Vertebrates, titanotheres, etc. Airspace above the valley is part of the Panamint Military Operating Area, restricted to US military use. Later researchers discovered that the region had experienced substantial tension that pulled large blocks of crust apart. (1974) showed that the turtlebacks include many linear structures parallel to the direction of strike slip, ranging from minute slickenslides to fault mullions tens or hundreds of meters in amplitude (Wright et al., 1974, p. 54). A hapsiphyllid tetracoral, Triplophyllites was collected immediately south of Rest Spring. 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. The change from Basin and Range extension to strike slip between 8 and 3 Ma seen in the Death Valley region is very close to age ranges of changes in similar tectonic settings seen in several other localities in the ECSZ (Stockli et al., 2003; Faulds et al., 2005; Oldow et al., 2008; Lee et al., 2009; Andrew and Walker, 2009). Cambrian-Late Precambrian Further implications of this update will be discussed elsewhere. See text for details. Death Valley National Park is not a summertime destination, at least in my opinion. WMWhite Mountains; IRInyo Range. From here Badwater Basin can be seen, which McKenna and Hodges (1990) mapped extensional structures at Trail Canyon. 26 Ely Springs Dolomite 1 and 2; Miller and Pavlis, 2005). Most of the holes in the basalt are vesicles that were formed when gas escaped from the cooling lava. The main visitor center of the park is located here as well as the Oasis at Death Valley resort complex. the remaining members contain a variety of Middle Cambrian trilobites. Includes many rhyolite and lesser trachyte and comendite masses, many of them associated with calderas. Darwin Falls is a waterfall located on the western edge of Death Valley National Park near the settlement of Panamint Springs, California. No fossils. (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). 22 Perdido Formation LCSLittle Chief Stock (10.6 Ma granite; Hodges et al., 1990). Ninemile is light-to moderate-brown shaly siltstone and black and gray silty limestone and dolomite. 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. Miocene Permian-Pennsylvanian a. Streptelasmatid corals: Grewingkia, Bighornia, Brachiopods. Dips of the flanks of the Panamint Range are shallow, averaging 10. Along the road to the canyon stands Leadfield, a ghost town dating to the 1920s. 1). Its summit rises 11,331 feet (3,454m) above Badwater Basin, the lowest point in Death Valley at 282 feet (86m). This unfortunate thrust fault term was used by Hunt and Mabey, even though they recognized the extensional origin of the younger-over-older structural relationship at Tucki Mountain (Hunt and Mabey, 1966, p. A99). Round Trip Time: 1.5 to 4.5 hours depending on route. Unit is about 345 to 380 m thick in the Spring Mountains and southern Sheep Range, 365 m thick in the northern Last Chance Range, 457 m in the Panamint Range area, about 530 m thick in the Nopah Range and in the Cottonwood Mountains, 766 m thick in the Pahranagat Range, 720 m thick in the NTS area. An alternation of shaly and silty members with limestone members transitional between underlying clastic formations and overlying carbonate ones. Death Valley National Park Self-Guided Audio Driving Tour. Numerous trilobite trash beds in lower part yield fragments of olenellid trilobites. At Tucki Mountain, the detachment tracks over the top of the anticline that forms Tucki Mountain (Fig. The interpretations presented above offer some new ideas for the evolution of Death Valley. a. c. Widely exposed in map area. Lower contact with Eurkeka Quartzite is major disconformity; upper contact with Laketown Dolomite (Silurian) in eastern park of quadrangle is disconformable, in western part of quadrangle, upper contact with Hidden Valley Dolomite reported as gradational and conformable. Location Fall Canyon is located in the Grapevine Mountains, towards the less-traveled north end of Death Valley National Park.It is close to Titus Canyon, another colorful ravine that is popular because of the rough one-way track that extends through it - this is a 4WD route that starts from road NV 374 in Nevada, crosses the flat Amargosa Valley into California and then winds through the . The canyon follows faults that formed when the rocky crust of the Death Valley region began stretching just a few million years ago. Mosaic Canyon was named for a rock formation known as the Mosaic Breccia. Death Valley is currently building a rock collection of the parks stratigraphy. Further justification for the detachment geometry shown in Figure 7 comes from the southwestern flanks of the Panamint Range. 1 Alluvial fan and lacustrine deposits The cross section was made by extracting topography from the DEM data (Fig. 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. Booming Dunes: For reasons not yet fully understood, sand sliding down the slipface of a dune can produce booming noises at startling volumes. (2002). a. If the detachment system along the east side of the Panamints is the one along which the Panamints moved, as in the model of Stewart (1983), then there is a correlation problem. Unit is 580 m to 1,700 m thick in the NTS area, about 1,000 m thick in the Cottonwood Mountains, 1,150 to 1,350 m thick in the Montgomery Mountains and Nopah Range respectively, about 610 m thick in the norther Last Chance Range, 445 to 900 m thick in the Spring Mountains and southern Sheep Range, and reaches a maximum thickness of 1,633 m in the Groom Range area, Lincoln County. 7), probably because this section is the oldest that covers the entire area. Along the road to the canyon stands Leadfield, a ghost town dating to the 1920s. Racetrack Playa is a seasonally dry lake (playa) located in the northern part of the Panamint Mountains that is famous for rocks that mysteriously move across its surface. They also lie on the flank of a Proterozoic rift basin filled with Pahrump Group sediments, as mapped by Wright et al. Miller and Pavlis (2005) give an excellent overview of current data and understanding of the turtlebacks. Stratigraphic nomenclature for the Proterozoic and Early Paleozoic section of the Death Valley area. a. Difficulty: Moderate to Difficult Elevation Gain: 1,200 ft (366m) Cross sections in Figures 6, 8, and 9 are labeled A, B, and C. APAguereberry Point; ARArgus Range; BWBadwater; BMBlack Mountains; CCCopper Canyon; CHConfidence Hills; CMCottonwood Mountains; DPDarwin Plateau; DVDeath Valley; EMEagle Mountain; FMFuneral Mountains; FPFuneral Peak; GMGrapevine Mountains; GRGreenwater Range; HCHanaupah Canyon; HMHunter Mountain; IRInyo Range; KRKingston Range; MPMormon Point; NDFZNorthern Death Valley fault zone; NRNopah Range; PRPanamint Range; PVPanamint Valley; SDFZSouthern Death Valley fault zone; TBTecopa Basin; TCTrail Canyon; TMTucki Mountain; TPTelescope Peak. Ammonites, smooth-shelled brachiopods, belemnites, and hexacorals. a. b. These will be used to build a structural model for evolution of the basin, but before doing that, it is useful to examine the geometry of Basin and Range detachment faults in the basin. Based on research, 61 formations are known to exist in the park. Over time, the sediments compressed into limestone and a related calcium-magnesium carbonate called dolomite. Dokka and Travis (1990b) favored an initiation age of 106 Ma for the Mojave portion of the ECSZ. With the northwest strike of the turtleback structures, parallel to the inferred direction of strike slip, an origin of these features as a result of the strike slip is suggested. This part of the valley has numerous cotton top cactus, blister beetles and cholla cactus. These strong winds pick-up dust and sand (mostly from the two closest alluvial fans), which literally sand-blast exposed surfaces. Goniatite coquina beds, formed chiefly of the cephalopod Cravenoceras hesperiam, occur within this formation. Unit forms massive cliffs, 975 m thick in northwestern Spring Mountains, 1,100 m thick in the Montgomery Mountains, 2,100 m thick in the Funeral Mountains, 1,500 m thick in the Belted Range and 700 m thick at Bare Mountain. The Lower Limestone Member was collected and is described as predominantly limestone of intermediate grays, in 1- to 3-foot beds, much of it containing silt, sand, or siliceous pebbles; interstratified with shale, partly carbonaceous; small, dark-gray spheroidal chert nodules in limestone near base. Ash beds, conglomerate, marl beds, mudstone, tephra beds. So both flanks of the Panamint Range display fault geometries that indicate detachment surfaces tracking over the top of the range, rather than underneath it. Presumably deposited in a basin like present-day Death Valley, these sediments are today located up to 800 m above the valley floor. Death Valley lies between two sets of mountains, the taller Panamint Range to the west and the dryer Amargosa Range along the Nevada-California border. Extension along the Harrisburg fault (HF, Fig. The Devil's Golf Course is a large salt pan on the floor of Death Valley. The low-angle detachment surfaces in the latter category are normal faults linking the strike-slip faults. These structures are created when the surface of the earth is under extensional, or a pulling force. 25 Hidden Valley Dolomite (1999) as 200 10 kA. 4), the canyon cuts through mylonized dolomite. 17 Butte Valley Formation The middle section contains bryozoans and some brachiopods, while the lower section has no fossils. Extrapolating this age to the 4.7 km maximum depth in the Badwater Basin (Blakely and Ponce, 2002) yields an age of 4.85.3 Ma for the base of the section. Today, however, these formations all show significant structural dip, such as the 30 NE dip of the Furnace Creek Formation seen at Zabriskie Point (Greene, 1997). Events associated with Basin and Range extension occurred in the Miocene to very early Pliocene. The event that commenced at 15.6 Ma included 16 westward tilt of the Inyo Range and 5300 m of uplift of the eastern flank, at a rapid rate of 1.9 mm/a. Saratoga Springs (.mw-parser-output .geo-default,.mw-parser-output .geo-dms,.mw-parser-output .geo-dec{display:inline}.mw-parser-output .geo-nondefault,.mw-parser-output .geo-multi-punct{display:none}.mw-parser-output .longitude,.mw-parser-output .latitude{white-space:nowrap}354054N 1162525W / 35.68167N 116.42361W / 35.68167; -116.42361[11]) is a desert oasis located in southern Death Valley National Park. At ca. These rocks are found along the full length of the Panamint Range (Fig. Neogene sediments preserved within Death Valley record the latest phases of structural evolution of the basin. per adult. *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. Further south, between the Copper Canyon and Mormon Point turtlebacks, the Mormon Point Formation is also in fault contact with basement rocks, in this case the Mormon Point turtleback (Hayman, 2006; MP, Fig. Eocene and Paleocene At the canyon mouth water spreads out and deposits its sediment load, gradually building up a large wedge-shaped alluvial fan that extends down toward Stovepipe Wells. (1974) do not suggest that the turtlebacks themselves are mullion structures, but a comparison with oceanic megamullions suggests that this is what they are. Ordovician Massive quartzite, with thin-bedded quartzite at base and top, 350 feet thick. The crust responds to this force by sending a large and long roughly v-shaped block of crust down which forms the bedrock of the valley floor (see Basin and Range). Dates. Plant life includes common reeds, bulrush and saltgrass. Recommended. At some locations, such as in the Spring Mountains, has sandy carbonate beds and collophane nodules, and in Panamint Range area, lower part contains mostly silty and sandy dolomite, argillaceous quarzite, and minor shale. Previous Friday folds from Mosaic Canyon can be seen here and here and here and here. This means that the structures are young, created in the last 3 m.y., although the rocks that make up the turtleback megamullions formed the footwall to the Basin and Range extensional system and were tectonically exhumed in the Miocene. Papoose Lake Member is mostly dark-gray dolomite with distinctive brownish-gray to grayish-orange burrow mottles; sparse limestone and silty dolomite beds. The turtlebacks are therefore formed of rocks that were exhumed due to extension and at the same time were intruded by a variety of igneous rocks. 10 Timber Mountain Group It is located in the Basin and Range extensional province (Sonder and Jones, 1999; Burchfiel et al., 1992), in the Walker Lane belt (Stewart, 1988), and also in the Eastern California Shear Zone (ECSZ; Dokka and Travis, 1990a). 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. The two events responsible for the chaotic appearance of the Amargosa Chaos did not occur until over half a billion years later, during Mesozoic or Early Tertiary time. Modern geologists have documented four major deformational events that faulted and folded the Amargosa Chaos. 33 Zabriskie Quartzite Conglomerate, equivalent to the Funeral Formation? The age of fill in Death Valley is not directly observed. Hunt and Mabey (1966) recognized this structure and correlated it with the Amargosa Thrust of Noble (1941). Sand dunes cover 3 square miles (8km2) of Eureka Valley, rising 680 feet (207 m) as one of North America's tallest dunes.
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