Abstract A prevailing hypothesis for the central Cascade Range of Washington State is that it underwent regional extension or transtension during the Eocene. This hypothesis is based on the idea that kilometers-thick, clastic, Eocene formations were deposited syntectonically in local basins. Our mapping and structural analysis indicate that these formations are preserved in fault-bounded, regional synclines, not in separate depositional basins. Thus, the type area for the hypothesis, the so-called Chiwaukum graben, is here renamed the Chiwaukum Structural Low. The Eocene arkosic Chum-stick Formation, which was thought to have been syntectonically deposited in the graben, is the proximal equivalent of the Roslyn Formation 25 km southwest of the graben. Because the name “Roslyn Formation” has precedence, the name “Chumstick Formation” should be abandoned. Additionally, several areas previously mapped as Chumstick Formation in the Chiwaukum Structural Low probably are parts of the older Swauk Formation and younger Wenatchee Formation. The southwestern boundary of the Chiwaukum Structural Low includes the Leav-enworth fault zone, which consists of postdepositional, northwest-striking reverse faults with adjacent northwest-striking folds. The reverse faults place the regionally extensive early-Eocene, arkosic Swauk Formation over the mid-Eocene, arkosic Chumstick Formation. A diamictite, which previously was placed in the Chumstick Formation and inferred to have been syntectonically derived from the Leavenworth fault zone, is part of the older Swauk Formation. We mapped a 0.6–1-km-thick conglomerate-bearing sandstone as a robust marker unit in the Chumstick Formation; instead of being spatially related to the bounding faults, this unit has a >30 km strike length around the limbs of folds in the structural low. The northwest-striking reverse faults and fold hinges of the structural low are cut by north-striking strike-slip faults, which likely are late Eocene to Oligocene; these north-south faults partially bound the structural low. The Eocene folds and faults were reactivated by deformation of the Miocene Columbia River Basalt Group; this younger folding largely defines the regional map pattern, including the structural low. A model to account for the above characteristics is that all of the Eocene formations, not just the Roslyn Formation, are kilometers thick and are remnants of regional unconformity-bounded sequences that were deposited on the Eocene margin of this part of North America. Their present distribution is governed by younger faults, folds, and erosion. Thus, the Eocene to Recent history of the central Cascade region is characterized not by crustal extension, but by episodes of folding (with related reverse faults) and strike-slip faulting.

Abstract This road log uses mileposts (MP) as a reference unless otherwise stated. The mileposts are green, numbered in white, and placed on the right side of the road on small metal poles. The times refer to the viewing direction: 12:00, straight ahead; 3:00, to right; etc. Geologic data are from Livingston (1963), Taboret al. (1982, 1987), Evans and Johnson (1989), Gresens(1983), Ottetal. (1986), and other data reported in this guidebook. Refer to Figures 1 and 2 in Evans (this guidebook) for a generalized geologic map and stratigraphic summary of the Cle Elum - Liberty - Wenatchee region. - Drive east of Seattle via Interstate 90 and take exit 84 into the town of Cle Elum (an Indian word meaning swift water). Travel through town. Cle Elumand the town of Roslyn several miles to the northwest lieon theMiddle to LateEocene RoslynFormation (arksoicsandstone, siltstone), whichdips gently to the south-southwest and containscoal whichwas mined at Roslyn. From about 1870 to 1960,60.1 million tons ofcoal was mined, largely for use by the Northern Pacific Railway, but later for electric power plants. The Roslyn is time-equivalent to the arkosic deposits of the Chumstick Formation in the Wenatchee area. It unconformaby overlies the t47 Ma Teanaway Basalt flows, which in turn overlie the more strongly folded , Early Eocene to Paleocene Swauk Formation, also an arksoic sequence. Locally, a sequence of arkosic sedimentaryrocks richer in volcaniclastic units, the SilverPass Sequence, unconfonnably overlies the Swauk beneath the Teanaway. - At the east end of town, continue straight, following route 970 east to Wenatchee. - MP 2 - Hills at distance at 11 :00 are capped by Miocene Columbia River Basalt dipping gently to the east-southeast. Low hills to left are Roslyn Formation. - MP 3 - On clear days, the peak of Mount Stewart can be seen at about 9:30. Mount Stewart is part of a 93 Ma granodiorite batholith which intrudes a metamorphic complex, including the accreted, Early Mesozoic, Ingalls Tectonic Complex of oceanic rocks which will beseen later. - MP 4 - Hills in distance at 10-12:00 are 47 Ma Teanaway Basalt flows stratigraphically beneath the Roslyn Formation. - MP 6 - Hills on skyline ahead are capped by nearly horizontal Columbia River Basalt. - MP 8.5 - Hills to left and ahead are Teanaway Basalt. - MP 10.2 - Interchange with US Route 97; proceed straight ahead to Wenatchee on 97.

Palynologie data have been obtained from 30 localities in the Swauk, Naches, and Roslyn Formations of central Washington and in the Puget Group of western Washington. Although the Swauk Formation previously has been assigned ages as old as Paleocene or Cretaceous, palynologie results show that the type Swauk Formation is Eocene and that the Swauk Formation of the Chiwaukum graben and Wenatchee areas is Eocene and Oligocene. Correlations based on palynomorph biozones show that the Swauk, Naches, Teanaway, and Roslyn Formations of central Washington are time-equivalent to the Puget Group of western Washington and are part of the same depositional sequences of Eocene and Oligocene age. Palynomorph biozones found useful in this study include the Pistillipollenites and Platycarya concurrent-range zone, early(?) and middle Eocene; the Platycarya and Bursera concurrent-range zone, late Eocene; and the Gothanipollis and Elaeagnus concurrent-range zone, Oligocene. These concurrent-range zones can be used to correlate the central Washington formations and Puget Group with other strata in southwestern Washington and in the Bellingham, Washington, and Vancouver, British Columbia, areas.

Abstract The Tertiary sedimentary and volcanic rocks of the Cascade Range unconformably overlie a crystalline basement of previously accreted terranes. The Tertiary strata are parts of four synthems, or interregional unconformity-bounded sequences of tectonic origin. Thus, the formations in these synthems were not deposited in local basins. The 55-38 Ma Challis synthem has five regional unconformity-bounded formations; the names with precedence are (from the base up) Swauk, Taneum, Teanaway, Roslyn, and Naches. Near Blewett Pass (nee Swauk Pass), the Challis fluvial and arkosic Swauk Formation is ~5 km thick and has several members in a generally upward-fining succession. The members of the Swauk do not interfinger, and some are separated by unconformities. The Oligocene to mid-Miocene andesitic and rhyolitic Kittitas synthem is almost absent in the area. The most voluminous lithostratigraphic unit in the mid-Miocene to Pliocene Walpapi synthem is the Columbia River Basalt Group. Clasts of Columbia River Basalt Group and older rocks in the ca. 4 Ma Thorp Formation of the High Cascade synthem record initial uplift of the Cascade Range to the west. North of Blewett Pass, the northwesterly segment of the Leavenworth fault is the Camas Creek reverse fault that places Swauk and Teanaway in the Blushastin anticline over a syncline in the Roslyn Formation. Northerly striking faults in the Leaven-worth fault zone are parts of a younger system that cuts the Camas Creek thrust and northwest-striking folds in Challis rocks. In style, scale, and age, the Camas Creek fault resembles the Easton Ridge thrust south of Cle Elum, the Eagle Creek fault in the Chiwaukum graben, and the Seattle fault in the Puget Lowland. These faults are on the steeper northeastern limbs of major anticlines in Challis rocks. Down plunge, these folds are more gentle in Walpapi rocks. These folds and faults are part of the regional Seattle-Wentachee-Kittitas fold-and-thrust belt. The Straight Creek fault is a major, north-south, dextral fault in the northern Cascade Range. The fault offsets all five of the Challis unconformity-bounded formations. The southeasterly curving discontinuity along which it was mapped east of Easton is due to unconformities at the base of the Taneum and Teanaway, not a fault. The Straight Creek fault is 2.7 km west of Easton and passes southward beneath Kittitas rocks. Although the fault dextrally displaces pre-Tertiary units >90 km, Tertiary displacement is &55 km. This may indicate two (or more) periods of displacement. Perhaps the displaced portion of the fault underlies Puget Sound. Two sets of post-Walpapi folds deform the Tertiary synthems. The Seattle-Wentachee-Kittitas fold-and-thrust belt is part of a set of northwest-striking folds. One of several north-trending regional anticlines causes the Cascade Range. The Cascade Range anticline, with an amplitude of ~3.5 km, has risen in approximately the past 3.5 m.y. This anticline causes the plunges of the Seattle-Wentachee-Kittitas fold-and-thrust belt folds. The two sets of folds cause a regional interference, or “egg-crate,” pattern that dominates the present topography of the Pacific Northwest.

Abstract A ruling hypothesis for the central Cascade Range in Washington is that the Eocene arkosic formations, which are kilometers thick, were deposited in local grabens, such as the Chumstick Formation in the putative Chiwaukum graben. However, the formations are regional in extent and are preserved in less extensive northwesttrending synclines. The Chumstick Formation in the Peshastin syncline is a more proximal equivalent of the Roslyn Formation, which is preserved in the Kittitas Valley syncline 25 km to the southwest. The Chiwaukum structural low is partially bounded on the southwest by the Leavenworth fault zone, which consists of northwesterly striking, northeasterly verging reverse faults (with associated northwest-striking folds). The reverse faults and the hinges of the folds are cut by N-S, dextral strike-slip faults, which also partially bound the Chiwaukum structural low. Conglomeratic units in the Chumstick Formation are not proximal to either set of bounding faults. The Leavenworth fault occurs on the steeper northeastern limb of a northwesterly trending, basement-cored anticline. The Eagle Creek and Ainsley Canyon anticlines also have reverse faults on their steeper northeastern limbs. In the Puget Lowland, the Seattle reverse fault is in a similar anticline. The regional distribution of the Eocene formations and uplift of the Cascade Range are caused by folding of the Miocene Columbia River Basalt Group since 4 Ma. The remnant of a 4 Ma andesite on Natapoc Mountain shows that the present low topography of the Chiwaukum structural low is erosional and young.

Abstract Eocene sedimentary and volcanic rocks on the eastern flank of the Cascade Range consist of five regional, unconformity-bounded formations of the Challis synthem. These formations define a series of northwesterly striking folds. Five anticlines are 9 to 28 km apart, have pre-Tertiary crystalline rocks in their cores, high-angle reverse faults on their steeper northeastern limbs, and pass down-plunge into more gentle folds in the Neogene Columbia River Basalt Group (CRBG). Such northwesterly trending folds extend from east of the Columbia River across the Cascade Range to the Puget Lowland. The Chiwaukum graben and Swauk basin, which heretofore were thought to be local, extensional, depositional basins, are, instead, the major northwesterly trending synclines in this series of folds. The Eocene formations were preserved, not deposited, in these synclines. Dextral, N-S faults cut the reverse faults and the pre-CRBG portion of some of the folds. The post-CRBG folds control the regional distribution of the Eocene formations. The Cascade Range is a southerly plunging, post-CRBG anticline. Clasts in the Thorp Gravel indicate that this anticline began to rise ca. 4 Ma. The anticline has an amplitude of ∼3.5 km, and it causes the plunges of the northwesterly striking post-CRBG folds. The northerly and northwesterly post-CRBG folds form a regional interference pattern, or “egg-crate,” that dominates the present topography of Washington State.