b. Further justification for the detachment geometry shown in Figure 7 comes from the southwestern flanks of the Panamint Range. Generally classified as a quartz monzonite porphyry but in the area of Skidoo, it is mostly gneissic but in part porphyritic and has fluidal structures with dark phenocrysts of biotite. a. Along the eastern base of the Panamint Range, between Trail and Hanaupah Canyons (TC and HC, Fig. Stewart (1983) proposed that the Panamint Range forms the hanging wall of an extensional system that transported the Panamint Range westward from on top or east of the Black Mountains, with the latter forming the footwall of this extensional system. (Blair and Raynolds, 1999); (4) although there are angular unconformities within these formations, there are no data such as progressive tilt (Snow and Lux, 1999) to suggest that they were deposited in active grabens. Devonian-Silurian These data sets include digital geologic maps published by the U.S. Geological Survey (USGS) (Workman et al., 2002) and the California Geologic Survey (Saucedo et al., 2000), digital elevation model (DEM) topography (USGS DEM, 2009), and tectonic and sediment fill compilations (Blakely and Ponce, 2002). In lower beds: Protopliomerops , Kirkella , Orthid brachiopods. It takes some time for waves to gnaw away terraces like the ones seen on Shoreline Butte, so these benches provide records of times when the lake level stabilized long enough for waves to leave their mark on the rock. Other historic charcoal kilns in the United States include the Cottonwood Charcoal Kilns at Owens Lake, the Piedmont Charcoal Kilns in Wyoming, and the Walker Charcoal Kiln in Arizona. The dip on the eastern side of the basin is 50. At the one-mile mark, the canyon narrows for the first time to a width of roughly 40 feet across. Also in this area, McKenna and Hodges (1990) mapped the 8.69.4 Ma Trail Canyon volcanic sequence (Fig. The cross section was made by extracting topography from the DEM data (Fig. Through exploratory holes drilled by the Pacific Coast Borax Company, prior to Death Valley becoming a national monument in 1934, it was discovered that the salt and gravel beds of the Devil's Golf Course extend to a depth of more than 1,000 feet (300m). By far the largest national park in the contiguous United States, more than 90% of Death Valley's 3.3 million acres are protected as a designated Wilderness Area. 3.0 Hours of Monument Valley's Sunrise or Sunset 44 Tour. Upper and lower third of units consists of interbedded red and brown quartzite, brownish green micaceous siltstone and minor orange-weathering silty dolomite. This two-stage structural evolution of extensional faulting followed by strike slip is also seen in the Panamint Valley (Andrew and Walker, 2009) and, north of the Inyo Range, in the White Mountains (Stockli et al., 2003) and central Walker Lane belt (Oldow et al., 2008). [2005] include the Artist Drive and Greenwater in the Furnace Creek), but these differences are not substantial to this paper. $14.99. 18 to 5 Ma, low-angle Basin and Range extension transported allochthons consisting of Late Proterozoic through Early Paleozoic miogeoclinal section along detachment surfaces that, as extension continued, were exhumed from mid-lower crustal levels to the surface. In this formation, the placoderm Dunkleosteus (a small cladodont) and cochliodont tooth have been found. The Paleozoic extensional allochthons are located above this duplex. Pliocene (3.3 3.5 Ma) Topographic map of Fall Canyon - Death Valley NPS - Dan Kish Length: 6 mile (9.7km) out and back, round trip Time: 3.5 hours round trip Difficulty: Moderate to Difficult Elevation Gain: 2,460 ft (752m) Location: The 2.7 mile (4.3km) unpaved two-way section of Titus Canyon Road is located 11.9 miles north of CA-190 on Scotty's Castle Road. Eocene and Paleocene East of Death Valley, the Tecopa Basin (TB, Fig. Noteworthy among the geologic features of the Death Valley region of eastern California is an extensively exposed accumulation of sedimentary rock and sill-forming diabase, Precambrian in age, as much as 5,500 m thick, and essentially unmetamorphosed. *3 Members* upper and lower members are brownish-weathering dolomite/limestone and quartzite in the middle member lower member represents high water stand deposition with carbonate intervals overlain by fluvially-dominated terrestrial braidplain and braid-delta facies of the middle member also contains Ediacaran fossils upper member represents mainly marine deposition with abundant body and trace fossils typical of the Early Cambrian such as olenellid trilobites and Skolithos tubes found in the siltstone beds, also Helicoplacoid echinoderms and brachiopod molds and casts have been found above the archaeocyathan and olenellid-bearing limestones are green siltstones containing trilobites, echinoderms, and hyoliths. Mostly loose shingled pebble-size gravel; little sand or silt; few cobbles. Cichanski (2000) mapped the southern portion of the range front and found generally low-angle faults (dips 1534), with indications that these fault surfaces have been cut by steeper faults, but the vertical offset on these faults is minor. Over time, the sediments compressed into limestone and a related calcium-magnesium carbonate called dolomite. Topography is colored with a nonlinear scale ranging from pale blues below sea level through greens and browns to white of the Sierra Nevada peaks. *9 Members* alternating siliciclastic and carbonate facies lower four (of the nine) members and the lower part of the fifth member contain Early Cambrian olenellid trilobites. Cemen et al. (1976) relate to a Proterozoic aulacogen. Difficulty: Easy/Moderate. To accommodate as many events as possible, the time scale (from Gradstein et al., 2004) is shown with a variable vertical scale, logarithmic from 1000 yr to 1 m.y., then a linear scale from 1 to 5 m.y. Stromatolites, thrombolites, oncoids, and brachiopod fragments are common, pelmatozoan ossicles less common. b. Thick-bedded, fine-grained, and even-grained dolomite, mostly light color. 24 Lost Burro Formation 3 Ma, initiation of the East California Shear Zone started development of the present-day topographic depression of Death Valley, formed as a pull-apart basin associated with this strike slip. The first event metamorphosed Death Valley's Precambrian basement rocks and occurred around 1,700 million years ago. No fossils reported c. Unit is white, pale red, purple, pink, and gray, quarzite and sandstone, conglomeratic quartzite, and minor beds of light- to dark-brown micaceous siltstone. Prior to recognition of low-angle extensional faulting in Death Valley, Burchfiel and Stewart (1966), on the basis of the morphology of the valley and occurrence of strike-slip faults, suggested that Death Valley was formed as a strike-slip pull-apart basin, with the basin forming between the Northern Death ValleyFurnace Creek fault to the north and the Southern Death Valley fault zone to the south (Fig. The lower section contains Early Mississippian coral and the cephalopod Cravenoceras. Late Precambrian Please keep in mind that collecting rocks within Death Valley is illegal without a permit! Middle (?) (1999) as 200 10 kA. A siltstone/shale formation that is exposed in the northern part of Panamint Range in the Tucki Mountain Region. Along the east side of Tucki Mountain, extension is marked by Paleozoic sedimentary rocks in fault contact with Proterozoic rocks that have been tectonically exhumed from mid-crustal (greenschist; Hodges et al., 1987) levels. No fossils. The second event began while layered younger Precambrian sediments were being deposited on top of the beveled surface of older metamorphic basement rocks. Difficulty: Moderate to Difficult Elevation Gain: 1,200 ft (366m) This age is an important constraint on initiation of Basin and Range extension, as the Bat Mountain Formation is interpreted to have been deposited in a basin formed during the early stages of extension (Cemen et al., 1999). There is no apparent reason for these rocks to be in the footwall of the detachment at Tucki Mountain and in the hanging wall further south along the range, as they would need to be if the entire Panamint Range is allochthonous. 3). Death Valley is a playground for geology enthusiasts, maybe even more like a Mecca. 5 Funeral Formation Eocene The students stayed in a Beatty hotel and visited nine total sites in Death Valley National Park. The massive expanse of white is made up of almost pure table salt. Areas below sea level are in blue. Like the Black Mountains sections, these sediments show little evidence of syndepositional tectonism, yet are now highly deformed, with almost vertical dips in places (Beratan et al., 1999). (1999) question the correlation because the Funeral Mountains section is underlain by a Miocene conglomerate unit that does not occur at Tucki Mountain and there are differences in structures in the underlying Paleozoic section (a thrust fault in the Mississippian strata in the Funeral Mountains is not seen at Tucki Mountain). The Hunter Mountain fault connects to strike-slip faults on the west side of the Panamint Range; Burchfiel et al. c. Quartzite, conglomeratic quartzite, siltstone, shale and minor limestone and dolomite beds. A recent phase of this propagation was opening of the Gulf of California and initiation of the San Andreas fault as the plate boundary at 56 Ma (Lonsdale, 1989; Atwater and Stock, 1998). Noonday Dolomite is limestone that was formed 750 million years ago when Death Valley was part of the Pacific Ocean, before being buried, heated, and exposed to enormous amounts of pressure. Smooth, polished marble walls enclose the trail as it follows the canyon's sinuous curves. Death Valley is currently building a rock collection of the parks stratigraphy. the dolomite member contains conical calcareous fossils including metazoan small shelly fossils of Cloudina in another member there are rare occurrences of the trace fossil Planolites. ), such as Death Valley ephedra (Ephedra funerea), are spaced between them, with other xeric sub-shrubs and native bunchgrasses. Ubehebe Crater is the largest of more than a dozen of in the Ubehebe Craters field. Monument Valley Tour. c. White, pink, and red orthoquartzite; laminated to thick-bedded, commonly cross-bedded, and well cemented; has skolithos. Winds strong enough for sandblasting come from the north and the south. b. Mapped as 1 unit (Lee Flat, Perdido and Tin together). Ammonites, smooth-shelled brachiopods, belemnites, and hexacorals. 2) at 15.6 Ma, followed by a period of slow uplift then renewed normal slip at 2.8 Ma. The Noonday Dolomite (Fig. a. Every twist and turn you take in the park reveals a new display of buckled, distorted rock formations that boggle the mind as to how it was sculpted by nature. Syringopora have also been found. (1994) provide an interpretation of eruption volume versus time, which the sawtooth pattern in Figure 3 schematically follows. Dokka and Travis (1990b) favored an initiation age of 106 Ma for the Mojave portion of the ECSZ. (2009), in a detailed analysis of the Inyo Mountains, report a phase of normal faulting starting at 15.6 Ma and initiation of strike-slip faulting on the Hunter Mountain fault at 2.8 Ma. Mosaic Canyon is a geological art gallery filled with irregularly shaped fragments of tan-colored Noonday dolomite, sandy matrix and lime cement that creates complex murals in the canyon walls. Dashed line shows inferred location of the detachment fault across Tucki Mountain. 26 Ely Springs Dolomite This interpretation is similar to one shown by Hunt and Mabey (1996) in a cross section near Hanaupah Canyon (their fig. 9 Furnace Creek Formation 28 Pogonip Group Dunderberg Shale Member consists of reddish-brown to greenish-brown shale, thin-bedded limestone, and some siltstone; trilobite fragments are common. 1) developed and has forced deformation to the east, into the ECSZ. The slickenslides are on the southwest flanks of the turtleback surfaces and trend northwest with a plunge of 10 to 15 (Troxel and Wright, 1987); these structures imply both normal and strike-slip components of motion along the flanks of the turtlebacks. I've only ever hiked it in January and December, and even then it felt warm. This shale contains linguloid brachiopods and trilobite trash beds with fragments of "Ehmaniella." Typically located at the end-depositional sites in basin interiors. Open grooves in the ventifacts are called flutes. These structures are created when the surface of the earth is under extensional, or a pulling force. This fault pattern is not consistent with a low-angle detachment fault underlying Death Valley that would link the Black Mountains and Panamint Range, with the Black Mountains the footwall of the detachment and the Panamints the hanging wall. Tin Mountain Limestone 1000 feet thick, is black with thin-bedded lower member and thick-bedded upper member. These rocks are found along the full length of the Panamint Range (Fig. This relative timing can be seen in Figure 3, where events associated with Basin and Range extension predate deposition of most of the Artist Drive through Funeral Formations. Hidden Valley Dolomite, Lost Burro Formation, and the Tin Mountain Limestone. In the Ash Meadow area crinoidal columns have been found. TvTertiary volcanics. *5 Members* The upper member contains conodonts, microgastropod steinkerns, sponge spicules, and fish remains. Its summit rises 11,331 feet (3,454m) above Badwater Basin, the lowest point in Death Valley at 282 feet (86m). The canyon follows faults that formed when the rocky crust of the Death Valley region began stretching just a few million years ago. Death Valley NP is renowned world-wide for its exposed, complex, unique tectonics and diverse geologic resources. Also shown are the three Quaternary pluvial Lake Manly events when Death Valley was flooded (Anderson and Wells, 2003). The interpretations presented above offer some new ideas for the evolution of Death Valley. In the White Mountains northwest of Death Valley, Stockli et al. The Panamint Valley basin runs between the Panamint Range to the east and Argus and Slate ranges to the west for 65 miles (105km). The following list of geologic formations and corresponding ages represents what has been collected in the park and are available for viewing at our curatorial facility. A feature of these intrusives is that they are intruded along the structural top of each turtleback, with the Willow Springs diorite structurally beneath the younger (Fig. A poorly preserved brachiopod assemblage has been found. This correlation implies 2555 km of post-eruption offset between the two locations, the distance depending on details of how the intervening faults are restored (McKenna and Hodges, 1990). This, the nation's greatest evaporation potential, means that even a 12-foot (3.7m) deep, 30 miles (48km) long lake would dry up in a single year. There does not appear to be a high-angle fault along the west side of the Panamints. The main visitor center of the park is located here as well as the Oasis at Death Valley resort complex. a. Sediment age at the base of this well was estimated by Lowenstein et al. Along the road to the canyon stands Leadfield, a ghost town dating to the 1920s. These rock formation began as limestone deposited during Late Precambrian (about 850-700 million years ago) when the area was covered by a warm sea. The kilns were located here as the trees single-leaf pinyon pine (Pinus monophylla) and Utah juniper (Juniperus osteosperma) dominate the landscape in the upper Panamint Mountains. Faults are from the USGS Quaternary faults database (2009).

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