Following a right-hand bend and broader left turn, the canyon further constricts at 1.25 miles, forming orange- and gray-tinted narrows. Labels are colored for visibility only. Contact with overlying Bonanza King Formation is commonly marked by a change from slope-forming yellowish-weathering limestone of the Carrara to more massive cliff-forming limestone and dolomite of the Bonanza King formation. The structures are usually corrugated with mullion structures parallel to spreading direction and Tucholke and Lin (1998) relate them to continental metamorphic core complexes. A few scattered olenellid trilobites and archaeocyathids in upper part of formation. 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. As Figure 4 shows, outcrops of Paleozoic sediments along the eastern side of the range are continuous from Tucki Mountain southward along the eastern slope of the Panamints, and these Paleozoic sediments are interpreted to be Basin and Rangestyle extensional allochthons. Mostly thick-bedded arid massive dark-colored dolomite, thin-bedded limestone member 500 feet thick 1 000 feet below top of formation, 2 brown-weathering shaIy units, upper one fossiliferous, about 200 arid 500 feet, respectively, below thin-bedded member. The other period of interruption occurred between 350 and 250 Ma when sporadic pulses of mud swept southward into the Death Valley region during the erosion of highlands in north-central Nevada. b. Dolomite, with some limestone, at base, shale unit in middle, massive dolomite at top. The upper part of this limestone is highly fossiliferous and characterized by the corals Syringopora and Zaphrentites. Unlike at the Devils Golf Course, significant rainstorms flood Badwater, covering the salt pan with a thin sheet of standing water. c. Interbedded limestone, silty limestone, silstone, sandstone, and shale. 2) at 15.6 Ma, followed by a period of slow uplift then renewed normal slip at 2.8 Ma. Upper and lower third of units consists of interbedded red and brown quartzite, brownish green micaceous siltstone and minor orange-weathering silty dolomite. 32 Carrara Formation Each newly formed lake doesn't last long though, because the 1.9 inches (48mm) average rainfall is overwhelmed by a 150-inch (3,800mm) annual evaporation rate. The three turtleback structures in the Black Mountains, as pointed out by Miller and Pavlis (2005), are keys to understanding tectonic evolution of the area. Other layers have been sliced out of their original sequence altogether. 15 Hall Canyon Pluton Two quartzite beds, each about 3 feet thick, near base, numerous sandstone beds 8001 000 feet above base. The highest strandline is one of the principal clues that geologists use to estimate the depth of the lake that once filled Death Valley. Vegetation in the area is sparse, largely confined to hearty sagebrush. is a cherty argillaceous unit containing Lower Devonian fish, the pteraspidids Blieckaspis and Panamintaspis from the Trail Canyon area. In the second phase, transtensional faulting began east of the White Mountains at 6 Ma, followed at 3 Ma by initiation of strike slip in the Owens Valley (Fig. Artist's Palette is an area on the face of the Black Mountains noted for a variety of rock colors. From 1.8 billion-year-old metamorphic rocks exposed in the Black mountains, to recent playa sediments deposited in the valley basins, Death Valley possesses a superb geologic record. Seismic reflection data (Louie et al., 1992) show 140 m of flat-lying section below the 5.12 Ma basalts, this section lying unconformably on tilted and faulted sediments. b. Based on these comparisons, I suggest that the turtlebacks are megamullions formed as a result of strike-slip faulting in Death Valley. Furnace Creek is a spring, oasis, and village that sits on top of a remarkably symmetrical alluvial fan. . 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. Sediment age at the base of this well was estimated by Lowenstein et al. Round Trip Length: 2-7.8 miles (3.2-12.6 km) depending on route. 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. The Late Miocene intrusives consist of the mafic Willow Springs pluton and the felsic Smith Mountain granite. 35 Stirling Quartzite AMAvawatz Mountains; ARArgus Range; BMBlack Mountains; CMCottonwood Mountains; DPDarwin Plateau; DVDeath Valley; FMFuneral Mountains; FCFZFurnace Creek fault zone; GMGrapevine Mountains; HMHunter Mountain; HMFHunter Mountain fault; IFZInyo fault zone; IRInyo Range; KPKingston Peak; NDVFZNorthern Death Valley fault zone; NRNopah Range; OVOwens Valley; PRPanamint Range; PVPanamint Valley; SMSpring Mountain; SDVFZSouthern Death Valley fault zone; SVSaline Valley; SWNVFSouthwest Nevada Volcanic Field; TMTucki Mountain. 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. 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. The detachment fault in the Black Mountains is known as the Amargosa detachment (Wright et al., 1974). Several springs overflow into pools totaling 6.6 acres (2.7 ha) in area, making the site the third largest marsh in the park. Stromatoporoids. It features megabreccia and other rock formations, petroglyphs, and wildlife of various kinds, including bighorn sheep. In lower beds: Protopliomerops , Kirkella , Orthid brachiopods. Cambrian Wright et al. The Noonday Dolomite has since been tilted from uplift. a. Itinerary. Above this unit is an upper crinoidal limestone, which was deposited on an offshore bar or bank. The tiny grains of quartz and feldspar that form the sinuous sculptures that make up this dune field began as much larger pieces of solid rock. Locally, fair dolomite near middle arid at top. To understand more about structural evolution of Death Valley, it is useful to consider the area's position in relation to structural provinces that have been defined in western North America. Light-to moderate-brown, dusky-yllowish brown, varicolored red, and white to light-brown quartzite and sandstone; sand grains are fine to medium-grained. Death Valley National Park is one of many units within the National Park service established because of its underlying geologic theme. Extrapolation of measured sedimentary rates in the upper flat-lying section yields an age of between 5 and 7 Ma for the unconformity above the fault blocks, suggesting that Basin and Range extension ceased in the Late Miocene in the Tecopa Basin (Calzia and Rm, 2000). Pennsylvanian Also in the last few years, several important data sets relevant to a regional understanding of the geology of the Death Valley area have become available. The Miocene-aged formation is made up of cemented gravel, playa deposits, and volcanic debris, perhaps 5,000 feet (1,500m) thick. The rocks on its exposed and barren ridge are famous for being shaped by wind erosion and are called ventifacts. I would like to thank Dave Reynolds and Stefan Boettcher for introducing me to Death Valley geology. Cambrian-Late Precambrian The gneiss displays mylonitic fabric consistent with westward displacement of the extensional allochthons (McKenna and Hodges, 1990). Its summit rises 11,331 feet (3,454m) above Badwater Basin, the lowest point in Death Valley at 282 feet (86m). Lee et al. In summary, the turtlebacks are antiformal structures that strike and dip toward the northwest, exposed along the range front bordering Death Valley. It is intriguing that the ocean megamullion matches fairly well with the shape of the basement surface of the Badwater turtleback. Mostly shale, in part olive brown, in part purple. Events associated with Basin and Range extension occurred in the Miocene to very early Pliocene. Antelope Valley is medium-gray, finely to coarsely crystalline limestone and silty limestone, and dark-yellowish-to-orange, grayish-orange and dark-yellowish brown limestone, and yellowish-orange to pink silty partings; beds are commonly burrowed, and have yellowish-orange to pale red tracks and trails on bedding planes; contains orthocone cephlapods, gastropods (Maclurites and Palliseria) pelmatozoans, Receptaculites, and trilobites; also contains ooids and oncoids. Cichanski (2000) suggests that the higher-angle faults are part of the Panamint Valley strike-slip fault. Most of the so-called 'sailing stones' are from a nearby high hillside of dark dolomite on the south end of the playa. It features megabreccia and other rock formations, petroglyphs, and wildlife of various kinds, including bighorn sheep. The first category described by Miller and Pavlis (2005) is the Rolling Hinge model as proposed by Stewart (1983), Hamilton (1988), Wernicke et al. Formed of steep cliffs, it is composed of red colored oxidized rocks and is visible from Zabriskie point and the Golden Canyon trail. 12 Titus Canyon Lack of preserved basinal section equivalent to the Black Mountains Artist Drive Formation and younger formations across the top of the Panamint Range suggests that the range was a high by 8 Ma, although the northwestern flanks were low enough at 10 Ma to begin accumulation of Nova Basin sediments (Fig. Tucholke and Lin (1998) compiled dimensional data on 17 oceanic megamullions. 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. (2002) and, for the area west of the Panamint Range, from Saucedo et al. 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 3 Ma restoration is shown in two phases for convenience. b. As shown in Figure 6, this section is also seen in the extensional allochthons on the east flank of Tucki Mountain. 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). This interpretation is similar to one shown by Hunt and Mabey (1996) in a cross section near Hanaupah Canyon (their fig. When the Death Valley pull-apart basin started to form ca. *deposited in marine basins during Precambrian continental rifting algal marine dolomite. (2002) and Hunt and Mabey (1966). (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). These megamullions are similar to those seen at oceanic spreading centers. The canyon offers a suite of folds on almost all scales and styles to bedazzle the geologically-inclined visitor. a. 28 Pogonip Group The only fossiliferous bed is shale below limestone member neat middle of formation. 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. b. Mapped as 1 unit (Lee Flat, Perdido and Tin together). a. (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. Quartz grains are usually fine- to medium-grained. Called the Artist Drive Formation, the rock unit provides evidence for one of the Death Valley area's most violently explosive volcanic periods. As discussed earlier, the present-day contact between the Artist Drive Formation and basement of the Badwater surface is faulted, but the geometry shown in this restoration shows that the Artist Drive Formation could have been originally deposited on basement, with faulting seen today a result of postdeposition emergence of the Badwater turtleback. Eocene and Paleocene Uplift history of the range is uncertain with present data. Plant life includes common reeds, bulrush and saltgrass. 18 Owens Valley Formation 37 Noonday Dolomite b. Basal unit is well-bedded quartzite above 1,650 feet thick ' shaly Unit above this 520 feet thick contains lowest olenellids in section; top unit of dolomite and quartzite 400 feet thick. This part of the valley has numerous cotton top cactus, blister beetles and cholla cactus. 41 formations are listed with a number correlating them to the original reference used to describe and locate them. Widely distributed fusilinids. The mountain that Dante's View is on is part of the Black Mountains which along with the parallel Panamint Range across the valley from what geologists call a horst and the valley that is called a graben. 10 Timber Mountain Group See text for details. Based on research, 61 formations are known to exist in the park. A mix of carbonate and siliciclastic sequences from a shallow, near-shore depo. Late Precambrian The steeply dipping faults seen in Figure 9 make interpretation of Death Valley as a pull-apart basin more realistic than the low-angle fault interpretation. Located 1/4 mile west of Stovepipe Wells Village, the 2-mile gravel access road climbs 1000 ft. to the parking area. Permian-Pennsylvanian 22 Perdido Formation The Wildrose Charcoal Kilns were completed in 1877 by the Modock Consolidated Mining Company, above Death Valley in the Panamint Range, and were used to reduce pinyon and juniper tree wood to charcoal in a process of slow burning in low oxygen. The Lippincott Member (?) In the first stage, lasting from ca. In between many of the dunes are stands of creosote bush and some mesquite on the sand and on dried mud, which used to cover this part of the valley before the dunes intruded (mesquite was the dominant plant here before the sand dunes but creosote does much better in the sand dune conditions). Locally metamorphosed to subgreenschist to lower greenschist facies south of NTS in Funeral Mountains and Specter Range. Vertebrates, titanotheres, etc. Compiled from Wright et al. 2 Playa Salt Deposits Ammonites, smooth-shelled brachiopods, belemnites, and hexacorals. 7 Warm Spring Granite Cemen et al. These volcanics were deposited partly on the exhumed detachment surface from the earlier phase of Basin and Range extension. These events include exhumation of the detachment surfaces now exposed in the Black Mountains (Holm et al., 1992; Holm and Dokka, 1993) and, outside Death Valley, extension in the Cottonwood Mountains (Snow and Lux, 1999), the Inyo Range (Lee et al., 2009), and the Kingston PeakTecopa Basin area (Calzia and Rm, 2000). a. Unit is 457 m thick in the northwestern Spring Mountains, 500 m thick in the Striped Hills and 350 m thick at Bare Mountain, 420 m thick in the Montgomery Mountains. It should not be confused with an actual golf course in Furnace Creek, also in Death Valley. 3). The Wood Canyon also marks the base of the Paleozoic succession that, in the Death Valley region, commonly forms Basin and Range extensional allochthons like the Funeral Mountains and Nopah Range (McAllister, 1976; Burchfiel et al., 1983; Hamilton, 1988). Prior to this time, a thick sedimentary sequence was deposited in what is now the northern Black Mountains, with early sedimentation being mostly volcanics. Geosphere 2011;; 7 (1): 171182. Pressure and heat transformed the stone into the metamorphic rock we call marble. 7) is a platformal carbonate deposited unconformably across a Neoproterozoic rift basin that marks the onset of Proterozoic through Paleozoic miogeoclinal deposits of the western North American passive margin ( Wright et al., 1978 ). Syringopora (closely spaced colonies). First narrows of Fall Canyon If there's a moon,. Death Valley is a playground for geology enthusiasts, maybe even more like a Mecca. It also coincides with final opening of the northern Gulf of California and initiation of the southern portion of the San Andreas fault (Dorsey et al., 2007). 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). Abundant large gastropods in massive dolomite at top: Palliseria and Maclurites, associated with Receptaculites. Conglomerate, equivalent to the Funeral Formation? b. Holocene+Pleistocene= Fan gravel; silt and salt on floor of playa, less than 100 feet thick. Cross section across the Panamint Range and Black Mountains, profile C in previous location maps. Ordovician The Pahrump Group is found in the western Panamint Range and southern Black Mountains region, in a configuration that Wright et al. It was named after a line in the 1934 National Park Service guide book to Death Valley National Monument, which stated that "Only the devil could play golf" on its surface, due to a rough texture from the large halite salt crystal formations.[5]. 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. With an elevation several feet above the valley floor at Badwater, the Devil's Golf Course remains dry, allowing weathering processes to sculpt the salt there into complicated formations. Interpretations of tectonic settings in Figure 3 come from Snow and Lux (1999) for formations in the Cottonwood Mountains (Tub, Tpn, Tnv), from Knott et al. These age estimates are very uncertain, but do indicate that the bulk of the fill of Death Valley could be Pliocene and younger, i.e., postBasin and Range extension (Fig. Although the ECSZ today accommodates 25% of Pacific-North America relative motion, timing of initiation of this shear zone is poorly known. 26 Ely Springs Dolomite The last two columns in Figure 3 show tectonic events and interpreted tectonic regimes. The springs were probably named in 1871 by the Wheeler Survey after the resort town of Saratoga Springs, New York, and were an important water source for the twenty-mule teams of the 1880s. 4. Goniatite coquina beds, formed chiefly of the cephalopod Cravenoceras hesperiam, occur within this formation. Scolithus ? The wetland lies at the southern tip of the Ibex Hills, on the floor of Death Valley and just northeast of the Amargosa River. DPDarwin Plateau (Snyder and Hodges, 2000); WSPWillow Springs Pluton (Calzia nd Rm, 2000); SMGSmith Mountain Granite (Miller and Pavlis, 2005); MSGgranite of Miller Spring (Calzia and Rm, 2000); SWNVFSouthwest Nevada Volcanic Field (Sawyer et al., 1994); TC+RTTrail Canyon volcanics and Rhodes Tuff/Sheepshead andesite (McKenna and Hodges, 1990). Within Death Valley, the best region for slot canyons seems to be Tucki Mountain, south of Stovepipe Wells village.Here are found Grotto Canyon, Mosaic Canyon, Stretched Pebble Canyon and Little Bridge Canyon, all quite close to CA 190, though others to the south and east are much further away from the highway.These canyons typically have many short enclosed sections ending beneath a dryfall . In the Ash Meadow area crinoidal columns have been found. (2009) suggest that the later event at 2.8 Ma dates onset of strike-slip faulting along the Hunter Mountain fault zone and initiation of strike slip in this portion of the ECSZ. (2005). Cretaceous (67 Ma, 87 Ma) from. The Walker Lane belt and ECSZ therefore together form a single strike-slip zone, which will be referred to as the ECSZ in this paper. 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. Blakely et al. 29 Nopah Formation Mostly shale, some limestone, abundant spherical chert nodules. Wildrose Canyon has 2 campgrounds above the kilns, Thorndyke at 7,490 feet and Mahogany Flat at 7923 feet. periodically flows at the surface. A better interpretation is that the Hanaupah detachment does indeed correlate with the Tucki detachment and that this detachment tracks up the flank and over the top of the Panamint Range, just like the Tucki detachment tracks over the top of Tucki Mountain. At Mosaic Canyon, for instance, where the detachment surface is exposed (TD, Fig. 25 Hidden Valley Dolomite Thickness uncertain because of faulting; estimate 750 feet. The west side of the basin shows a steep segment bordering the main basin and a gently dipping surface that joins to the Panamint Range. Pleistocene-Pliocene (1990). (2002; Fig. The Death Valley region has played a key role in development of models of Basin and Range extension. Total thickness Uncertain because of faulting; estimated about 3,000 feet in Panamint Range, 2,000 feet in Funeral Mountains. Mosaic Canyon was named for a rock formation known as the Mosaic Breccia. Skolithos) and some interbedded bioturbated silstones. Geology of the Death Valley area, from Workman et al. Top 200 feet is well-bedded limestone and quartzite. contains the lowest dry point in North America. On the alluvial fan above the springs there are 2-3 thousand year old petroglyphs from the extinct Mesquite Spring culture. 2; Cemen et al., 1999). As groundwater exploded into steam due to the heat of magma underneath, an empty pit was left behind and the debris spread around the field. Neogene sediments preserved within Death Valley record the latest phases of structural evolution of the basin. The first event metamorphosed Death Valley's Precambrian basement rocks and occurred around 1,700 million years ago. Several lakes have occupied Death Valley since the close of the Pleistocene epoch 10,000 years ago, but these younger lakes were quite shallow compared to Lake Manly (See Badwater and Devils Golf Course above). Total Round Trip Distance: 260 miles. occur in this formation at Dolomite Canyon. Natural Bridge Canyon is found on the east side of the park and is one of the few canyons with an official trailhead. b. Thick-bedded, fine-grained, and even-grained dolomite, mostly light color. Middle (?) Death Valley National Park Self-Guided Audio Driving Tour. 4), several outcrops of Proterozoic gneissic basement were mapped by Hunt and Mabey (1966) as the footwall of the Amargosa Thrust. This Proterozoic gneiss is overlain by east-tilted Basin and Range fault blocks consisting of Wood Canyon Formation through Ordovician section, like other extensional allochthons in the region and also structurally similar to the east flank of Tucki Mountain (Fig. It is a showcase of geologic features as well as a beautiful example of one of Death Valley's many canyons. The strong link between Pacific-North America plate motion and structural evolution of the ECSZ is emphasized by this synchronous timing. These recent studies indicate that strike-slip faulting and extension occurred in separate phases. This dolomite has been correlated to the Noonday Dolomite (Hunt and Mabey, 1966; Williams et al., 1976), which is also found in the footwall of the Black Mountains detachment fault at Copper Canyon and Mormon Point (Williams et al., 1976), although Miller and Pavlis (2005) question details of this correlation. The second event began while layered younger Precambrian sediments were being deposited on top of the beveled surface of older metamorphic basement rocks. Thickness 300-1,400 feet. a. Interbedded fluvial and marine sequences fine-grained, cross-stratified, locally conglomeratic sandstone, intervals of siltstone and carbonate rocks in the Funeral Mnts. When to Hike the Golden Canyon. The northern nose of the Panamints is formed by an extensional core complex, Tucki Mountain (Hodges et al., 1987; Wernicke et al., 1988b). South of Mormon Point, another important data point for structural evolution is in the Confidence Hills (CH, Fig. Miocene Fossils include brachiopods, colonial and solitary corals, gastropods, pelmatozoan ossicles, and stromatoporoids. The suggestion illustrated here is that the Black Mountains, with their present-day asymmetric structure typical of footwall uplift geometry, formed as a result of footwall uplift associated with the Death Valley pull-apart graben. Further implications of this update will be discussed elsewhere. Basement geometry below Death Valley shows a steep-sided basin nearly 5000 m deep. Unit is from 6 to 150 m thick. a. Natural Bridge Canyon: On the east side of the park . (1994) provide an interpretation of eruption volume versus time, which the sawtooth pattern in Figure 3 schematically follows. Typically located at the end-depositional sites in basin interiors. 3 Lake Manly Deposits For the SWNVF, Sawyer et al. b. Cemented gravel; playa deposits, much volcanic debris, perhaps 5,000 feet thick. Titus Canyon is a narrow gorge in the Grapevine Mountains near the eastern boundary of Death Valley National Park. 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. 2) and geology from the digital map of Workman et al. (2002), in this case supplemented from the map of Hunt and Mabey (1966). Using this very rough estimate of 1.81 Ma (base of Quaternary) for a third of the section and assuming a constant sedimentation rate, the base of the section would be at 5.4 Ma. *3 Members* upper member (Papoose Lake Member) is a fossiliferous shale containing trilobites of Glossopleura middle member (Informal Middle Member)contains trilobite "hash beds" with fragments of Ehmaniella and with linguloid brachiopod beds within a shale layer lower member (Banded Mountain Member) contains no fossils. *3 Members* a large, cliff-forming carbonate unit with three members (Dunderberg/Halfpint Members, Smokey Member) basal shale and silty limestone beds of this formation are persistently fossiliferous characterized by trilobites, conodonts, and the brachiopod Linnarssonella - Dunderberg/ Halfpint Members are divided into seven facies and contain sponge Hintzespongia, spicule-like elements of Chancelloria, eocrinoid fragments, lingulid and acrotretid brachiopods, trilobites, and single-element species of paraconodonts and protocondonts - Smokey Membercharacterized by the black and buff colored banded dolomite also contains stromatolites and thrombolites within packstones and grain stones, a dark dolomite above the middle of the Nopah Formation contains small-silicified Trempleauan gastropods, a singular mollusk Matthevia, and trilobites.
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