formed late, between 18–14 ka. Except for crystalline bedrock of the Okanogan Highlands, the dikes penetrate all formations exposed in the Channeled Scablands, including Miocene Columbia River Basalt, Miocene-Pliocene Ellensburg/Latah Fm sediments, Miocene-Pliocene Chenoweth Fm and other Dalles Group sediments, Pliocene Ringold Fm, a distinctive Pliocene-Pleistocene calcrete-fanglomerate-loess complex ("Cold Creek unit"), pre-Late Wisconsin cemented gravels, silt-pebble diamicts, and loess. The dikes cut the Mount St. Helens Set S tephra (16 ka), but not the Mazama Ash (6.8 ka). No dikes are known to intrude Holocene alluvium east of the Cascade Mountains.

Touchet-type dikes are slender, sheeted, and wedge-shaped. Each Missoula flood rhythmite, numbered R1 through R7, represents a separate flood. A clastic dike that descends through the section originates at the base of the youngest bed, R7. Other dikes nearby descend through the stack the same way. Note the dike cuts a clean path through the host sediment and does not follow an older fracture set or a rubbly zone between laterally-spread blocks. Bedding contacts are not offset along the dike or tilted into it. No low angle sliding surface is present in the outcrop. The stack of Touchet Beds lies in its original position atop basalt bedrock, exposed at the base of the cut. The sediment that fills the dike was supplied from above, not by a liquefied layer somewhere below R1; it does not feed a sand blow (i.e., Obermeier, 1998). The top and bottom of the dike clearly visible. It begins at the base of R7, widening from a small sag. Bedding in R7 grades smoothly up from the sag as if diking occurred at the beginning of deposition. Both branches taper to a point. This dike is typical of clastic dikes found throughout the megaflood region. Burlingame Canyon in Walla Walla Valley near Gardena, WA.

Initiation revealed in small dikes. Diking is sometimes halted early, resulting in very small dikes. These small, unassuming features often reveal far more than their larger, more spectacular counterparts about how the fracture-and-fill process begins. Here, two small, single-fill dikes descend from the coarse-grained base of a Missoula flood rhythmite. The dikes propagated downward and were filled from above. No visible flaw appears to control where either initiated. Because it is sourced at the base of the bed, we can assume diking was triggered by the initial onrush of water up the Tucannon Valley. The dike on the left strikes obliquely to the face of the outcrop and appears much wider than the one on the right, which strikes perpendicular to the face. However, the width of both dikes is about the same (~3 cm). Starbuck, WA.

Lessons from Warden Canal. I discovered this canal cut through ~10 sandy rhythmites a few years ago near Warden, WA. It contains many important features and relationships rarely seen roadside exposures. Sags, load casts, contorted bedding, and sets of small wedge-shaped dikes occur at nearly every bedding contact and formed during the deposition of each bed. A large dike is truncated by a prominent erosional surface with wetland soil features above (long hiatus between flood events, persistent high water table). A conspicuous 5 cm-thick gray layer just above the truncation surface is probably reworked volcanic ash; I've found it in other outcrops nearby. Near the top of the exposure, deformed wetland deposits were overridden by a late flood carrying gravel, causing them to liquefy. If you interpret the dikes as seismites, then you must ignore the obvious relationships between dikes, sags, and deposition elsewhere in this particular exposure and in many others around the region. Deformation was coincident with the deposition of individual beds and repeats.

Injection during flooding. My conceptual model for sheeted clastic dikes in the megaflood region developed from relationships observed in the field. Downward injection occurred only during Pleistocene overland flood events and associated periods when slackwater lakes were present. Flood loads fractured the relatively dry, brittle substrate allowing sediment circulating at the base of the flood (or soupy lake bottom) to immediately fill the fractures, forming dikes.

Flood injectites vs. sand blows. (A) The sketch illustrates differences between clastic dikes formed by liquefaction (sand blows and fluid escape structures) and those formed by floodwater loading and hydrofracture (flood injectites). Liquefaction dikes propagate upward and are sourced in wet, sandy beds deposited sometime in the past and remobilized by strong shaking. Liquefaction often produces feeder dikes that vent to the surface as sand blows (volcanic edifices of sand). Flood injectites are sediment-filled filled hydrofractures that propagate downward from the surface. The fractures are immediately filled with sediment sourced in circulating bottom currents of glacial floods. Liquefaction dikes in A cut younger strata and are filled with older sediment. Injection dikes in B cut older strata and are filled with younger sediment. (B) My dike-fill generations concept sketch explains the formation of sheeted clastic dikes in aggrading flood sediments (each bed = one flood). The four geometries represent the range of forms found in the study area: a). Unsheeted - Single-fill, b). Sheeted - Multi-fill Compound, c). Sheeted - Single-fill Composite, d). Sheeted - Multi-fill Composite. Compound = Multiple fill bands injected during a single event. Composite = Multiple fill bands injected during two or more events separated in time.

Dike abundance, shape, and grainsize. Sediment porosity (millidarcy, mD), permeability (percent, %), and dike shape are correlated. (A) The tightness of the formation, a function of grainsize in flood deposits, determines whether pore fluid pressures will build or disperse and whether slender or stubby dikes will form. Silty mixtures are tight and fracture when stressed (pore fluids move in fractures). Sandy-gravelly mixtures accommodate the same stress via matrix flow (pore fluids flush through interconnected pores). (B) Diking can occur in all phases of flooding, but dike fills are sourced at or very near the surface. Coarser fills correspond with the initial flood rush (coarse sand and gravel dikes), while finer fills correspond with the slackwater phase (silt-sand dikes). If a flood carries only finer material (no gravel), then all dikes will contain silty fills (i.e., northern Walla Valley, Skyrocket Hills, and loess islands in the Marengo-Benge area). Dikes with coarse fills were triggered by floods. Dikes with fine fills were triggered by lake loads.Dikes with coarse fills were triggered by floods. Dikes with fine fills were triggered by lake loads. (C) Numerous slender, sheeted dikes correspond with high silt content source beds, slackwater settings, prolonged loading (deep lake), and better preservation (protected valley settings). Sparse, crudely-sheeted, stubby dikes form in coarse sand, laminated sand, and gravelly bar deposits that lack silt.

Importance of a dry vadose zone. A dry vadose zone sandwiched between the base of the flood and the water table may have created a wet-over-dry-over-wet situation that facilitated diking. Brittle fractures initiated at the ground surface (top of the dry interval), resulting in wedge-shaped dikes rather than upward-pinching liquefaction dikes.

Discrete deformation. Dikes fill tensile, Type I fractures. Shear is rarely involved. Deformation associated with diking does not extend beyond the dike wall. Material surrounding the dikes is extended slightly to accommodate the fill, but otherwise tends to remain undeformed. Clear bedding contacts and delicate bedforms in the host sediments continue across each dike in the photo. Dikes in the photo are filled with gray Touchet Bed sediment and intrude oxidized, quartzite-bearing, fluvial sandstones of the Miocene Ellensburg Fm. Snipes Mountain near Granger, WA.

Clean crosscuts. A sand-filled dike cuts cleanly across several silt-sand rhythmites at Starbuck, WA.

Younger dikes intrude older deposits. A sheeted dike sourced in late WisconsinTouchet Beds cuts a thick stack of older cemented loess, calcrete, and weathered fanglomerate near Finley, WA.

Pleistocene dikes in Miocene basalt. Sheeted sand-silt dikes, intrude Columbia River Basalt in certain locations where Touchet Beds overlie flood-scoured basalt.The dikes exploit joints in the bedrock. A.) Weaver Pit near Gardena, Walla Walla Valley, B.) Hwy 12 at Alpowa Creek, Lewiston Basin, C.) Hwy 14 near Alderdale, Umatilla Basin.

Gravel infill from above. Unconsolidated flood gravel fills a clastic dike in tuffaceous sandstone of the Chenoweth Fm at The Dalles, OR.

Pleistocene dikes in Ellensburg sandstone. Silt-sand dike cuts a crossbedded fluvial sandstone of the Ellensburg Fm at West Foster Creek near Bridgeport, WA. The location was overridden by glacial ice several times.

Sheeted fills in fractured basalt. Sheeted sand dike fed from above cuts Columbia River Basalt at Prosser, WA. An old fracture in the rock appears to have been widened a combination of floodwater erosion (incipient block topple similar to Finley Quarry) and by incremental injections of pressurized sediment during the slackwater period.

Early to Middle Pleistocene dikes cut Pliocene Ringold Fm. Emplacement of downward-tapering dikes, now partially-cemented, is associated with ancient scabland flooding at Ringold Road at White Bluffs, WA.

Gray dike in red fan gravel. Gray dike sourced in unconsolidated flood-laid sediment cuts older, reddened fanglomerate shed from the north flank of the Saddle Mountain anticline. Smyrna Bench, WA.

Liquefaction in Eastern Washington

Liquefaction occurs in unconsolidated sandy sediment when pore fluid pressure increases suddenly, causing the loss of resistance to shear, fluid escape, and reorganization of the grain-to-grain support framework (Lowe, 1975). Pore water commonly escapes upward from a liquefied bed toward the surface (down the pressure gradient), dragging sediment with it before grains resettle into a new, consolidated configuration. The expulsion of the water-sediment slurry can form clastic dikes and sand blows if dikes vent to the surface.

To date, no liquefaction features have been unambiguously identified in seismic trenches in Eastern Washington or nearby portions of northeastern Oregon. Certainly, no widespread liquefaction pattern is apparent in the region.

• Ahtanum Ridge-Burbank trench near Yakima, WA (Bennett and others, 2016).

• Toppenish Ridge trenches above Pumphouse Rd (Campbell and Bentley, 1981; Campbell and others, 1995).

• Wenas Valley trench (Sherrod and others, 2013).

• Saddle Mountains trenches at Smyrna Bench (Bingham and others, 1970, Plates 4,5,6).

• Buroker trench southeast of Walla Walla (Farooqui and Thoms, 1980).

• Lind Coulee trenches at O'Sullivan Dam-Lind Coulee (GEI/West & Shaffer, 1988).

• Gable Mountain trenches at the Hanford Site (Bingham and others, 1970; Golder Associates/PSPL, 1982).

• Spencer Canyon trench near Entiat, WA (Sherrod and others, 2015).

• Starthistle/SUK trench east of Wallula Gap (Angster and others, 2020).

• Kittitas Valley trench (Huddleston, 2022; Dr. Walter Szeliga, personal and written communications, 2023).

• Gate Creek trench near Mt. Hood, OR (Bennett and others, 2021; Madin and others, 2021).

Two studies report finding liquefaction features near Wallula, WA. Kienle/Foundation Sciences (1980) reported possible liquefaction at Finley Quarry west of Wallula Gap (Wallula Fault Zone). The blobby forms are small, disconnected from a source bed, and partially trend with bedding. A USGS geologist later interpreted the features as products of strong shaking (Sherrod and others, 2016), but co-investigators disputed the interpretation in a separate report (Coppersmith and others, 2014). Angster and others (2020) reported liquefaction in dry Holocene loess exposed in a trench opened east of Wallula Gap. The surface lineament targeted for trenching has since been revealed to be an old ranch road, not a fault scarp. Remnants of old pavement are clear in the trench wall and in aerial photographs. No fault was discovered in the trench and Touchet Beds beneath the "liquefied" loess remain undeformed. Read my critique of the Starthistle trench project HERE. At both sites the purported liquefaction features are few, small, and anomalous. Nearby outcrops do not contain similar features. In both cases, I believe the features have been misinterpreted.

Paleoseismic trench locations in the Yakima Fold Belt. Trench locations across surface scarps and mapped Quaternary faults. The Spencer Canyon site is located ~60km north of the Kittitas Valley site. Paleoseismic trenching has revealed no connection between sheeted clastic dikes and movement of Yakima Fold Belt faults. Basemap by Lidke and others (2003). Box area on map is ~44,000 km2 (17,000 square miles).

Soft sediment deformation triggered by floods and slumps

Soft sediment deformation caused by rapid sedimentation, loading, and mass wasting, but sometimes misinterpreted as earthquake-triggered liquefaction are shown below.

Deformation of soupy and firm sediments. The swirls, flames, and dike-like features pictured here formed during a Missoula flood, that is, during sedimentation. The now-deformed sediments were first laid down flat and partially consolidated. At some later date, the soupy sediments were overridden by a flood and thoroughly reorganized. A combination of loading by sediment and water and drag by fast-moving currents is responsible for the pattern of deformation seen here. White Bluffs, WA.

Deformation during deposition. Flame structures in the light-colored mud formed during a flood, which deposited a thick bed of gray sand. A dense, sand-choked current moved left to right over the soupy, unconsolidated bed, dragged some of the bottom sediment upward and into the flow. The silty-clayey sediment holds together, forming spectacular flames. White Bluffs, WA.

T-shaped mudsquirts are syndepositional structures. Rapid deposition of a sand bed on top of soupy lake bottom mud with consolidated varved beds below triggered the rise of t-shaped mudsquirts. Note how sand swirls with the mud "dikes". The deformation resulted from rapid deposition and loading, not shaking. The gray sand was dumped by a Missoula flood, which temporarily disrupted quiet-water deposition in Glacial Lake Columbia. West shore of Sanpoil Valley, WA.

Flood and repeat. Three flood rhythmites exhibiting an identical bedform progression - clear indication of repeated, syn-depositional fluidization in the soupy, upper portion of a few Touchet Beds. Ringold Rd, WA.

Slumps in proglacial lake beds near the northeastern limit of scabland flooding. Deformation in varve sets at Priest River, ID.

Wrinkled lakebeds. Typical mass wasting, not worrisome seismicity at Priest River, ID.

Slumps and flames. Liquefaction triggered by mass wasting within a thick pile of muddy varves (lake bottom deposits) punctuated by flood-laid sand beds at Priest River, ID. A sketch from my fieldbook from April 2020. BS = Bedded sand, DS = Deformed sand, DM = Deformed laminated lacustrine mud (varves), FM = Flat-lying laminated mud, MS = Deformed massive sand. Read more about the Priest River site HERE.

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In Depth: Gable Mountain Seismic Trenches The Gable Mountain trenches opened across two thrust faults by Golder Associates/Puget Sound Power and Light at the Hanford Site are instructive (Bingham and others, 1970 Plates 8, 9; Golder Associates/PSPL, 1982). The South Fault displaces Miocene basalt and the Rattlesnake Ridge sedimentary interbed that separates Pomona and Elephant Mountain flows ~50'. The overlying Hanford Fm sediments (Missoula flood deposits) were not displaced. The Central Fault displaces the Rattlesnake interbed by 182' and the Hanford Fm by only 0.2' (Reidel and others, 1992, p. 43-44). No liquefaction was found in any trench at Gable Mountain. A single clastic dike, sourced from above and filled with flood-laid gravel, descends into brecciated basalt (Trench log GT-2 in Reidel and others, 1992, Figure 39, p. 45). No other dikes were noted in the 92'-long trench.

J.A. Blume and Associates Engineers (1970) summarized what geologists observed at Gable Mountain,

These anticlinal features were investigated by surface mapping and trenching. The presence of previously mapped, transverse faults at Gable Butte could not be substantiated. A well defined thrust fault with about 70 feet of displacement was exposed by trenching at Gable Mountains. This fault is known to be older than 10,000 years and probably is 40,000 years old. It was concluded that faults there are inactive. A second thrust fault was also identified at Gable Butte and similar conclusions were reached.

Philip S. Justus, project geologist for the Nuclear Regulatory Commission, clearly linked the dikes to flooding, not faulting. His report to management is outlined below (Justus, 1980),

• Flood deposits on Gable Mountain bear a close resemblance to typical Missoula flood deposits.

• Two distinct cycles of [Ice Age flood] deposition are present on the north side of Gable Mtn; possibly three on south side.

• Clastic dikes on Gable Mountain are similar in lithology and fabric to those found elsewhere in the Pasco Basin.

• Clastic dikes associated with each overlying [flood] cycle are found in Trenches CD-8, G-2, and G-3.

• The youngest clastic dikes originate from the base of the coarse upper unit of flood deposits which is bounded at the top by St. Helens S ash as found in Trenches CD-4 and G-1.

• Clastic dikes in Trenches CD-5 and G-3 are displaced by shearing on the fault plane (CD-5) and in the hanging wall (G-3).

• In Trench G-3 displacements in the flood deposits appear to post date the youngest clastic dike.

• Shears, possibly associated with the thrust fault, appear to cross and slightly displace clastic dikes in the footwall in an area of Trench CD-6.

• Clastic dikes along fault plane in Trench CD-6 have slickensides surfaces with strikes parallel to the dip of the fault.

• Oriented slickensides in clastic dikes parallel to slickensides in gouge on fault breccia (Trench CD-5).

• Wherever fine-grained material is present along fault plane, slickensides are present.

Key takeaways from the Gable Mountain trenches are a.) clastic dikes that intrude fractured basalt are sourced unconsolidated Missoula flood deposits and are typical of Touchet-type dikes observed elsewhere in the region, b.) the dikes are not large or numerous despite their close proximity to mapped faults and surface scarps, c.) liquefaction features were not observed in the trenches, d.) crosscutting relationships suggest most, if not all, of the faulting occurred prior to Late Wisconsin flooding and only a small movements on Gable Mountain faults post-date flooding and diking.

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In Depth: Lower Lind Coulee Fault Seismic Trenches

Paleoseismic trenches opened across the Lind Coulee Fault by Michael West/GEI exposed a few clastic dikes in sheared basalt. The Lind Coulee Fault is an eastern extension of the largerFrenchman Hills thrust. The fault, which places Miocene Roza basalt over Pleistocene Palouse loess, is well-exposed in a shoreline bluff along the south shore of O'Sullivan reservoir west of the Rd M SE bridge.

Lind Coulee West Trench Site. Trenches at Lind Coulee were opened in the 1980s as part of a seismic safety study of O'Sullivan Dam. The U.S. Bureau of Reclamation operates the dam which spans the head of Drumheller Channels near MarDon Resort. The dam impounds Potholes Lake. Lower Crab Creek, empties from the west through Lind Coulee. Hwy 262 crosses the dam.

Findings in the Lind Coulee West Trench are similar to those at Gable Mountain, but took the team of investigators more time and a considerable amount of back and forth to arrive at an acceptable interpretation (Grolier and Bingham, 1971, 1978; Galster/USBOR memo, 1987, "Area No. 2"; Lefevre and MCConnell memo, 1987; West and Shaffer, 1988; Shaffer and West, 1989; Reidel and Campbell, 1989, "Stop 21-A", Figure 14; Geomatrix Consultants Inc., 1990, "East Fault Exposure"; Reidel and Fecht, 1994; Schuster and others, 1997; Lidke and Haller, 2016).

Pleistocene dikes intruding fault gouge initially got investigators excited,

The Lind Coulee trench initially presented strong circumstantial evidence for fault displacement of [basalt, a very old reverse-magnetized loess, and a younger less cemented loess]. The evidence for displacement was magnified by the protruding knob of brecciated basalt [seven meters from west end of NE-trending trench], the apparent overturned contact with flood deposlts on the north side of the knob, flood sands injected along a shear plane in the fault zone and discontinuity of the petrocalcic horizon and infiltration of loess north of Station 7 [near west end of trench]. The geometry of flood deposits overlying the paleosol on the footwall block was also suggestive of colluvial wedge geometry.

Upon further investigation, West and Shaffer modified their interpretation,

In spite of this body of circumstantial evidence, we could find no evidence of shearing, tectonic displacement or colluviation characteristic of surface fault rupture. The [flood-deposited] sands along the shear plane appear to have been injected hydraulically along the plane rather than dragged along it.

They ultimately conclude dike injection post-dated faulting,

The lacustrine silt [that separates “intermediate” flood deposits from “youngest” flood deposits] could be traced as a continuous, uninterrupted horizon across the main fault zone, indicating with 100% certainty that the fault had not moved since deposition of the silt layer. Careful excavation of Unit 5B [“intermediate”] flood deposits disclosed no evidence of shearing or tectonic colluviation. These deposits were in intimate contact with the eroded basalt surface on the hanging wall and exhibited an open-work fabric that we attribute to high energy flood deposition.

Busacca and McDonald (Appendix V) conclude the flood deposits exposed in the trench are not related to the most recent episodes of flooding (about 12 to 16 Ka) but are older…based on soil development and stratigraphic position that the age of flood deposits in the Lind Coulee West area is 40 to 50 Ka. The last surface fault displacement, therefore, occurred before 40 to 50 Ka.

The apparent injection of flood sands along a shear plane in the fault zone is more difficult to explain. We are of the opinion that the sand was injected hydraulically from the top down. The sands filling the shear however do not appear to be continuous with flood deposits mapped as Unit 5 [“intermediate” flood deposits].

Similar injection of flood sands along shear planes was noted in fault trenches excavated on Gable Mountain (DOE/Westinghouse, 1987b).

The authors invoke interpretations by Woodward-Clyde Consultants (1981), namely the few dikes formed by,

…either hydraulic injection associated with catastrophic flooding or hydraulic injection resulting from fault movement and liquefaction offer reasonable interpretations for the origin of clastic dikes including the feature in the Lind Coulee West trench.

They dutifully entertain an alternative origin for the dikes (liquefaction), though no evidence was found,

Another possibility is that the sands were injected from below and are part of an older flood deposit preserved deeper in the footwall. The exposures in both cross-cut trenches suggest older flood deposits are indeed involved in faulting and could be preserved at depth in the footwall and locally along shear planes…

Lind Coulee Fault at O'Sullivan Reservoir. The Lind Coulee Fault is a south-dipping thrust that places Miocene basalt (Wanapum Roza flow) over younger sediments. There are several splays. Grolier and Bingham first identified the fault (Grolier and Bingham, 1971; 1978 Figures 14, 23). West and Shaffer trenched it in the 1980s. Easily accessible exposures remain. The photo and sketches above show Roza basalt shoved over alluvial Ringold Fm sediments and at 2-3 generations of loess. The fault shatters the Roza basalt. A thin white gouge zone is observable in places. Gouge is 10-20cm wide and associated with boudin-like lenses of deformed dark and light brown mudstone, rock flour, or broken basalt. Beneath the gouge is a sliver of brown mudstone (hanging wall) and cemented loess. Faint bedding in the loess confirms its vertical to overturned tilt beneath portions of the fault. The shattered footwall Roza is weathered above the fault and takes on a greenish-yellow hue. The rubbly zone grades upward to competent basalt then to spheroidally weathered basalt at the flow top. The boulder-sized spheroidal forms are also exposed along nearby Hwy 262. My own investigations of the Lind Coulee Fault Trench site and all nearby bluffs have yielded no evidence of liquefaction. Lind Coulee Fault is part of the larger Frenchman Hills thrust, known to have Quaternary movement (Reidel and Fecht, 1994; Schuster and others, 1997; Lidke and Haller, 2016). USBOR memos recount some details of West's trenching work from the perspective of the client (Lefevre and O'Connell, 1987; Galster, 1987). Much of the work on the Lind Coulee Fault was done pre-Internet, which makes written reports difficult to find. Relevant articles include Grolier and Bingham (1971, 1978), Galster/USBOR memo (1987, "Area No. 2"); Levfevre and MCConnell memo (1987), West and Shaffer (1988), Shaffer and West (1989), Reidel and Campbell (1989, "Stop 21-A", Figure 14), Geomatrix Consultants Inc. (1990, "East Fault Exposure"), Reidel and Fecht (1994), Schuster and others (1997), Lidke and Haller (2016). A big thanks to Brian Sherrod for sending me a scanned version of West and Shaffer (1988, Vol. 2).

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In Depth: Willamette Valley, Lower Columbia Gorge, and Coastal Areas

The Missoula floods backflooded the Willamette Valley dozens of times, depositing gravels and silt-sand rhythmites across the valley floor from Portland to Eugene (170 km south of the Columbia River). Hundreds of ice-rafted erratics are mapped throughout the Willamette Valley (Allison, 1935; Minervini and others, 2003) and nearby Columbia Gorge (Bretz, 1919). In general, Pleistocene deposits in the valley contain few dikes, though the exposure is limited due to dense development and vegetation.

PhD student Jerry L. Glenn (1965) found a few sheeted dikes in Missoula flood rhythmites (Willamette Silt) at his River Bend and Irish Bend sites near Corvallis. An Ira Allison photo shows a clastic dike cutting rhythmites near St. Paul, OR (1978, Figure 14). Dikes were exposed in highway excavations at Portland (Ian Madin, 2014 written communication and photos) and in dirt walls in the basement of the Capital Building at Salem during seismic refitting (Ray Wells, written communication and photos).

Thurber and Obermeier (1996) reported finding 16 clastic dikes at 7 sites along the lower Calapooia River, a tributary to the Willamette River. The largest features measured 5 m long x 10 cm wide. They attributed the dikes to liquefaction triggered by a Holocene earthquake. The Calapooia report contains no photos of dike fills or relationships between the dikes and the sediments they intrude, which makes independent evaluation difficult. Consultant John Sims (2002) reviewed Thurber and Obermeier's report, finding their data set too small to support the interpretation,

The limited area surveyed by [Thurber and Obermeier] in the Willamette Valley does not allow for a high level of confidence in determining if the features result from large subduction events or local intracrustal events. The age of the structures is somewhat in doubt as few radiocarbon dates are available for the host deposits and Thurber and Obermeier (1996) do not report any radiocarbon dates as part of their study. They also do not mention any evidence for liquefaction in post Pleistocene deposits of which there are many in the banks of the Willamette River and its tributaries. Thus, with incomplete coverage and lack of dating of paleoliquefaction features, the question of source zones is moot. Earthquake source determination can only be addressed with broader coverage of liquefaction features and better age data to constrain timing of events and to allow regional correlations of liquefaction features. In addition, we need a more complete picture of the size distribution of similar-aged features for the purposes of evaluating the magnitudes of prehistoric earthquakes.

River Bend section. Glenn (1965, Figures 3 and 15) reported finding a few clastic dikes in Touchet Bed-equivalent flood rhythmites (Willamette Silt) along the Willamette River. Note the lack of deformed bedding. Outcrop photos taken prior to dense urban and residential development of the Portland area as well as serviceable unit descriptions are found in Bretz (1925, 1928), Allison (1932, 1933, 1936, 1953, 1978), Piper (1942), Treasher (1942), Lowry and Baldwin (1952), Baldwin and others (1955), Allison and Felts (1956), Wells and Peck (1961), Trimble (1957, 1963), Balster and Parsons (1969), Hampton, (1972), Robert (1984), McDowell (1991), Yeats and others (1996), and McDowell and Roberts (1987).

Obermeier and Dickenson (2000) describe "relict liquefaction features" in low shoreline bluffs of sandy islands in the Columbia River between Astoria, OR (Marsh Island) and Kalama, WA (Bonneville Dam) and in cutbanks of 10 rivers east of the Cascade divide (Hood River). The thickest dikes measured 30 cm. The thickest sills 5 cm. The authors attributed the dikes to lateral spreading, hydraulic fracturing, and surface oscillations (ground shattering and warping) triggered by earthquakes. Similar investigations by USGS and DOGAMI were conducted in the Columbia gorge (Obermeier, 1993; Peterson and Madin, 1997; Atwater, 1994) and contain some of the same information as earlier reports.

Atwater (1994) and Takada and Atwater (2004 + Appendix A Supplement) describe sandy riverbank sediments in the lower Columbia River gorge deformed by the 1700 AD Cascadia earthquake. Their Holocene dikes of fluidized sand were generally narrow and outnumbered by sills that "mostly follow and locally invade the undersides of mud beds. The mud beds probably impeded diffuse upward flow of water expelled from liquefied sand. Trapped beneath mud beds, this water flowed laterally, destroyed bedding by entraining (fluidizing) sand, and locally scoured the overlying mud."

Peterson and Madin (1997) and Peterson and others (2014) describe sand dikes and sills (unsheeted fluid escape structures) intruding Holocene overbank muds at sites along the lower Willamette River and along Pacific beaches near the mouth of the Columbia. They interpreted the sand dikes as features triggered by seismicity at the Cascadia margin, possibly the 1700 AD event. A field guide was prepared for the Friends of the Pleistocene (Peterson and others, 1993).

The dikes and sills described by Atwater (1994), Thurber and Obermeier (1996), Obermeier and Dickenson (2000), Sims (2002), Takada and Atwater (2004), and Peterson and others (2014) are fluid escape features formed west of the Cascade divide, not wedge-shaped, sheeted injection dikes associated with scabland deposits. Their earthquake interpretation is reasonable, though their published field notes and photographs do not clearly document a source bed for the dikes. Perhaps unpublished information would clarify.

Holocene liquefaction dikes in the lower Columbia gorge. Caption for Figure 13b in Atwater (1994) reads, "Dikes with raised edges at upper Wallace Island [near Longview, WA]...The dikes transect mud beds that extend parallel to shoreline." This is the same dike pictured in Peterson and Madin (1997, Fig. 11b) and probably the largest example seen by all parties involved. Guessing that's Atwater's shovel in the photo.

Model for liquefaction features exposed along Pacific beaches. Caption for Figure 2 in Peterson and Madin (1997) reads, "Drawing of subsurface fluidization features including clastic dikes and sills and flames. Internal structures include intruded contacts with host deposit and disoriented mud blocks in sandy matrix. Fluidization features such as clastic sills are often enhanced under thin capping deposits of mud overlying thick source beds of sand." A nearly identical cartoon in Obermeier (2005, Fig. 2) similarly shows the various components of an idealized liquefaction dike scenario.

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In Depth: Toppenish Ridge

Two large gravel pits at Toppenish Ridge near Granger, WA expose conglomerates of the Miocene Ellensburg Fm. The active Toppenish Ridge Fault is mapped between the two pits. At the Lower Pit (225-250 m elevation) several large, sheeted dikes sourced in Touchet Beds cut downward through the flat-lying cobble conglomerate with its numerous sandy lenses. The Touchet Beds are inset into the conglomerate. At the Upper Pit (265-295 m elevation), located <200m from the fault, the conglomerate dips steeply south (>50 deg). Very few dikes were found in the tilted beds.

Toppenish Ridge exposures near Granger, WA. In the Yakima Valley, Ellensburg sediments, deposited by the ancestral Columbia River and smaller streams draining the Cascades, interfinger with and overlie the Columbia River Basalts. Green areas of the map are Miocene Ellensburg Fm sediments. Light brown areas are basalt flows. Gray areas are late Pleistocene Touchet Beds. Yellow is recent alluvium of the Yakima River. Sheeted dikes and Touchet Beds occur in the Lower Pit (minimally deformed strata), but not the Upper Pit (steeply tilted strata). Landowner is the Yakama Indian Reservation.

Dikes missing from Upper Pit at Toppenish Ridge. Steeply-dipping, partially lithified fluvial sediments contain almost no clastic dikes and no liquefaction features despite abundant sand lenses. Sheeted dikes are present in a thin remnant of tilted(?) Touchet rhythmites at the top of the exposure (~295m elevation). The Toppenish Ridge Fault, an active structure, is mapped less than 200 m away (Schuster and others, 1994; Lidke and others, 2003; online USGS Quaternary Fold and Fault Database for the United States).

Many dikes in Lower Pit at Toppenish Ridge. Flat-lying Touchet Beds are the unambiguous source for dikes cutting older gravels off Tule Rd. Diking at this lower elevation fall within the Ice Age floodway and appear to be related to flooding, not faulting or seismicity. The dikes do not rise from a liquefied source bed. They post-date deposition of the Ellensburg and most, if not all, of the tilting.

Seventeen kilometers to the west, four seismic trenches were opened across faults of Toppenish Ridge by Newell Campbell, Tom Ring, and Ted Repasky. The work was supported by the Yakama Indian Tribe and USGS (Campbell and others, 1995). Trench 1 was excavated across the Mill Creek Thrust (see below). Trenches 2, 3, and 4 were dug across nearby extensional structures. No liquefaction features or clastic dikes were observed in the trenches.

Trenching at Toppenish Ridge. The last movement on the Mill Creek Thrust offset the modern soil, L-1 loess containing Mt. St. Helens Set S tephra (13 ka), and a dark-brown "chocolate" soil (~40 ka) by 3.5 m. Age of the latest movement was estimated at 500-700 years BP, consistent with previous reporting (Campbell and Bentley, 1981) and local Indian legend. Evidence for two older ruptures involving cemented fan gravel and loess indicate the fault has been active twice in the past 40,000 years.

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Pliocene-age Dikes in the Ringold Formation

Clastic dikes contained in sedimentary beds between Miocene basalt flows or sourced in Pliocene sediments that overlie the basalt are rare, even where the units are tilted and deformed. A sparse set of thin, short, mud-filled dikes does appear in certain fine-grained beds in the Pliocene Ringold Fm at Smyrna Bench, White Bluffs, Othello, Sunnyside, and Selah. The vertical structures are rarely thicker than a notebook or more than a meter long. They are associated with a hard, white claystone bed and a prominent, gray, tuffaceous sandstone that thickens toward the Columbia River. These dikes are rarely encountered and have not been studied in detail. They do not appear to form polygonal networks or feed sand blows. Their fills are mostly unsheeted and otherwise bear little resemblance to fills in Touchet-type dikes. I interpret them as incidental features common to sandy sedimentary successions worldwide.

Small dikes in Ringold sediments at Saddle Mountains. A few small white dikes cut an oxidized alluvial fan gravel atop Elephant Mountain basalt. Dikes in this same layer occur at Smyrna Bench.

Small dikes in the Ringold Fm. Small, single-fill dikes cut a white claystone at Othello Canal. I examine these dikes in a YouTube video Pliocene Clastic Dikes at Othello Canal.

Mineralized dikes along Columbia River Road near Richland, WA. Mineralized dikes cut tens of meters through Ringold sediments at White Bluffs. Mineralization is a recent phenomenon, a result of irrigated agriculture. The dike's white color comes from calcite and gypsum precipitated from irrigation water applied to crops at the top of the bluff that infiltrates to deep levels in the subsurface. Mineralization indicates that the dike either a.) forms a preferential pathway for excess runoff to enter the formation, or b.) the dike's fill retains mineral-rich groundwater longer than the surrounding sediment, therefor precipitating more salts. According to those who champion the latter explanation, the formation drains more rapidly than the dike fills. However, this dike's fill and the fills of others nearby is sandier than the silty-clayey lakebeds of the Ringold. Even the most casual weekend geologist would take note of the bright white dikes and suspect that dike and host interact with pore water differently. Logic would suggest that a more-mineralized dike has passed more water and more dissolved salts through its fill than the less-mineralized, bedded sediments adjacent to it. I just disagree with George Last, who thinks this stuff is more complicated. Its not.

Small dikes in Pliocene strata in Yakima Valley. A thin clastic dike, truncated at its top, cuts fluvial-lacustrine strata at Houghton Rd north of Sunnyside, WA. These quiet water sediments closely resemble those at Snipes Mountain (mapped as Miocene Ellensburg or undifferentiated Miocene) and at many locations in Pasco Basin, where they are mapped as Pliocene Ringold). The contact between Ellensburg and Ringold is not well defined in western Pasco Basin. On this matter I side with Merriam and Buwalda (1917): a separating unconformity is not present in most exposures. Outside the Pasco Basin, middle/upper Ringold sediments lie atop folded Ellensburg or basalt. Thanks to Grandpa Carl of Granger, who first showed me this outcrop.

Do Clastic Dikes Indicate Paleoseismicity?

Clastic dikes are commonly observed in earthquake-prone regions of the world and often highlighted in post-quake damage assessments (i.e., Walsh and others, 1995). Methods for logging trenches and describing deformation features have been developed by USGS, state geological surveys, and consultants (McCulloch and Bonilla, 1970; Gohn and others, 1984; Atwater, 1994; Obermeier, 1996, 2009; Peterson and Madin, 1998; McCalpin, 2009; Holtzer and others, 2011) tempered by words of caution (Holtzer and Clark, 1993; Moretti and van Loon, 2014). Maps of dike width can help define the spatial extent of deformation caused by shaking. The value of such maps largely depends on the size of the dataset. A small number of measurements or measurements collected within a small area (i.e., a trench) have low value because they lack statistical power and may not scale with the actual pattern of damage. Borradaile (1984) highlights inappropriate use of dike measurements and other mistakes that can skew findings and mislead policy makers.

Misinterpretation of dike sources, taper direction, geologic triggers (origin), and subtle, but key field relationships can also be a problem, especially for inexperienced staff or where exposure is poor. Where outcrops are sparse or the geology unfamiliar, investigators should be especially aware of their biases and those of management. Its easy to fall back on preexisting assumptions when fieldwork offers only ambiguities. The assumption that all clastic dikes form by liquefaction and are triggered by earthquakes has led too often features formed by aseismic processes as seismites.

Seismic hazard in the Columbia Basin vs. New Madrid. Earthquake hazard probability based on the 2023 USGS model (fault-slip rates, frequency, magnitude), showing a simplified 2% in 50-year probability of exceedance map for fixed VS30 760 m/s. Red-orange indicates high probability for damaging quakes. Green-blue indicates low probability. Note the stark difference between the Columbia Basin (green-yellow) the New Madrid Fault Zone (dark red-red-orange). Dikes in the Columbia Basin are wedge-shaped and filled from above. Dikes in the New Madrid Seismic Zone are feeder conduits to sand blows. Columbia Basin dikes occur entirely within the Ice Age floodway. New Madrid dikes occur in floodplain deposits of the lower Mississippi River and valleys of large tributaries.

Modest shaking east of the Cascades. Map of earthquake epicenters recorded between 1970-2015 (Brocher and others, 2017, Fig. 2). East of the Cascade divide, quakes are mostly small magnitude, shallow, and locally clustered (i.e., Entiat and certain Yakima Fold Belt faults). Plenty of epicenter dots fall nowhere near mapped faults and belong to no clusters (Gomberg and others, 2012). The distribution and sizes of clastic dikes do not correspond with the locations of recent epicenters. YFTB = Yakima Fold Thrust Belt, GRZ = Goat Rocks zone, SHZ = St. Helens zone, UL = Umtanum lineation, WRZ = Western Rainier zone. Quaternary faults are heavy gray lines.

Double Bluff on Whidbey Island, WA. An example from seismically-active Puget Sound for comparison. Deformed clay-rich units (orange-tan) are interbedded with thick sands (brown-gray). Though the grainsizes are not too different from many exposures in the megaflood region, the setting and the deformation features are. This is an estuarine outwash plain and the features are t-shaped mudsquirts, not sheeted, wedge-shaped dikes (or sand blows). Depositional hiatuses and low angle unconformities are seen here and there in the stack; its not one big sediment dump. There is rhythmicity here; sand-clay-sand-clay. The entire section is deformed, though deformation changes from top to bottom and appears partitioned according to the grainsize and strength characteristics of the different layers. Dike-like flame structures rise from each clay-rich bed and intrude the overlying sand. Height of clay flames scales with the thickness of the clay beds. Bedding in the formerly flat-lying sands now swirls sympathetically with the margins of the clay flames and mud squirts. All of the layers here were remobilized and deformed after they were deposited. According to local geologists, the deformation was caused by mass wasting triggered by seismic shaking. We can see the effects of mass wasting and loading, but have to infer a seismic trigger; no data links a specific quake to this deformation. Curious to know where the locals believe the shoreline bluff was during that shaking event? Hasn't the erodible cliff face retreated a considerable distance since glacial times? To my eye, all of the deformation visible in the bluff occurred in buried strata, hundreds of meters back from the steep escarpment that today is being eroded by waves, wind, and tides. Was a steep coastal bluff here during glacial times? Where was sea level? Was the deformation caused by a single event or several? A few glacial floods dumping slugs of sand into a muddy trough could explain everything we see here, no?

In 2017, an international conference was convened to coordinate proper reporting on seismites in sedimentary sequences. The conference emphasized the need for caution (Feng, 2017). It seems “seismite” (Seilacher, 1969; Montenat and others, 2007; Van Loon, 2014) has for some time been assigned too liberally to features of nonseismic or ambiguous origin, making reexamination of "classic" seismite localities necessary. Clear-eyed geoscientists who participated reattributed many features formerly identified as seismites to nonseismic processes, most commonly to rapid sedimentation and loading (Moretti and Van Loon, 2014; Shanmugam, 2016 and references therein). The following quotes capture the feelings of some participants:

“Nonseismic events can create structures that are virtually indistinguishable from seismically-deformed sediments, or seismites. Therefore, paleoseismologists must correlate candidate seismites over regions and rule out nontectonic origins before concluding that an earthquake occurred.”

– L.B. Grant

“A great progress has been made in researches [sic] of soft-sediment deformation structures (SSDs) and seismites in China. However, the research thought was not open-minded. About the origin of SSDs, it was almost with one viewpoint, i.e., almost all papers published in journals of China considered the beds with SSDs as seismites. It is not a good phenomenon.”

– Z-Z. Feng

“At present, there are no criteria to distinguish...soft-sediment deformation structures formed by earthquakes from SSDs formed by the other 20 triggering mechanisms...the current practice of interpreting all SSDs as “seismites” is a sign of intellectual indolence.”

– G. Shanmugam

Maximum Width Method is Inappropriate for Sheeted Dikes

Relationships between liquefaction and shaking intensity are well established (Ambraseys, 1991; Galli, 2000; McCalpin, 2009; Zhong and others, 2022). Shaking intensity maps prepared in the wake of damaging earthquakes are constructed from field observations (i.e., locations of surface ruptures, toppled structures, water spouts, sand blows/boils, foundered slopes, etc.) and from measurements of liquefaction features (i.e., widths of clastic dikes). Liquefaction dikes feed sand blows and the widest dikes are thought to form near the epicenter.

Obermeier's method, here called the "maximum width method", involves measuring the width of the widest feeder dike at many sites and contouring the values in order to produce a bullseye map revealing the epicenter. Since seismic shaking is most intense near the epicenter and drops off with distance away as energy attenuates, the largest dikes and most intense liquefaction should occur where ground acceleration is greatest and pore pressures highest.

An often-cited liquefaction-feature mapping study conducted in the New Madrid Seismic Zone by USGS geologist Steve Obermeier employs this method  (Obermeier, 1998; Obermeier and others, 2005). His study linked past earthquakes to sand blow eruptions in broad alluvial valleys. The study improved upon earlier field reports by others (Fuller, 1912; Boyd and Schumm, 1995). Obermeier measured the widths of sand blow feeder dikes triggered by magnitude 7.2–8.2 quakes with Modified Mercalli Intensities >VIII that struck the region in 1811-1812 as well as two earlier events. Wet sand was vented over hundreds of square kilometers, remnants of which are still visible on aerial photos.

Clustering of large clastic dikes at New Madrid. Obermeier (1998) used the maximum widths of sand blow feeder dikes to delineate the region affected by earthquake-triggered liquefaction and reconstruct the location of a paleoepicenter. Three sizes of black circles correspond to his width categories (15 cm, 15-50 cm, >50 cm). Dashed ovals are the interpreted damage halos associated with 19th century quakes. I find odd that Obermeier identifies six separate clusters of large dikes in his study area. Clustering appears more consistent with local conditions and/or multiple events rather than a single, regional one. The expression of liquefaction (dike width) appears to vary similarly within each valley and may have resulted from a number of earthquakes with different epicenters, rather than single large earthquake centered near Vincennes, IN. Also, the map would benefit from the addition of topographic contours or depth to groundwater contours, which would more clearly delineate valleys from interfluves. Measurements were collected on dikes intruding wet, valley-bottom alluvium (larger floodplains). None were collected in pockets of fine grained alluvium or windblown deposits in the surrounding uplands.

However, Obermeier's "maximum width method", while appropriate for sand blows, cannot be applied to all types of clastic dikes. The method because it assumes feeder dikes are single-fill structures that rose from a liquified source bed at depth during a single triggering event. It uses dike width measurements (fracture aperture) to predict the strength of shaking. But sheeted clastic dikes require different assumptions. In sheeted dikes (compound and composite dikes), width grows incrementally over time by the addition of subparallel fillings with apertures of varying widths. Compound dikes widen sheet by sheet during the course of a single event. Composite dikes widen during two or more events that may be separated by decades to millennia. The widths of single-fill dikes and sheeted dikes are not comparable. The failure mode is different: injection of sand into hydraulic fractures propagated downward vs. fluid escape and venting of sand to the surface. An apples-to-apples comparison of the sand blow feeder dikes like those at New Madrid to sheeted injection dikes like those in Columbia Basin, would be the widest liquefaction dike at each site vs. the widest sheet at each site.

Columbia Basin Crust vs. New Madrid Crust The tectonic settings of the two regions, composition of the crust beneath each, and the potential for faults to generate strong shaking are not comparable. The New Madrid is an ancient failed rift in crystalline basement. Seismicity >M 7.0 is generated by deep, steep faults in strong crust. The Columbia Basin in WA and OR, by contrast, is a young back-arc flood basalt province resting atop extended Tertiary crust capable of ~M 7.0 quakes (Madin and others, 2021). At New Madrid, Holocene floodplain deposits liquefied during shaking and vented sand upward. In Columbia Basin, dikes were injected downward into various substrates during Ice Age megaflood events.

Bedrock geology or floodway processes? Sheeted clastic dikes riddle sediments in Pasco Basin, Yakima Fold Belt, Palouse, and Willamette Valley, but are not found in sediments overlying thinner basalts of the Blue Mountains or Idaho-Nevada Graben. Basaltic bedrock does not appear to be a control on diking. Map modified from Tolan and others (2009, Figure 1).

Missing Holocene Deformation

Thick, unconsolidated alluvium in dozens of valleys across Eastern Washington lack clastic dikes. The absence of dikes (and liquefaction features) in wet, fine-grained sediments in Holocene floodplains suggests that a.) faults of the region do not currently generate large enough earthquakes to produce dikes, but did so in the past, b.) modern floodplain sediments do not deform like older sediments, c.) Pleistocene dikes are not seismites, but products of another process specific to that time, or c.) the recurrence interval for large earthquakes is much longer than 15,000 years; strong shaking and dikes just haven't arrived yet.

Undeformed Holocene alluvium. Thick sections of Holocene floodplain alluvium (>4m) like this along Dry Creek near Walla Walla, WA show no evidence of strong shaking, pre- or post-Mazama ash. The bright white ash is conspicuous in many roadcuts, railcuts, and cutbanks in the Walla Walla Valley. If present, convolute bedding, soft sediment deformation features, and faults would have long ago been identified by local geologists, farmers, and soil scientists given the strong visual contrast between the ash and darker alluvium. Photo location is the intersection of Harvey Shaw Rd and Dague Rd ~8 km north of Walla Walla. Mapped Quaternary faults in the vicinity include the Wallula Fault Zone (21 km away), Hite Fault (33 km away), Kooskooskie Fault (23 km away), and Promontory Point Fault (6 km away). Photographed in June 2021.

Thick undeformed alluvium. No soft sediment deformation or dikes has been found in the floodplain of Union Flat Creek near Dusty, WA.

Undeformed alluvium. Thick alluvial fills along Willow Creek near LaCrosse, WA are undeformed.

Undeformed late Pleistocene deposits and Holocene alluvium. A mix of sandy Ice Age flood deposits, reworked colluvium, and varved lake beds capped by younger alluvium containing Mazama Ash is exposed along Latah Creek west of Spokane, WA. Lake beds along the creek near Qualchan Golf Course are especially prone to landsliding. Touchet Beds above contain numerous sheeted dikes, while exposures >2km upstream of the Hatch Rd bridge remain largely undeformed and without dikes. I've seen nothing in the upper reaches of Latah/Hangman Valley resembling liquefaction. Local folds of centimeter to meter scale are occasionally encountered - rollups formed where coarse bedload gravels overrode finer-grained sediments (high energy backflood flows). Photo is a cutbank below Hangman Valley Rd northwest of Hangman Valley Golf Course.

Shaking Intensity-Liquefaction Distance Relationships Fail

Shallow, intraplate faults in the study area are believed capable of producing magnitude >6.5 earthquakes and MMI VII–VIII shaking (Lidke and others, 2003). However, sheeted clastic dikes are found at distances far beyond the limits for soft sediment deformation established by Galli (2000) and Zhong and others (2022).

• An epicenter at Wallula Gap (Wallula Fault Zone) is located >285 km from large dikes near Kettle Falls, WA.

• An epicenter at Burbank, WA (Umtanum–Gable Mountain Fault) is >260 km from large dikes in Lewiston Basin, ID.

• An epicenter on the Hite Fault is >265 km from large dikes near Granger, WA in the western Yakima Valley.

• An epicenter near Arlington, OR (Arlington–Shutler Fault Zone) is >230 km from dikes in the central Willamette Valley, OR.

• An epicenter at Smyrna, WA (Saddle Mountains Fault) is 225 km from large dikes at Kettle Falls, 205 km from Tammany Creek, ID, 135 km from Cecil, OR, and 120 km from Bridgeport, WA.

• An epicenter at Wyeth, OR (Mount Hood Fault Zone) is 250 km from large dikes at Warden, WA, 375 km from Lewiston, ID, and 395 km from Latah Creek, WA.

• An epicenter at Spencer Canyon near Entiat, WA is >210 km from large dikes at Touchet, WA.

Magnitude–distance curves. Liquefaction outer-distance limits compiled from studies on several continents (Galli (2000; Qiao and others, 2017); Zhong and others, 2022). A robust relationship exists between earthquake magnitude and the radial distance away from an epicenter liquefaction features will form. The limit of liquefaction from an M 6.5 earthquake is ~75 km. For an M 7.5 quake, the limit approaches 150 km. Many large dikes documented in this study are located at distances >150 km from mapped Quaternary faults.

Distances from an assumed epicenter. Radial distances measured from an assumed epicenter at Wallula Gap (Wallula Fault Zone) to outcrops containing clastic dikes are shown (circles). Most dikes occur within 150 km of the assumed epicenter, but many are found at distances far beyond liquefaction limits established by Galli (2000), which suggests the dikes are not liquefaction features. Black bars represent the boundaries of subbasins along the Ice Age floodway. Subbasin count, at bottom of figure, is a proxy for exposure. Outcrops are more numerous in valleys near Wallula Gap, where several rivers converge. Dikes are, in general, largest and most abundant in exposures immediately upstream and downstream of Wallula Gap, though very large dikes are found in several distant exposures. Subbasins: CC = Crab Creek Valley, GT = Gorge Tributary valleys downstream of Wallula Gap to The Dalles, LB = Lewiston Basin, OK = Okanogan Valley, PB = Pasco Basin, RP = Rathdrum Prairie, QB = Quincy Basin, SR = Snake River Valley, TV = Tucannon River Valley, UB = Umatilla Basin, UC = Upper Columbia River Valley, WC = Willow Creek Valley, WW = Walla Walla Valley, WV = Willamette Valley, YV = Yakima Valley.

Large dikes hundreds of kilometers from the OWL. One of several very large Touchet-type clastic dikes in the Upper Columbia River gorge, some 285 km north of Wallula Gap. Colville River mouth south of Kettle Falls, WA.

Weak Evidence for Strong Shaking East of the Cascades

If the dikes in the Channeled Scablands are the products of seismic shaking, then one or more of the Yakima Fold Belt structures would be the likely trigger. However, the dikes are distributed over too large an area for a single fault to be the culprit. If movement on the Saddle Mountains Fault, for example, triggered diking, then we should expect repeated diking in the same area according to its recurrence record. Since the Saddle Mountains have been rising for at least the past 15 million years, dikes should be abundant in Miocene, Pliocene, Pleistocene, and Holocene strata. Likewise, Neogene sediments cut by other YFB faults such as those at Toppenish Ridge, Lind Coulee, Kittitas Valley, Wenas Valley, and Naches Valley should host dikes and SSDs. Dozens of published sections by numerous authors for the Ellensburg, Latah, and Ringold Formations should show abundant liquefaction features, but do not. If hazard study predictions are correct, a radial pattern of strong shaking by YFB faults should be clearly preserved in the stratigraphy of Eastern Washington. No such pattern is observed in the field or in field notes, strat columns, unit descriptions, figures, or photographs published since geologists first entered the region (i.e., Russell, 1893).

Fault zone investigations have likewise failed to reveal a pattern of strong shaking in Eastern Washington. The often-referenced Stateline earthquake of 1936 that struck the Walla Walla Valley was a sub-magnitude 6.0 event that formed no sheeted dikes and caused no damage to speak of beyond its immediate epicenter, the tiny community of Umapine, OR. The Hite Fault, located in the Blue Mountains southeast of Walla Walla, appears to be inactive. I am aware of no reports of liquefaction or other seismites associated with the Hite Fault. Widespread liquefaction was not reported following the 1872 North Cascades earthquake (~M 7) and its many aftershocks (Milne, 1956; Sherrod and others, 2015; Brocher and others, 2018) despite vast quantities of silty-sandy glaciofluvial and glaciolacustrine sediments in terraces along the nearby Columbia, Wenatchee, Methow, Okanogan, and Sanpoil Rivers. It is entirely possible that the YFB ridges rose one M 5.9 quake at a time.

Accounts of the 1872 Chelan/North Cascades quake, the largest on record for Eastern Washington, came mainly from Wenatchee's newspapermen, whose job it was then and remains today to amplify the spectacular and sell newspapers. News reports should be taken with a grain of salt, especially those from 150 years ago. The quake, thought to have been centered at Entiat, caused water spouts, ground cracks, small landslides, and collapsed cabin roofs (Washington Standard Newspaper 11 Jan 1873; Coombs and others, 1976; Brocher and others, 2018, Appendix B), but some historical context is needed. Wenatchee in 1872 was a frontier town. Residents - all 100 of them - occupied a community that would not be platted for another 20 years. Chelan County didn't exist at that time. The light bulb and the telephone had not yet been invented. Ulysses S. Grant was President. Washington, Idaho, Colorado, Wyoming, Utah, New Mexico, and Arizona were not yet States of the Union. Just 6 rudimentary seismographs monitored ground motions for the entire PNW region, including parts of British Columbia, the same array in use until the mid-1960s.

Saddle Mountains Fault. Excellent exposures of sandy interbeds and tilted basalt flows (Elephant Mountain) are found along the Saddle Mountains front (Lower Crab Creek). None contain sheeted clastic dikes. The thin, light-colored fractures in the photo at right are not liquefaction features, but bleached shear bands, structures common in deformed sandstones worldwide.

Saddle Mountains crest. I've worked methodically along the entire crest of the Saddle Mountains, Smryna Bench, and Taunton Bench, examining Pliocene and Pleistocene sediments preserved there (Cooley, 2023). I found no sheeted clastic dikes above ~360 m elevation. In fact, surprisingly little evidence of strong shaking is found in numerous tilted sections along the 85 km-long fault.

Minimally deformed interbeds. Ebinghaus and others (2012) examined Miocene-age sedimentary interbeds (Ellensburg Fm) at 14 sites in Pasco and Quincy Basins near the Saddle Mountains and Frenchman Hills Faults. Minor soft sediment deformation - flame structures and load casts - were noted at 3 sites. At his Wagon Road 1 and 2 (Moses Coulee) and Mabton (Yakima Valley) sites deformation occurred at contacts between mudstones and overlying sands. Flame structures and load casts are commonly found where sand is repeatedly spilled through openings in levees onto off-channel muds. No clastic dikes were reported. Ebinghaus' findings are consistent with my own observations at dozens of exposures in the region and those of others (i.e., Schmincke, 1964; Hays and Schuster, 1983; Smith, 1988a,b; Humphrey, 1996).

Mostly undeformed White Bluffs. The White Bluffs of the Columbia River expose Pliocene Ringold Fm and Pleistocene flood deposits over some 50 km. The continuous section tilts gently, but is otherwise undeformed. Recent landslides caused in part by irrigation water from above provide many fresh exposures. Most of the area is on public land and accessible to hikers.

Other evidence deserves consideration. Strong seismic shaking has not been recognized in a.) hundreds of borehole cores logged at the Hanford Site, b.) in dozens of measured sections at White Bluffs published by several geologists, c.) in cores from alpine lakes in the Cascades and Okanogan Highlands, d.) in ODP cores off WA and OR, e.) in thick Ellensburg/Thorp/Latah Fm sections in Kittitas, Yakima, and Naches Valleys, f.) in Neogene sediments in the Dalles-Umatilla syncline, and g.) in thick and thin sedimentary interbeds in the CRBs across the region. A strong paleoseismic signal remains largely unrecognized despite more than a century of geological investigation by USGS, USBOR, Washington Geological Survey, various mapping crews, university researchers, graduate students, and others.

Strong shaking produced by a Puget Sound fault or by the Cascadia Subduction Zone are far-fetched explanations for the presence of dikes in Eastern Washington. Shaking generated west of the Cascade divide would attenuate long before reaching the Columbia Basin (Peterson and others, 2011; Wood and others, 2014). No evidence of megathrust shaking at 1700 AD (Atwater and others, 2005) is recognized in Eastern Washington. Likewise, no shaking effects are known from the 1918 Vancouver Island M 7.2, 1946 Vancouver Island M 7.5, 1949 Olympia M 6.7, or 2001 Nisqually M 6.8 quakes.

To date, no study has established an association between Yakima Fold Belt seismicity and sheeted clastic dikes. Instead, an aseismic driver - large overland floods - appears to control where, when, and how the dikes formed (see Footnote 6).

Lost near Lyons Ferry. About 15 Touchet Beds overlie a thick bar gravel in the Snake River canyon near Lyons Ferry. John Whitmer photo (WGS Archive No. 03144).

Sheeted Dikes Without Earthquakes

Examples of sheeted, per descendum clastic dikes that closely resemble those in Columbia Basin are reported in other regions. In all cases, overloading, rapid sedimentation, and hydrofracture were involved. Sheeted, wedge-shaped dikes intrude muddy deposits beneath tidewater glaciers in Sweden (Von Brunn and Talbot, 1986; Jolly and Lonergan, 2002; Le Heron and Etienne, 2005; Phillips and others, 2013), New England (Kruger, 1938), and in sediments of alpine glacial lakes (Sutherland and others, 2022). Sheeted dikes intrude lahar deposits on the side of an Aleutian volcano in Alaska (Herriott and others, 2014) and beneath ash flows in the Lake Atitlan caldera, Guatemala (Brocard and Moran-Ical, 2014). Winglike sand intrusions formed by hydrofracture during turbidite-fan deposition propagate downward, upward, and laterally in deep water clastic systems (Jenkins, 1930; Duranti and Hurst, 2004; Huuse and others, 2007; Monnier and others, 2015; Cobain and others, 2015, 2016). Wedge-shaped sand dikes descend from the base of debris flow deposits at Black Dragon Canyon in the San Rafael Swell, UT (author's field notes).

Lahar at Mount Spurr, AK. Sheeted dikes with characteristics identical observed to dikes in the Touchet Beds were discovered by Herriott (2014) in sandy lahar deposits on the side of an Aleutian volcano. Rapid deposition, surface loading, wet over dry sediments, and hydraulic fracturing were all involved. The red arrows are Herriott's and point to silt skins. Image courtesy of Herriott.

Subglacial dikes at Voss, Norway. Clastic dikes in subglacial settings often indicate high fluid pressures developed in muddy substrates by ice loading. Laminated dikes identical to dikes in the Touchet Beds descend into outwash sand at Voss, Norway. Wall-parallel laminations formed by "a repetitive process" (Mangerud and Skreden, 1972; Mangerud and others, 1981; Larsen and Mangerud, 1992). Similar downward-injected dikes formed in glacial settings are reported in Scandinavia, Iceland, British Columbia, Quebec, Ontario, and New England (Kruger, 1938; Dionne and Shilts, 1974; Amark, 1985; Boulton and Caban, 1995; Brunn and Talbot, 1986; Broster and Clague, 1987; Dreimanis and Rappol, 1996; Rijsdijk and others, 1999; Crossen, 2014; Ravier and others, 2015).

Subglacial dikes at Hat Creek, British Columbia. Gravel dike from above penetrates underlying outwash sand in British Columbia (Broster and Clague, 1987).

Subglacial dikes in southwest BC. Sheeted gravel-sand dikes filled from above in British Columbia (Broster, 1991, Fig. 9b).

Subglacial dikes in Wrangell-St. Elias National Park, AK. Sheeted dike intrudes sandy outwash of the Bering Glacier. Photo by Crossen (2014).

Sub-debris flow dikes at Black Dragon Canyon, UT. Wedge-shaped clastic dikes sourced in an overriding debris flow are injected downward into cross-bedded sandstone below. San Rafael Swell.

Downward dikes at Big Pumice Cut, CA. Gravel dikes sourced from above cut through thick pumice and pinchout in the underlying till. (Sharp, 1968). Hwy 395, Eastern Sierras.

In Patagonia. Sheeted dike in varved glaciolacustrine sediments in the northern Patagonian Andes (Perucca and Bastias, 2008, Fig.11). Pocket knife in shadow.

Subglacial dikes in Sweden. Top-loading by a grounding glacier forces wedge-shaped, till-filled dikes into a muddy substrate. Figure by von Brunn and Talbot (1986, Fig. 16).

Polish coal mine. A sheeted dike nearly a meter wide with fill characteristics identical to those in the Touchet Beds descends from unconsolidated overburden into fractured bedrock. Dike follows an tension fracture developed in the crest of a small anticline (Haluszczak and others, 2007, Fig. 6e). Identical dikes fill tension fractures in Columbia River Basalt at Prosser, Lewiston, and sites in the Columbia Gorge below Wallula.

Sand injectite complex in the Vocontian Basin, France. 3D representation of an injectite network formed offshore in a turbidite fan setting (Monnier and others, 2025 Fig. 8). Dikes of remobilized sand at scales approaching the resolution of modern seismic imagery connect larger and thicker sills. Though the stress gradient in the deep-water setting is opposite that associated with terrestrial floods, many similarities between the two systems exist, including hydraulic fracture and downward injection (Gottis, 1953; Parize, 1988; Huang, 1988; Jolly and Lonergan, 2002; Rowe and others, 2002; Parize and Fries, 2003; LeHeron and Etienne, 2005; Scholz, 2009, 2010; Jonk, 2010; Kane, 2010; Beyer and Griffith, 2016; Dodd and others, 2020). Oil industry geologists who met with Hanford staff in 2007 were first to recognize the dikes there as sand injectites comparable to those formed offshore (Braccini and others, 2008). Their keen observation appears to have ended research on seismites at Hanford.

Sand injectite in South Africa. Kilometer scale fluid migration and injectite growth in the Karoo Basin, South Africa. Downward and lateral injections propagate when fluid pressure in the sand body exceeds the confining strength of the seal. Figure redrawn from Cobain and others (2026).

Idaho vs. Utah. On the left is a sketch of a Touchet-type clastic dike at Lewiston, ID that I measured in several places (sheeting not shown). On the right is a cartoon of a typical deep sea sand injectite from a slideshow by Dr. Lansing Taylor, formerly of the University of Utah's Energy & Geosciences Institute. I flipped the injectite image upside down. In both examples, fractures follow the most efficient pathway that alternate between horizontal and vertical in response to changes in grainsize (porosity, permeability).

Branching at contacts between contrasting formations. The dike shown here is sourced in Missoula flood rhythmites that unconformably overlie the Snipes Mountain conglomerate, a Miocene-age, quartzite-bearing fluvial gravel deposited by the ancestral Columbia River. The upper part of the dike (out of photo) is vertical and gradually pinches as it descends. At the contact between the two formations, the dike abruptly divides into two horizontal branches (sills) and continues within the silty strata above the contact for a few meters before pinching out. The silty beds are able to maintain pore fluid pressure, where the underlying gravel cannot.Both dike and sill segments are sheeted and the fracture propagation direction is clear. The dike fed the sills. Identical features are found at Lewiston, ID where Touchet Beds overlie Bonneville flood gravel. Location is private land below Emerald Rd near Granger, WA.

Sheeted sills. Sheeted sills are more or less identical to sheeted dikes. Sills branch off from dikes. Intrusion of both dikes and sills occurred together and at shallow depths. Because dikes greatly outnumber sills, it would appear easier to initiate vertical fractures with horizontal slip along bedding planes (horizontal extension, vertical dikes) than to open horizontal fractures by lifting the overburden against gravity (vertical extension, horizontal sills). At very shallow depths, where the vertical and horizontal stresses may be approximately equal, small stratigraphic or grainsize differences may control whether dikes or sills form. Bedding planes, for example, may temporarily act as slightly more efficient pathways to fractures than paths pioneered vertically across bedding. Sill formation may be favored for a brief period during a flood loading event and/or may be depth-dependent. Hwy 240 at the Hanford Site.

Rubbly Injectites at Indian Creek, WA

In November 2017, I discovered and measured several breccia-filled dikes that cut varved Glacial Lake Columbia beds along lower Indian Creek Rd (Hawk Creek) east of Lincoln, WA. The intrusions formed in sediments deposited in a protected side canyon in response to subaqueous slumping of house-sized blocks of varved sediment. A highstand lake was present at the time. Several blocks were exposed in high tractor-bladed slopes, now covered by erosion control matting. Fills are unsheeted and contain broken, stratified clasts torn from the host material during injection. The dikes intrude the lower portion of the >20 m-thick section of at least 24 rhythmites (alternating lake varves and flood sand intervals).

Indian Creek. Pleistocene injectites exposed in the northernmost portion of the Ice Age floodway.

Rubbly fills. Rubbly injectite crosscuts clay-rich varves at a low angle.

Rip-ups. Rubbly, unsheeted fills contain stratified rip-up clasts - chunks liberated from the surrounding material.

Parallel and crosscutting. A light-colored sand-filled injectite intrudes clayey varves of Glacial Lake Columbia. Both crosscutting (stair-stepping base) and bedding-parallel (separates bedding) relationships are clear. Indian Creek is located north of Davenport, WA and also goes by Olson Canyon and Hawk Creek.

Field Work Matters

The origin of clastic dikes in sedimentary sequences can be ambiguous. Earthquakes, though often involved, are not required. In fact, clastic dikes are reported in many settings where active seismicity played no role whatsoever (Shanmugam, 2016). Lessons learned from coastal California or the Wabash Valley do not apply universally. Only when anchored by evidence gathered at the outcrop will an investigation into the origin of clastic dikes tilt toward a correct interpretation. Office-generated theories and probability models serve society best when they are rooted in and remain subordinate to field observations.

Dikes are threshold features that, if interpreted one way, may prompt policy makers to brand a landscape hazardous and unfit for occupation and/or future development. Interpreted another way, the same dikes become Ice Age relicts of little importance to anyone other than academics and megaflood enthusiasts.

Careful field work that involves a significant number of observations, measurements, descriptions, samples and a study area scaled to the geological phenomenon under investigation should be de rigueur. Overuse of "seismite", shoddy field documentation, and the application of methods poorly suited to the region are unacceptable practices.

Project planning is the responsibility of the Field Geologist. The subdiscipline Paleoseismology will hopefully remain a field-based discipline going forward, one focused on determining the timing and effects of prehistoric earthquakes, not getting one's name in the newspaper (or on NPR). Data gathered in the course of a paleoseismic investigation (fault slip rates, event dates, and shaking effects) are critical inputs to building codes, hazard planning documents, and land use policies. Data from the field informs and often drives policymaking, which affects the lives of real people. Unlike journal articles and tables of recurrence probabilities, maps constructed from field measurements are easily understood by all audiences. They are uniquely influential and tend to find their way into land use policy documents, which persist for decades.

Dike geometries in outcrop. (A) Twin-tapering forms that do not look like typical dikes. They are axe blade-shaped fractures propagating laterally and emerging from the face of the outcrop. A trick of geometry in the third dimension (see Arris and Aperture figure earlier in article). (B) Three dikes that lack a taper direction are truncated at their tops by erosional surfaces (bedding contacts). (C) Buried sediment remobilized in response to shaking vents sand upward to a higher stratigraphic position (sill) or to the surface via a feeder dike (sand blow). May be sourced from above or below. (D) Upward and downward tapering dikes. Local shearing may have offset a single dike, causing it to appear as two with opposite tapers. A trick of limited exposure. Excavate features or keep looking to find more conclusive relationships. (E) Downward tapering dike-sill geometry with upward-curving intersections are sourced from above. (F) Upward tapering dike-sill geometry with upward (tree branch-like curving intersections are sourced from below.

Know your SSD. Many soft sediment deformation features are distinctive, but many others can look alike. This is because ductile material is involved, more than one process may be at work, and features at an early stage of development may morph into very different shapes over time. Careful observation is usually the key to sorting things out correctly.

Key Characteristics of Clastic Dikes Assessable in the Field

Three key physical characteristics of clastic dikes - vertical sheeting, taper direction, and truncation at bedding contacts - are readily assessable in the field.

• Sheeted Fills - Sheeting is the result of repeated fracturing and sediment injection. Dikes in the study area grew in staccato fashion by filling of newly opened fractures by new pulses of sediment. Sheeting in dikes found elsewhere likely records a similar pattern of reinjection along preexisting weaknesses. New sheets erode older ones; rip-ups derived from adjacent bands should be present in abundance. Small packages of parallel sheets, typically up to six or so in the case of study area dikes, commonly crosscut older packages and reveal variations in the way fractures propagate. If new sheets tap progressively younger source beds, small collapses should be present above fractures opening below. At some of my study sites, multiple collapses appear in successive rhythmites, each initiating a dike. Brief periods of dike widening alternate with longer periods of inactivity (hiatus), a pattern that tracks with cyclic filling and spilling by proglacial lakes.

  
  

• Taper Direction - Taper direction is strongly tied to dike origin as it often reveals how fractures propagated, the mode of fracture, and the orientation of the fluid pressure gradient. In many cases, taper direction reveals the source of dike fills. Upward-tapering dikes rise from a buried sediment source layer and formed by upward escape of fluidized sediment under a normal pressure gradient (higher deeper, lower shallower). During shaking, pore fluid pressure rises. If the pressure exceeds the confining stress, then wet sediment is expelled upward, down the pressure gradient. Downward-tapering dikes indicate injection from above (the ground surface) and a temporarily inverted pressure gradient. Fluid driven fractures propagate downward and are filled by sediment circulating at the surface. Upward-tapering dikes are almost always the result of seismic shaking. Downward-tapering dikes (per descendum) form in response to rapid loading and hydraulic fracture. Fractures tend to follow efficient pathways within the substrate.

  
  

• Truncations - The tops of downward-tapering dikes are truncated at bedding contacts or unconformities. Dikes truncated tops constrain the timing of injection. A set of dikes truncated by depositional or erosional contacts is evidence of a repetitive trigger and repeated diking over time.

Flood counts and the development of vertical sheeting. Stacks of rhythmites (Touchet Beds) deposited by Pleistocene megafloods accumulated to different thicknesses in different parts of the Channeled Scabland. Rhythmite counts vary depending on location. The most complete rhythmite sections occur in slackwater basins repeatedly filled by Lake Lewis, Lake Condon, and Lake Allison. Lake Lewis filled the Walla Walla Valley (Waitt, 1980; 1985), Lewiston Basin (Bretz, 1929 field notes; Webster and others 1982), and Tucannon Valley (Smith, 1993). Lake Condon filled the Umatilla Valley (Benito and O'Connor, 2003), Willow Creek Valley (Cooley, 2015), and Sixmile Valley. Lake Allison filled the Willamette Valley (Glenn, 1965). Glacial Lake Columbia filled the Sanpoil Valley (Atwater, 1986), Upper Columbia Valley (Kiver and Stradling, 1982; Hanson and Clague, 2012), Latah Creek Valley (Rigby, 1982; Kiver and Stradling, 1982; Waitt, 1983; Meyer, 1999), and Foster Coulee (Russell, 1893). Rhythmites also occur in the Glacial Priest Lake basin (Walker, 1967; Breckenridge, 1989). The rhythmite count at a site approximates the flood count. All floods flowed through Wallula Gap and slackwater lakes that ponded there were the deepest anywhere in the region (>200m). Consequently, the largest dikes occur in full rhythmite sections in the southern Pasco Basin, eastern Umatilla Basin, and western Walla Walla Valley. Fill band counts (sheet counts) record repeated flood-loading, substrate failure, and sediment injection. Sheet counts (injections) are a multiple of rhythmite counts (flood counts), though a one-sheet-per-flood isn't the pattern. The sheet count data suggest that up to about 10 sheets may form in a given dike during a single flood. Local conditions seem to play a role (flow regime, water depth, valley configuration, grainsize, slackwater lake residence time, etc.). Very large composite dikes widen by the addition of new fractures and new sediment injections, so their widest portions occur near the base of rhythmite stacks (lower in the section) rather than near their tops (higher in the section). Dikes can appear to taper upward because newer fills that tapped successively younger flood beds intruded alongside older fills.

Truncated dikes at multiple levels. Sheeted dikes intrude more than a dozen geologic units exposed along the Ice Age floodway. Here, I've revisited key sites reported by others and redrawn their stratigraphy to include dikes. The sketches above are representative of studies published to date and show diking was recurrent with flooding. (A) Walla Walla Valley sites from Spencer and Jaffee (2002). (B) Lind Coulee site from Daugherty (1956). (C) Moxee Mammoth site from Lillquist and others (2005). (D) Hanford's FMEF site from Bjornstad and others (1990). (E) Rulo site from Bader and others (2016). A = Alluvium, C = Colluvium, CRB = Columbia River Basalt, DIA = Silt diamict, EG = Exotic-clast bearing gravel, FG = Fanglomerate/Alluvial fan gravel, L = Loess, P = Paleosol, S = Sandy, SCR = Silt-clay rhythmites, TB = Touchet Beds/Hanford Fm.

Warden Canal. All dikes do not cut from top to bottom through stacks of rhythmites. Several beds overlie this truncated dike near Warden, WA. Diking occurred many times during the Ice Age.

Silt-sealed Cracks and Hydrofracture

Sand-propped hydraulic fractures are used to stimulate oil and gas reservoirs, the procedure commonly known as "fracking". Hydrofractures are induced by shutting in a portion of the well, adding a proppant slurry (sand + water + chemicals), and using pumps to jack up the fluid pressure. When fluid pressure exceeds the formation's resistance, the rock surrounding the wellbore fails and fluid-driven fractures begin to propagate outward. The pressurized proppant slurry immediately fills the expanding fractures and holds them slightly open, permitting hydrocarbons to flow back to the well. Fractures propagated beyond the well bore exponentially increase a well's effective surface area and open new pathways into the reservoir.

Unlike a shut-in wellbore, however, sediments that host the dikes are typically unconsolidated and sandy with no low-permeability layers that might act as a seal. Yet clastic dikes abound. Two key factors explain the formation of the dikes: high strain rate and the rapid formation of silt skin walls.

• High strain rate - When loaded by a catastrophic flood, pressure in the shallow subsurface built so rapidly that hydraulic fracturing was induced. The normally loose (ductile) material failed in the brittle mode at the high strain rate. Pressure rose above that required for fracture and exceeded the sediment's capacity to dissipate pressurized fluid through its pore network. Rapid loading alone appears adequate to initiate fracture in a low tensile strength material with no true seal such as the Touchet Beds.

• Silt skin walls - Once fractures began to form and fill, silt skin walls began to build. The sealing effect of the low-permeability skins delayed leakoff and facilitated further fracture. New fractures as well as natural flaws (cracks, soil macropores, burrows, etc.) provided low-resistance routes for new fractures to follow. Fractures immediately filled with sediment, the injected slurry (a natural proppant) sourced from within the overriding flood. Dewatering (leakoff), integral to the formation of the skin wall, begins the moment sediment enters a fracture. The skin-sealed crack begins to behave as a pressure vessel almost immediately. Pressure inside of the sealed fracture (pore fluid pressure, Pf) rises until it exceeds the confining strength of the material (Pf > 03) and the crack tip advances or, if leakoff loss exceeds Pf, the fracture closes. The fracture propagates in the 01–02 plane (vertical), widening against 03. As the fluid pressure equilibrates to the confining pressure (Pf = 03), the fracture tip halts, filling ceases, the crack closes down on its proppant, and pressure begins to build again if the load is still present. Each time Pf exceeds 03, the tip jumps forward or a new fracture initiates nearby. With each increment of widening, fluid pressure drops (volume increase = pressure decrease), but soon rebuilds. This loading-driven crack-fill-seal cycling created the dikes’ vertically sheeted fabric. 

Sheeted infill illustrated. Fluid pressure-driven crack and fill (crack volume cycling) is shown at the scale of a dike (nearfield scale) during a flood loading event. Time steps 1 through 12 in the pressure-time curve correspond with crack tip locations. During overloading, dike growth corresponds with pressure-volume cycling where fluid pressure remains between the minimum and maximum principal stress values. Silt-sealed fractures become sheeted dikes in my study area and in other geologic settings where silt is present and similar overloading has occurred (lahar, grounding glacier, debris flow, etc.). Diking seems to have occurred twice during a flood-load event. The first is the initial onrush of the overland flood (or backflood). The second occurs once a slackwater lake has formed (sustained load). Gravelly or sandy dikes are likely produced by the overland flood, while silty-sandy dikes result from the lake.While hydraulic fracture is well understood, the development of wall-parallel laminae (sheeting) in clastic dikes by a combination of rapid loading, hydraulic fracture, and silt wall seals, as I've illustrated here, has not previously been described in detail. Figure 9 in LeHeron and Etienne (2005) is the closest I've seen. My illustrations are not copied from anyone; I created them to clarify my thoughts and convey my argument to others.

Sheeting forms pulse by pulse. Cyclic fluid-driven fracture results in the growth of dikes with vertically-sheeted fills during flood events (a single hydrofracture event). The cross sections correspond to the gray shaded portion of the pressure-time curve in the figure above. During hydraulic fracture, new fractures open, propagate, and fill. Here I show 4 pulses corresponding to 4 episodes of adjacent diking (2a, 3a, 3b-c, 4b, 4c) and nonadjacent diking (1a, 2b, 4a). Incremental growth of dikes involves the cycling of fluid pressure, the repeated opening of new fractures, and near simultaneous infilling by sediment carried by a flood. Evidence of repeated flooding (stacks of rhythmites) and repeated fracture injection (sheeted fills) is a pattern observed throughout the Channeled Scablands.

Near field and far field fracture. I modified the stress-strain curve for hydraulic fracture to illustrate my concept of sheeted diking during floods. The curves relate floodwater loads imposed over a broad area (far field flood load) to cyclic pressure pulses that occur at the local scale (near field injections). The fracking/leak-off test framework captures most of the important elements. Leak-off begins when a fracture opens (not at closure) and continues after the fracture closes, but that point, somewhat secondary, is not well captured in this diagram. See Footnote 15 for relevant equations.

Deep sea analogs? A 2m-wide sand injectite intrudes pillow basalts erupted off Angola (Hurst and Cartwright, 2007, Fig. 4). Deep sea injectites are larger than terrestrial Touchet-type dikes and the orientation of crustal stresses is different, yet important similarities exist.

Evaluating Proposed Origins

In this section, I evaluate seven proposed origins based on my observations and the literature.

(A) Desiccation hypothesis - Little evidence supports a desiccation origin. Dike geometry, distribution, size, sedimentology, and internal characteristics are fundamentally at odds with an origin involving the passive infilling of meters-deep, open-standing cracks. The dikes are not filled mudcracks.

(B) Ground ice hypothesis - Permafrost is soil that remains below 0 degC for at least two years. Ice wedges are common in permafrost lowlands of northern North America, Europe, and Asia. Ice wedges grow by annual freeze-thaw cycling where ground cracks open and fill with ice and washed- or blown-in sediment. Fossil ice wedge casts can persist for centuries in sediments near former ice margins (Horber, 1949; Dylik, 1966; Burbidge and others, 1988; Stone and Ashley, 1992; Demoulin, 1996). The wedges commonly contain vertically-laminated fills (sheeting) and coalesce to form polygonal networks (Lachenbruch, 1962; Romanovskiy, 1973; Ghysels and Heyse, 2006) much like some clastic dike networks. Ice wedge growth at middle latitudes, relatively common during the Pleistocene, is rare today in valley settings.

A few geologists have interpreted the clastic dikes in south-central Washington as fossil ice wedge casts based on polygonal networks, vertically-laminated fills, and age (Alwin and Scott, 1970, Lupher, 1944, and Black, 1979), though all express some hesitation. While the dikes do bear some resemblance to fossil wedges in mid-latitude England (Briant and others, 2004), France (Antoine and others, 2005), The Netherlands (Van Huissteden and others, 2000), Poland (Zoller and others, 2022), Germany (Grube, 2012), Mongolia (Owen and others, 1998), Niger (Denis and others, 2010), Patagonia (Perucca and Bastias, 2008), and certain high-latitude sites (Van Vliet-Lanoe, 2005), additional evidence is needed to corroborate the past presence of frozen ground in Eastern Washington.

Though the southern limit of the Cordilleran Ice Sheet is well defined across northern Washington (Porter and others, 1983; Atwater 1986; Cheney, 2016), a corresponding periglacial zone remains loosely delineated. Murton (2020) identifies only a narrow permafrost zone south of the Okanogan Lobe, implying the southern limit of periglaciation extended only a short distance from Withrow. Periglacial features abundant in the 200 km-wide swath south of the continental Laurentide Ice Sheet (Pewe, 1983; Clark and Ciolkosz, 1988) are sparse south of the maritime Cordilleran Ice Sheet (Orme, 2002; French and Millar, 2013; French, 2017).

No permafrost. Compiled climate-proxy information indicates permafrost never formed in Columbia Basin during Late Wisconsin glacials or interglacials.

Periglacial features are not abundant in the nearby Blue Mountains or Cascade Mountains. While frost-cracks are found in soil profiles of the Palouse/Umatilla Plateau, and rock glaciers linger in cold hollows east of the Cascade divide (Lillquist and Weidenaar, 2021), and frost-shattered Columbia River Basalt is exposed over thousands of square kilometers, Pleistocene cold does not appear to have reached the intensity of the modern Arctic. Cirque elevations in the Rocky Mountains (Pierce, 2003, Fig. 1) project well above the crests of Yakima Fold Belt ridges. No mention of soil wedges, frost stirring, or gelifluction is made in NRCS Soil Surveys for the Colville Indian Reservation (NRCS, 2002), Okanogan County (NRCS, 2010), Chelan County (USDA, 1975), Douglas County (NRCS, 2008), Grant County (USDA, 1984), or Lincoln County (USDA, 1981). Small frost wedges in varved beds of Glacial Lake Missoula (Chambers, 1984; Chambers and Currey, 1989; Levish, 1997; Hanson and others, 2012; Hanson, 2013; Smith, 2014, 2021) have not be found in varved beds of Glacial Lake Columbia (Lake Roosevelt, Lake Rufus Woods, Banks Lake). Fossil soil wedges such as those in Idaho's Lemhi Range (Butler, 1984; D.R. Butler written communication), at the Owl Cave-Wasden Site on the Snake River Plain (Dort, 1968; Butler, 1969), in terrace gravels near Lewistown, MT (Schafer, 1949), in prairie soils near Browning, MT (unpublished field notes by the author) and Laramie, WY (Grasso, 1979; Mears, 1981, 1987; Nissen and Mears, 1990; Munn and Spackman, 1991; Dillon and Sorenson, 2007) apparently never formed west of the Rocky Mountains. Silt mounds (mima mounds) are common to dusty landscapes, whether glaciated or unglaciated (Busacca and others, 2004). Silt mounds are found from central Mexico to the Arctic and some in Washington clearly date to the Holocene. Mima mounds indicate abundant wind, dust, and some aridity. Little else.

Stacked Pleistocene paleosols in the Palouse Hills and Channeled Scablands contain abundant evidence of soil life. Phytoliths, rodent burrows, and cicada burrows are incompatible with deep, prolonged freezing. Backfilled burrows that riddle the Touchet Beds attest to rapid recolonization after each outburst flood event. Pollen samples from lake bottom cores indicate both cold-tolerant plant species and conifers occupied the landscape throughout the Lake Wisconsin (Blinnikov and others, 2002; Whitlock and Brunelle, 2006). Mammoth that once roamed inland plains were nourished by steppe-grassland forage, not tundra plants (Fry, 1969; Last and Barton, 2014).

Ice wedges in the literature. Hundreds of studies have been published on fossil ice wedges, ice wedge casts, and soil wedges formed in permafrost (Lachenbruch, 1962; Pewe, 1973; Romanovskij, 1973; Mears, 1987; Yershov, 1998; Bockheim, 2002; Murton, 2020, etc.). Several lines of evidence from climate-proxy archives indicate the Columbia Basin was never glaciated and free of permafrost, even during the very coldest parts of the Pleistocene. Eastern Washington's clastic dikes are not fossil ice wedge casts, despite their laminated fills, tendency to form polygons, and speculation by authors (Lupher, 1944; Alwin and Scott, 1970; Black, 1979). At its coldest, the Pleistocene Columbia Basin was "tundra-like" (Cooley, 2008) and perhaps best described as a "cold steppe" with widespread sagebrush and pockets of pine forest supporting species commonly "found in alpine and sub-alpine valleys in the [present-day] Cascade Mountains of Washington...cool-to-cold, moist, open-park conditions...consistent with the presence of continental ice to the north" (Spencer and Knapp, 2010). While the use of "periglacial" may persist among certain groups (O'Geen and Busacca, 2001; Gaylord and others, 2003), Eastern Washington was never tundra and always contained trees.

Ice wedges active and relict. Left: Ice wedge penetrating thick silt at the USACE Permafrost Tunnel Research Facility near Fairbanks, AK (www.erdc.usace.army.mil/CRREL/Permafrost-Tunnel-Research-Facility). Right: A fossil ice wedge cast (sand wedge) penetrating sandy alluvium in northern Europe. Photo by Richter/Freiberg Instruments.

Wedges in Glacial Lake Missoula varves. Small wedges descend from numerous horizons in Glacial Lake Missoula "varve" beds exposed in the Clark Fork River Valley, MT. Specific sites include Rail Line (A,B), Jocko River (C), Crow Dam, and Garden Gulch sections (Chambers, 1971, 1984; Chambers and Curry, 1989; Levish, 1997; Hanson and others, 2012; Hanson, 2013; Smith, 2014, 2021). These structures are though to have formed during lowstand periods (shoaling, subaerial exposure) and resemble wedges commonly found in the Arctic. A combination of desiccation and shallow ice wedging seem to be at play. Similar wedges are not known in varved beds in northern Washington. Photo B by Michelle Hanson. Photos A and C are mine.

Soil wedges in Montana. These wedges formed 465 km east of Grand Coulee Dam in treeless prairie soils. Periglacial wedges like these help define a periglacial zone south of the Laurentide Ice Sheet (Murton 2020, French 2017). Similar wedges are not known in Eastern Washington. Roadcut is along Hwy 89 between the Two Medicine River and Badger Creek south of Browning, MT.

(C) Lateral spreading hypothesis - Lateral spreading (lateral extension) can form wedge-shaped cracks and commonly involves liquefaction. Surface cracks open when a block of earthen material slides sideways along a low-angle slip plane. The figure below shows three scenarios where wedge-shaped cracks may form in thick sediments and gentle terrain given a 'free face'. Space is needed to accommodate spreading.

According to the model, tension fractures will form atop escarpments. The implies the dikes are mass wasting and surface cracks, thus dikes, will be more numerous along topographic breaks. However, the densest networks of clastic dikes in the study area occur in broad valleys and coulee bottoms, gently concave areas under weak compression. Incised channels and steep bluffs necessary to accommodate spreading are simply not found in exposures of Touchet Beds or other formations that host the dikes. Valleys filled with Touchet Beds were too flat to translate blocks of sandy sediment sideways. Today, remnants of the fill forms benches that appear quite stable despite having lost lateral support. Slide blocks in unchanneled valley fills had little reason to form and, if formed, had nowhere to go.

Lateral spreading falls short. (A) Lateral spreading scenario - Channel incision removes support and creates a free face that can facilitate lateral spreading in shoreline bluffs. Block sliding due to gravity. (B) Liquefaction scenario - Seismic shaking that triggers liquefaction in a wet, sandy layer at depth can produce clastic dikes (water escape structures). Sediment is vented to the surface, forming sand blows. Cone-shaped sheets and "volcanic" sand edifices are formed. (C) Load-triggered hydrofracture scenario - A large vertical load imposed by a megaflood (overland flood, backflood, slackwater lake) increases pore fluid pressures in the underlying sediments and trigger hydraulic fracture. Fractures immediately fill with sediment sourced from the surface. Hydraulic fractures initiated at the ground surface propagate downwards. Fractures are propped by the sandy fill to become clastic dikes. Internal sheeting develops during single events (pressure-volume cycling) and over time as new dikes form during subsequent flood events. New dikes merge with older ones. Repeated flooding creates both compound and composite dikes.

Free face, block translation, and slide plane. A set of wedge-shaped gravel dikes with massive fills near Hunters, WA unambiguously formed by lateral spreading. Unstable shoreline bluffs composed of varved glacial lake sediments capped by an outwash gravel have slipped and partly toppled into the Columbia River. These dikes check all the boxes for lateral spreading - free face accommodation, block translation, and a subhorizontal slide plane at depth. More about Hunters geology HERE.

(D) Rebound following slackwater lake drainage - Ice Age floods imposed enormous loads on the crust. In the southern Pasco Basin, the depth of Lake Lewis depth exceeded 200m. Each flood imposed a transient load for hours. Each lake a load for days to weeks. While we can assume the crust was depressed a bit during flooding and rebounded as the water drained away, we don't know the of total amount of depression, the rate of depression and recovery, or whether the effects of loading and unloading are preserved in the geologic record. No one has studied the effects of floodwater loading on surficial sediments.

Belly up to the bar. Wedge-shaped fractures result from up-bending caused by removal of floodwater load by drainage.

(E) Seismic shaking and liquefaction hypothesis - According to many, fault movements independent of floods or possibly in tandem with floods are capable of triggering earthquakes and forming clastic dikes. If the dikes are the products of strong seismic shaking, then liquefaction is the diking mechanism. However, the dikes discussed here do not resemble liquefaction features formed during earthquakes (seismites). As mentioned previously, no liquefaction features (sandblows, etc.) have been found in seismic trenches in Eastern Washington. Liquefaction dikes in the lower Columbia River Gorge credibly attributed to the 1700 Cascadia earthquake (Dickenson, 1997; Obermeier and Dickenson, 1997; Atwater and others, 2005, 2015) are Holocene features sourced from below. They are feeder conduits to sand blows like those found at New Madrid (Fuller, 1912; Obermeier, 1989), coastal WA-OR (Peterson and Madin, 1997), the Bay Area (Sims and Garvin, 1995), and Anchorage (McCulloch and Bonilla, 1970). Atwater (2000) noted discontinuous liquefaction in visually-similar deposits of the lower Gorge and suspected the mechanical properties of sand islands and river banks vary in ways not anticipated. Sheeted dikes in the Channeled Scablands, by contrast, are ubiquitous in flood deposits that contain silt, formed only during the Pleistocene, are nearly identical everywhere found, and are not associated with sand blows or remobilized source beds. Diking recurrence does not match the rupture history for any fault in the region, therefor faulting does not appear to be a primary control on diking.

(F) Flood-generated vibration hypothesis - Ice Age floods would have produced a tremendous rumble as they coursed through the countryside. The cataclysm must have terrified humans and animals who witnessed their passage. In addition to a roar, overland floods may have induced a vibratory resonance in certain rocks and sediments. The dikes may be somehow related to resonant deformation, though the mechanism remains elusive. No clear analog has yet come to light, though research into seismicity generated by large, sediment-laden floods is underway at Université de Grenoble-Alpes, France as of 2023 (Kristen Cook, Florent Gimbert, Alain Recking).

(G) Hydraulic fracture triggered by floodwater loading hypothesis - This is my preferred origin, the evidence for is presented in this article.

Numerous non-seismic triggers. Clastic dikes often form in response to rapid sedimentation and overloading. Dikes are widely documented in both seismically-active and low-seismicity areas and in a variety of geologic environments and deposits. While earthquakes commonly trigger liquefaction and can a produce clastic dikes, they are most commonly unsheeted, upward-tapering, and small. Dike morphology indicates whether liquefaction was involved. Evaluate taper direction, internal sheeting, and the connection to source bed to distinguish each type, its trigger, its origin. Not all clastic dikes are seismites. Figure modified from Shanmugam and others (2016, Figure 16).

Dike-sill-dike. Fluid-driven fracture and Darcy flow are concepts central to the formation of sheeted clastic dikes in the Touchet Beds. An understanding of how hydraulic fractures initiate and propagate is necessary. This can be taught at the undergraduate level. Read Jolly and Lonergan (2002), perhaps Bons and others (2022), any paper from the 1970s on liquefaction, and half a dozen short articles on sand injectites from the folks at Aberdeen. Students will pick it up. If you avoid the physics, then floundering about with earthquakes and the OWL will be your fate.

Different Features, Same Floodway

The same floods produced different types of deformation features depending on the grainsize and rheology of the sediment they encountered. Same stimulus, different response. In silt-sand rhythmites near Walla Walla, Lewiston, Cecil, and Zillah, we find sheeted, wedge-shaped dikes in the hundreds. In varved beds of the upper Columbia Valley, we find abundant t-shaped mud squirts, a few rubbly injectites, and features associated with mass wasting. In eddy bars near Umatilla and Washtucna, we find a few stubby, gravel-filled dikes with crude vertical sheeting. In silty, gravel-free silt rhythmites near the upper limit of flooding (i.e., Palouse Hills), a few thin dikes appear here and there. Where basalt was exposed at low elevation to energetic flows (Snake and Columbia gorges), a few sheeted dikes cut the bedrock. Coarse, laminated pebble-sands like those at at Qualchan, the mouth of Rock Creek, and the big quarry north of Corfu are nearly devoid of dikes. Same floods, same forces, different substrates, different features.

Deformation style varies along the flood route. Various types of soft sediment deformation structures occur in the Channeled Scablands (light blue area). Each map symbol represents multiple outcrops. Wedge-shaped sheeted dikes are common in slackwater deposits to the south, while t-shaped mud squirts are common to the north, in varved lacustrine sediments. The particular type of feature(s) present at any given location appears governed by grain size, sediment thickness, water depth, lake residence time, and perhaps others. Dikes in different facies take slightly different forms (i.e., slender in slackwater rhythmites, stubby in bar gravels), but otherwise maintain distinctive 'Touchet-type' characteristics. Dashed blue line follows a longitudinal profile of the Columbia River matched to syntheses by Atwater (1987, Figure 2) and O'Connor and others (2020, Figure 8).

Conclusions

This article summarizes my work on sheeted clastic dikes in the Channeled Scablands of WA, OR, and ID, an inland region repeatedly swept by colossal glacial floods during the Pleistocene. Thousands of sheeted clastic dikes documented here occur exclusively within the margins of the Ice Age floodway, are identical at all locations (size, shape, sedimentology, age), and formed by the same mechanism. Sand dikes can form three ways, (a) where overpressure develops resulting in hydraulic fracture followed by rapid fluidized infill (injection dikes), (b) where sand falls into an open fracture under gravity (passively-filled cracks), (c) where sand is carried in suspension by flowing water and swept into pre-existing cracks or cracks formed coincident with inundation (dikes of ambiguous origin). Field evidence supports the third option. Megafloods moving overland and deep, slow-draining slackwater lakes imposed enormous loads on sedimentary and bedrock substrates, opening wedge-shaped fractures that rapidly filled with sediment sourced from a circulating flow. Vertical sheeting reflects crack-and-fill cycling during each flood event (simple and compound dikes). New dikes followed the paths of older dikes, faults, and some bedding planes (composite dikes). Skin walls indicate leakoff began the instant sediment entered a fracture. Flutes on the interior surfaces of skin walls are directional indicators that unambiguously indicate infilling from above. New fractures must have opened from the surface and filled during successive flood events, as no dikes are filled with non-flood sediment. Dike widths roughly scale with rhythmite counts (flood events) and the largest dikes occur near basin centers, where floodwaters were deepest and rhythmite stacks thickest. Unlike most clastic dikes in the literature, the features described here did not form by liquefaction triggered by earthquakes; they are not feeder conduits to sand blows. They are flood injectites, not seismites. This study confirms a hydrofracture origin first proposed by Pogue (1998), but does not confirm lateral spreading as defined by Varnes (1978). I observed no rubble dikes filling gaps between blocks of sediment slid sideways atop a liquefied plane.

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This article expands on one published in Northwest Geology v. 49 in August 2020. Northwest Geology is published annually by the Tobacco Root Geological Society in conjunction with the TRGS field conference. TRGS is a Montana-based group of geoscience professionals. I update this online version from time to time as new information becomes available. Online version was first posted here 15 Sept 2020.

LAST UPDATED: 1 Jan 2025

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Footnote 1 Bruce Bjornstad, a retired career Quaternary geologist at Hanford, has, more than any of his PNNL colleagues, mentioned the clastic dikes in his writing, beginning with his university work in the late 1970s and continuing with his recent guidebooks on scabland geology. The primary focus of his professional career was the hydrogeological behaviour of megaflood deposits at the Hanford Nuclear Site and, to a lesser extent, sediments of the Ringold Formation. Though an author of numerous agency reports, Bjornstad has never published original work on clastic dikes. He is listed as a coauthor on Fecht and others (1999) - a mystifying publication. I believe it was compiled from Fecht's notes. The list of quotes below reveals Bjornstad's drifting opinion on the origin of the dikes through time. What accounts for these changes in opinion remains unclear. Based on their 40 years of writing, I consider Bjornstad and his Hanford colleagues to be casual observers of the dikes. They failed to seriously address the dike problem during their time.

a.) Bjornstad (1980)

"The assemblage of sedimentary structures within the Touchet Beds comparable to turbidites ...suggest periodic, rapid, subaqueous deposition of successive rhythmites by turbidity-like currents created by flood surges during a single flood. Additional evidence suggesting that flood surges rather than separate floods were responsible for rhythmite formation [includes]...the possible association relating clastic dikes with soft sediment deformation."

b.) Bjornstad (1990)

"These dikes are thought to represent dewatering structures that developed during compaction and settling of cataclysmic flood deposits during or soon after floodwaters drained from the Pasco Basin (Bergeron and others, 1987)." "Most clastic dikes, ubiquitous in flood deposits throughout the Pasco Basin, appear to have formed through forcible injection during waning stages of flooding (Black, 1979; WCC, 1981) during this time."

c.) Bjornstad and Teel (1993)

"In the Pasco Basin, clastic dikes are believed to be dewatering structures associated with lake draining following cataclysmic floods." d.) Bjornstad and others (2001)

"The dikes signify soft-sediment deformation during or soon after flooding, perhaps associated with flood-induced seismicity (Cooley and others, 1996; Fecht and others, 1999)."

e.) Bjornstad (2006)

"Clastic dikes formed during or soon after Ice Age flooding, perhaps because of ground shaking during earthquakes...If earthquakes occurred more frequently, we might expect to see more dikes in sequences of flood beds with truncations atop flood beds. But this is not the case..."

f.) Bjornstad and Lanigan (2007)

"Clastic dikes may be the result of ground shaking, which caused the wet sediments to liquefy and flow along paths of weakness down into or up along vertical earthquake-generated cracks in the flood deposits."

Footnote 2

I have not yet submitted this, or some version of it, manuscript to an academic journal. A reasonably complete version was published in Northwest Geology v. 49 published by the Tobacco Root Geological Society (Cooley, 2020). That manuscript was reviewed and approved by Mike Stickney, Director of Earthquake Studies Office at Montana Bureau of Mines and Geology and Jeff Lonn, Research Geologist also at Montana Bureau of Mines and Geology. Supporting TRGS's excellent annual field conference is far more important to me than whatever prestige I might gain through publication in a traditional journal. Thousands have read this article because it is offered free online. A few dozen might find it if it were tucked behind a journal's paywall. Paying exorbitant page rates so that others might publish my work seems a bit anachronistic, given the tools available today. When the project is complete (I consider everything here draft information), I will likely submit a much leaner version emphasizing the measurement data to Northwest Science Journal for review. Or maybe Whitman College or the Washington Geologic Survey would be interested.

Footnote 3 In our work as Whitman College geology students (Cooley, 1996; Cooley and others, 1996) and follow on studies (Niell and others, 1997; Pogue, 1998), we imprecisely stated that the dikes penetrate from top to bottom through the entire stack of rhythmites, thus were late-flooding and/or post-flooding features formed by lateral spreads triggered seismic shaking. While many dikes do cut from top to bottom through the stack, their internal structure - their vertical sheeting - preserves a more nuanced history of incremental growth coincident with flooding. Vertical sheets of sediment that comprise large dikes (sheets = dikelets = fill bands), are often truncated at their tops by depositional contacts between rhythmites and surfaces within rhythmites that correspond to abrupt changes in flow regime (i.e., upvalley flow, slackwater, downvalley drainage). The dikes do not descend from the top of the rhythmite stack.

As geologists, we think of a "clastic dike" as a single structure, but sheeted dikes are actually compound structures (multiple parts) and many are composite structures (new parts added over time). While the "dike" may crosscut an exposure, each sheet (or packages of sheets) traverses only a portion of it. The dikes grew as single fills and sheet packages during single events, and by the addition of new sheets/packages through time, each sourced from a different rhythmite. Dike growth occurred in tandem with Ice Age flood cycles, which punctuated the Pleistocene. As students, we regularly observed truncated sheets (and entire dikes) and were somewhat puzzled by them. We routinely commented to one another about them, photographed them, and sketched various truncation relationships in our field books. We did not, however, fully recognize, much less emphasize the fundamental importance sheet/package truncation plays in dike growth. The dikes are composite structures that grew wider and deeper by reinjection during dozens of catastrophic glacial outburst flood events. Truncated sheets indicate the dikes are not single-event structures injected at the tail end of Missoula flooding (crosscutting features that post-date deposition of all or most floodbeds), as our clumsy early interpretations suggest. Rather, they are long-lived structures that grew in pulses during floods over time. Many large dikes grew by repeated sheet injection over thousands of years. Their growth recurrence interval is the flood interval.

College try. My undergraduate thesis suggested slope stability controlled dike distribution in the Walla Walla Valley (Cooley, 1996). The working model, developed from readings and observations at ~30 outcrops, invoked earthquake-triggered lateral spreading to explain higher dike counts along the sloping valley sides. Listric normal faults and dikes were thought to be closely linked (i.e., the dikes are sedimented-filled tensile fractures). I recall struggling to reconcile my own field observations with diking mechanisms proposed by others: slumping during flooding (Baker, 1973) and post-flood lateral spreading (McCalpin, 1996). Neither seemed to fully explain the relationships in outcrops. This sketch approximates a flawed understanding of the factors that control diking I held at that time.

Footnote 4

The term injection has no directional implication. Injected material may have moved upward, downward, or sideways. Injection describes fracture-filling where wet or slurried material is mobilized and moves into fractured sediment or rock. The usage of injection and injectite in this article is consistent with the relevant geoscience literature (sediments and structure of petroleum reservoirs), not general textbooks on sedimentology and stratigraphy. For example, injection wells move water from the surface to the subsurface. Hydraulic injection involves the lateral propagation of fractures and proppant from the well bore into the formation. Fluidized injection is commonly used to describe both upward-pinching clastic dikes and dikes that were filled from the top.

Footnote 5 Burlingame Canyon is on private land is not accessible to the public without permission from landowners.

Footnote 6 In the course of my investigation of calcrete-bearing sediments of Plio-Pleistocene age near Othello, WA, I have not observed soft sediment deformation consistent with strong, recurrent shaking in the two dozen sections I have described. I recently correlated 28 detailed stratigraphic columns from White Bluffs by Kevin Lindsey (Lindsey and others, 1996 Appendix A), finding no evidence of repeated, widespread shaking. Soft sediment deformation in Pleistocene sediments is plainly syn-depositional. Local deformation and some small, unsheeted fluidization structures in Ringold sediments are found along Saddle Mountains' frontal thrust. Trenching by Michael West and others decades ago documented young faulting higher on the mountain. Steve Reidel never mentioned seismites in reports on Yakima Fold Belt uplifts or in map unit descriptions accompanying his geologic maps. Smith (1988a,b) and Ebinghaus and others (2012) studied CRB interbeds (Ellensburg Fm), finding no evidence of strong shaking. About 10 paleoseismic trenches opened across YFB faults and logged by USGS and others contain no liquefaction features.

Footnote 7

A package of fill bands injected during a single flood. Three fill bands comprise a composite clastic dike in the idealized example above. Each band formed at a slightly different time during a megaflood event. Each fracture opening corresponds with a slightly different flow regime, taps a slightly different stratigraphic level within a rhythmite as it forms, and accesses sediment of a different grainsize. Substitute different flood beds for stratigraphic position within a single bed to explain reinjected dikes in the region. At a larger scale, dike fills reflect the caliber of the sediment available to them. Grainsize in flood deposits is primarily determined by the local flow regime - high-energy channel, backflooded valley, slackwater lake. Since the configuration of most valleys and bedrock water gaps were not radically changed by flood erosion, successive floods produced more or less the same flow regimes and deposited the same grainsizes in the same places over and over. For example, the protected Touchet Valley received mostly medium to fine sand and silt. Dikes there are filled with the same. The Starbuck area, situated close to high-velocity coulees, received more gravelly sand. Dikes there are filled with coarser material. A page from one of my field books.

Footnote 8

I update this online document from time to time as new information becomes available. This seems a modern way to do things. I prefer to provide updates as they come rather than wait for some journal to publish something formatted to their liking.

Footnote 9

If my work informs yours, you should cite this web-based article or the original print article (Cooley, 2020). What is presented here is new work and original work. It is entirely my own. Please include the date you accessed it in your citation.

Cooley, S.W., date accessed, Sheeted clastic dikes in the megaflood region, WA-OR-ID-MT, www.skyecooley.com/single-post/2020/09/15/Sheeted-Clastic-Dikes-in-the-Megaflood-Region

Cooley, S.W., 2020, Sheeted clastic dikes in the megaflood region, WA-OR-ID-MT in Lonn, J; English, A.; McDonald, K.; Hargrave, P. (editors), Northwest Geology: Journal of the Tobacco Root Geological Society, 45th Annual Field Conference - Geology of the Bitterroot Region and Other Papers v. 49, p. 1-17

Footnote 10

Where cementation has not occurred, sedimentary dikes may act as conduits through which fluids introduced long after intrusion may migrate (Jenkins, 1930; Dixon and others, 1995; Jonk and others, 2003; Mazzini and others, 2003; Huuse and Mickleson, 2004; Ross, 2013). Fluids such as hydrocarbons and chemical waste are particularly important.

A 1996 Final EIS for tank wast remediation (USDOE/WADOE, 1996) reveals a fundamental lack of understanding of the dikes by geohydrologists at Hanford.

As with the genesis of [the] clastic dikes, little is known about their hydraulic characteristics...the inferred hydraulic nature of the dikes is that of potentially a minor barrier to flow perpendicular to the dike. The clay content and lack of sand stringer continuity suggest that clastic dikes do not function as preferential flow paths for vertical flow.

Concerns over the potential for dikes to serve as preferential conduits for liquid waste leaked to subsurface aquifers have been raised by a number of Hanford researchers (Cushing, 1994; Finfrock, 1994; USDOE, 1996; Caggiano, 1996; Fecht and Weekes, 1996; Fayer and Ritter, 1999; Faybishenko and others, 2000; Murray and others, 2001; Serne and others, 2002; Dinwiddie, 2003; Fendorf and Jardine, 2003; Caggiano and others, 2004; Gee and others, 2007; Murray and others, 2007; Reidel and Chamness, 2007; Fayer and others, 2010; Rockhold and others, 2015; Springer and others, 2017; Zhou and others, 2023; INTERA/Nichols, 2023). Such concerns justified an infiltration field experiment on a large dike in Touchet Beds off Army Loop Road (Murray and others, 2003, 2007; Ward and Gee, 2003; Ward and others, 2006).

A lithified clastic dike penetrating bedrock at the Rocky Mountain Arsenal in Colorado raised similar concerns decades before the Murray report (Miller and others, 1979). Liquid waste introduced deliberately to the suburface was also a problem at RMA. Characterization of clastic dikes as lateral barriers to migrating fluids is an idea adopted by Hanford authors, though few geological similarities between dikes in Washington and Colorado exist,

A vertical, tabular body embedded in fine-grained, tuffaceous, calcareous sandstones, siltstones, and shales has been reported at the Rocky Mountain Arsenal. The tabular body has the mineralogy and structure of an igneous dike, but it may also be a clastic dike of sedimentary origin. The possibility that the body may be an igneous dike is of concern to the staff geologists at the Arsenal because it could extend to great depth and be impermeable enough to provide a barrier to laterally migrating ground water or, conversely, it could be relatively permeable and provide an aquifer.

The figure below shows the results from an infiltration test where water-borne dye tracer was introduced to the ground surface via driplines and allowed to spread by gravity into in a.) a large, vertical, sheeted clastic dike, b.) a large, sheeted, subhorizontal sill joined to the dike, and c.) non-dike Touchet Bed sediment surrounding both. Red and yellow areas indicate high reflectance values (high moisture content). Odd how reflectance values and moisture values in the chart below disagree. The figure is redrawn from Murray and others (2001, Fig. 7.33, 7.34). I've reframed their nearly unintelligible artwork, thus presented their study's key finding clearly. Note the sill at left is as wet or wetter (containing and conducting as much or more dye tracer) as the vertical dike at center. The report did not address the intersecting sill.

The Murray experiment, a follow-on project to Sisson and Lu (1981), is regularly referenced despite its flawed design. The experiment failed to consider flow in the large sill connected to the dike and did not test flow in a multi-dike network, the typical configuration of dikes beneath Hanford. The various progress reports gives the impression that the field effort was a start-and-stop affair involving many enthusiastic lab scientists doing something (outdoors!) for the first time. Ten collaborators are listed.

If Hanford geologists actually wanted to find out how clastic dikes conduct fluids leaked from the surface, they would have repeated this experiment at several locations, evaluating flow in dike-sill networks and various grainsize combinations of dike fills and host materials (i.e, fine grain dikes in a gravelly host, gravel dike in fine-grained host). The Murray team studied one dike at one location. Hardly the rigorous investigation of which our National Labs are capable. But gee whiz, Murray gave it the old College Try, didn't he?

I redrew this key figure to make it intelligible.

Clastic dike exposed in the Army Loop Road excavation. Grid on lowest tier is 2m wide x 1m high. Blue tent covers infiltration dripline equipment. Photo: Murray team.

Clastic dike and sill are much finer-grained than host sediment. Photo: Murray and others, 2003, Fig. 10.

Infiltration in dike, sill, and host sediment after 3 days. Murray and others, 2003, Fig. 16.

Infrared image (top) and a composite photograph of the experiment pit face. Black vertical dike is on the left in both images. Sill is the long, black, horizontal feature extending from the right side of the dike. It looks like bedding. Photo: Murray and others, 2003, Fig. 12.

Clastic dike polygonal network along the Army Loop Road near the infiltration study site. Google Earth photo.

Footnote 11

J Harlan Bretz did not pay much attention to clastic dikes in the Channeled Scabland, but a few mentions do pop up in his copious field notes (see Bretz's newly found notebooks archived at nickzentner.com). On August 7, 1928 at "Gardena Cliffs" just south of Touchet, WA he writes, "Clastic dikes are prominent, some of them wedging out halfway down the cliff, some continuing to the bottom of the section...Wedges of the fine sand at angles of 40 degrees from horizontal penetrate or appear to penetrate up into the gravel for three or four feet" (1928 typed field notes, p. 27). On August 10, 1928 in the Walla Walla Valley, he reports, "Clastic dike of marvellous development abundant in these sections. But tho they contain the coarse black sand, they are not responsible for the pockets and lenses [ice rafted berg mounds containing non-basaltic clasts]. One clastic dike has seams of sand separated by seams of clay in the prevailing mode but seams of good brown sand" (1928 typed field notes, p. 34-35). On July 29, 1928 at Willow Creek, WA he finds, "fingers of the black sand extend from the gravel into the silt." (1928 typed field notes, p. 8). Dikes are again observed near Clarkson and Asotin in his 1928 field notes (p. 43). Bretz also describes aseismic deformation in the Touchet Beds in his typed field notes and in one article (August 14, 1923; Bretz, 1928b, Fig. 9 photo above; July 15, 1929).

The caption for the 1928 photo above reads,

Contorted bedding in silt and fine sand, Walla Walla Valley. Etched into relief by the wind.

In the body of the article, he notes,

Marked irregularities in stratification of sandy phases occur. One such structure is illustrated in Figure 9. No satisfactory explanation for this is at hand.

In 1923, Bretz writes,

Along Sunset Hiway, 4-5 miles north of Wenatchee, is a cut showing a seasonably banded silt about 200 ft above the altitude of Wenatchee. 30-foot section. Silt is pale buff in color. Some portions a very fine sand, somewhat more gray or brown colored. The seasonal banding is far from perfect thruout...In most summer bands, is a delicate foreset or current bedding, showing very gentle southward drift of the material along the bottom. This doesn't seem right for a water body which recorded varve clays. And there are several other unorthodox things too. Portions of the deposit which do not show varve clay stratification are composed of fine sand to silt, not of clay. Current bedding is prominent in this, much more so than in the summer varves. Here and there in the section are worn pebbles and cobble not of basalt or the local granite. These undoubtedly show the presence of floating ice. In certain layer of the finer silt are most peculiar contortions of the laminae, tho the strat immediately above or below are not affected. Some of these contortions were sketched. In each sketch, one prominent continuous lamina has been shown. The others are squeezed or thickened to conform. In [sketch 3] the little triangular areas show fragmentation and porosity. These plications or contortions have a strike. They are rolls! And the strike is essentially parallel to the wall of the valley here. Other evidence, in the existence of gentle flexures in the strata themselves, seems to point to settling of the material down a subaqueous slope toward the deeper parts of the valley as the cause for the distortion.

Bretz's only mention of clastic dikes arrives on July 15, 1929 in typed field notes on Tammany Bar at Lewiston, ID. This is four years after publication of the first article on Touchet Bed clastic dikes by O.P. Jenkins, who visited this same exposure. At Lewiston, Touchet Beds ("silts") overlie a boulder gravel bar left by the Bonneville flood.

The silt rests directly on the rough bouldery surface of the gravel deposit, some boulders a foot or two in diameter setting up on top of the gravel project for their full diameter into the silt...The silt is well sorted, no scattered particle of basalt, etc., rather irregular bedding. Lenses of black coarse sand occur irregularly, the contact of sand on silt being so irregular that it seems like a cross section of miniature mountain topography. To add to the puzzle, clastic dikes can be traced up in the deposit, thickening with increasing height and some of them abruptly ending at various levels. This silt looks more like a normal stream alluvium, the cracks developing at successive intervals while the accumulation was going on per saltum, thus some of the cracks being filled and covered over before other cracks were formed. Yet there is no such sand on top of the silt today from which the the major number of the cracks (coming to the top) could be filled. Such sand deposit may once have been present, and now gone by erosion.

Footnote 12

Future Work. My field data collection effort has spanned many years, yet could be repeated if the outcrops remain. I have taken copius field notes and built an organized archive of information on the outcrops I have visited. If a future geologist is interested in revisiting sites at which I ahve collected measurements, they would complete the task much quicker since a map now exists to guide them. Locating and accessing dozens of new (previously unreported) outcrops throughout this large study area took hundreds of days in the field. If you are a student or geologist interested in conducting your own project on clastic dikes, please feel free to contact me. Happy to help.

Footnote 13

Newman and others titled their 2002 article "High frequency electromagnetic impedance imaging for vadose zone and groundwater characterization". The first sentence of the Executive Summary reads,

Executive Summary - A geophysical experiment is described for characterizing the clastic dike systems, which are ubiquitous within the vadose zone at the Hanford Nuclear Reservation.

The Abstract contrasts markedly with the Executive Summary. It also removes the words "clastic" or "dike". The author replaced "clastic dike" with the word "heterogeneity". Who does that?

Abstract - Accurate description of transport pathways on the gross scale, the location of contamination, and characterization of heterogeneity within the vadose zone, are now realized as vital for proper treatment, confinement and stabilization of subsurface contamination at Department of Energy (DOE) waste sites. Electromagnetic (EM) methods are ideal for these tasks since they are directly sensitive to the amount of fluid present in porous media, as well as fluid composition. At many DOE sites it is necessary to employ lower frequency (<1 MHz) or diffusive electromagnetic fields because of the inability of ground penetrating radar (GPR) to penetrate to sufficient depths. The high frequency impedance method, which operated in the diffusive frequency range (10 Hz to 1 MHz), as well as the low end of the spectrum employed by GPR (1MHz-10 MHz), is an ideal technique to delineate and map the aforementioned targets. The method has clearly shown the potential to provide needed information on variations in subsurface saturation due to local storage tanks and perched water zones, as well as mapping geological structures related to the subsurface hydrological properties and heterogeneity within the vadose zone. Although it exhibits certain advantages over other EM methods, the impedance method comes with a set of assumptions and practices that can limit its potential. The first is the desire to locate receivers in the far-field of the transmitter which allows the use of magnetotelluric (MT) inversion codes to interpret the data. Unfortunately, one does not precisely know when one is in the far-field of the transmitter, because this depends on the geology we wish to image. The second limiting factor is the scarcity of complete 2D and 3D inversion schemes necessary to properly invert the data. While approximate 2D schemes are now emerging, rigorous 2D and 3D inversion codes are needed to bound the range of applicability of the approximate methods. We propose to address these problems in the following manner: (1) implement full non-linear 2D/3D inverse solutions that incorporate source coordinates and polarization characteristics, (2) use these solutions to study improvements in image resolution that can be obtained by making measurements in the near- and mid-field regimes using multiple source fields, (3) collect data at the Hanford Reservation with recently developed earth impedance measurement systems, and (4) interpret the field data with the newly developed inversion capability, as well as with additional and independent information such as well logs from boreholes. The benefit of this research to the DOE would be a combined measurement/interpretation package for non-invasive, high-resolution characterization of larger transport pathways, certain types of contamination, and heterogeneity within the vadose zone at the Hanford reservation, as well as other DOE facilities.

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Dikes in Patagonia. The caption reads, "Another detail of the clastic dike, which reveals the exceptional apophyseal body, the only dike like this in this group of clastic viens in Tierra del Fuego. ar = Tertiary sandstone, ae = Tertiary claystone." Source: Borrello, A.V. (1962), Sorbre los diques clastico de Tierra del Fuego (About the clastic dikes of Tierra del Fuego), Universidad Nacional de la Plata, Facultad de Ciencias Naturales y Museo, Revista del Museo de la Plata, Tomo V, Geologia No. 32, p. 155-191

Footnote 14

In 2016, while living in Alaska, I received a phone call from Steve Obermeier, a USGS geologist with whom I'd not previously corresponded. He called to discuss clastic dikes and offer me a co-authorship on an article he was preparing for publication. I was excited, but wary. Excited because its not every day one receives a call from a USGS geologist. Wary because I was familiar with Obermeier's excellent work on sand blows in the southeastern U.S. (New Madrid) as well as his sketchy work on clastic dikes in Eastern Washington. We spoke for about 15 minutes and I asked if he would send me the manuscript to review. Instead, he sent two articles from some engineering journal. A follow up email and the manuscript eventually arrived. At the top of the document was the note below, from the internal reviewer at USGS. Obermeier and coauthors had drafted up an incredibly weak article containing no new data and several figures that looked suspiciously like my own. I would likely have been excluded entirely, but for the reviewer's suggestion that someone should contact me, the only person working on clastic dikes in Washington at the time. Just as well. Odd that Kevin Pogue, a listed co-author and my former undergraduate thesis advisor (Cooley, 1996; Cooley et al., 1996; Pogue, 1998), didn't call me, but Steve did. I wrote Obermeier a few days later to decline co-authorship and any further involvement. Their manuscript was never published.

Footnote 15

Relevant equations. This article provides limited discussion on the set of equations relevant to fluid-driven fracture and diking. The equations above are basic elements of undergraduate-level courses in Fracture Mechanics. Quality YouTube channels teaching this stuff include Nicholas Espinoza, Scott Ramsay, Taylor Sparks, and others. Elastic Pressure (Pe) describes properties of the fractured material. Specifically, the stress perpendicular to a crack required to keep it open, where h is crack width, L is crack length, G is the shear modulus, and v is Poisson's ratio. Source Pressure (Pr) is fluid pressure of the source, considered here to be the pressure of the sediment-water slurry at base of a megaflood or slackwater lake, measured at the opening (top) of the crack. Source Pressure is assumed to be constant during diking. E is Young's modulus of the host sediment or rock, delta p is the density difference between host and the injected fill, g is gravity, Q is the volumetric flux of material injected into the crack, and u is the average injection velocity. Viscous Pressure Drop (Pv) is the pressure change along its length from crack opening to crack tip, where n is the slurry viscosity. Fracture Pressure (Pf) is the pressure required to propagate the crack tip forward, where Kc is the critical fracture toughness. Hydrostatic Pressure (buoyancy) is ignored for near-surface sedimentary dikes at atmospheric temperatures.

Footnote 16

The term "neptunian dike" is occasionally encountered in the literature. Usage of the somewhat obscure term is all over the map and can cause confusion. Neptunian dikes are fissure fills found primarily in marine carbonates and some brackish terrestrial deposits (Smart and others, 1988). They most commonly form underwater by passive infilling of tension cracks along reef escarpments at rates determined by the depositional setting. Their fills may be sheeted or unsheeted and typically consist of locally-derived sedimentary material, including sand grains, oolite, grainstone, biomicrite, and/or calcite cement. Some are chert-filled and others are dolomitized. Many show evidence of incremental widening (refracture), repeated infill, and rapid re-cementation. Lengths of neptunian dikes range from meters to kilometers and widths from centimeters to meters. Sills with the same characteristics are sometimes encountered with the dikes.

Curious cracks. The Russian geologist P.M. Alekseevich snapped this photo of clastic dikes in Siberia c. 1910 during an expedition through the Lovozersky District on the Kola Peninsula. The dikes are filled with sediment (not ice), appear to have sheeted fills, and are associated with lighter-colored horizons (sandy layers in shale?). Smaller dikes branch off from larger dikes and overprint a polygonal fracture network. Source: Pavlov M. Alekseevich archive, Library of Congress and V.K. Arseniev Museum of the Far East in Vladivostok.

Footnote 17

Hanford's Problematic Contributions - Eighty years of reporting on dike-riddled deposits by geoscientists at the U.S. Department of Energy's Hanford Site (Pacific Northwest National Laboratory) provides no clarity as to dike origin. Fundamental questions posed by workers there remain unresolved decades later. Do the dikes intrude upward or downward? Are they seismites? How old are they? Are dike walls composed of clay or silt? Do they intersect the water table? Do they serve as fast conduits for liquid waste to subsurface aquifers? Hanford's collective contribution to clastic dike research is remarkably weak, especially considering it is a well-funded, well-staffed National Lab (Cushing, 1994; Finfrock, 1994; USDOE, 1996; Caggiano, 1996; Fecht and Weekes, 1996; Fayer and Ritter, 1999; Faybishenko and others, 2000; Murray and others, 2001; Serne and others, 2002; Dinwiddie, 2003; Fendorf and Jardine, 2003; Caggiano and others, 2004; Gee and others, 2007; Murray and others, 2007; Reidel and Chamness, 2007; Fayer and others, 2010; Rockhold and others, 2015; Springer and others, 2017; Zhou and others, 2023).

Publications on clastic dikes in the Channeled Scablands. Approximately 104 articles, abstracts, field guides, agency write-ups, and consultant reports have been published on the clastic dikes in Eastern Washington since 1925. Most simply mention the dikes in passing. Few contain measurements of any kind. Several of the Hanford articles in the 2000s are progress reports that derive from a single infiltration experiment conducted on one large dike located off Army Loop Road.

Instead of peer-reviewed journals, Hanford self-publishes many of its geological reports directly to the web through PNNL. Older reports are scanned and made available to the public via searchable archives, yet certain publications remain buried. For example, Fecht and Weekes (1996), a relatively recent, seemingly important study referenced several times in a Final EIS for a tank farm clean-up project, does not appear in searches of the Hanford Administrative Record, WADNR Geology Library, University of Washington Library, WorldCat, or Google Scholar. A FOIA request was needed to produce a copy of the minor report. Other oddities are regularly encountered. Some Hanford authors substitute the word "heterogeneities" for "clastic dikes" or neatly tailor report titles to confound keyword searches (i.e., Newman and others, 2002). The same article (Murray and others, 2007) comprised 6 of the first 10 results returned in a recent search of OSTI.gov on "clastic dikes" (search made 5 January 2025). Consultant's reports are often no better. For example, a 2023 INTERA report (Nichols, 2023) bungles basic facts about the dikes,

The source of the dikes is assumed to be sediment from the Ringold Formation...and found to extend through the Hanford formation and Holocene to the surface.

Mystifying and myopic, Hanford geologists' understanding of clastic dikes in the Columbia Basin harkens from some strange netherworld, where field skills have atrophied and rumors about the geology have supplanted first-hand observation. Replete with internal inconsistencies (see Footnotes 1 and 13), their reporting stands apart from the rest of the published literature on the topic, which continues to progress. Other than subsurface borehole logs and the occasional photograph, the Hanford literature on dikes is best read and promptly forgotten.

References

Alwin, J.A., and Scott, W.E., 1970, Clastic dikes of the Touchet Beds, southeastern Washington: Northwest Science, v. 44, p. 58. Ambraseys, N.N., 1991, Engineering seismology: International Journal of Earthquake Structural Dynamics, v. 17, p. 1-105. Atwater, B.F., 1986. Pleistocene glacial-lake deposits of the Sanpoil River Valley, northeastern Washington: U.S. Geological Survey Bulletin 1661, 39 pgs. Atwater, B.F., 1994, Geology of Holocene liquefaction features along the lower Columbia River at Marsh, Brush, Price, Hunting, and Wallace Island, Oregon and Washington: U.S. Geological Survey Open-file Report 94-209, 64 pgs. Bader, N.E., Spencer, P.K., Bailey, A.S., Gastineau, K.M., Tinkler, E.R., Pluhar, C.J., and Bjornstad, B.N., 2016, A loess record of pre-Late Wisconsin glacial outburst flooding, Pleistocene paleoenvironment, and Irvingtonian fauna from the Rulo site, southeastern Washington, USA: Palaeogeography, Palaeoclimatology, Palaeoecology, v. 462, p. 57-69. Baker, V.R., 1973, Paleohydrology and sedimentology of Lake Missoula flooding in Eastern Washington, Geological Society of America Special Paper 144, 79 pgs. Baker, V.R., and Bunker, R.C., 1985, Cataclysmic Late Pleistocene flooding from Glacial Lake Missoula, A review: Quaternary Science Reviews, v. 4, p. 1-41. Baker, V.R., Bjornstad, B.N., Gaylord, D.R., Smith, G.A., Meyer, S.E.,Alho, P., Breckenridge, R.M., Sweeney, M.R., Zreda, M., 2016, Pleistocene megaflood landscapes of the Channeled Scablands: in Lewis, R.S., and Schmidt, K.L., eds., Exploring the Geology of the Inland Northwest: Geological Society of America Field Guide 41, 73 pgs.

Beaulieu, J.D., 1974, Geologic hazards of Hood River, Wasco, and Sherman Counties, Oregon: Oregon Department of Geology and Mineral Industries Bulletin, v. 91, p. 18.

Benito, G., and O'Connor, J.E., 2003, Number and size of last-glacial Missoula floods in the Columbia River valley between the Pasco Basin, Washington, and Portland, Oregon: Geological Society of America Bulletin, v. 115, p. 624-638. Bennett, S.E.K., Sherrod, B.L., Kelsey, H.M., Reedy, T.J., Lasher, J.P., Paces, J.B., and Mahan, S.A., 2016, History of recent surface rupturing earthquakes on the Burbank fault, Yakima Folds, central Washington: American Geophysical Union Fall Meeting, Abstract T41B-2908. Bingham, J.W., and Grolier, M.J., 1966, The Yakima Basalt and Ellensburg Formation of south-central Washington: U.S. Geological Survey Bulletin 1224-G

Bjornstad, B.N., 1982, Catastrophic flood surging represented in the Touchet Beds of the Walla Walla Valley, Washington: American Quaternary Association 7th Biennial Conference Program and Abstracts, p. 72.

Bjornstad, B.N., 2006, On the trail of the Ice Age Floods: A geological field guide to the Mid-Columbia Basin, Keokee Books, 308 pgs. Bjornstad, B.N., Fecht, K.R., and Tallman, A.M., 1990, Quaternary stratigraphy of the Pasco Basin area, south-central Washington: Rockwell International Report RHO-BW-SA-563A, 24 pgs. Bjornstad, B.N., and Teel, S.S., 1993, Natural analog study of engineered protective barriers at the Hanford Site: Pacific Northwest Lab Report PNL-8840 UC-510. Bjornstad, B.N., Fecht, K.R., and Pluhar, C.J., 2001, Long history of Pre-Wisconsin Ice Age cataclysmic floods: Evidence from southeastern Washington State: Journal of Geology, v. 109, p. 695-713. Bjornstad, B.N., and Lanigan, D.C., 2007, Geologic descriptions for the solid-waste low level burial grounds: Pacific Northwest National Lab Report PNNL-16887. Black, R.F., 1979, Clastic dikes of the Pasco Basin, southeastern Washington: Rockwell Hanford Report RHO-BWI-C-64, 65 pgs. Braccini, E., Boer, W., Hurst, A., Huuse, M., Vigorito, M., and Templeton, G., 2008, Sand injectites: Oilfield Review, v. 20, p. 34-49. Bretz, J H., 1929, Valley deposits immediately east of the Channeled Scabland of Washington: Journal of Geology, v .37, p. 393-427.

Bretz, J H., 1929, Unpublished field notes, University of Chicago Library Archives Boyd, K.F., and Schumm, S.A., 1995, Geomorphic evidence of deformation in the northern part of the New Madrid seismic zone: U.S. Geological Survey Professional Paper 1538-R, p. 1-35.

Brown, D.J., and Brown, R.E., 1962, Touchet clastic dikes in the Ringold Formation: Hanford Atomic Products Operation Report HW-SA-2851, 11 pgs.

Busacca, A.J. and 5 others, 2004, Eolian sediments, Developments in Quaternary Science, v. 1, p. 275-309

Campbell, N.P.; Repasky, T.R.; Ring, T.E.; Becenti, T.C.; Busacca, A.J., 1994, Recurrent Holocene to Recent movement in the Toppenish Ridge fault system, south-central Washington, GSA Abstracts with Programs, v. 26, p. 187

Campbell, N.P., Ring, T., Repasky, T., 1995, Final report, 1994 NEHRP grant earthquake hazard study of the vicinity of Toppenish Basin, south-central Washington: Technical report to USGS (Contract 1434-94-G-249), in M.L. Jacobson (compiler), National Earthquake Hazards Reduction Program (NEHRP) Annual Project Summaries XXXVI, USGS Open-file Report 95-210 Part I, p. 291-306

Carson, R.J., McKhann, C.F., and M.H. Pizey, M.H., 1978, The Touchet Beds of the Walla Walla Valley: in Baker, V.R., and Nummedal, D. (eds.), The Channeled Scabland: National Aeronautics and Space Administration, p. 173-177. Cobain, S.L., Hodgson, D.M., Peakall, J., and Shiers, M.N., 2016, An integrated model of clastic injectites and basin floor lobe complexes, implications for stratigraphic trap plays: Basin Research, v. 29, p. 816-835. Coppersmith, R., Hanson, K., Unruh, J., and Slack, C., 2014, Structural analysis and Quaternary investigations in support of the Hanford PSHA in Hanford Sitewide Probabilistic Seismic Hazard Analysis: Pacific Northwest National Laboratory Report No. 23361, 173 pgs. Cooley, S.W., 2015, The curious clastic dikes of the Columbia Basin: in Carson, R.J., Many Waters, Natural history of the Walla Walla Valley and vicinity: Keokee Books, p. 90-91 Cooley, S.W., Unpublished photograph of clastic dikes descending from the base of a debris flow deposit in Black Dragon Canyon, San Rafael Swell, UT:

https://commons.wikimedia.org/wiki/File:Dikes_in_black_dragon_canyon_UT.JPG Cooley, S.W., 2014, Exposures of large clastic dikes in Columbia Basin: A geologic traverse through Washington, Oregon, and Idaho, in Northwest Geology, Tobacco Root Geological Society Guidebook v. 43, p. 133-147

Clastic Dikes Field Guide_Northwest Geology Journal v43_TRGS_SWCooley 2014.pdf

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Cooley, S.W., Pidduck, B.K., and Pogue, K.R., 1996, Mechanism and timing of emplacement of clastic dikes in the Touchet Beds of the Walla Walla Valley, south-central Washington: Geological Society of America Abstracts with Programs, v. 28, p. 57.

Fecht, K.R., Bjornstad, B.N., Horton, D.G., Last, G.V., Reidel, S.P., and Lindsey, K.A., 1999, Clastic injection dikes of the Pasco Basin and vicinity: Bechtell-Hanford Report BHI-01103, 217 pgs. Feng, Z.Z., 2017, Preface of the Chinese version of "The seismite problem": Journal of Palaeogeography, v. 6, p. 7-11. Flint, R.F., 1938, Origin of the Cheney-Palouse scabland tract: Geological Society of America Bulletin, v. 46, p. 169-194. Foundation Sciences, Inc., 1980, Geologic reconnaissance of parts of the Walla Walla and Pullman, Washington, and Pendleton, Oregon 1 x 2 degree AMS quadrangles: U.S. Army Corps of Engineers-Seattle District, Report DACW67-80-C-0125, 144 pgs. Fuller, M.L., 1912, The New Madrid earthquake: U.S. Geological Survey Bulletin 494, 129 pgs. Galli, P., 2000, New empirical relationships between magnitude and distance for liquefaction: Tectonophysics, v. 324, p. 169-187. Glenn, J.L., 1965, Late Quaternary Sedimentation and Geologic History of the North Willamette Valley, OR: PhD Dissertation, Oregon State University, 248 pgs. Gohn, G.S., Weems, R.E., Obermeier, S.F., and Gelinas, R.L., 1984, Field studies of earthquake-induced, liquefaction-flowage features in the Charleston, South Carolina, area: U.S. Geological Survey Preliminary Report, 29 pgs. Hanson, M.A., Lian, O.B., and Clague, J.J., The sequence and timing of large late Pleistocene floods from glacial Lake Missoula: Quaternary Science Reviews, v. 31, p. 67-81. Herriott, T.M., Reger, C.J., Wartes, R.D., LePain, M.A., and DL Gillis, R.J., 2014, Geologic context, age constraints, and sedimentology of a Pleistocene volcaniclastic succession near Mount Spurr volcano, south-central Alaska: Alaska Division of Geological and Geophysical Surveys, Report of Investigation RI-2014-2, 35 pgs. Holtzer, T.L., Noce, T.E., and Bennett, M.J., 2011, Strong ground motion inferred from liquefaction caused by the 1811-1812 New Madrid, Missouri, earthquakes: Bulletin of the Seismological Society of America, v. 105, p. 2589-2603. Hyashi, T., 1966, Clastic dikes in Japan: Japanese Journal of Geology and Geography, v. 37, p. 1-20. Jenkins, O.P., 1925, Clastic dikes of eastern Washington and their geologic significance American Journal of Science: v. 57, p. 234-246. Jolly, R.J., and Lonergan, L., 2002, Mechanisms and controls on the formation of sand intrusions: Journal of the Geological Society, v. 159, p. 605-617. Jones, F.O., and Deacon, R.J., 1966, Geology and tectonic history of the Hanford Area and its relation to the geology and tectonic history of the state of Washington and the active seismic zones of western Washington and western Montana: Douglas United Nuclear, Inc. Consultants Report DUN-1410, 50 pgs. Kiver, E.P., Stradling, D.F., Roberts, S., and Fountain, D., 1982, Quaternary geology of the Spokane area: Tobacco Root Geological Society 1980 Field Conference Guidebook, p. 26-44.

Kruger, F.C., 1938, A clastic dike of glacial origin, American Journal of Science 5th Series, v.35, p. 305-307 Le Heron, D.P., and Etienne, J.L., 2005, A complex subglacial clastic dyke swarm, Myrdalsjokull, southern Iceland: Sedimentary Geology, v. 181, p. 25-37. Lidke, D.J., Johnson, S.Y., McCrory, P.A., Personius, S.F., Nelson, A.R., Dart, R.L., Bradley, L., Haller, K., and Machette, M.N., 2003, Map and data for Quaternary faults and folds in Washington State, U.S. Geological Survey Open-file Report 03-428, 16 pgs. Lindsey K.A., 1996, The Miocene to Pliocene Ringold Formation and associated deposits of the ancestral Columbia River system, south-central Washington and north-central Oregon: Washington Division of Geology and Earth Resources, Open-file Report 96-8, 176 pgs. Lupher, R.L., 1944, Clastic dikes of the Columbia Basin region, Washington and Idaho: Bulletin of the Geological Society of America, v. 55, p.1431-1462. McCalpin, J.P., 2009, Paleoseismology (2nd Edition), Academic Press, 613 pgs. Meyer, S.A., 1999, Depositional history of pre-Late and Late Wisconsin outburst flood deposits in northern Washington and Idaho, Analysis of flood paths and provenance: MS Thesis, Washington State University, 91 pgs.

Miller, C.H.; Odum, J.K.; Lindvall, R.M.; Collins, D.S., 1979, Preliminary magnetic, seismic, and petrographic investigations of a possible igneous dike at the Rocky Mountain Arsenal, Denver, Colorado, USGS Open-file Report 79-1685, 18 pgs. Montenat, C., Barrier, P., d'Estevou, P.O., and Hibsch, C., 2007, Seismites: An attempt at critical analysis and classification: Sedimentary Geology, v. 196, p. 5-30. Moretti, M, and Van Loon, A.J, 2014, Restrictions to application of 'diagnostic' criteria for recognizing ancient seismites: Journal of Palaeogeography, v. 3, p. 162-173.

Murray, C.; Ward, A.; Wilson, J., 2003, Influence of clastic dikes on vertical migration of contaminants in the vadose zone at Hanford, Pacific Northwest National Lab report, PNNL-14224, 41 pgs. Neill, A. R., Leckey, E.H., and Pogue, K.R., 1997, Pleistocene dikes in Tertiary rocks: Downward emplacement of Touchet Bed clastic dikes into co-seismic fissures, south-central Washington: Geological Society of America Abstracts with Programs, v. 29, p. 55. Newcomb, R.C., 1962, Hydraulic injection of clastic dikes in the Touchet Beds, Washington, Oregon, and Idaho: Geological Society of the Oregon Country Bulletin, v. 28, p. 70. Obermeier, S.F., 1996, Use of liquefaction-induced features for paleoseismic analysis: An overview of how seismic liquefaction features can be distinguished from other features and how regional distribution and properties of source sediment can be used to infer the location and strength of Holocene paleoearthquakes: Engineering Geology, v. 44, p. 1-76. Obermeier, S.F., Olson, S.M., and Green, R.A., 2005, Field occurrences of liquefaction-induced features: A primer for engineering geologic analysis of paleoseismic shaking: Engineering Geology, v. 76, p. 209-234. Obermeier, S.F., 2009, Chapter 7: Using liquefaction-induced features for paleoseismic analysis: in McCalpin, J.P., ed., Paleoseismology, Academic Press, p. 497-564. Obermeier, S.F., 1998, Liquefaction evidence for strong earthquakes of Holocene and latest Pleistocene ages in the states of Indiana and Illinois, USA: Engineering Geology, v. 50, p. 227-254. Obermeier, S.F., 1998, Seismic liquefaction features: Examples from paleoseismic investigations in the continental United States: U.S. Geological Survey Open-file Report 98-488 (web version only), https://pubs.usgs.gov/of/1998/of98-488. Obermeier, S.F., Martin, J.R., Frankel, A.D., Youd, T.L., Munson, P.J., Munson, C.A., and Pond, E.C., 1993, Liquefaction evidence for one or more strong Holocene earthquakes in the Wabash Valley of southern Indiana and Illinois, with a preliminary estimate of magnitude: U.S. Geological Survey Professional Paper 1536, 27 pgs. Obermeier, S.F., Olson, S.M., and Green, R.A., 2005, Field occurrences of liquefaction-induced features: a primer for engineering geologic analysis of paleoseismic shaking: Engineering Geology, v. 76, p. 209-234. Peterson, C.D., and Madin, I.P., 1998, Coseismic paleoliquefaction evidence in the central Cascadia margin, USA: Oregon Geology, v. 59, p. 51-74. Phillips, E.; Lipka, E., and van der Meer, J.J., 2013, Micromorphological evidence of liquefaction, injection and sediment deposition during basal sliding of glaciers: Quaternary Science Reviews, v. 81, p. 114-137. Pogue, K.R., 1998, Earthquake-generated(?) structures in Missoula flood slackwater sediments (Touchet Beds) of southeastern Washington: Geological Society of America Abstracts with Programs, v. 30, p. 398-399.

Pritchard, C.J., and Cebula, L., 2016, Geologic and anthropogenic history of the Palouse Falls area: Floods, fractures, clastic dikes, and the receding falls: in Lewis, R.S., and Schmidt K.L., eds.: Geological Society of America Field Guide, v. 41, p. 75-92. Rigby, J.G., 1982, The sedimentary, mineralogy, and depositional environment of a sequence of Quaternary catastrophic flood-derived lacustrine turbidites near Spokane, WA: MS Thesis, University of Idaho, 132 pgs. Russell, I.C., 1893, A geological reconnoissance in central Washington: U.S. Geological Survey Bulletin 108, 108 pgs. Seilacher, A., 1969, Fault-graded beds interpreted as seismites: Sedimentology, v. 13, p. 15-159. Shanmugam, G., 2016, The seismite problem: Journal of Palaeogeography, v. 5, p. 318-362. Shaw, J., Munro-Stasiuk, M., Sawyer, B., Beaney, C., Lesemann, J., Musacchio, A., Rains, B., and Young, R.R., 1999, The Channeled Scabland: Back to Bretz?: Geology, v. 27, p. 605-608. Sherrod, B.L., Barnett, E.A., Knepprath, Nichole, and Foit, F.F., Jr., 2013, Paleoseismology of a possible fault scarp in Wenas Valley, central Washington: U.S. Geological Survey Scientific Investigations Map 3239. Sherrod, B., Blakely, R.J., Lasher, J.P., Lamb, A.P., Mahan, S.A., Foit, F.F., and Barnett, E., 2016, Active faulting on the Wallula fault zone within the Olympic-Wallowa lineament, Washington State, USA: Geological Society of America Bulletin, v. 128, p. 1636-1659. Silver, M.H., and Pogue, K.R, 2002, Analysis of plan-view geometry of clastic dike networks in Missoula Flood slackwater sediments (Touchet Beds), southeastern Washington: Geological Society of America Abstracts with Programs, v. 34, p. 24. Smith, G., 1993, Missoula flood dynamics and magnitude inferred from sedimentology of slack-water deposits on the Columbia Plateau: Geological Society of America Bulletin, v. 105, p. 77-100.

Smith, G.A., 1988a, Neogene synvolcanic and syntectonic sedimentation in central Washington, GSA Bulletin, v. 100, p. 1479-1492

Smith, G.A., 1988b, Sedimentology of proximal to distal volcaniclastic s dispersed across an active foldbelt: Ellensburg Formation (late Miocene), central Washington, Sedimentology, 35, p. 953-977 Spencer, P.K, and Jaffee, M., 2002, Pre-late Wisconsinan glacial outburst floods in southeastern Washington, the indirect record: Washington Geology, v. 30, p. 9-16.

Sutherland, J.L.; Evans, D.J.A., Carrivick, J.L.; Shulmeister, J.; Rother, H., 2022, A model of ice-marginal sediment-landform development at Lake Tekapo, Southern Alps, New Zealand, Geografiska Annaler: Series A - Physical Geography, p. 1-33

Takada, K.; Atwater, B.F., 2004, Evidence for Liquefaction Identified in peeled slices of Holocene deposits along the lower Columbia River, Washington, Bulletin of the Seismological Society of America, v. 94, p. 550-575

Tolan, T.L.; Martin, B.S.; Reidel, S.P; Anderson, J.L.; Lindsey, K.A.; Burt, W., 2099, An introduction to the stratigraphy, strucutral geology, and hydrogeology of the Columbia River Flood-Basalt Province: A primer for the GSA Columbia River Basalt Group field trips, Geological Society of America Field Guide 15, p. 599-643

USDOE/WADOE, 1996, FEIS for the tank waste remediation system, Hanford Site, Richland, WA Van Loon, A.T., 2014, The Mesoproterozoic "seismites" at Laiyuan (Hebei Province, E China) re-interpreted: Geologos, v. 20, p. 139-146. Von Brunn, V., and Talbot, C.J., Formation and deformation of subglacial intrusive clastic sheets in the Dwyka Formation of northern Natal, South Africa: Journal of Sedimentary Research, v. 56, p. 35-44. Waitt, R.B., 1980, About forty last-glacial Lake Missoula jokulhlaups through southern Washington: Journal of Geology, v. 88, p. 653-679. Waitt, R.B., 1983, Tens of successive, colossal Missoula floods at north and east margins of Channeled Scabland: Friends of the Pleistocene Rocky Mountain Cell Guidebook for the 1983 Field Conference, 29 pgs. Waitt, R.B., 1985, Case for periodic, colossal jokulhlaups from Pleistocene glacial Lake Missoula: Geological Society of America Bulletin, v. 96, p. 1271-1286. Waitt, R.B., Breckenridge, R.M., Kiver, E.P, and Stradling, D.F., 2016, Chapter 17: Late Wisconsin Cordilleran Ice Sheet and colossal floods in northeast Washington and Northern Idaho: in Cheney, E.S. (ed.), The Geology of Washington and Beyond, from Laurentia to Cascadia; University of Washington Press, p. 233-256. Walker, E.H., 1967, Varved lake beds in northern Idaho and northeastern Washington: U.S. Geological Survey Professional Paper 575-B, p. 83. Ward, A., Conrad, M.E., Daily, W.D., Fink, J.B., Freedman, V.L., Gee, G.W., Hoverston, G.M., Keller, M.J., Majer, E.L., Murray, C.J., White, M.D., Yabusaki, S.B., Zhang, Z.F., 2006, Vadose zone transport field study summary report, U.S. Department of Energy Report DE-AC05-76RL01830, 288 pgs Woodward-Clyde Consultants, 1981, Task D3: Quaternary sediments study of the Pasco Basin and adjacent areas: Report to Washington State Public Power Supply System, 33 pgs.