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INSIDE THIS ISSUE 1 Field sketches of late-1840s eruptions of Mount St. Helens, Washington, p. 3 WASHINGTON STATE DEPARTMENTOF I Preliminary observations on marine stratigraphic sequences, central and western Olympic Peninsula, Washington, p. 9 Natural Resources I Palm fossils from northwest Washington, p. 21 Jennifer M. Belcher - Commissioner of Public Lands 1 Application of reflection seismology to the hydrogeology of the Kaleen Cottingham - Supervisor Spokane Aquifer, p. 27 I WASHIII\IGTON Goal-Based Management in the Department of GEOLOGY Natural Resources Vol. 23, No. 2 June 1995 Raymond Lasmanis, State Geologist Washington Department of Natural Resources Washington Geology (ISSN 1058-2134) is publi shed fuur times Division of Geology and Earth Resources each year by the Washington State Depar tment of Natural PO Box 47007, Olympia, WA 98504-7007 Resources, Division of Geology and Earth Resources. This pub lication is free upon reques t. The Division also publishes bulle ti ns, information circulars, reports of investigations, geologic uring the regular 1993 Legislative sess ion, Engrossed maps, and open-file reports. A list of th ese puhl ications will be Substitute House Bill 1372 was passed into law. This bill sent upon request. D established a state policy mandating that each state agency es tablish mission or goals statements. The bill further stated that DIVISION OF GEOLOGY AND EARTH RESOURCES each agency shall establish program objectives for each major Raymond Lasmnnis. Srure Geolo,:ist program in its budget. J . Eric Schuster, A Z Washington Geology, vol. 23, no. 2, June 1995 Field Sketches of Late-1840s Eruptions of Mount St. Helens, Washington David K. Yamaguchi Patrick T. Pringle Donald B. Lawrence Forestry and Forest Products Research Institute Washington Department of Natural Resources Department of Plant Biology 7 Hitsujigaoka, Toyohira Division of Geology and Earth Resources University of Minnesota Sapporo 062, Japan PO Box 47007, Olympia, WA 98504-7007 St. Paul, MN 55108-6097 INTRODUCTION & Ashes shot up into the Air, and hung as a Canopy over the dazzling Cap contrasting strongly with the Clear blue On two occasions in September 1845, British spy Henry Warre Sky behind it; this was an incipient Eruption, and my curi saw and sketched watercolors of eruption columns forming osity was excited the more from being the first Volcano I over the north flank of Mount St. Helens, Washington. Yet have ever seen in action. ... Warre's drawings have not been widely known. No prior men tion of them has been made in the scientific literature on the A f ew Miles above the Cowlitz, on the left bank of the volcano's erupti ve hi s tory. (See Pal lister and others, 1992, and Columbia River, is a ... singular isolated Rock. ... Further down 011 the right [Washington} bank is another peculiar references ci ted by these authors.) This situation occurred feature, called Mount Coffin ... . [Figs. 2 and 3] largely because Warre's watercolors had not been publi shed when Holmes ( 1955) wrote his classic paper on 19th-century Cowlitz accounts of Mount St. Helens activity (Hol mes, 1980). CANADA On two days in March 1847, artist Paul Kane observed "' Mount Baker eruptions from the same vent. Kane made watercolors in the field of each scene he witnessed; his second sketc h inc ludes an eruption column. K ane later used his sketches and associated journal entries as the basis for three oil paintings, one of which WA has been widely publi shed and extensively studied by geolo OR gists and historians (see, for example, Hoblitt and others, 1980, and Harris, 1988). rn the famous painting (see cover), River the eruption has been transformed into an incandescent ni ght eruption; other artistic embelli s hments include eight Native MountainSpud A ® American spectators, streaming clouds of opaque smoke, and a reflection of the eruption on the surface of the water (paint Mount W ing previously reproduced in Holmes, 1955; Harper, 1971; St. Helens Harris, 1988; and elsewhere). While the artistic nature of this painting has previously been recognized (Holmes, 1955, 1980; Majors, 1980), Kane's second field sketch and his remaining two paintings have largely been ignored. Yet, based on Kane's journal entries, these three artworks more accurately depict the scenes that he witnessed. This article presents the fi eld sketches of Warre, the for N gotten sketch and paintings of Kane, the associated journal ac counts, and related background information. We then consider A the geological significance of the set as a whole. THE FIELD SKETCHES, PAINTINGS, 45030· N ,o 20 mi AND NARRATIVES 10 2.0 JO km In 1845, Warre wrote in his journal (Warre, 1976): Fort Between Vancouver and the mouth ofthe Cowelitz River /sic/there is not much to attract the Eye or worthy ofnotice . The Views are certainly very pretty and the dista11ce is al ways broken by the presence of one of the several snowy 123° W Mountains standing high above the surrounding Moun tains .... Mou11t Hood & Mt. St. Helens being the nearest & Figure 1 . Maps showing vantage points for field sketches and other therefore the most conspicuous... . [Fig. I] text localities. The Cowlitz Farm locality (46°28'28"N, 122°47'32"W) The Momi11g was Lovely and as we were descending one was determined from a description of the mission near the farm by an of the long reaches in the [Columbia/ River my attention other traveler (Harper, 1971, p. 98) and from George Herron (resident, Winlock, Washington), whose grandfather's farm occupied part of the to was attracted Mount St. Helens standing as it were, at the Cowlitz Farm site. The mission site is shown on the U.S. Geological head of the bend! .. .Suddenly a long black Column of Smoke Survey 7 .5-minute Toledo quadrangle (1993). Washington Geology, vol. 23, no. 2, June 1995 3 Figure 2. "Mount Coffin and Mount St. Helens (volcanic)", a watercolor by Henry James Warre, September 13(?), 1845 (cou rtesy of the American Antiquarian Society, Worcester, Massachusetts, Warre sketch no. 26). Previously published in Warre (1970) and Holmes (1980). Figure 2 is the first of two simi lar sketches Warre made from Mount Coffin (Majors, I 98 1) . The Public Archives of Canada have assigned a date of September 13, 1845, to the second, more finished sketch, based on Warre'sjournal entries (Warre, 1976). The latter sketch is available in Warre (1976), as Majors' (1980) frontispiece, and in Holmes (1980). Within a few days of his original sketches, Warre made a third sketch fr om Co wlitz Farm, a trading post along the Cowlitz River (Fig. 4). While Warre made no journal entries for this sketch, lt was probably done between September 17 and September 20, 1845, based on his earlier and later notes. Kane's 1847 journal reads: March 25th.- I started from the Fort [Vancouver] for Vancouver's Island in a small wooden canoe, with a couple of Indians, and encamped at the mouth of the Walhamette /sic]. March 26th.-When we arrived at the mouth of the Kat tlepoutal { Lewis] River, twenty-six miles from Fort Vancou- Figure 3. Comparative historical photograph of Mount Coffin taken between 1916 and 1929 (courtesy of the Cowlitz County Historical Mu seum, Kelso, Washington, item 61.2.13). The scene supports the verac ity of Warre's watercolor by confirming that the foreground he sketched existed. It also places Warre's sketch vantage on the northeast shore of Lord Island in the Columbia River opposite the 'Mount Coffin' locality on U.S. Geological Survey 7.5-minute Kelso quadrangle (1970). Mount Coffin was almost completely mined for construction aggregate and rlprap in the 1930s. (Photographs of the operations are on file at Cowlitz County Historical Museum.) The building behind the man, Weyer haeuser Longview sawmill number 1, no longer exists. 4 Washington Geology, vol. 23, no. 2, June 1995 .. Figure 4. "Mount St. Helens from settlement on Cowalltz River [sic]" (Cowlitz Farm), a watercolor by Henry James Warre, September 17- 20, 1845 (courtesy of the American Antiquarian Society, Warre sketch no. 24) . Previously publi shed in Warre (1970) and Holmes (1980). Figure 5. "Mount St. Helens, with smoke cone", an oil painting by Paul Kane (courtesy of the Stark Foundation, Orange, Texas, item WOP 10, CRIV-461 ). Although Kane probably witnessed the steam plume he described, his "smoke cone" is actually an altocumulus standing lenticular cloud, formed when moist air is rapidly li ft ed orographically . Previously published in Harper (1971 ) and Holmes (1980). Washington Geology, vol. 23, no. 2, June 1995 5 Figure 6. "Mount St. Helens seen from the Lewis F!iver", a watercolor by Paul Kane (courtesy of the Royal Ontario Museum, Toronto, Canada, item 946.15.184). Note that the museum name of this sketch is in error. The sketch's Cowlitz Farm setting is evident from many features, including the presence of Mount Adams (on horizon at left) and of Spud Mountain (the tall mound-shaped peak al the base of the vo lcano). Here we assign a date of March 30, 1847, to this sketch, based on Kane's journal entry. Previously published in Majors and McCollum (1980). Figure 7. "Mount St. Helens", an oil painting by Paul !Kane based on the Fig. 6 field sketch (courtesy of the Stark Foundation, WOP 21 , CRIV-464). Previously published in Harper (1971) and Holmes (1980). 6 Washington Geology, vol. 23, no. 2, June 1995 ver, I stopped to make a skelch of the volcano, Mount St. Table 1 . Examples of historical accounts of Mount St. Helens erup Helen 's, distant, I suppose, about thirty or forty miles.... /r tions probably related to Goat Rocks dome growth•. (F), first person is of very great height, and bei 11 g eternally covered wi1h account snow, is seen at a great diswnce. There was nut a cloud Date Account Recorder Ref.** visible in the sky at !he time I commenced my sketch, a11d no! a brealh uf air was perceptible: sudden Iv a scream of Summer 1831 Ashfall-indueed darkness Meredith Ho. M white smoke shot up from the crater of the nwu11tain, and Gairclner hovered a short time over its .wmmit; it then settled dow11 August 1831 Ash fall and related darkness at 1'1. Samuel Ho. M Vancouver; white snowy n an ks of Parker like a cap. This shape it retained for about a,1 hour a11d volcano darke ned (same event as a-half: and then gradually disappeared.... [Fig. 5J above) March 301h.- We landed at the Cowlitz/arm, which be Oec. 1842- "Cinde rs and scoria" and dear! fis h Modeste Ho, Ha longs to the Hudsnn 's Bay Company. Large qua11tities of Fch. 1844 in Tourle River Demers 11 ·heat are raised al this place. I had a fine view of Mou111 St. (CowlitL Helen 's throwin g up a long column of dark smoke into the Mission) clear blue sky [Figs. 6 and 7l Here I remained un!il the 5th June 1844 S moke column above volcano (F) J. T. Heath M of April. ... (Harper, 1971) Feb. 15, 1845 Eruption column (F) S. B Ha Crockett Warre's eruption columns appear to originate from a small Feb. 15- l li, 1845 ,S.:1ght rumbling di stinct from J . T . Heath M dome on Mount St. Helens' lower north flank. Kane's sketch thunder; thought ro originate from and Cowlitz Farm painting clearly show an eruption column volcano (F) issuing from a north flank vent. Sept. 17- 20. 1845 Eruption cutumn from north base H. J. Warre TR of peak (F) (Fig. 4) SIGNIFICANCE Lme Feb. 1854 S moke columns above volcano (F) W . H. H. Ho. M llalls. Warre's and Kane's drawings and narratives strengthen his Charles torical evidence for continuing volcanic activity al Goal Rocks Stevens dome, a subsidiary dacite cone on Mount St. Helens' north *Table supplements 21 s imil ar observations from 1835-1857 summarized by northwest flank, during the late 1840s. The existence of the Yamaguchi and Lawrence (1993; their table 2). dome was first documented in the early 1840s; it may have **Ho, Ho lmes ( 1980): M , Majors ( 1981); Ha. Harris ( t 988); TR, thi s reporl. appeared in the early 1830s, or possibly even earli er (Table I). It was probably the most active belween November 22, 1842, and Septemher 20, 1845. when it was observed to be in erup horizon to be Goat Rocks dome. To evaluate this possibility, a tion on at least 13 different occas ions. Goat Rocks dome was colleague photographed the view for us from a s ite 3 km up destroyed by Mount St. Helens' May 18, 1980 eruption (Lip stream of Warre's vantage (Fig. 8; Warre's Lord Island view man and Mullineaux, 1981). poinl is relatively inaccessible). Warre' s billowing ash clouds suggest an emission gener The photograph shows Northwest dome, actually a thick ated by dome coll apse. Kane's eruption columns confirm that section of andesite lava flows on the northwest flank, near the the dome was still hot in March 1847. They might represent horizon. (The dome name was applied hastily and incorrectly steam douds generated by a phreatic explosion (Fig. 5) or a in 1980 but has unfortunately stuck). Yet Goat Rocks dome plume generated by ash-and-gas emissions or a rock avalanche (2,316 m) was only 158 m higher than Northwest dome at the dome (Figs. 6 and 7). (2,158 m). Thus, Goat Rocks dome would also have appeared A possible problem with these interpretations is that the low on the horizon, behind Northwest dome, lo Warre. Lipman north-flank dome in Warre's sketches might be too low on the and Mullineaux ( 1981 , their figs. 33 and 89) and Crandell Figure 8. Mount St. Helens from 3 km upstream of Warre's Lord Island vantage, March 8, 1993. Dark area on left flank Is "Northwest dome". (Photograph taken with 300-mm lens by David Wieprecht.} Washington Geology, vol. 23, no. 2, June 1995 1 ( 1987, his fig. 54) illustrate the similar heights and former Harper, J. R .. editor, 1971, Pau l Kane's frontier; including Wander proximity of Goat Rocks dome and Northwest dome. ings of an artist among the Indians of North America: Universi ty Warre's and Kane's artwork and journal entries contribute of Texas Press. 350 p. Lo a scenario of a hot dome that intermitte ntly grew, crumbled. Harris. S. L .. 1988. Fi re mountains of the west- The Cascade and and steamed from at least late 1842 into the 1850s (Yamaguchi Mo no Lake volcanoes: Mountain Press Publis hing Company and Lawrence, 1993). In March 1847, dome extrusion was evi I Missoula. Mont.]. 379 p. dently still ongoing or only recentl y completed. Hoblitl. R. P.; Crandell. D. R.; Mullineaux. D.R., 1980. Mount St. Mo re generally, the two accounts increase our under Helens eruptive behavior during the past 1.500 yr: Geology. v. 8, no. 11. p. 555-559. standing of Mount St . Helens' past eruptive behavior. Such Holmes, K. L., 1955, Mount St. Helens' recent eruptions: Oregon I Ii s understanding is central Lo anticipating its possible future be torical Quarterly, v. 56, no. 3. p. 196-210. havior. llolmes. K. L.. 1980, Mount St. Helens-Lady with a past: Salem Press [Salem. Ore.]. 48 p. ACKNOWLEDGMENTS Lipman, P. W.; Mullineaux. D. R .. editors. 1981. The 1980 eruptions We thank the staffs of the American Antiquarian Society, the of Mount St. Helens. Washi ngton: U.S . Geological Survey Pro Cowlitz County His torical Museum, the Royal Ontario Mu fessional Paper 1250, 844 p., I plate. seum, and the Stark Museum fur the cover photo and Figures Majors, H. M ., 1980, Paul Kane's drawing of Goat Rock t 847: North 2- 7. publication permission, and ins ightful discussions. Cyn west Discovery, v. 1. no. 2. p. 106-108. thia Gardner found Figure 3 when she and David Wieprecht Majors. H. M .. 1981. Mount SL Helens, the 1831 and 1835 eruptions: s topped at the Cowlitz County Museum o n their way home Northwest Discovery, v. 2. no . 8, p. 534-540. from s hooting Figure 8. Weyerhaeuser Company, Longview. Majors. H. M.; McCollum, R. C .. ed itors, 1980, Frontispiece: North Washington, identified the building in Figure 3. Shirley Lewis west Discovery. v. 1. no. 3, pl. 126. lent us photos she took of Mount St. Hel ens in t\pril 1980 from Pallister. J. S.; Hobl itt . R. P.: Crandell, D. R. : Mullineaux, D. R. , Winlock (northwest of Toledo) that were useful in evaluating 1992. Mount SL Helens a decade after the 1980 eruptions- Mag the s ketc hes done at Cowlitz Farm. Partial funding was pro matic models, chemical cycles, and a revised haza rd assessment: Hulletin of Yolcanology, v. 54, no. 2. p. 126- 146. vided by a Science and Technology Agency of Japan fellow ship to Yamaguchi and by a grant from the Univers ity of Colo Warre. H. J., 1970, Sketches in North America and the Oregon Terri rado Program Enric hme nt Fund. Comments from Donald tory: Imprint Society [Barre. Mass.], 26 p. Swanson, Ric hard Waitt, William Scott, John Lockwood, Warre. H.J. (Major-Fregeau. M .. editor). 1976. Overland to Oregon in 1845-lmpressions of a journey across North America: Puhlic Richard Hoblilt, Dennis Geist, and Cynthia Gardner improved Archive~ of Canada [Ottawa] . 149 p earli er vers ions of the manuscript. Yamaguchi, D. K .; Lawrence. D. B. , 1993, Tree-ri ng evidence for 1842- 1843 eruptive activity at the Goal Rocks dome, Mount St. REFERENCES CITED Helens. Washing ton : Bulletin o f Volcanology. v. 55. no. 4, Crandell . D. R .. 1987, Deposits of'pre-1980 pyroclas tic flows and la p. 264-272. • hars from Mount St. Helens volcano, Was hi ngton: U.S . Geologi cal Survey Professional Paper 1444, 9 1 p .. I plate. 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Orders can be placed by Fcu: 360-274-2101 8 Washington Geology, vol. 23, no. 2, June 1995 Preliminary Observations on Marine Stratigraphic Sequences, Central and Western Olympic Peninsula Washington ' William S. Lingley, Jr. Washington Department of Natural Resources Division of Geology and Earth Resources PO Box 47007, Olympia, WA 98504-7007 INTRODUCTION sugge~ts v.ery high sand/shale ratios. However, good expo This article describes preliminary res ults from field investiga sures m r.h1s area are found mainly on sub-summits of ridges tions of Tertiary rocks that crop out between the easternmost cr_eated by ri~ers that flow southwest down the regional slope Olympic Mountains and the Pac ific Ocean. These rocks form of the accrctJonary pris m. Many of the sub-summits result the "Core Complex" of Tabor and Cady ( I 978a,b) and lie out from second-order streams that 'hook' around resistant sand board of the Crescent terrane (Babcoc k and others, 1994). For stone units and a few volcanogenic bodies, both of which have the most part, they comprise hemipelagic sed iments that were limited extent along strike. ln coastal areas, drill data (Palmer depo~ited directly on the Juan de Fuca plate. Thin- to medium and Ling ley, 1989) indicate a hi gher sand/shale ratio th an is bedded units and thick multistory sandstones or conglomer observed in outcrop because the shales (claystones) are more ates, together with volcaniclastic rocks and basic to intermedi resistant than the coarse-grained sandstones. ate(?) fine-grained crystalline igneous rocks, make up most o f In general, exposures arc progressively better to the north the Core Complex. east, so mapping is more detai led in that region. for example, These ongoing investigati o ns ha ve been performed since bundles o f two or three sandstone beds, each less than 3 m 1989 as part o f the Washington Department of Natural Re thic k, arc depic ted in the Mount Angeles quadrang le (Tabor sources, Division of Geology and Earth Resources' state geo and Cady, 1972, 1978a), whereas far thicker sandstone units logic map program (Schuster, 1994). We made our observa located 5 km southeast of Kimta Peak and on Matheny Ridge have not been mapped. tions during four multiweek traverses on foot in the Olympic Mountains and during reconn aissance traverses along a large Rocks in much of the Olympic Peninsula are metamor proportion of the remaining logging roads in the western phosed; grade increases eastward from the foothi ll s to the cen Olympic Peni ns ula (Fig. I). tral part of the Olympic Mountains (Tabor and Cady, 1978a; T his work was undertaken in order to: Brandon and Calderwood, 1990). However, mapped units are generally defined by sedimentary protolith rather than on the I Clarify the relations among undifferentiated units, basis of metamorphic grade (Tabor and Cady, 1978a; Rau, identify unmapped structures, and eliminate 'scratch' 1975, 1979). For the purposes of thi s report, all rocks com boundaries on existing maps (e.g., Tabor and Cady, posed of c lay minerals arc referred to as shale even though 1978a); these are c laystones in many coastal areas and slates in the I Provide data for forest practices applications, central portion of the peninsula. All sandstones are reported as petroleum assessments, and seismic risk studies; such, a lthoug h some have a schistose appearance ("semi I Determine whether the Core Complex is composed of schists" of Tabor and Cady, 1978a). The coarse-grained sili ci ( I) two or more discrete terranes or (2) a single terrane c lastic rocks are chiefly feldspathic litharenites with lesser or accretionary depositional se4uem;e, which renects amounts of lithofeldspathic arenite (Stewart, 1970; Grady, several provenances and has been dissected by 1985; Koch, 1968; this study). multiple thrusting events (Boyer and Lingley, 199 1, Foraminifera identified by W . W . Rau (in samples col 1994). ~ected _as ~art of this study and various U.S. Geological Survey 1nvest1gat1ons; see Rau, 1975, 1979, 198 I) include faunas that The fo ll owi ng interpretation is subject to considerable un apparently range from late middle Eocene (Narizian stage) to certainty owing to dense vegetative cover, overlying glacial middle Miocene (Relizian stage). A few d iagnostic benthic depos its, s teep te rrain, poor induration in coastal areas, for~ms indicate bathyal conditions, but most forms are plank sheared and distorted outcrops, and wretched weather. Many tonic. Rau (Dept. of Natural Resources, retired, oral commun., logging roadcuts that were useful for previous fie ld studies are 1991) has observed that "most of the turbidites are barre n" . now overgrown or are being intentiona lly obliterated by land Except for a few lowermost and uppermost Oligocene forms management agenc ies. confirmed 01 igocene (Zemorrian stage) faunas are absent. Fis~ Cursory examination of the Tertiary stratigraphic section sion-track dates (Brandon and Vance, 1992) corroborate the exposed in the western foothills of the O lympic Mountains biostratigraphic ages and suggest an 8-m.y.-long hiatus or a Washington Geology, vol. 23, no. 2. June 1995 9 124° 00' /1 Lake L( i:..___.,_,,.l j PlP.asa,nt, 48° oo' • Forks Mt Olympus Ho h ... Head j. Kimfa Peak 3~ / J AREA WAS HINGTON 1 0 5 10 ••• -- - - - 10 Washington Geology, vo 1. 23, no. 2, June 1995 Dungeness 123°30' Spit EXPLANATION Ediz Hook Lith ofocies I: Primarily monotonous Port th in-bedded shales and laminated sillstones (D3 and G f acies). The Angeles • unit also includes a few isolated sandstone beds that ore generally less than 1 m thick. Lithofocies I: Ma inly monotonous II shale with minor siltstone (G focies) 2 o f t he Elwho Lithic Assembla ge. 48° oo' Fl Lithofocies II: Most ly 0.5- to 25-m t;:~ thick nongroded sandstones and 3 conglomerates t hat ore laterally dis continuous and vertically separat ed by O to > 100 m of thin-bedded Deer shales and laminated siltst ones (B Park with D3 a nd G facies) o r by med ium - bedded sandstones and ~Ml finer grained s iliciclastic rocks ( B, Fairchild D, and E facies). . Lithofacies Ill: Chert-pebble con a. g lomerates that are laterally dis 4 continuous and vertica lly separated ( Ml by O to > 1 00 m o f t hin-bedded shales and laminat ed siltston es (A with 03 and G facies) or by Do dwe/1-Rixon medium-bedded sandstones and J Pass finer grained s iliciclastic rocks ( 8, D, and E f a c ies). n Lithofacies IV: Mostly 0 .5- to 1-m LJ thick nongraded sandstones vertica lly 5 se parated by O t o > 25 m o f shales ( B with D 3 and E (?) facies) . Complete Bouma sequences: Sandstones, s iltstones, and sha les w it h Ta -Te div isions ( Bo uma and Bro uwer, 196 4) (C f ocies). Strata with indicators of possi ble D s hallow-water deposition such as 7 f loser bedding and trough c ross bedding. 4 7° .301 Figure 1. Traverse routes (heavy lines) and dominant lake lithofacies (sedimentary protoliths) observed during this Cushman reconnaissance study. 123° 30 1 Washington Geology, vol. 23, no. 2, June 1995 1 1 A lsw Figure z. A hypothetical southwest-to-northeast balanced (geometrically correct) cross section showing possible confii urations of thrust faults within the Juan de Fuca accretionary prism and adjacent regions (section by S. E. Boyer, Univ. of Washington, and the auttior). Unlabeled polygons southwest of th e Hurricane Ridge fault represent the Core Complex of Tabor and Cady (1978a) and its offshore depositional continuation on the Washington continental margin. Unlabeled polygons between the Hurricane Ridge and Leech River faults reflect rocks of the Fuca- Tofino basin. The unlabeled polygon northeast of the Leech River fault represents Mesozoic metamorphic rocks. The northwestern part of the study area (Fig_ 1) is shown. period of slow deposition in a starved basin during much of the gests that some o f the boundaries between the lithic assem Oligocene. blages arc tectoni c. Heller and others ( 1992) found that a few while micas from MAJOR LITHIC ASSEMBLAGES the Western Olympic LiLhi c Assemblage are isotopically simi lar to those from the Omineca crystalline belt of British Co Tabor and Cady (1978a) subdivided rocks of the Core Com lumbia. Micas from sandstones in lithic assemblages located plex into major lithic assemblages, mainly on the basis of sub farther east in the Core Complex resemble those in coeval tle differences among large packets o f remarkably monoto sandstones from the Fuca-Tofino basin and Puget troug h. nous lithologie~ . The Elwha Lithic Assemblage, for example, w hich are located north and east of the Core Complex (Pig. 2). is la rgely composed of homogeneous, thin-bedded, fin e Except in the central part of Lh e Olympic Mountains, many grai ned silic iclasti c rocks, whereas Lhe Needles-Gray Wolf primary sedimentary structures are recognizable, even in the Lithic As emblagc is composed of homogeneous. thin-bed metamorphosed rocks. Areas of greatest deformation include ded, fine-grained silic iclastic rocks w ith a few areall y re disharmonically folded semischists in a mylonite developed s tricted, massive sandstone units, some of which contain mi within a few tens of meters o f the Southern Fault Zone at nor basaltic detritus. The Western Olympic Lithic and the Grand Valley Lithic Assem blages are composed mostly of homogeneous, fi ne-grained siliciclastic rocks with many are all y restricted, massive sandstone units. These s ubtle differences among the major liLh ic as semblages apparently led to some scratch boundaries and undifferentiated units (for ex ample, unit "Tur" and Lh e "Tsc"/"Tgs" contact on Tabor and Cady, 1978a). The mapping and facies analysis described be low support the positions of contac ts and choices of lithic assemblages as shown on Ta bor and Cady ( 1978a). Although the effects of tectonic Lelescoping cannot be quantified, geo metric relations s uggested by Tabor and Cady ( 1978b) and unpublished work by S. E. Boyer and the author indicate considerable thrust du plication (Fig. 2). Most existing mapping lacks sufficient detai l to determine whether individ ual contacts arc normal lithologic boundaries, accreted terrane boundaries, thrus ts (whether seaward- or arc-dipping), or norma l faults. However, the juxtaposi tion of rocks laid down Figure 3 . Monotonous lithofacies I beds consisting of very fine grained sandstone, siltstone, and shale, which are generally laminated but not graded. This section is lo in d issimilar deposilional environments s ug- cated east of Kalaloch. 1 2 Washington Geology, vol. 23, no. 2, June 1995 ~ A" NE I I Strait of Leech River Pan Ame rican Hurric ane Ridge P-014-1 coastline f au lt Juan d e Fuca fa ult Well ~~~~~-STUDY AREA ~~~~--, I Mount Skoko mi sh and rocks near Dodwel I Rixon Pass (M. T. from Multi and Ricci Lucchi, l 978). Many of these beds are Brandon, Yale Univ .. o ral commun., 1991 ; Brandon and oth parallel laminated. Graded bedding is uncommon, but a few ers, 1991 ). units are composed of a basal sandstone bed that grades up ward into si ltstone and (or) shale in turn. A majority of bed LITHOFACIES ding sequences observed during thi s study show no obvious coarsening or fining-upward trends. Most lithofacies I sand To date, fo ur volumetrically significant lithofacies and several stone and siltstone beds have rectangular weathering profiles minor lithofacies have been observed in the study area (Fig. and form a colluvium with 3-cm blocks. Weathering colors are I ). The thick-bedded lithofacies (II and III as defined herein) generally dark gray, medium reddish brown, or, in coastal ar include sequences of rocks similar to the thinner bedded litho eas, a di stinctive orange-brown. facies (I and IV). Folds, faults, and multiple cleavages are common through out many exposures of lithofacies I, so unit thicknesses cannot Llthofacies I be measured or estimated. However, this lithofacies makes up This sequence is composed of monotonous interbedded silt at least half of all exposures we have observed within the Core stones, very fine grained sandstones, and shales that vary in Complex. thickness from millimeters to a few centimeters (Figs. 3, 4, 5). The Needles- Gray Wolf, northeastern Grand Valley, and Few ripples, traces of bioturbation, macrofossils, or skeletal much of the Elwha Lithic Assemblages are composed chiefly remnants have been observed to date. Foraminifera are mostly of lithofacies I. Lithofacies I beds are also common in coastal open-water planktonic forms, but some bathyal assemblages areas mapped by Rau (1975, 1979) and in unmapped areas have been recogni zed. These are flysch sequences composed northwest of Lake Quinault. Unit "Tors" on Tabor and Cady of 0 3 and (or) G facies (alphabetic terminology used herein (1978a) is representative of this li thofacies. Shale (slate) argillaceous Rip-up clasts, (L indicates laminated) Lithic tuffaceous and platy Siltstone, silty Feldspathic Laminations Sandstone (fine, medium, coarse) Muscovite Obscured Conglomerate Rip-up clasts, platy (granules, pebbles) (relative size indicated) l'-....A..A,_/ I Ripples Figure 4. Key to Figures 5, 7, and 13. Washington Geolog y, vol. 23, no. 2, June 1995 13 mal channels rather than from the distal margins of turbi Lithofacies II This lithofacies is composed mainly of 3- to 42-m-thick multi story massive sandstone units. It also includes sandstones of - Sample WSL 10-93-6 s imilar thicknesses that have massive bases and w idely 0.5 spaced, parallel laminations and (or) parallel banding devel oped within a meter of the top of individual beds (B facies). Lithofacies II sandstones are commonly conglomeratic; the granules or pebbles (less common) have roughly the same composition and weathering color as the finer matrix. All of the conglomerates arc matrix supported. These sandstones are separated by 'thin-bedded turbidites' or by thin- to medium-bedded sandstones with fine elastic in 1.0 terbeds, which resemble lithofacies I and LY , respectively. Sandstone to shale ratios of lithofacies II are varied, depend ing on the vertical separation between mu! ti story sandstone units. This vertical separation can excee 14 Washington Geology, vol. 23, no. 2, June 1995 clasts parallel bedding. In a few outcrops, how ever, localized g roups of rip-up clasts a re aligned nearly perpendicular to bedding (s ug gesti ng liq uefacti on?). Many of the tabular rip up clasts taper to very thin, fragile edges. North of Kalaloch, some of the intraclasts are pris matic, indicating th a t these were selectively plucked from rhe intersections of bedding and nearl y orthogonal cleavage surfaces. These c lasts are erod ed " pencils" (see Tabor and Cady, 1978b). Within the Core Complex, cleav ages are developed in areas that have been ex humed from dee pe r parts of the subductio n complex and have higher metamorphic grade (Tabor and Cady, 1978a; Bra ndo n and Calder wood, 1990). Northeast of Kalaloch, one unit composed of massive sandstone beds grades into a Bouma sequence. The massive sandstones and sandstones with laminated and (or) banded tops are abun dant in all of Tabor and Cady' s lithic assem blages, especiall y in parts of th e Western Olym pic Lithic Assemblage, the Grand Valley Lithic Assemblage, and in the eastern portion of the undiffr.rentiated unit "Tur" (between Lake Quinault and Matheny Ridge). Lithofacies 11 sandstones and conglomerates are interpreted as channel-fill sequences depos it ed from hi g h-dens ity turbidity currents or sandy debris flows. Lithofacies Ill Lithofacies III is also composed of conglomer ates and finer elastic rocks. It is distinguished from lithofacies II by composition, larger mean clast diameter, and clast support. Lithofacies Ill Figure 6. View south to a typical section of lithofacles II sandstone, here conglom eratic. This section is located about 300 m east of Lake Lillian near the headwaters of conglomerates (A2) are separated by Oto I 00 m the Lillian River in unit "Tgst" of Tabor and Cady (1978a). The stratigraphic top is to the of 'thin-bedded turbidites' (D3 and G facies) or left, and the sandstone unit is 42 m thick. by thin- to medium-bedded rocks similar to lithofacies JV. Like lithofacies II cong lomer- ates, these are also discontinuous along strike. This lithofacies Ludden Peak, Huelsdonk Ridge, Mount Octopus, and 11 km is made up of pebble and lesser amounts of cobble conglomer west-northwest of Lake Quinault are typical of lithofacies III. ates composed in part of very dark gray chert cl asts not ob The variety of clast lithologies, varying clast induration, served in the other lithofacies. unit morphology, and limited lateral extent suggests that litho Many of these beds have a very small proportion of matrix. facies III rocks are submarine channel deposits. Most lithofacies ITT conglomerates are disorgani zed (lacking internal flow structure) but we ll bedded; thicknesses range Lithofacies IV from 0.5 to 4 m. A few beds near Yahoo Lake show poorly This lithofacies consists of fine- to coarse-grained sandstone developed imbrication of e longate clasts. Conglomerate units beds mostly ranging from 15 cm to 1.0 m thic k, together with we have mapped consist of IO or more beds. very thin bedded sandstones, siltstones and lesser amounts of Clas ts are composed of sedimentary and metasedimentary shale in units ranging from 0.5 to 50 cm thick (Fig. 11). The rocks that may have been derived from Lhe Core Complex and sand/shale ratio in lithofacies IV commo nly exceeds 0.75. For cherts and other rock types that probably had an extrabasinal Lhe mosl part, the sandstones are not graded. The very thin origin (Fig. 10). The pebbles are typically subspherical to ob bedded sandstones are separated by thin shale beds or less late a nd measure 2 to 8 cm along the long axis and 1 Lo 3 cm commonly by parallel shale laminae that are typically 2 mm in section. A few cobbles are present. In some outcrops, clast wide and 5 cm long. Lithofacies IV includes B, D, E, and G induration is varied (Fig. IO) . The more indurated lithologies facies. It is distinguished from lithofacies II by finer grain are rounded to subrounded, but some of the weaker sedimen size, thinner mean bed thickness, a high sandstone/shale ratio, tary pebbles and cobbles are subangular. Conglomerates at and less vertical separati on between sandstone beds. Washington Geology, vol. 23, no. 2, June 1995 15 ;...,, ...... ,..., .. . /·, •. :: .~·-·. .. :,·.: .... .''.. ~ :0 ·.': ·. ·_. :...... :: -~. ·. ·. ·. ·~ : ..., .:.·. ~. 14 • ~: '. ·.'_' : :0>: ... I,' ...... , . . . . . •' ...... , .. . . ·.. · ~<:0~.:-:· ... :.- ~·.·. ~·.·· -:- .· . . . . . ,· . ·. : ·. ·.. ~ ...... Meters .. "'· .. 0-r"<:Cc------::,-, . . ·:: .. .. ':, . , .. . ·,; ·. ·.~ ... : . ... ,'-'-< .. 16 2 ...... 4 .. :'?: \~ :' ..:__.: .'·<· ·. . ' . . . . '\,. . ' .. ·.:··.-·-.·-: .- ._.- -_ -.. ·· . -~·-··-.-·· · -- · ...·. 6 . ...::...... \ ' . / , . . >.. .. -:--::~~--·: :_;~:··:':· /:.. •' •' ~- I • • ' • : ·..._: .. ' .... . 22 , . , · ,\ ... · · . -'' . . - . / .. - ': . ·' . -~--- .· .. :...... :~: .. ~· .. -~-~-.·. >. ' / .'/, . . \ . . . . ' . , 8 ... / . ' : _-.:.. ·. . / . . .\' . ,\ . • ,-: , · • ;., • o I o: ..; ' ; ·. \ .· . : : : . ,: . .• < ... • c:,.. \' . / .-.. :,: . /• ...... _. ·.:.. . . .,,. 'I. . . . 10 ·' · , ..• ..: • / . . \.__;/ -; ...... : . 26 . . . . _., .. \ .,, . / ,\·~·.,. ·: .·.·..-:.· · 12 "'· . . . ' '\,"' .."' ,.. 28 Figure 7. Columnar stratigraphic section showing b,ed forms and other structures typical of lithofacies II. The location is given in Figure 6. Note scour between meters 37 and 38 , channeling, and the distribution and orientation of claystone and siltstone intraclasts. While uniform grading patterns are not apparent, most sandstone beds show widely spaced laminations and (or) banding near the stratigraphic tops. 16 Washington Geology, vol. 23, no. 2, June 1995 ...... ·--~--0 ~ -· '--I · ~ · ·. _·_ -_._0 30 '.<';::;_·· :<_.-": ~-/.' '-} :'i\:- . . •'. .· ,-: . . . .:0 :~:-.-: ~,:·:: ~~\(·;~0/. ".. . . . / ·.... : ._.. " ·.·· ... ~ ·.. .-:· . • • · . ~ -~ • . • ; .... . a::,, .• <) · . 32 , : .. -~O, • O• D: ~< ,'Q•~,• ~ • I ' • • • ~ ." : • • • _·_j .• ·.: •• ·_,. _...... / , ·.· .. .. 0 . ...:.. · 1 •. · . · \ ' ... : • : 0- ·.. • • I' • -:- . ~ .. , .... /. - ~. · · 34 ,- . . . ' . . . . / ...... / . ./ ., . .· .. / . . .. ~ ... ·,,- ...... ·' . . "~~ .: ... ' : .· . . / ' Figure 8. Detail of meters 36-38 of the lithofacies II columnar strati graphic column (Fig. 7). The stratigraphic top is to the left. Note banding and laminations near the top of the lower sandstone bed (darker gray, fine-grained sandstone) and the scouring (at hammerhead) at the base of the upper bed (light gray, coarse-grained sandstone). --·-· 38 -~- Lithofacies IV sandstones in the Matheny Ridge area ap pear to have lateral continuity on the order of several hundred meters. These sequences are mostly observed adjacent to, or grading into, lithofacies II sandstones. Some scouring is pre . .... ·. . . : :.··:-~:- .:_: ::: ~·.· ... . · ·. . · .. · .·. sent, but many units maintain constant thicknesses over tens -: ~·· ·.· .. ·.~. a · ~~~-o~a::~·o of meters (Fig. 11 ). Lithofacies IV sandstones and finer elastic rocks are inter a· ·P= <=? .·· :c:::,o:~~c:,~···- · -. 40 :. - ·.·. ·.-:_·_._-: · : ~ -:·.: preted as submarine levee and overbank deposits. Minor Lithofacies Complete Bouma sequences have been observed in only a few outcrops in the western and central parts of the Olympic Pen insula. Bouma sequences are best exposed near Browns Point north of Kalaloch (Grady, 1985; Rau, 1979). It seems unlikely that more extensive Bouma sequences are present but not ex 42 posed because ubiquitous thrusting (Fig. 2) would have re vealed parts of any extensive midfan sandy lobe se4uence. Igneous rocks in the Core Complex consist of basic to in termediate(?) lavas and heterogeneous volcaniclastic rocks. Sedimentary structures and heterogeneous lithologies at Sore Thumb, and possibly at Steeple Rock, suggest that some of the Washington Geology, vol. 23, no. 2. June 1995 17 well-documented examples. A 5-km-wide band of intense shearing and phacoid devel opment that parallels regional structure and extends for about JO km northwest from Lake Quinault may be the result of thrust faulting. In this area, shear sets are oriented subparallel to or at about 60 degrees to the lithologic layering. A scaly cleavage and crudely aligned phacoids are also subparal lei to bedding (Fig. 12). Many simi lar features are mapped by Rau (1975, 1979). Except for minor slumps, we have not observed tur bidite landslide deposits (F facies) in the Core Complex. The lateral continuity of the bands of shearing and phacoids suggests that these are not rel ict submarine debris flows. DISCUSSION Lithofacies II and III are interpreted here as submarine channel-fill sequences. Lithofa cies IV beds are probably levee and overbank Figure 9. Detail of meters 30-40 of the llthofacies II columnar stratigraphic column (Fig. 7). The stratigraphic top is to the left. Note the size and distribution of shale and silt deposits associated with these channels. The stone rip-up clasts. 'thin-bedded turbidites' of lithofacies I are thought to be mainly interchannel/overbank deposits. Shales in the Elwha Lithic Assem volcaniclastic units may be c hanne l-fill sequences similar to blage are the only rocks that may be the distal equivalent of those of lithofacies III. these channel deposits. These relations are shown in Figure If the accretionary prism developed in a normal sequence, 13 . Faunal paleobathymetry and a lack of bioturbation suggest progressive westward shoaling th rough time could be ex these rocks were mostly deposited on the outer shelf or slope. pected. However, the incomplete faunal record indicates The Olympic Core Complex contains abundant marginal mainly deep marine biofacies. The few she) fal forms observed wedge sequences (lithofacies I) that are commonly associated are mixed with deeper water assemblages, suggesting redepo with major rivers e lsewhere (Multi and others, 1992). These sition. Heller and others ( 1992) noted flase:r bedding and deposits, together with the large apparent width of some chan cross-bedding in the Grand Valley Lithic Assemblage, sug nel deposits, suggest that a single large river could have fed gesting shallow-water deposition. We have observed small the e ntire depositional system. scale trough cross-beds near Mount Hopper and Sentinel Peak By middle Eocene time, Crescent Formation basalts and cross laminations in many other parts of the Core Com formed a fairly continuous highland that may have isolated the plex. Thin coal stringers and traces of bioturbation are present Core Complex from adjacent terranes (Palmer and Lingley, in a few outcrops. However, none of these features are neces 1989). However, the 'Sequim gap'. localed between two prob sarily indicative of shoaling. (See Mutti and others, 1992.) able eruptive centers in the northeastern Olympic mountains Most 'melanges' described in the Core Complex are bro (Babcock and others, 1994), may have allowed a paleo-Fraser ken formations typical of rocks in thrust belts worldwide. Me or paleo-Columbia river to issue out onto the Eocene shelf and langes appear to be limited to muds injected along thrusts, carve an extensive submarine channel system. During the Oli di api rs, and late Miocene strike-slip faults (Palmer and Lin gocene, adjacent basins in the Puget trough foundered (Lin gley, 1989; Orange, 1990). The Clearwater River Shear Zone gley and others, 1993; Johnson and others, 1994) . These deep of Stewart ( 1970), which cuts across regional structure, and basins may have pirated rivers that supplied detritus to the the equant Duck Creek diapir (Rau and Grocock, 1974) are Juan de Fuca plate, thus starving the Core Complex between 34 and 27 Ma. Following early Miocene filling of the adjacent Conglomerate (n=S) subbasins, rapid sedimentation continued in the Core Com plex, possibly in thrust-bounded piggyback basins (Boyer and Chert, black (n=29) Lingley, 1994). Initial uplift of the Olympic mountains may have begun as Sandstone, Volcanics, poorly tuffaceous early as 17 Ma, as evidenced by abundant Crescent-like detri indurated sandstone tus in cores from coastal wells that penetrated the Hoh Lithic (n=6) (n=26) Assemblage (Palmer and Lingley, 1989; Rau, 1973) and a Jack of basaltic detritus in many sections of the younger Montesano Formation, which unconformably overlies rocks of the Core Quartz (n=6) Complex (Bigelow, 1987; Palmer and Lingley, 1989). This in Figure to. Relative abundances of some lilhofacies Ill clasts ob cipient uplift of the Olympic mountains may have exhumed served east of Yahoo Lake, south of Mount Octopus, on Huelsdonk and eroded foliated Elwha Lithic Assemblage slates. Pencils Ridge, and southwest of Matheny Ridge. plucked from these slates may have been redeposited from a 18 Washington Geology, vol. 23, no. 2, June 1995 sma ll er channel system(s) in areally restricted midfan sandy lobes on a localized fan(s) now Iocated near the coast Ii ne. Boundaries between lithic assemblages mapped by Tabor and Cady and by Rau are ex pl icablc in terms of facies associations and rhrust tectonics. Jt is not necessary to invoke rerrane boundaries to explain contacts. A possi ble exception is in the nonhwesternmost Olym pic Peninsula where Jurassic and Cretaceous rocks mapped by Snavely a nd others (1993) may be a hanging-wall imbricate of a buried Mesozoic terrane. However, lithologic monot ony of Paleogene strata s uggests that most of the Core Complex is a single terrane. Acknowledgments This study was partially funded by a grant from the Minerals Management Service as part of the Continental Margins Program (Subagreement No. 14-35-0001 -30643). We thank Cathy Dun Figure 11. Typ ical exposes of lithofacies IV sandstones and fine siliciclastic rocks kel for her support. located southwest of Matheny Ridge. Bill Phillips, Weldon Rau, Josh Logan, Leslie Lingley, Joe Dragovich, Wendy Gerstel, Hank Schasse, Dave Norman, and Kevin Kelly assisted with field work and related projects. Mark 13randon and Eric Schuster assisted with logistic~. Kitty Reed, Jari Roloff, and Matt Brune ngo edited this text, and Keith Tkerd drafted the maps and sections. This study would not have been possible without the benefit of previous mapping by Rowland Tabor. REFERENCES CITED Bahcock, R. S.; Suczek, C. A.; Engebretson, D. C., 1994. The Crescent "terrane," Olympic Peninsula and southern Vancouver Island. fo Lasmanis, Raymond; Cheney. E. S., convenors, Regional geology of Washington State: Washington Divi sion of Geology and Earth Resources Bulletin 80, p. 141 - 157. Bigelow, P. K. , 1987, The petrology, stratigraphy and has in history of tbe Montesano Formation, south Figure 1 z. Penetratively sheared sandstones, shales, and siltstones on Matheny western Washington and southern Olympic Pen Ridge. Note the sandstone phacoid on the left, which is subparallel with the dominant insula: Western Washington University Master of shear set (weathered nonresistant layers rising to the left) and large rotated phacoid Science thesis, 263 p. ('map of Africa' on the right). Bouma, A. H.; Brouwer, A. , editors, 1964, Tur bidites: Elsevier Puhlishing Company Develop ments in Sedimentology 3. 264 p. Boyer, S. E.; Lingley, W. S., Jr.. 1991 , Structure and ki nematics of the Brandon, M. T .; Feehan, J. G.; Paterson, S. R., 1991, Volume strain Olympic subduction complex, NW Washington, and implications associated with pressure-solution deformation in sandstones from for mechanical models of accretionary prisms [abstract]: Geologi high P-low T terrains- A third of the rock's missing! Lahstract]: cal Society of America Abstracts with Programs. v. 23. no. 5. Geological Society of America Abstracts with Programs, v. 23, p. A428. no. 5, p. A362. Boyer. S. E.; Lingley. W . S., Jr., 1994, A model for tbe structural Brandon, M. T.; Vance, J. A. , 1992, Tectonic evolution of the Ceno evolution of parts of tbe Olympic subduction complex and asso zoic Olympic subduction complex, Washington State, as deduced ciated piggyback basins [abstract): Geological Society of Amer from fission track ages for detrital zircons: American Journal of ica Abstracts with Programs, v. 26, no. 7, p. A-188. Science, v. 292, no. 8, p. 565-636. Brandon, M. T .; Calderwood. A. R., I 990. High-pressure metamor Grady. M. T., 1985, Stratigraphy, sedimentology, and hydrocarbon phism and uplift of the Olympic subduction complex: Geology, potential of the Hoh turbidite sequence (Miocene), western Olym v. 18, no. 12. p. 1252-1255. pic Peninsula, Washington: University of Idaho Master of Science thesis, 192 p. Washington Geology, vol. 23, no. 2, June 1995 19 LITHOFACIES Ill Multi , Emiliano; Ricci Lucchi, R ., 1978, TurbitliLes or the northern (Conglomerates only) Apennines-Introduction to facies analysis: American Geologi cal Institute Reprint Series 3, 40 p. Orange, D. L., 1990, Criteria helpful in recognizing shear-zone and diapiric melanges-Examples from the Hoh accretionary com plex. Olympic Peninsula, Washington: Geological Society of America Bulletin, v. 102, no. 7, p. 935-951. Palmer, S. P.; Lingley, W. S., Jr., 1989, An assessment of the oil and gas potential of the Washington outer continental shelf: Univer sity of Washington, Washington Sea Grant Program, Washington State and Offshore Oil and Gas, 83 p., 12 plates. Channel (A) Rau , W.W., l973, Geology of the Washington coast be tween Point Grenville and the Hob River: Washing ton Division of Geology and Earth Resources Bulle ~ LITHOFACIES II tin 66, 58 p. (Sandstones only) Rau . W.W., 1975, Geologic map of the Destruction ls land and Taholah quadrangles, Washington: Wash oo ooa 0 o ington Division of Geology and Earth Resources ~ 0 0 0 0 o o oO o a Geologic Map GM- I 3, I sheet, scale I :63,360. 0 20 Washington Geology, vol. 23, no. 2, June 1995 Palm Fossils from Northwest Washington George E. Mustoe Wes L. Gannaway Geology Department 1604 Brookwood Drive Western Washington University Ferndale, WA 98248 Bellingham, WA 98225 INTRODUCTION knowledge of a ncient flora comes from the Early Tertiary, ·Ancient forests', 'global climate change', 'destruction of the when the landscape was dominated by lowland environments rain forest' - these phrases appear almost daily in the pages of conducive tu both luxuriant plant growth and preservation of our newspapers, describing phenomena that are interpreted as leaf imprints. Fossils from these deposits indicate that semi important barometers of environmental change. We can also tropical rain forests flourished on an extensive plain that ex look at these 'barometric' concepts in a very different way, isted prior to the ri se of the Cascades. The abundance of palm fossils in the Eocene Chuckanut Formation provides promi using fossils to study evolutionary progressions that occurred eons before humans arri ved on the scene. Plant remains are nent evidence that these plant communities were much differ ent from the temperate forests that exist today. These fossils particularly important for understanding our region's hi story because they provide an accurate indication of am:ient climate include large leaf imprints, wood casts, and poll en grains and topography, and they are much more abundant than animal (Figs. 1-4). Palm fronds are on display at the Burke Museum fossi ls. (Univ. of Washington) in Seattle and at the Western Washing Cretaceous leaf impressions provide the earliest evidence ton University Geology Department in Bellingham. of Washington plant communities, but our first comprehensive GEOLOGIC SETTING The Chuckanut Formation consists of nearly 6,000 m of strata exposed in a 20 km by 60 km outcrop belt that extends from Puget Sound to the foothills of the North Cascades in western Whatcom and Skagit Counties (Fig. 5). Johnson (1984) subdi vided the Chuckanut Formation into seven stratigraphic mem bers that represent different depositional environments within an ancient fluvial system. Leaf impressions are particularly abundant in silts tones of the Bellingham Bay and Slide Moun tain Members. These strata represent wetlands that bordered the ancient river, where the abundance of vegetation and con ditions of sedimentation combined to offer an ideal environ ment for the preservation of fossils. In contrast, the arkosic sandstones and conglomerates that make up much of the Chuckanut Formation were deposited along beaches and river bars; they contain many driftwood impressions but few fossil leaves. Fission-track dating of detrital zircon grains and volcanic interlayers suggests that Chuckanut sediments were deposited during the Eocene epoch and are younger than the Late Creta ceous-Paleocene age estimate previously deduced from plant fossi ls (Pabst, 1968). Johnson (1984) estimates that the base of the formation is no older than 55 Ma and the the youngest strata were deposited about 40 Ma. He reported a tuff layer, 2,700 m above the base of the formation, that has a fi ssion track age of 49 ± 1.2 Ma. An interbedded rhyolite flow of un certai n stratigraphic position has been dated at 52.7 ± 2.5 Ma (Whetten and others, 1988). PALEONTOLOGY Descriptions of Chuckanut Formation fossils include brief re ports by Lesquereux ( 1859), Newberry ( 1863, 1898), Knowl ton (1902), LaMotte (1938), Chaney (1951), and Butala and Figure 1 . Palm frond Imprints exposed on a bedding plane In the Cridland ( 1973). Pabst ( 1968) studied fossi I ferns, conifers, Mount Baker foothills near Canyon Lake, Whatcom County, Washing and horsetails, and her unpublished manuscripts contain de- ton. Washington Geology, vol. 23, no. 2, June 1995 Z 1 Figure 2. Cast of palm trunk preserved in growth position, discovered Figure 3. Reconstruction of Saba/ires (Berry, 1930). near the summit of Bacon Peak, North Cascades. Photo by R. A . Haugerud, USGS. scriptions of many flowering plants (Pabst, 1952). Pollen ha<; been examined by Crickmay and Pocock (1963), Hopkins (1966), Griggs ( 1970), and Reiswig (1982). Other fossi ls in clude a turtle, fresh-water mollusks, and tracks of a heron-like bin.l (M ustoe and Pevear, 1981 ; Mustoe, 1993). The Chuckanut flora probably represents a paratropical rain forest, as defined by Wolfe (l 977). These forests have more open canopies than true tropical rain forests and have a 1---1 greater abundance of large single trees. Paratropical rain for 10µ ests occur in humid climates that have a mean annual tempera ture of 20-25°C. The lowland forests of southern China pro vide a modern example. Sabal granopollenites Liliacidites Dicotyledonous leaves are common fossils in the Chuck anut Formation, but few have so far been identified. However, Figure 4. Fossil pollen from the Chuckanut Formation. (Sources: 1, Hopkins, 1966; 2, Griggs, 1970; 3, R'eiswig, 1982.) their vegetational characteristics (such as the abundance of large, simple leaves having smooth margins, and the relative scarcity of lobed or serrate margins) are typical of plants that PALM FOSSILS inhabited a humid frost-free climate. Distinctive semitropical taxa include a tree fern, Cyathea pinnata (MacGinitie) La Early paleobotanists commonly attempted to classify ancient Motte, and a variety of climbing plants (such as the climbing frond imprints using genus names previously established for fern lygodium kaulfussi Heer, and two flowering vines, living palms, an approach that proved to be unreliable. Instead, Tetracera and Goweria). However, the flora is diverse and in Read and Hickey (1972) proposed a classification scheme that cludes Platanus (sycamore), A/nus (alder), Cory/us (hazel), di_vides ancient palms into 'form genera' based on leaf shape, Sassafras, and other genera that now inhabit temperate forests. without regard to actual genetic relationships. Palmate (fan Conifers consisted of lowland-dwelling members of the shaped) fronds are identified as Sabalites or Palmacites, de Taxodiaceae (yew family) and Cupressaceae (cypress family) pending on the geometry of the leaf base; pinnate (feather such as Taxodium, Mesocyparis, and Glyptostrobus. shaped) fronds are placed in the form genus Phoenicites. A 22 Washington Geology, vol. 23, no. 2, June 1995 Swauk and Chuckanut Formations appear to have been deposited as part of a single depositional basin (Frizzell, 1979). Brown (1962) claimed that palms from the Chuckanut formation were actually Sabalites grayanus, a species na me first used to describe Eocene fronds from the southeastern U.S. (Lesquereux, I 878). Knowlton (1919) stated that Newberry·s specimens of S. campbelli included a sec ond species of palm, Sabal(?) ungeri, an allegation re peated by Knowlto n ( 1930) and LaMotte ( 1952). Thorne ( 1976) inde pe ndently observed that th e Chuckanut flora contains at least two types of palms. Leaves of Sabalites campbelli (New berry) Lesquereux a re the most common palm fossil in the Chuckanut flora (Fig. 6). Brown (1962) claims that these frond im prints should be ide ntified as Sabalites grayanus. Lesquereux is doubtful for sev eral reasons. The name S. grayanus was ori ginall y assigned to Eocene palm fossils from L afayette County, Mississippi , by Lesquereux ( I 869), but his published de 125° 123° scription is vague, and the original speci EXPLANATION mens have been lost for nearly a century. Middle to late Eocene (46-36 Ma) The best available definition of the species is that of Berry ( 19 16), who studied speci HU, Huntingdon Formati on R-C, Roslyn and Chumsti ck formations mens from Lesquereux's type locality and PG , Puget Group* about 40 other sites in Mississippi, Arkan NA. Naches Formation* sas, Louisiana, Texas, and Tennessee. Ex amination of leaf cuticle indicates that these Early to middle Eocene (55-40 Ma) fronds actually represent several coryphoid B-K , Burrard* and Kitsi lano Formations palms that have similar leaf shapes (Dil SW, Swauk rormation* c her, I 968; Daghlian, 1978). S. grayanus MA, Manastash Formation has also been used as a catchall term to de CK, Chuckanul Formation* scribe a wide variety of palmate leaf im Figure 5 . Early Tertiary nonmarine sedimentary rocks in western Washington and adjacent pressions from the western U.S. For exam British Columbia. *. contains fossil palms. References: Heller and others (1987), Griggs ple, Brown ( 1962) uses this name to include (1970}, and Gresens (1982). eleven forms that he considered to be syn- onymous. similar form genus system has long been used to describe Fronds o f S. campbelli and S. grayanus both have petioles other types of plant ti ssue; fossil palm wood is identified as that extend into to the underside of the leaf as an acutely ter Palmoxylon, whi le seeds similar to to those of living palms are minated triang le (acumen) having concave margins. On the named Palmocarpon. Fossilized roots, flowers, and pollen are upper leaf surface, the acumen is very short with a rounded or identified using other generic names. Although this system re broadly triangular margin. Despite these structural similari sults in the organs of a single plant being given a variety of ties, fronds from the Chuckanut Formation are much larger in scientific names, it provides a workable solution to a difficult diameter than specimens of S. grayanus from type locations in taxonomic si tuation. the southeastern states. S. grayanus fronds typically have di Palm leaf fossi Is collected from Bellingham Bay by the ameters of about I m, approximately half the size of typical I 84 I Wilkes Exploring Expedition were named Sabal camp Chuckanut S. campbelli imprints. Although the size of a par he/li (Newberry, 1863, 1898), amended to Sabalites camphelli ticular palm leaf may be related to stage of growth, environ by Lesquereux ( 1878). These identifications were later ques mental factors, or conditions of fossilization that selectively tioned by other paleobotanists. Duror ( 1916) identified im favor intact preservation of small fronds, the consistently ob prints from the Swauk Formation near Skykomish, Washing served differences in leaf diameter indicate that S. campbelli ton, as Sabal powelli, a species first reported from the Eocene and S. grayanus are not synonymous. In addition. paleo Green Ri ver Formation of Wyoming (Newberry, 1883). If out geographic barriers that separated the Pacific Northwest from crop map patterns are corrected for an estimated 190 km of the southeastern region probably would have hindered the north-south relative motion along the Straight Creek fau It dur transcontinental dispersal of either species. ing the subseque nt ri se of the North Cascades range, the Washington Geology, vol. 23, no. 2, June 1995 23 Table 1. Occurrence of Tertiary palms In western North America. Data from La Motte, 1952; Lakhanpal, 1958; Tula, 1967; Wolfe, 1968; Gre gory, 1969 1 Location Formation PALEOCENE: Colorado Springs, Colorado Dawson Arkose Pagosa, Colorado Animas Formation Golden, Colorado Denver Formation Fishers Peak. Colorado Raton Formation ~ -----....._ Petiole ,/ Raton Mountains, New Mexico Raton Formation Yellowstone River, Montana Fort Union Formation 1----, 10cm EOCENE: Figure 6. Sketches showing leaf base architecture of Chuckanut For Plumas County, California La Porte flora mation palm imp rints . 1, Sabalites campbelli (upper leaf surface); 2, s. Nevada County. California Chalk Bluffs flora campbe/li (lower leaf surface); 3, Sabalites cl. S. ungeri (lower leaf sur Clarno, Oregon Clarno Formation fa ce) . Specimens showing the upper surface of the latter species have Green River, Wyoming Green River Formation yet to be found . Tipperary, Wyoming Bridger Formation Bellingham, Washi ngton Chuckanut Formation Skykomish, Washington Sabalites campbelli occurs abundanLly in fossiliferous Swauk Formation King County, Wa shington strata of the C huckanut Formation, regardless of geographic Puget Group Gulf of Alaska va ri ous locatio n and stratigraphi c positio n. Less commonly, o utcrops Vancouver, British Columbia Burrard Formati on, contain fronds of a second type, recognizable by the extension Kitsil ano Formation of the petiole into the lower surface of the leaf for a distance of I 5 cm or more. This acumen is in the form of a narrow, OLIGOCENE: straight-sided triangle, in contrast to the curved acumen mar Cottage Grove, Oregon Rujada flora gins characteristic of S. campbe/li. These leaves closely re Multnomah County, Oregon Eagle Creek Formation Skamania County, Washington semble descriptions of Sabal(?) ungeri (Lesquereux) Knowl Eagle Creek Formation ton from the Paleocene Raton Formation of New Mexico ( Knowlto n, 1917), later renamed Sabalites ungeri ( Dorf. MIOCENE: 1939). Tehachapi, California not listed The presence of two types of fronds is consistent with pa Barstow. Cali fornia not listed lyno logic evidence. Griggs ( 1970) identified Sabal gnuw pollenites Ro use from outcrops al o ng C huckanut Drive near PLIOCENE: Bel lingham, a palynomorph that is similar to pollen of the Last Chance Canyon, California Ricardo beds modern Sabal palmetto. Griggs also recognized abundant oc Rosamond, Mohave area, California not listed currences of liliacidites, a form genus of uncertain botanical affini ty that he believed to be from a palm because of its pres ence in strata that also contain frond imprints. Although S. in sediments of the same age that were deposited at paleoalti campbelli and S. ungeri fronds have not yet been found to tudes exceeding approximately 300 m (Axelrod, 1968). Exam gether, the mutual occurre nce of Sabal granopollenites a nd ples of Earl y Tertiary upland floras where palms are absent liliacidites pollen at sites spanning approximately 2,700 m of include Republic (Wolfe and Wehr, 1987) and Pipestone Can stratigraphic section exposed along Chuckanul Drive suggests yon , W ashington (Royse, 1965), and Thunder Mountain, that the two taxa were contemporaneous and broadly distrib Idaho (Axelrod, 1990). uted in time. S. granopollenites and Liliacidites have also been Evidence from the middle Eocene Allenby Formation near identified from other sites in the C huckanut Formation (Hop Princeton, British Columbia, is more complicated. Although kins, I 966; Reiswig, 1982). silicified palm stem and leaf fragments are abundant in a thick sequence of chert beds, palms are absent in the nearby elastic sediments. Fossils in these shales indicate a mixed deciduous PALEOECOLOGY inland forest. Tn contrast, the chert unit was deposited wi thin Sabalites and Palmicites leaf imprints occur in other Tertiary a marshy environment rich in monocotyledons (Erwi n and formations in the Pacific Northwest, extending from Alaska lo Stockey, I 99 1). This botanical variation within a single geo Cali fornia (Table I), and their distribution provides important logic formation is significant because our knowledge of an indications of paleogeography and paleoclimate. Although cient plants mostly comes from fossils collected from shales early palms show great latitudinal range, their distribution was and siltstones, which do not necessarily represent the only fa restricted to regions of low e levation and frost-free c limate. vorable palm habitat. Prior to the o nset of the Cascade Range orogeny at the close of Palms began to disappear from the Pacific Northwest near the Eocene, a broad coastal plain extended well into central the c lose of the Eocene Epoch in response to climatic cooling Oregon and Washington, providing suitable habitat for palms (Wolfe, 1978) and geographic changes associated with uplift and o ther subtropical vegetation. These p lants are not present of the Cascade and Coast Ranges. This orogeny destroyed the 24 Washington Geology, vol. 23, no. 2, June 1995 extensive coastal plain, altered the pattern of rainfall, and re ti o ns of the continents, fu ture climate c hange may possibly be duced the influence of warm ocean currents on inland climate. due to the effects of ai r pollution. Extinction of species is com Of these multiple factors, the decline in g lobal temperatures monly a result of habitat destruction, and unexpected patterns seems Lo have been the most important factor in causing the of successio n may result when pests, predators, and d isease extinction of palms. This observation is based o n the presence producing microbes are transported to distant regions o n ships of Sabalites imprints in the middle to late Eocene Swauk For or planes. For these reasons, modern forests may be experie nc mation of central Washington and their absence in the slightly ing trans ition rates quite unlike the ir Cenozoic counterparts. younger Ros lyn and Chums ti ck Formati o ns. The petrologic similarity of these arkosic formations suggests that they were ACKNOWLEDGMENTS a ll deposited in similar flu vial settings and that paleobotanical differences are largely due to climatic variation rather than We thank W es We hr for revie wing the manuscript and K. M. geographic cha nge. Reed for editorial he lp during preparation of the final draft. Sahalites occurs in the Rujada flora near Cottage Grove, Oregon (Lakhan pal, 1958), and in the Eagle Creek flora of the REFERENCES Columbia Gorge (Chaney, 1920). These s ites are believed to Axelrod, D. I., 1968, Tertiary floras and topographic history of the be of Oligocene age, although neither has been dated with cer Snake River bas in, Idaho: Geological Society of America Bullc tainty. If these age estimates are correct, these fossils are the Lin, v. 79, no. 6, p. 713-734. youngest known occurre nce of palms in the Pac ific Northwest. Axelrod, D. I., 1990, Environment of th e middle Eocene (45 Ma) By the middle Tertiary, palms had re treated to the frost-free Thunder Mountain flora , central Idaho: National Geographic Re reg ions of southern California, as indicated by various Mio search, v. 6. no. 3. p. 355-36 1. cene and Pl ioccnc fossils (Tuta, 1967). At present, the only Berry, E. W .. 1916, Th e lower Eocene fl oras of southeastern North re maining nati ve palms of western North America are three America: U.S. Geologi cal Survey Professional Paper 9 1. 48 1 p. species of Washi11gto11ia that inhabit the dry inte ri o r regions of Berry, E. W., I 930, Revision of the lower Eocene Wilcox flora of th e southe rn California and Mexico. southeastern states, with descriptions of new species, chiclly from What ecologic lessons can be learned from the extinction Tennessee and Kentucky: U.S. Geological Survey Profession al of the palms that once inhabited the Pacific Northwest? For Paper 156, 196 p. one thing, the phenomenon points out our poor understanding Brown, R. W., 1962, Paleocene flora of the Rocky Mountai ns and of g lobal c limatic trends, as we have little explanation for the Great Plains: U.S. Geological Survey Professional Paper 375, Eocene- Oligocene temperature shift. The fossils also provide 1 19 p., 69 photo plates. a re minder that major biologic transitions are not reversible. If Butala, J. R.; Cridland. A. A., 1973, Juniperus washingtunensis, a we were able to c hange o ur region's c limate back to the tem synonym of Glyptostrobus nurdenskioldi: Taxon, v. 22, no. 5-6, perature and rainfall conditions of the Eocene Epoch, our for p. 577-578. ests would again take on a semitropical character, but they Chaney, R. W., 1920, The flora of the Eagle Creek Formation (Wash would not revert to the orig inal fl o ral compositio n. This is ington and Oregon): Chicago Un iversity Walker Museum Contri partly because many Early Tertiary plants became extinct, butions, v. 2, no. 5, p. 115-181 , 22 plates. leaving no c lose modern relatives. In addition, we would see a Chaney, R. W., 195 l , A revision of fossil Sequoia and Taxodium in western North America based on the recent di scovery of mela pro Ii feration of introduced species as the decorative pla nts of sequoia: American Philosophical Society Transactions. new se our greenhouses a nd living rooms escaped to the freedom of ries v. 40, part 3, p. 170-263. the great outdoors. If palms returned to a new Was hing ton cli Crickmay, C.H.; Pocock, S. A. J., 1963, Cretaceous of Vancouver, mate, they would like ly be relatives of courtyard palms of ho British Columbia, Canada: American Association of Petroleum tels and shopping malls, rather than descenda nts of Sabalites Geologists Bulletin, v. 47 , no. 11 , p. 1928- 1942. campbel Li . Daghlian, C. P., 1978. Coryphoid palms from the lower and midd le It' s also important to realize that the global-cooling epi Eocene of southeastern North America: Paleontographica, Abtei sode that so greatly affected the ancient Pacific Northwest for lung B, v. 166, no. 1-3, p. 44-82. ests probably occurred at a rate that would have been undetect Dilcher, D. L., 1968, Revision of Eocene palms from southeastern able by climatologists. Indeed, if the s urvival Lime of Homo North America based upon cuticular analysis [abstract]: Ameri sapiens as a species proves to be si milar to that of other spe can Journal of Botany, v. 55, no. 6, part 2, p. 725. c ialized mammals, our entire existence could have been Dorf, Erling, 1939, Fossil plants from the Upper Cretaceous Aguja played oul during the Early Tertiary without our ever noticing Formation of Texas: American Museum Novitates IOl5, p. 296. a c hange in the weather. Duror, C. A., 1916, Report on the flora of the Swauk Series; Report Finally, modern plants and animals face environmental in on the fauna of the Maloney series: Journal of Geology, v. 24, fl uenccs uni i ke those that existed SO mil lion years ago. Fossil p. 570-582. palms are evidence of a major botanical shift that resulted Erwin, D. M. ; Stockey, R. A., 1991, Silicified monocotyledons from from gradual natural processes, but the patterns of biologic the middle Eocene Princeton chert (Allenby Formation) of British c hange we observe today are different. Compared to the domi Columbia: Review of Palaeobotany and Palynology, v. 70. p. 147- na n t organisms of the Early Tertiary, humans have an 162. astonishing ability to a lter the environment. We have become Frizzell , V . A., Jr., 1979, Petrology and stratigraphy of Paleogene important agents of geologic and biologic change, and our ac nonmarine sandstones, Cascade Range, Washington: U.S. Geo tivities influence the survival and extinction of many of the logical Survey Open-File Report 79-1149, 151 p., 3 plates. organisms with whom we share the planet. Rather than being Gregory, Irene, 1969, Fossilized palm wood in Oregon: Ore Bin, caused by the uplift of new mountain ranges or changing posi- v.31, no . 5, p. 93-110. Washington Geology, vol. 23, no. 2, June 1995 25 Gresens. R. L., 1982, Early Cenozoic geology of central Washington Newberry, J. S., 1863. Description of fossil plants collected by Mr. State; 1. Summary of sedimentary, igneous, and tectonic events: George Gibbs, geologist to the United Stales Northwest Boundary Northwest Science. v. 56, no. 3. p. 218-229. Commission: Boston Journal of Natural History, v. 7, p. 506-524. Griggs. P. H .. 1970, Palynological interpretation of the type section, Newberry, J. S., 1883, Brief descriptions of fossil plants. chi eny Ter Chuckanut Formation. northwestern Washington. In Kosanke. R. tiary. from western North America: U.S. National Museum Pro M.; Cross, A. T., editors, Symposium on palynology of the Late ceedings, v. 5, p. 502-514. Cretaceous and early Tertiary: Geological Society of America Newberry, J. S., 1898, The later extinct floras of North America. U.S. Special Paper 127, p. 169-212. Geological Survey Monograph 35 , 294 p. Heller. P L.; Tabor, R. W.; Suczek, C. A., 1987, Palcogcographic Pabst. M. B., 1952. A report on some fossil plants from the Chuckanut evolution of the United States Pacific Northwest during Paleo Formation of northwestern Washington, 41 p.; Further notes on ge ne time: Canadian Journal of Earth Sciences. v. 24, no. 8, the flora of the Chuckanut Formation, 63 p.: unpublished manu p. 1652-1667. scripts. Wes Wehr papers, Un iversity of Washington Allen Li Hopkins. W. S ., Jr .. 1966. Palynology of Tertiary rocks of the What brary. com basin. southwestern British Columbia and northwestern Pabst, M. B .. 1968, The t1ora of the Chuckanut Formation of north Washington: University of British Columbia Doctor of Philoso western Washington-The Equisetalcs. Fi licales, Coniferales: phy thesis, 184 p., 4 plates. University of California Publications in Geological Sciences, Johnson. S. Y., 1984. Stratigraphy, age. and paleogeography of the V . 76, 85 p. Eocene Chuckanut Formation. northwest Washington: Canadian Read. R. W.; Hickey, L. J .. 1972, A revised classification of fossil Journal of Earth Sciences. v. 21, no. I, p. 92-106. palm and palm-like leaves: Taxon, v. 21 , no. I, p. 129-137. Johnson. S. Y .. 1985. Eocene strike-slip faulting and non-marine ba Reiswig, K. N., 1982, Palynological differences between the sin formation in Washington. In Biddle, K. T ; Christie-Blick. N., Chuckanut and Huntingdon Formations, northwestern Washing editors, Strike-slip detormation, hasin formation, and sedimenta ton: Western Washington University Master of Science thesis, tion: Society of Economic Paleontologists and Mineralogists Spe 61 p. cial Publication 37, p. 283-302. Royse. C. F., Jr., 1965, Tertiary plant fossils from the Methow Valley, Knowlton, F. H .. 1902, Preliminary report on fossil plants from the Washington: Northwest Science, v. 39, no. 1, p. 18-25. State of Washington, coll ected by Henry Landes, 1901: Washing Thorne, P., 1976, Fossil palms, Vancouver, Bellingham, and ton Geological Survey Annual Report, v. 1, p. 32-33. Nanaimo: Canadian Rockhound, v. 20, no. 6, p. 14-20. Knowlton, F. H .. 1917. Fossil floras of the Vermejo and Raton forma Tuta, J. A., 1967, fossil palms: Principes, v. 11. p. 54-71. tions of Colorado and New Mexico. ill Lee. W. T.: Knowlton, F. Whetten, J. T.; Carroll, P. l.; Gower, II. D.; Brown. E. H. : Pessl, Fred. H .. Geology and paleontology of the Raton Mesa and other re Jr.. 1988, Bedrock geologic map of the Port Townsend 30- by gions in Colorado and New Mexico: U.S. Geological Survey Pro 60-minute quadrangle. Puget Sound region. Washington: U.S. fessional Paper IO I, p. 223-450. Geological Survey Miscellaneous Investigations Series Map 1- Knowlton . F. H .. 1919. A catalogue of the Mesozoic and Cenozoic 1198-G, I sheet, scale 1: 100,000. plants of North America: U.S . Geological Survey Bulletin 696. Wolfe, J. A., 1968, Paleogene biostratigraphy of nonmarine rocks in 8 15 p. King County, Washi ngton: U.S. Geological Survey Professional Kn owlton . F. H., 1930, The flora of the Denver and associated forma Paper 571 , 33 p .. 7 plates. tions of Colorado: U.S . Geological Survey Professional Paper Wolfe, J. A., 1977, Paleogene floras from the Gulf of Alaska region: 155, 142 p. , 59 photo plates. U.S. Geological Survey Professional Paper 997, 108 p., 30 photo La Motte, R. S., 1938, An Upper Cretaceous florule from northwest plates. ern Washington [abstract]: Northwest Science, v. 12, no. 4, p. 80. Wolfe, J. A., 1978, A paleobotanical interpretation of Tertiary cli LaMolle, R. S ., 1952, Calalogue of the Ceno1.0ic plants of North mates in the northern hemisphere: American Scientist, v. 66, America through 1950: Geological Society of America Memoir no. 6. p. 694-703. 51,381 p. Wolfe, J. A.; Wehr, W. C., 1987, Middle Eocene dicotyledonous Lakhanpal, R. N., 1958, The Rujada flora of west central Oregon: plants from Republic, northeastern Washington: U.S. Geological University of California Publications in Geological Sciences, Survey Bulletin 1597, 25 p., 16 photo plates. • v. 35, no. I, p. 1-65, 11 photo plates. Lesquereux, Leo, J 859, Species of fossil plams collected by Dr. John Evans al Nanaimo (Vancouver Island) and al Bellingham Bay, Free Guide to Oregon Museums Washington Territory: American Journal of Science, 2nd series, v. 27, no. 81, p. 360-363. A free 1995 Pocket Guide to Oregon Museums has just Lesquereux, Leo. 1869, On species of fossi l plants from the Tertiary been published by the Oregon Museum Association, the of the State of Mississippi: American Philosophical Society Oregon Historical Society, and museums throughout the Transactions, new series, v. 13, p. 411-433. state. It lists locations, hours, general contents, and admis Lesquereux, Leo, 1878, Contributions to the fossil flora of the West sion charges, if any, of over 130 museums. ern Territories; Part 2, The Tertiary flora : U.S. Geological Survey The guide tells you where you can find out about Ore of the Terrilories Report, v. 7, p. 112. pl. 12. gon's history, art, geology, wildlife, plants, natural re Mustoe, G. E .. 1993, Eocene bird tracks from the Chuekanut Forma sources, and industries and which museums have hands tion, northwest Washington: Canadian Journal of Earth Sciences, on displays and activities where you can learn by doing. v. 30, no. 6, p. 1205-1208. The guide is available at most Oregon museums. Single Mustoe, G. E.: Pevear, D. R. , 1981 , Vertebrate fossils from the copies may be obtained by sending a self-addressed, Chuckanut Formation of northwest Washington: Northwest Sci stamped, legal-size envelope to the Nature of the North ence, v. 57, no. 2, p. 119-124. west Information Center, 800 NE Oregon Street #5, Port land, OR 97232. 26 Washington Geology, vol. 23. no. 2. June 1995 Application of Reflection Seismology to the Hydrogeology of the Spokane Aquifer Stephen P. Palmer Michael King Washington Department of Natural Resources SeisPulse Development Corporation Division of Geology and Earth Resources PO Box 3355 PO Box 47007, Olympia, WA 98504-7007 Lacey, WA 98503-9998 Charles R. Gruenenlelder Stan Miller CH2M Hill Spokane County Lars Hendron 9 South Washington, Suite 400 1026 West Broadway City of Spokane Spokane, WA 99204 Spokane, WA 99204 Spokane, WA 99204 INTRODUCTION posits in tributary valleys. The deposits overlie relatively im The Spokane Aquifer is part of a regional ground-water sys permeable Precambrian to Cretaceous crystalline bedrock and tem termed the Spokane Valley-Rathdrum Prairie Aquifer, Miocene sedimentary rocks of the Latah Formation ard Co which encompasses portions of the north Idaho panhandle and lumbia River basalts. The flood deposits are typically 400 to eastern Washington near Spokane (Fig. I). The aquifer is 600 ft thick in the main valley east of Spokane and more than known to he one of the most transmissive alluvial-type aqui 700 ft thick north of Spokane in the Hillyard trough. The aqui fers in the United States and is the designated sole-source fer is unconfined throughout most of the valley and typically aquifer for more than 350,000 people living in the Spokane exhibits a strong degree of hydraulic interconnection with the Valley area. Spokane River. Howe ver. previous water balance estimates The Spokane Aquifer consists predominantly of sand- to for the Spokane Aquifer have relied upon little direct data on boulder-size sediments deposited by catastrophic outburst aquifer thickness. floods from episodic draining of Pleistocene glacial Lake Mis The bedrock topography beneath the valley floor is the pri soula. These unconsolidated deposits cons ist of coarse main mary control on aquifer thickness and, in turn, affects the di channel sediments in the Spokane Valley and finer eddy de- rection, rate, and quantity of ground-water flow. Shallow seis- 117°30 ' \ wmon I e ~ I Mead / - \ ~ I r '-- - 47' 45' \ [ ( \ Fivemlle I.... I o_,, \ Prairie / " \ I --~ -- I ba'-'"aarY / ·,t\, , ______appro x. aquifer ./ / - - / Airway He ights /,,,...-..., tz '-- ~------l 2: r--- HAVANA ST \ \ \ Figure 1. Location map of the greater Spokane Valley and v_icinity. The Spokane Valley-Rathdrum Prairie Aquifer is outlined. The location of the Harvard Road, Havana Street, and York Avenue se1sm1c profiles is shown. Washington Geology, vol. 23, no. 2, June 1995 27 .,... > ~ Shallow bedrock Shotpoint 1 0 102 130 150 170 190 210 230 250 270 290 310 330 350 370 ~ 390 410 430 0 .-,... ,_.I:"' 100 ... I: ·.: ~ > ::OI >, 200 ----- North Figure z. Seismic profile acquired along Harvard Road; we interpret the highlighted reflector as originating at the aquifer-bedrock contact. Shotpoint numbers are shown along the top edge of the profile; north is to the left. The five identical traces at the very left of the profile are Record synthetic seismograms developed from the Harvard Road check-shot 1 2 3 4 5 6 7 8 9 10 11 12 13 14 15 16 survey. mic reflection profi Ii ng was conducted to provide better defi nition of the aquifer thickness and bedrock topography. This information will be used in aquifer-management investiga tions conducted by Spokane County and in wellhead protec tion stud ies performed by the City of Spokane and other water purveyors. Seismic profiles acquired in the eastern Spokane Valley (Fig. 1) will provide constraints on aquifer thickness and geometry, which are critical parameters in any future esti mate of water balance and supply. Seismic reflection data ob tained in an area between Spokane Falls and Five Mile Prairie (Fig. I) will be used to refine boundary conditions for a well head protection ground-water flow model and may influence future location of municipal water supply wells. METHODOLOGY The seismic renection data were acquired using a new impul sive seismic source that inhibits ground roll (large amplitude seismic waves that travel on the ground surface from source to receiver). The lack of ground-rol I interference from the source enables the implementation of a near-offset method of reflec tion seismic surveying in which a short source-receiver offset, as close as 5 ft, is employed using a limited number of geo phones (usually 2 or 3). The short offset and limited number of geophones permits rapid collection of vertically summed reflection data. This near-vertical ray path eliminates the need for long cable layouts used in the acquisition of Common Depth Point reflection data, and reduces the data processi ng to a few basic steps: appropriate temporal filtering, static correc tion, and amplitude scaling. Preliminary processed sections can be available on a next-day basis, which allows the tlexibil ity to locate "today's" profiles on the basis of "yesterday's" data. Additionally, the near-offset method's flexibility and Figure !I. Waveform data from the Harvard Road check-shot survey. minimal source noise impacts allow it to be used in a wide The direct seismic wave traveling from source to downhole geophone variety of hydrogeologic settings, including noise-sensitive is the high amplitude event arriving between 20 and BO msec. urban environments. 28 Washington Geology, vol. 23, no. 2, June 1995 0 I Spokane I I ._ North River 20 ------'~ 1500 ± 90 ft/s 2500 40 2300 60 ~ ;J' ,:::---_, rJ) .c 80 P. ~ 2100 -~ I~ _, 100 0 "'" C ~~ 120 3030 ± 85 ft/s -~ 1900 -- ~ 140 I I~ t I "'-,~ ~ 1700 I 160 I I 1500 180 0.0 10.0 20.0 30.0 40.0 50.0 60.0 70.0 80.0 Traveltime (msec) 1300 100 140 180 220 260 300 340 380 420 Figure 4. Traveltime- depth curve developed from th e Harvard Road Shotpoint check-shot data shown in Figure 3. Figure 5. Cross section showing the depth to th e bedrock surface along Harvard Road developed from the seismic profile and velocity data. The aquifer thickness exceeds 500 It in the center of the main REGIONAL SEISMIC PROFILING valley. Seismic refl ecti on profiles acqui red in the eastern Spokane Valley provide data about the depth and configuration of the velocity increases to 3,030 ft/s. Check-shot surveys performed aquifer-bedrock contac t that will be used for future water bal in other water well s in the Spokane Valley indicate that the ance analyses. A north-south profile shot along Harvard Road seismic velocit y of saturated sand and gravel is approximately (Fig. I) provides an excellent example of our approach 10 map 5,500-6,000 ft/s . Crystalline bedrock can have seismic veloci ping the aquifer-bedrock contact. ties ranging from I 0,000 to 15,000 ft/s. Figure 2 presents the Harvard Road seismic re fl ection pro A synthetic reflection trace was generated from the veloc fil e; the spacin g between individual traces (shotpoints) is ity data obtained in the Harvard Road well for comparison to I 00 fl. We interpret the strong, fl at-ly ing refl ection observed the refl ection data acquired near the well. The five identical between s hotpoints 250 and 430 at approximately 220 to 240 traces displayed on the left in Figure 2 are the syntheti c seis millli seconds (msec) two-way lraveltime as ori g inating from mograms developed from the check-shot data. The aquifer the aquifer-bedrock contact. Starting at shotpoint 240 this re bedrock interface appears on both the synthetic seismogram flector begins to c limb, and between shotpoints 150 and 190 and the seismic profile as a s trong refl ector at 100 to 125 msec the bedrock contact is very near the ground surface. Wate r two-way traveltirne. The fl at-lying reflection at about 40 msec well s drilled near shotpoi nt 170 penetrated crystalline bedrock two-way traveltime results from a velocity increase of 1,500 at depths ranging from 20 to 50 ft ; bedrock outcrops can also to 3 ,030 ft/s occurring at a depth of 30 ft. The check-shot sur be observed adjacent to this portion of the profile. North of vey confi rms our interpretation of the bedrock refl ector , as shotpoi nt 150, a prominent reflector can be observed between well as explaining the origin of the flat-lying, shallow reflec 100 and 125 msec two-way traveltirne, which is interpreted as tor observed along the Harvard Road profile. the bcdrock-aqu ifer contact. Water we! Is located near this seg Two-way travel times of the aquifer-bedrock contact were ment of the profile encountered crystalline bedrock at depths converted to depth-below-ground-surface using the seismic o f 150 to 200 ft. velocities estimated from the check-shot surveys. The eleva We ll-velocity, or check-shot, surveys are performed in or tion of the bedrock surface was then calculated using these der to (I) estimate seismic velocities for the rock or soil units depths and topographic profiles. Fig ure 5 presents the depth penetrated in a well and (2) obtain the two-way traveltime to profile developed fro m the Harvard Road sei smic reflection stratigraphi c interfaces that give rise to strong reflections (for data. example, the aquifer-bedrock contact). A check-shot survey involves lowering a geophone to kno wn depths in a well and then measuring the seismic wave traveltime from a source lo SITE EVALUATIONS FOR THE CITY OF SPOKANE cated near the wellhead to the downhole geophone. Figure 3 presents the check-shot data for a waler well near A seismic reflection profile was shot along Havana Street to the north end of the Harvard Road seismic profile. The data determine the thickness and configuration of the aquifer near were recorded in 10-ft depth intervals from a depth of IO ft a major well field operated by the City of Spokane (profile (record I) to 160 ft (record 16). The check-shot well penetrates location shown in Fig. 1). The 2.5-mile-long seismic traverse 180 ft of unsaturated aquifer sand and gravel lying over crys across the entire width of the valley was made in an area where talline bedrock. Water is produced from fractured bedrock j ust the aquifer was locally constricted. The seis mi c reflection data below this contact. A traveltime-depth curve (Figure 4) was along Havana Street reveal a hummocky, irregular basement constructed from the c hec k-shot data, and seismic velocities topography and an aquifer thickness that locally exceeds 450 were estimated. We find that unsaturated sand and gravel in feet. The seismic survey data from this transect will be used to the upper 40 ft has a velocity of 1,500 ft/s; below this depth the refine the aquifer thickness estimates essential for estimating Washington Geology, vol. 23, no. 2, June 1995 29 Shotpoint 110 120 130 140 150 160 170 180 190 200 210 220 230 u -~ "'e 100 100 -~ .§ ~- => --..... =~ 200 I 200 0 ~ 300 West----+ Figure 6. York Avenue seismic profile showing the Trinity Trough and a central ridge that acts as a 'weir' for ground-water movement. Bedrock outcrops both north and so uth of this east- west profile. ground-water th rough- flow and understanding the overall hensive aquifer management and wellhead protection deline aquifer water balance. ation. Many other ground-water sources in Washington con Seis mi c reflection profiling in northwest Spokane, used in sist of unconfined gravel and sand aquifers overlying imper conjunction with a limited borehole exploration program, al meable bedroc k and are analogous in thi s way to the Spokane lowed accurate delineation of a previously unknown buried Aquifer. Consequently, the near-offset seismic reflection bedrock channel of the ancestral Spokane River. This channel method should be applicable to both regional and site-speL:ific feature, termed the Trinity Trough, is approximately I mi wide evaluation of the bedrock depth and geometry of these other and % mi long and is filled with more than 300 ft of flood aquifers. • deposit materials. The channel was cut through a north-trend ing bedrock basalt ridge that extends from downtown Spokane to Five Mil e Prairie, a prominent basalt-capped mesa north Nature of the Northwest Info Center west of the city (see Fig. I). The bedroc k ridge acts as a hy Receives Hammer Award draulic barrier to ground-water flow and, along with Five Mile Prairie, separates the aquifer into two distinct segments. The The Oregon Department of Geology and Mineral Industries Trinity Trough channel is believed to act as a subsurface (DOGAMI) and the U.S. Department of Agriculture Forest 'weir', controlling ground-water flow between two portions of Service received the Hammer A ward on May 30 in Portland. the aquifer that previously were believed to have little direct The award was presented by Doug Farbrother of Vice Presi hydraulic connection. Figure 6 is an east-west seismic profile dent Al Gore's National Performance Review Team. along York Avenue (see Fig. I) showing a cross-sectional The award was given to DOGAMI and the Forest Service view of the Trinity Trough and its 'weir' . Knowledge of the for their partnership in running the Nature of the Northwest channel's existence and its overall geometry will be important Information Center, one-stop shopping for information about in developing a representative ground-water flow model of the outdoor recreation and natural resources in the Pacific North aquifer and is expected to influence decisions regarding siting west. The center is located on the first floor of the State Office of future municipal water supply wells. Building at 800 NE Oregon St. in Portland. It carries bro chures, publications, and maps from a variety of state (Wash ington included), federal, and local governments, as well as CONCLUSIONS commercial publications related to outdoor recreation. The near-offset method of reflection seismic surveying imple The Hammer Award gives special recognition to govern mented in thi s investigation has been successfully used to de mental teams that have made a significant contribution in sup termine bedrock topography beneath the Spokane Aquifer. port of National Performance Review principles- putting cus Bedrock topography strongly affects the direction, rate, and tomers first, cutting red tape, empowering employees, and quantity of ground-water flow as it determines both the aquifer slashing government spending. The award, named for the infa thickness and overall aquifer flow geometry. Better definition mous $600 hammer, consists of a hammer (not the same one) of these aquifer characteristi cs is vitally important for comp re- framed with a signed citation from Vice President Gore. 30 Washington Geology, vol. 23, no. 2, June 1995 Selected Additions to the Library of the Division of Geology and Earth Resources February 1995 through April 1995 THESES northeast Washington: Washington State University Doctor of Burkcll. S . E .. 1991, Groundwater and water and nutrient budget stud Philosophy thesis. 190 p . ies of Newman Lake. Washington: Washington State University Waquar. Rizwan, 1994, Fini le-difference groundwater flow model of Master of Science thesis. 159 p. the sand aquifer in Minnie C reek and Marshall Creek vall eys, Dueker. K. G .. 1994, Origin of western United States upper mantle Spokane County. Washington: Eastern Was hington University seismi c heterogeneity: University of Oregon Doctor of Philoso Master of Science thesis, 112 p. phy thesis. 160 p. Xia. Ganyuan, 1993. Moment-tensor inversion for regional earth Gilbertson. L. A. , 1994. Geochemical. optical. and X-ray diffraction quakes in the Pacific Northwest: Oregon State University Master studies of tourmalines in Washi ngton and Oregon-Discrimina of Science thesis, 87 p. tion between mineralized and barren occurrences: Western Wash ington University Master of Science thesis. 152 p. U.S. GEOLOGICAL SURVEY REPORTS Graham. W . A .. 1994. Hydrogeologic characterization and reconnais Published reports sance water quality s tudy of the Chilco channe l area. Kootenai Esposito, K. J.; Whitney, Gene, 1995. Thermal effects of th in igneous County. Idaho: Eastern Washington University Master of Science intrusions on diagenetic reactions in a Tertiary basin of south thesis. 127 p. western Washington: U .S. Geological Survey Bulletin 2085-C, Han. Y . H .. 1993. Forsterite grain growth in naLUral olivines and syn 40 p. th et ic forslcritc/spinel compositions: University of Nevada, Reno Evarts, R. C.: Ashley. R. P. , 1993, Geologic map of the Spirit Lake Doctor of Philosophy thesis. 193 p . West quadrangle, Skamania and Cowlitz Counties, Washington: Hattenburg. T . G .. 1994. Geology and hydrology of the Minnie Creek U .S. Geological Survey Geologic Quadrangle Map GQ-1681. drainage basin with an emphasis on Queen Lucas Lake. Spokane I sheet. scale 1: 24,000, with 11 p. text. County. Washington: Eastern Washington Cniversity Master of Grosz, A. E.; Schruben, P. G., 1994, NURE geochemical and geo Science thesis. 198 p. physical s urveys-Defining prospective tcrranes for United Kirtland. J. A., 1995, Sediment production and delivery in the upper States placer exploration: U.S. Geological Survey Bulletin 2097, South Fork Nooksack River, northwest Washington. 1940-1991: 9 p., I plate. Western Washington Uni versity Master of Science thesis, 163 p. Johnson, S. Y.; O'Connor, J. T., 1994, Stratigraphy. sedimentology. Knaack, C. M .. 1991. Geology and geochemistry of th e Long Alec and provenance of the Raging River Formation (early? and middle Creek plucon. Ferry County. Washington: Washington State Uni Eocene), King County. Washington: U.S. Geological Survey Bul versity M aster of Science thesis. 93 p .. I plate. letin 2085-A, 33 p. Koerber. S. M .. 1991 , Comparison of fault morphology and geometry Krebs. W. N.; Bradbury. J. P., 1995, Geologic ranges of Jacustrine in different rock types: Washington Stace University Master of Actinocyclus species, western United States. In Bradbury. J. P. : Science thesis. 97 p. Krehs, W. N ., editors, The diatom genus Actinocyclus in the west Matt, V. J., 1994. Hydrology and hydrogeology of the Spokane Indian ern United States: U.S. Geological Survey Professional Paper Reservation. northeastern Washington State: Eastern Washington 1543-B, p. 49-73. University Master of Science thesis, 209 p. U.S. Geological Survey Nationa l Oil and Gas Resource Assessment Olness, I. A., 1993, Formulation of a finite-difference groundwater Team, 1995, 1995 national assessment of United States oil and flow mode l for the Spokane Valley aquifer. Washington: Eastern gas resources: U.S. Geological Survey Circular 1118, 20 p. Washington University Master of Science thesis, IO I p. Russell. L. C., 1993. Geochemistry of Tertiary igneous rocks in the Open-File and Draft Reports eastern half of the Chewelah quadrangle, Pend Oreille County, Kilburn, J. E.; Whitney, G. C.; d' Angelo, W. M.; Fey, D. L.; Hopkins. Washington: Eastern Washington University Master of Science R. T. ; Meier. A. L. ; Motooka, J. M.; Roushey, B. H.; Sutley, S. J. . thesis. 323 p. 1994, Geochemical data and sample locality maps for strcam Sabin. A. L. . 1994, Holocene and latest Pleistocene paleoceanography sediment, heavy-mineral-concentrate, mill tailing, water, and pre of the northeast Pacific and its relationship to climate change in cipitate samples collected in and around the Holden mine, Chelan the Pacific Northwest: Oregon State University Master of Science County, Washington: U.S. Geological Survey Open-File Report thesis, 93 p. 94-680A. 33 p.; U.S. Geological Survey Open-File Report 94- Shore, F. E., 1991 , The structural geology of th e Squaw Creek area, 6808, l floppy disc. Stevens County, Washington: Washington State University Mas Nelson, L. M., 1993, Flood elevations for the Soleduck Ri ver at Sol ter of Science thesis, 9 1 p., I plate. Due Hot Springs, Clallam County, Washington: U.S . Geological Sinclair, K. A .; Hirschey, S. J., 1992, A hydrogeologic investigation Survey Water-Resources Investigations Report 83-4083, 17 p. of the Scatter Creek/Black River area, southern Thurston County, Obermeier, S. F., 1995, Preliminary estimates of the strength of pre Washington State: Evergreen State College Master of Environ historic shaking in the Columbia River valley and the southern mental Studies thesis, 192 p., 8 plates. half of coastal Washington, with emphasis for a Cascadia subduc Suydam, J. D., 1993, Stratigraphy and sedimentology of the Klondike tion zone earthquake about 300 years ago: U.S. Geological Sur Mountain Formation, with implications for the Eocene paleo vey Open-File Report 94-589. 46 p. geography and tectonic development of the Okanogan Highlands. Washington Geology, vol. 23, no. 2, June 1995 31 Smith. V. K.; Koski. R. A .. 1994. Descriptive and chemical data for Steele, T . D.; Paschis, J. A.; Koenig. R. A., 1988, Hydrogcologic hydrothermal s ulfide-sulfate-silica chimneys from the northern c haracteri zation of basalts-The northern rim of the Columbia C left segment. Juan de Fuca Ridge: U.S. Geological Survey Pl a teau physiographic province and of the Creston study area, Open-File Report 94-15. 20 p. eastern W ashing ton: U.S . Nuclear Reg ulatory Commission U. S. Geological Survey, 1995, Database for II national mineral re NUREG/CR-5 I 07, 4 sheets microfiche [234 p.]. source assessment of undiscovered deposits of gold, si Iver, cop Terich, T. A.; Schwartz, M. L. ; Joh11nncssen, J . W., 1994, Annotated per. lead, and zinc-Conterminous United States: U.S. Geological bibliographies on shore line hardening effects, vegetative erosion Survey "Draft for Review," 2 v . control, and beach nourishment: Washington Department of Ecol ogy Publi cation 94-75: Coastal Erosion Management Studies, OTHER REPORTS ON WASHINGTON GEOLOGY V. 2, 51 p. Roettche r, Scou , I 995, Overview-Regulatory overlap and the met Thom, R. M.; Shreffler, D. K.: Macdonald , Kei th. 1994, Shoreline als mining and milling industry; Report to the 54th session. Was h armoring e ffects on coastal ecology and biological resources in ington State Legislature: Washi ngton Department of Ecology Puge t Sound, Washington: Washington Department of Ecology Publication 95-250, I v. Publ icati on 94-RO; Coastal Erosion Management Studies. v. 7. Canning. D. J.; Shipman, Hugh, I 995, Coastal erosion marrngement I V . studies in Puget Sound Was hington-Executive s ummary: Was h University of Washington Geophys ics Program, 1995, Quarterly net ington Department of Ecology Publication 94-74; Coastal Erosion work report 94- D on scismicity of Washington and western Ore Manageme nt Studies. v. I, 100 p. gon, Octoher I through December 3 1, 1994: University of Wash Christman, R. A., 1984, repr. 1995, Mount St. Helens-Science ac ington Geophysics Program, 23 p. ti vi ti es for secumlary; revised : Creative Dimensions [Bellingham, Washington Department of Health, Division of Radiation Protection, Wash.], 96 p. 1994, Closure of the Dawn Mining Company uranium mil lsite in Cox. Jack; Macdonald, Ke ith; Ri gcrt, Tom, 1994, Engineering and Ford, Washington-Final supplemental environmental impac t geotechnical techniques for s horeline erosion management in statement: Washington Department of Health, 1 v. Puget Sound: Washington Department of Ecology Publication 94- Western States Seismic Policy Council. 1994, WSSPC-95 catalog of 77; Coastal Erosion Manageme nt Studies, v. 4, I v . member states' earthquake preparedness and hazard mitigati on Dalton, Olmsted & Fuglcvand, Inc., 1994, Proposed water injection. products: Western States Seismic Policy Council, 141 p. Jackson Prairie Gas Storage Project. Lewis County, Washington: Withers poon, Boykin; Rawli ngs, Richard, 1994, Shoreline access de Dalton, Olmsted & Fuglevand. Inc .. I v. sign guidelines for Washington marine shoreline habitats: Wash King County Department of Public Works Surface Water Manage ington Division of Aquatic Resources, 58 p. ment Division, 1993, Guidelines fo r bank stabilization projects in the riveri ne environments of King County: King County Depart PAPERS ON WASHINGTON GEOLOGY ment of Public Works. I v. Atwater, 8 . F.; Ne lson, A. R. ; Clague. J. J.; Carver, G. A.: Yama Macdonald, Keith ; Simpson, David; Pa ul son, Bradley; Cox, Jack; guchi , D. K.; Bobrowsky, P. T.; Bourgeois. Joanne; Palmer, S. P.; Gendron, Jane. 1994, Sho reline armoring effects on physical and others, 1995, Summary of coastal geologic evidence fu r past coasta l processes in Puget Sound, Washington: Washington De great earthquakes at the Cascaclia subduction zone: Earthquake partment of Ecology Publication 94-78; Coastal Erosion Manage Spectra,v.11 , no. 1, p. 1-18. ment S tudies, v. 5, I v. Balistrieri, L. S.; Murray, J . W.; Paul, Barbara, 1994. The geochemi Macdonald, Keith; Witek. 8 . M., 1994, Management options for un cal cycling of trace elements in a biogenic meromictic lake: Geo stable bluffs in Puge t Sound. Washington: Washington Depart c himica et Cosmochimica Acta. v. 58. no. 19, p. 3993-4008. ment of Ecology Publication 94-81 ; Coastal Erosion Management Ballanty ne, Rich, 1995, Transporting refined products in a crude oil Studies, v. 8. 1 v. pipeline: BC Professional Engineer, v. 46, no. I, 16-17, 20. McCabe, G. H.; Wel lman. K. F., 1994, Policy alternatives for coastal Berg, R. B., 1995, Geology of western U.S. talc deposits. In Tabilio, erosion management: Washington Department of Ecology Publi Marialena; Dupras, D. L., editors, 29th Forum on th e Geology of cation 94-79; Coastal Erosion Management Studies, v. 5 , 77 p. Industrial Minerals-Proceedings: California Division of _M ines McCabe, G. H .; Wellman, K. F., I 994, Regional approaches to ad and Geology Special Publication 110, p. 69-79. dress coastal erosion management: Was hington Department of Bostock, M. G.; VanDecar, J. C., 1995, Upper mantle structure of the Ecology Publication 94-82; Coastal Erosion Management Stud northern Cascaclia subduction zone: Canadian Journal of Earth ies, v. 9, 42 p. Sciences. v. 32, no. I, p. I -2. Mead, R. D., 1995, The direct and cumulative effects of gravel mining Burk, R. L. ; Moser, K. R., 1988, Spirit Lake Me morial Highway on ground water within Thurston County, Washington: Thurston Geologic investigations in a zone of natural aesthetic change. /11 County Public Health and Soc ial Services Department, 40 p. Youd, T . L.; and others, convenors, Proceedings of the 39th an Northwest Federation of Mineralogical Societies, 1994, Membership nual Highway Geology Symposium-Construction to minimize directory of Northwest Federation of Mineralogical Societies: environmental impact: Highway Geology Symposium, p. 358- Northwest Federation of Mineralogical Soc ieties, 136 p. 370. Northwest Mining Association, 1995, 1995 service directory: North Clague, J. J ., 1995, Early historical and ethnographical accounts of west Mining Association, 278 p. large earthquakes and tsunamis on western V ancouver Island, Omernik, J.M.; Gallant, A. L., 1986, Ecoregions of the Pacific North British Columbia: Geological Survey of Canada Current Research west: U.S. Environmental Protection Agency EP A/600/3-86-033, I 995-A, p. 47-50. 39 p., I plate. Cook. T . L. ; Stakes, D. S., 1995. Biogeological mineralization in Pierce County Department of Planning and Land Services, I 993, Fi deep-sea hydrotherma l deposits: Science, v. 267, no. 5206, p. I 975-1979. nal supplemental environmental impact statement-Fife Sand & Gravel surface mine, C-3 POD rezone (Z I 3-9 I ) and major Dawson, A. G ., 1994, Geomorphological effects of tsunami run-up amendment to U.P. 12-78: Pierce County Department of Planning and backwash: Geomorphology, v. 10, no. 1-4, p. 83-94. and Land Services, 126 p. 32 Washington Geology, vol. 23, no. 2, June 1995 Driscoll. C. T .; Otton. J . K.; lverfeldt, Ake, 1994, Trace metals spe Monger. J. W. H.; Journeay, J.M., 1994, Basement geology and tec c iati on and cycling. ill Moldan. Bedrich; Cerny. Jiri. editors. Bio tonic evolution of the Vancouver region. /11 Ylonger, J . W . H., geochemistry of s mall catchments-A tool for e nvironmental editor, Geology and geological hazards of the Vancouver regio n, research: Jo hn Wiley and Sons. SCOPE 51. p. 299-322. southwestern British Columbia: Geological Survey of Canada EMCON Northwes t. Inc .. 1992, R & R Joint Venture hydrogeological Bulletin 481, p. 3-25. investigation for the aggregate mining operation, Walt Musa Montgomery, D. R., 1994, Road surface drainage. chc1nnel initiation, property, Clark County. Washi ngton: EMCON Northwest. Inc .. and slope instability: Water Resources Research. v. 30, no. 6. l v. p.1925-1932. Evans. J .E.: Ristow, R. J.. Jr .. 1994. Depositional history of the south Mustard, P. S., 1994, The Upper Cretaceous Nanaimo Group, Georgia eastern outcrop be lt of the Chuckanut Formati on-Impli cations Basin. In Monger. J . W. I I., editor, Geology and geological haz for th e Darrington- Devil's Mounta in and Straight Creek fault c1 rds of the Vancouver region, southwestern British Columbia: zones, Washington (A.): Canadian Journal of Earth Sciences, v. Geological S urvey of Canada Bulletin 48 1, p. 27-95. 31. no. 12, p. 1727- 1743. Mustard, P. S.; Rouse. G . E .. 1994, Stratigraphy and evolution of Ter Goedert, J. L. : Campbel l. K. A .. 1995, An early Oligocene chemosyn tiary Georgia Basin and subjacent Upper Cretaceous sedimentary thetic.: community from the .Maka h Formatio n, northwestern rocks, southwestern British Columbia and northwestern Washing Olympic Peninsula. Washington: The Veliger, v. 38, no. I. p. 22- ton. !11 Monger, J. W . H., editor, Geology and geological hazards 29. of the Vancouver region. southwestern British Columbia: Geo Goldstein. B. S .. 1994. Drumlins of the Puget Lowland. Washington logical Survey of Canada Bulletin 481 , p. 97-169. State. USA: Sedimentary Geology, v. 9 1, no. 1-4, p. 299-31 I . cwton, D. J.. Associates. Incorporated; and others, 1992, Draft en llamilton. T. S.; Dostal, J ., 1994. Middle Tertiary erup1ivc rocks in vironmental impact statement, proposed Coal Creek surface mine the Vancouver area. /11 Monger, J. W. H., editor, Geology and expansion, Cowlitz County, Washi ngton : Cowlitz County Depart geological hazards of the Vancouver region. southwestern British ment of Community Development, 2 v. Columbia: Geological Survey of Canada Bulle tin 481, p. I 7 1- Pe lto. M. S .. 1993, Changes in water supply in alrinc regions due to 179. glacier retreat. In Bras, Rafael, editor. The world at risk-Natural I lasselgren, E. 0.: C lowes. R. M .. 1995, Crustal structure of northern hazards and climate change: American Institute of Physics AIP Juan de Fuca plate from multic hanne l reflec tion data: Journal of Conference Proceedings 277, p. 61-67. Geophysical Research. v. I 00, no. 84. p. 6469-6486. Pendick, Daniel. 1995. Return to Mount St. Helens: Earth, v. 4. no. 2, He mphill-Haley, Ei lccn. 1995, Diatom evidence for cc1rthquake-i n p. 24-33. duc.:ed subsidence and tsunami 300 yr ago in southern coastal Rogers, G . C .. 1994. Earthquakes in the Vancouver area. /11 Monger. Washington : Geological Society of America Bulletin. v. 107. J. W . H., editor, Geology and geological hazards of the Vancou no. 3, p . 367-378. ver region, southwestern British Columbia: Geological Survey of He mphill-Haley. Ei leen, 1995. Intertidal diatoms from Willapa Bay. Canada Bull etin 481, p. 221-229. Washington- Applicati o n to s tudies of small-scale sea-level Schasse, H. W .. 1994, Washington. In Keyslonccoal industry manual. changes: Northwest Science, v. 69. no. I . p. 29-45. 1994: Maclean Hunter Publishing Company, p. S-l 69-S- 176. I le usser, C. L ; Jgarashi . Yc1cko. 1994. Quaternary migration pattern Squires, R. L .. 1995. First fossi I species of the chemosynthetic-com of Selaginella selagi11 oides in the North Pacific: Arctic and Al munity gastropod Provanna- Localized coal-seep li mestones in pine Research. v. 26. no. 2, p. 187- 192. upper Eocene and Oligocene rocks, Washington: The Veliger, Hickson. C. J.. 1994. C haracter of volcanism, volcanic hazc1rds, and v. 38, no. I , p. 30-36. risk. northern end of the Cascade magmatic arc, British Columbia Squires. R. L.; Goedert. J. L., 1995, An ex Lani species of Leptocltiton and Washington State. In Monger, J. W . H., editor, Geology and (Mollusca: Polyplacophora) in Eocene and Oligocene cold-seep geological hazards of the Vancouver region. southwestern British li mestones, Olympic Peninsula, Washington: The Ve li ger. v. 38, Columhia: Geological Survey of Canada Bulletin 481 , p. 231- no. 1, p. 47-53. 250. Spadaro, P. A.; Templeton. D. W.; Hartman, G . L.; Wang, T. S., 1993, Ke rr. R. A .. 1995. Faraway tsunami hints at a really big Northwest Predicting waler quality during dredging and disposal of contami quake: Science, v. 267. no. 5200, p. 962. nated sediments from the Sitcum Watcrwc1y in Commencement Leonard, Matthew: Plum. R. L.; Kilian, A. P., 1988. Considerations Bay, Washington, USA: Water Science and Technology, v. 28. affecting the c hoice of nailed slopes as a means of soi I stabiliza no. 8-9, p. 237-254. tion. /11 Youd , T. L. ; and othe rs. convenors. Proceedings of the Thomson, R. E. ; Davis, E. E.; Burd, 8 . J., 1995, Hydrothermal vent 39th annu c1 I llighway Geology Symposium- Construction to ing and geothermal heating in Caseadia Basin: Journal of Geo minimize environmental impact: High way Geology Symposium, physical Research, v. 100. no. 8 4, p. 6 12 1-6141. p. 288-302. Verdonck, David, 1995, Three-dimensional model of vertical defor Marsh. M. L.; Gianotti, C . M., 1995. Inelastic structural response to mation at the southern Cascadia subduction zone, western United Cascadia subduction zone earthquakes: Earthquake Spectra. States: Geology. v. 23, no. 3, p. 261 -264. v. 11 , no. 1, p. 63-89. Wc1 rren, Stephen; Fourr. Brian; England, Tom. 1994, Technology Mayer, L. M ., 1994. Relationships between mineral surfaces and or needs ide ntified for remote sensing of geologic conditions and en ganic carbon concentrations in soils and sediments: C hemicc1l Ge vironmental conta minant characterization at DOE Paci(ic North ology. v. 114. no. 3-4. p. 347-363. west region facilities. In Proceedings of the 10th Themati c Con Mc.:Caffrey , Robert; Goldf'inger. Chris. 1995, Forearc deformation ference on Geologic Remote Sensing-Exploration, Environ and great subduction ea.rthqu11kes- lmplications for Cascadia off me nt, and Engineering: Environme n tal Research Institute of sho re earthqua ke.: potential: Science, v. 267, no. 5199, p. 856-859. Michigan. v. I, p. 38-48. Meyers. P. A .. 1994. Preservation of elemental and isotopic source identific ation of sedimentary organic matter: C hemical Geology. v. 114. no. 3-4. p 289-302. Washington Geology, vol. 23, no. 2, June 1995 33 OTHER REPORT S, GENERAL TOPICS Monger, J. W. H., editor, 1994, Geology and geological hazards of the Adams, J.: Weichert, D. H.; Halchuk, S.; Basham, P. W., 1995, Trial Vancouver region, southwestern British Columbia: Geological seismic hazard maps of Canada, 1995- Preliminary values for se Survey of Canada Bulletin 481,316 p. lected Canadian cities: Geological Survey of Canada Open File Roddick, J. A.; Luternauer, J., 1994, GSC teacher' s field-trip guide to 3029, 48 p. the geology of the Vancouver area: Geological Survey of Canada Bolt. B. A .. 1993, Earthquakes: W . H. Freeman and Company, 331 p. Open Fi le 3021, 27 p. Britis h Columbia Geological Survey Branch, 1995, Reports, maps SAC Joint Venture, 1995, Steel moment frame connection: SAC Joint and geosciencc databases: British Columbia Geological Survey Venture SAC 95-1. 1 v. Branch Information Circular 1995-5, 76 p. Santa Clara County Department o r Health, 1994, Earthquakes-A Britis h Columbia Mineral Resources Division, 1995. British Colum survival guide for seniors: Santa Clara County Department of bia mineral exploration review 1994: British Columbia Mineral Health, 41 p. Resources Di vision Info rmation Circu Jar 1995- I • 24 p. Toppozada, Tousson; Borchardt, Glenn; Haydon, Wayne; Petersen, Dawson, F. M .. 1995, Coalbcd methane- A comparison between Mark; and others, l 995. Planning scenario in Humboldt and Del Canada and the United States: Geological Survey or Canada Bul Norte Counties, California for a great earthquake on the Cascadia letin 489, 60 p. subduction zone: California Division of Mines and Geology Spe cial Publication I I 5, I 59 p. EMCON Northwest, Inc., 1992. R & R Joint Venture hydrogeological investigation for the aggregate mining operation. Walt Musa U.S. Army Corps of Engineers, 1990?, Family preparedness: U.S property. Clark County, Washington: EMCON Northwest, Inc., Army Corps of Engineers I San Francisco, Calif.], 32 p. Iv. U.S. Federal Emergency Management Agency, 1986, Estimation of Fleischer. \11-ichael ; Mandarino. J. A .. 1995, Glossary of mineral spe homeless caseload for disaster assistance due to an earthquake: cies 1995: Mineralogical Record, Inc. , 280 p. U.S. Federal Emergency Management Agency, l v .. 2 plates. Geological Survey of Canada, 1995, Cordi JI era and Pacific margin: U.S. Federal Emergency Management Agency, 1994, Preserving re Geological Survey of Canada Current Research 1995-A. 183 p. sources through earthquake mitigation-National Earthquake Hazards Reduction Program biennial report to Congress, fiscal Grant, B.; Newell, J.M., editors, Geological fieldwork I 994-A sum years 1993-1994: U.S. Federal Emergency Management Agency. mary of field activities and current research: British Columbia I V . Geological Survey Branc h Paper 1995-1. 556 p. Whelen. Robert, 1994, Oregon's mineral industries-An assessment Mora. Z. D.: Miller, L.B., 1994, Dimension stone in Victoria, B.C.: of the size and economic importance of mineral extraction in British Columbia Geological Survey Branch Information Circular 1993: Oregon Department of Geology and Mineral Industries 1994-15. 43 p. Open-File Report 0-94-31, 15 p. • Additional Listings of Current Faculty and Student Geological Research at Washington Universities and Colleges CENTRAL WASHINGTON UNIVERSITY Crustal evolution processes on the Mendocino and Costa Rica Rift Faculty Research corridors-H. Paul Johnson Development of the capability to measure 'bare rock heat tlow'on the Mesozoic deformation of the Little Maria Mountains, southeastern sea floor-H. Paul Johnson California-R. D. Bentley Time-dependent changes in very young oceanic c rust-H. Paul Structural geology of the Yakima fold belt-R. D. Bemley Johnson Petrologic evolution of the Columbia River Basalts-R. D. Bentley Sediment properties in shelf and slope environments-Arrl111r R. M . The OWL is not a strike-slip fault-R. D. Bentley Nowell, Richard W. S1ernberg Sediment transport measurements in a regional seasonal ice cover Graduate Student Research Arthur R. M. Nowell, Richard W. Sternberg Tectono-geomorphic development of the Valle de San Filipe fault, Carbon-bearing fluids in the oceanic cru st-R,ussel/ E. McDuff, Debo northern Baja California. Mexico-Tracy Morgan Grover rah Kelley Quaternary history of the Cleman Mountains area, Yakima and Kitti Geophysical investigation of the Mid-Atlantic Ridge off axis using tas Counties-Steve Jensvold Hydroswcep- Jean-Christophe Sempere Mydrogeology of Kittitas Valley, K ittitas County, Washington-Ron Southeast Indian Ridge between 90°E and I 20°E: From a hot spot to Owens a cold spot-Jean-Christophe Sempere Field measurements of sediment transport processes in stratafurm: UNIVERSITY OF WASHINGTON Component I, extended d uration observations-Richard W. SCHOOL OF OCEANOGRAPHY Sternberg Faculty Research Investigations of sediment dynamics in the nearshore environment Integrated geological interpretation of deep tow sonar, submersible, Richard W. Sternberg and petrological observations of the upper and lower oceanic Analysis of absolute amplitudes observed in a marine seismic refrac crust-John R. Delany tion experiment-William S. D. Wilcock Arc upflow zones boundaries be tween adjacent hydrothermal sys tems? Geological and geochemical tests-John R. Delaney, Compiled by Rebecca A. Christie, Division of Geology and Earth Resources; Meghan Miller, Central Washington University; and Russell E. McDuff. Marvin D. Lilley Laurie K. Bryan, University of Washington. 34 Washington Geology, vol. 23, no. 2, June 1995 Extra Copies of U.S. Geological Survey Reports Are Available from the Division Library We have extra copies of the fo llowing U.S. Geological Survey re CIRCULARS ports. Single copies are available free while supplies last. Send your Effects of Mount St. Helens eruption on selected lakes in Wash requests by phone, fax, e-mail. or surface mail to Conni e Manson or ington by N. P. Dion and S.S. Embrey. 1981. Circular 850-G. Rebecca Christie. (Seep. 2 for addresses.) Highlights in marine research by S. H. Clarke, editor, Circular 938. BULLETINS PROFESSIONAL PAPERS Manganese resources of the Olympic Peninsula, Washington by C. F. Park, Jr., 1942, Bulletin 931-R. Foraminil'era from the northern Olympic Peninsula, Washington by W.W. Rau, 1964, Professional Paper 374-G. The Blewett iron-nickel deposit, Chelan County, Washington by C. A. Lamey, 1950, Bulletin 969-D. Botanical evidence of the modern history of Nisqually Glacier, Washington by R. S. Sigafoos and E. L. Hendricks. 1960. Profes The Cle Elum River nickeliferous iron deposits, Kittitas County, sional Paper 387-A. Washington by C. A. Lamey and P. E. Hotz, 1952, Bulletin 978-B. Paleogene bioslratigraphy of nonmarine rocks in King County, Dolomite deposit near Marble, Stevens County, Washington by Washington hy J. A. Wolfe, 1968, Professional Paper 571. Charles Deiss. 1955, Bulletin 1027-C. Stratigraphy and chronology of late interglacial and early Vashon MAPS glacial time in the Seattle area, Washington by D. R. YlulJineaux, Map showing non-metallic mineral resources in part of west-cen H. H. Waldron. and Meyer Rubin, J 965, Bulletin J J 94-0. tral King County, Washington hy William Rice, 1975. Miscellane The Yakima Basalt and Ellensburg Formation of south-central ous Investigations Series Map 1-852-D. Washington by J . W. Bingham and M. J. Grolier. 1966. Bulletin Geologic conditions r elated to waste-disposal planning in the 1224-G. southern Hood Canal area, Washington by R. J. Carson, Mackey S ummary report on the geology and mineral resources of Flattery Smith, and B. L. Foxworthy. 1975, Miscellaneous Investigations Se Rocks, Quillayute Needles, and Copalis National Wildlife Ref ries Map 1-853-D, I sheet, scale 1 :62,500. uges, Washington by A. E. Weissenborn and P. D. Snavely, Jr.. 1968, Relative slope stability of the southern Hood Canal area, Wash 8 ulletin 1260-F. ington by Mackey Smith and R. J. Carson. 1977, Miscellaneous Jn Sedimentary and igneous rocks of the Grays River quadrangle, vestigations Series Map 1-853-F. Washington hy E.W. Wolfe and E. H. McKee, 1972, Bulletin 1335. Preliminary geologic map and sections of the magnesite belt, Stevens County, Washington by Ian Campbell and J. S. HOW TO FIND OUR MAIN OFFICE Loofhourow, Jr., 1957. MF-117. Preliminary geologic map of part of the Turtle Lake quadrangle, Lincoln and Stevens Counties, Washington by G. E. Becraft, P. L. Weis, 1957, MF-135. Union /we. Preliminary geologic map of the Lead 11th Ave. point quadrangle, Stevens County, N Washington by R. G. Yates, J. F. Robert Natural son, 1958, YIF-137. A Resources Preliminary geologic map of the Deep Building Lake quadrangle, Stevens a nd Pend 14th ,__ ~ Oreille Counties, Washington by R. G. ------r--r--..:::<-...::, Ave. C: Yates, 1960, MF-237. Stat~ .,0 Capitol ~ Geologic map of the Hus um quadran .; i Mi'Jllilld H -, gle, Washington by R. A. Sheppard, £ 1------ 1964, MF-280. ·c. Maple Park Ave. t)"' Mineral resource potential of the Eagle Rock Roadless Arca, Snohomish and Division of Geology and Earth Resource Natural Resources Bldg., Room 148 King Counties, Washington by S. E. 1111 Washington St. S. E. Church, R. W. Tabor, and F. L. Johnson, Olympia, WA 98501 1983, MF-1380-B. (S eep. 2 for our mailing address.) Mineral resource potential map of the Visitor parking (VP) is available on Glacier Peak Roadless Area, Sno level P1 at $.50/hour. Use the homish County, Washington by S. E. Washington St. entrance. Church, R. W. Tabor, and F. L. Johnson, 1983, MF-1380-C. Washington Geology, vol. 23, no. 2, June 1995 35 Mineral resource potential of the Wonder Mountain Roadless Area, Mason County, Washington by S. E. Church, J. G. Frisken, R. CD-ROM Databases Available W. Tabor, and S. R. Iverson, 1983, MF-1418-B. The following CD-ROM databases arc available for use in the Di Mineral resource potential map of the Glacier Peak Wilderness vision Library: and adjacent areas, Chelan, Skagit and Snohomish Counties, Washington by S. E. Church, A. B. Ford, V. J. Flanigan, R. B. Stotel GeoRef References and selected abstracts to geology literature. Over 1.5 meyer, 1984, MF-1652-A. million bibliographic records covering North America since 1785 Mineral resource potential map of the Goal Rocks wilderness and and other areas since 1933. adjacent Roadless Areas, Lewis and Yakima Counties, Washing ton by S. E. Church, D. A. Swanson, D. L. Williams, G. A. Clayton, Earth Sciences Disc 1975-July, 1993 U.S. Geological Survey library database of bibliographic records T. J. Close. and T. J. Peters, 1983, Map MF-1653-A. • Earth Sciences Data Directory Information about earth science data sets. GEOINDEX Staff Notes A compilation of references to geologic maps of the United Heidi Thomsen, Clerk Typist 2, is at the front desk replacing Steve States. Luceno, who was promoted to auditor at the Department of Labor and Water Resources Abstracts Industries. Heidi was formerly with the Business Computer Training Bibliographic database of water resources literature since 1967. Institute in Lacey. Hydrodata Judy Henderson. Clerk Typist 3, replaces Karin Lang on accounts U.S. Geological Survey peak values-United States payable, travel, training, and payroll. Karin moved up to Electronic U.S. Geological Survey daily values-West 2 Parts Specialist for the Radio Shop at the DNR Compound in Lacey. Climatedata Judy was previously a Word Processing Specialist with the Wildlife Hourly precipitation-Western region Division of the Department of Fish and Wildlife. Summary of the day-West 2 Rebecca Christie has been promoted from Lihrarian I to Lihrary In NOAA & MMS Marine Minerals CD-ROM Data Set formation Specialist. Geophysics of North America Nancy Rhcrle, Cartographer 2, has returned to OGER after a one-year developmental assignment with the Forest Practices Division. She is acting as temporary geologist/public information officer, assuming a portion of the geologists' Rock Week duties fielding questions from Erratum for GM-41 the public. Nancy is also working on a departmental committee pre In the text accompanying Geologic Map 41, Liquefaction paring for National Geography Awareness Week, Nov. 12-18. Susceptibility for the Des Moines and Renton 7.5-minute Ch uck Gulick. Geologist 2, has transferred from the Spokane office Quadrangles, Washington, Figure 4 has been printed up Lo Colvil le as the new Northeast Regional Geologist. side down. WASHINGTON STATE DEPARTMENTOF BULK RATE Natural Resources U.S. POSTAGE PAID Jennifer M . Belch er - Commiss ioner of Public Lands Washington State Kaleen Cottingham - Supervisor Department ol Printing Department of Natural Resources Division of Geology and Earth Resources PO Box 47007 Olympia, WA 98504-7007 ADDRESS CORRECTION REQUESTED