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The Gran Desierto de Altar is one of the major portions of the Sonoran Desert of Mexico, including the only active erg dune region in North America. It extends across much of the northern border of the Gulf of California, reaching more than 100 kilometers east to west, and over 50 km north to south, and constitutes the largest continuous wilderness area within the Sonoran Desert. The eastern portion of the area is a biosphere reserve (the full title is Reserva de la Biosfera el Pinacate y Gran Desierto de Altar)

The Gran Desierto covers approximately 5,700 km2 , most of it in the Mexican state of Sonora. The northernmost edges overlap the border into southwestern Arizona. The dominant sand sheets and dunes range in thickness from less than one meter to greater than 120 meters. The total volume of sand in the Gran Desierto is about 60 km3. Most of that volume was delivered by the Pleistocene Colorado River which flowed through the present-day Gran Desierto area ~120,000 years before present. This Pleistocene delta migrated westward concomitant with strike-slip faulting and rifting associated with the opening of the Salton Trough and the Gulf of California.

Physiography: The eastern margin of the Gran Desierto abuts the Cenozoic volcanic complex of the Sierra Pinacate, a composite volcanic field covering more than 1,800 km2 with a summit elevation of 1,206 m. Aeolian sands have climbed onto many of the western slopes of the Sierras Pinacate, defining the eastern limit of the dune field. To the north, the sands thin out against the distal margins of alluvial fans from the Tinajas Altas and Tule Mountains along the Arizona-Sonora border. The southern border of the sand sea is the northern shore of the Gulf of California. The southernmost extension of the San Andreas Fault cuts across the area and lies beneath several prominent granite inselbergs, most notably the Sierra del Rosario mountains which are surrounded by the erg on all sides. The Sierra Enternada is a smaller inselberg almost completely buried by the sand near the boundary of the Gran Desierto and the Pinacate volcanic complex.

Sand Dune Distribution: The Gran Desierto is best-known for its magnificent Star Dunes, many in excess of 100 meters high. More than two-thirds of the Gran Desierto is covered by sand sheets and sand streaks. The remaining area is split equally between a western population of star dunes and an eastern set of transverse or crescentic dunes. Some of the larger crescentic dunes in the northeastern sand sea exhibit reversing crests, a transitional morphologic feature associated with star dunes. Flora: Vegetation assemblages of the Gran Desierto are typical of the lower Sonoran desert with a marked difference in vegetation type and density with location. Large areas of the southern and eastern sand sea, especially near the margins, have a moderately dense (up to 20%) cover of perennial low shrubs and herbs such as bursage (Ambrosia dumosa) and mormon tea (Ephedra trifurca) with creosote bush (Larrea tridentata) in areas of thin sand cover. Palo Verde/Acacia/Ocotillo communities occur on alluvial slopes on the northern side of the sand sea, particularly in arroyos and washes. Felger [1980] estimated total vegetation cover at 15% in the star dunes and about 10% in the low transverse or crescentic dunes areas. These percentages are substantially greater than in most active dune fields where vegetation covers of 15% are more typical [Seely and Louw, 1980]. Several teams (e.g. Van Devender et al. [1987] and Hall et al. [1988]) have examined the nests (middens) built by common wood rats as a proxy for ancient vegetation regimes. All have concluded that the Gran Desierto has been a refugia for desert plants since at least the late Pleistocene. The Gran Desierto has served as a refuge for most dominant Mojave Desert plant species during cooler pluvial epochs as well. Van Devender has also reported C14 dates for a midden from the Tinajas Altas Mountains showing assemblages of Juniper and Joshua trees coexisting with contemporary Gran Desierto flora and fauna more than 43,000 years before present. Although midden studies do not provide information beyond the late-Pleistocene, they do indicate that, in gross form, the climate of the Gran Desierto as recorded by plant communities has been desert-like since at least the peak of the Wisconsin ice age.

Climate: The Gran Desierto has a warm-to-hot arid climate. Mean annual rainfall, most of which occurs between September and December, is 73 mm at Puerto Penasco, Sonora (located on the southeastern margin of the sand sea) and decreases northward toward Yuma, Arizona (on the northwestern edge) to 62 mm per year [Lancaster et al., 1987]. Mid-summer highs in excess of 45°C are common in the central sand sea. Mid-winter lows of less than 10°C are rare. Winds are controlled in part by the position and strength of the Sonoran Low in summer, creating southerly winds, and by the Great Basin High in winter, with north-to-northeasterly winds.

Paleoclimate: Van Devender and Spaulding [1979] and Spaulding et al. [1983] report that the well-documented pluvial epochs which occurred over much of the southwestern United States during the most-recent (Wisconsin) ice age may not have extended as far south as the Gran Desierto. It appears that the climatic regime of the past 150,000 years at this site has been one of gradually increasing aridity with current hyperarid conditions being firmly in place by at least 43,000 years ago. As a minimum, it may be assumed that onshore coastal winds from the south were less important to sand movement when the Wisconsin shoreline was located 45 km seaward of its current position.

Tectonics: The Gran Desierto is located adjacent to a rapidly subsiding basin, the Salton Trough, which is a northern extension of the Gulf of California, an embayment created by rifting initiated during the Pliocene along the East Pacific Rise and the San Andreas fault system [Rusnak and Fisher, 1964; Larson et al., 1968; Angelier et al., 1981]. Regional subsidence has propagated to the northwest as rifting and strike-slip faulting continues into the present-day. The central portion of the nearby Salton Trough is more than 70 m below sea level; it is protected from marine embayment only by the natural dike of the Colorado River delta. Ongoing tectonic activity modifies the Gran Desierto today. The southernmost extension of the San Andreas fault system, the Cerro Prieto fault, passes directly through the area before continuing offshore into the Gulf of California [Merriam, 1965]. Strike-slip movement in the area is as high as 60 mm/yr. [Gastil et al., 1975; Curray and Moore, 1984]. Since 1900, one magnitude 6.3 and two magnitude 7.1 earthquakes have originated within the erg. Most seismicity within the Gran Desierto originates at depths of five to six kilometers, corresponding to the transition between deltaic deposits and basement crystalline rocks (Von der Haar and Howard, 1981 ]. Local uplift is still occurring along the Mesa Arenosa, a drag folded fault block forming the coastal boundary.

Origin: The history of the Gran Desierto is intimately linked to the opening of the Gulf of California and the capture of the ancestral Colorado River; source areas which were adjacent to the Gran Desierto have shifted in position, basement topography has been altered continuously, bedforms have been created, modified or completely destroyed and then reworked. The Gran Desierto sand sheets and dunes are located atop deltaic deposits of the Pleistocene Colorado River. Lucchitta [1988] showed that the lower Colorado River was captured by the Gulf of California 1.2 million years before present. This event places an upper bound on the age of the Gran Desierto with the Colorado's major clastic sediment sources. Conglomeritic sands and silts beneath the Mesa Arenosa were examined by Colletta and Ortlieb [1984] and dated at between 700,000 and 120,000 years before present. Vertebrate fossils found by Merriam [1965] within the deltaic deposits include Equis, Gomphoterium and Bison. and were assigned to Irvingtonian age (0.5 to 1.8 million years before present); dates consistent with the aforementioned capture of the lower Colorado River. Shaw and McDonald [1987] documented evidence of a Giant Anteater Myrmecophaga tridactyla in the deltaic deposits in the southern Gran Desierto. Van Devender notes that the specimen was found in association with fossils of mammoths, sloths and boa constrictors; a tropical faunal assemblage which supports a contention that the Colorado River delta of a previous interglacial period (>120,000 years ago) was much warmer and wetter than the present interglacial. Paleo-deltaic deposits near Salina Grande correlate with a ubiquitous indurated shell deposit dated by Io/U radiometric methods at 146,000 + 13,000/-11, 000 years of age [Colletta and Ortlieb, 1984]. Slate [1985] obtained K-Ar ages for basalt flows in the western Pinacates. Based on this work, some aeolian activity may have been present as early as 700,000 years ago, as evidenced by the dated accretionary mantles on basalt flows of the Pinacate volcanic field. Blount and Lancaster [1990] proposed that by late Pleistocene time, the Colorado River was a highly competent stream flowing through the area which is occupied today by the massive western star dune zone. The seashore at this time was at least 45 km south of its present-day location. Primary bed loads of poorly sorted gravel were deposited from present-day Yuma, Arizona to an area south of the present-day Sierra del Rosario mountains. As rifting of the Gulf of California progressed to the northwest, and uplift along the coast began, the river channel shifted westward, leaving primary bedload deposits in the former channel and floodplain. Deltaic sediments beneath the Gran Desierto may be as much as 6,000 meters deep (Biehler et al. [1964]; Colleta and Ortlieb [1984].) Annual sediment loads prior to the damming of the Colorado River were prodigious. Sykes [1937b] reported a single flood event which deposited an estimated 100,000,000 m3 of coarse to medium sand as a sheet deposit on the modern delta just south of the international boundary. Events like this, even if rare, could fill up the Gran Desierto in only a few millennia.

Offshore Features The synchronous development of the Colorado delta and the associated Gran Desierto sand sink continues offshore into the Gulf of California. Reports on the submarine topography of the Gulf of California by van Andel [1964], describe three former river channels on the seafloor: one originating at the present-day Colorado delta, another from the area of the paleo-delta between El Golfo and Salina Grande, and a third to the area of present-day Puerto Penasco. Rusnak et al. [1964] reported on sonar soundings which discovered the valleys and also describe two elongate depressions, each about 40 km in length, into which the valley networks terminate at a depth of ~180 m below sea level. Those incised valley systems were also interpreted as fluvial in origin.

Public Media

Some scenes for the 2007 movie Into the Wild were filmed in the Gran Desierto. Bill Hartman’s book Desert Heart is an extensive naturalist’s view of the area. Louis L’Amour set his intricately-researched pulp novel Kid Rodelo in the sand sea, but the 1966 movie by the same name was not filmed in the area.


References

Angelier, J., Colleta, B., Chorowicz, J., Ortlieb, L. and Rangin, C., Fault tectonics of the Baja California peninsula and the opening of the Sea of Cortez, Mexico, J. of Structural Geology, 3, 347- 357, 1981. Biehler, S., Kovach, R.L. and Allen, C.R., Geophysical framework of the northern end of the Gulf of California structural province, in Marine Geology of the Gulf of California, van Andel, T .H. and Shor, G.G., eds., A.A.P.G., Memoir 3, 126-143, 1964. Blount, Grady and Nicholas Lancaster, Development of the Gran Desierto sand sea, northwestern Mexico, Geology, v. 18, pp. 724–728, 1990. Colleta, B. and Ortlieb, L., Deformations of middle and late Pleistocene deltaic deposits at the mouth of the Rio Colorado, northwestern Gulf of California, in Malpica-Cruz, V. et al.(eds.), Neotectonics and sea level variations in the Gulf of California area: A symposium, University Nacional Auton Mexico, Institute Geolocia, 31-53, 1984. Curray, J.R. and Moore, D.G., Geologic history of the mouth of the Gulf of California, in, Crouch, J.K. and Bachman, S.B., eds., Tectonics and Sedimentation along the California Margin, Pacific Section-S.E.P.M., 17-36, 1984. Felger, R.S., Vegetation and flora of the Gran Desierto, Sonora, Mexico, Desert Plants, 2, 87-114, 1980. Gastil, R.G., Phillips, R.P. and Allison, E.C., Reconnaissance geology of the state of Baja California, G.S.A. Mem. 140, 170 p., 1975. Guzman, A.E., Petroleum possibilities in Altar Desert, Sonora, Mexico, abs., A.A.P .G., 64, 716, 1980. Hall, W.E., Van Devender, T.R. and Olson, C.A., Late Quaternary arthropod remains from Sonoran desert packrat middens, southwestern Arizona and northwestern Sonora, Quaternary Research, in press, 1988. Lancaster, N., Greeley, R. and Christensen, P.R., Dunes of the Gran Desierto sand sea, Sonora, Mexico, Earth Surface Processes and Landforms, 12, 277 -288, 1987. Larson, R.L., Menard, H.W. and Smith, S., Gulf of California: A result of ocean floor spreading and transform faulting, Science, 161 , 881-884, 1968. Lucchitta, I., Late Cenozoic uplift of the southwestern Colorado Plateau and adjacent lower Colorado River region, Tectonophysics, 61, 63-95, 1979. Lucchitta, I., History of the Grand Canyon and of the Colorado River in Arizona, Az. Geol. Soc., in press, 15 p., 1988. MacDougal, D.T., Across Papagueria, Bull. American Geographical Soc., 40, 705-725, 1908. Merriam, R., San Jacinto fault in northwestern Sonora, Mexico, Bull. G.S.A., 76, 1965. Ruznak, G.A. and Fisher, R.L., Structural history and evolution of the Gulf of California, in Marine Geology of the Gulf of California, van Andel, T.H. and Shor, G.G., eds., A.A.P .G., Memoir 3, 144-156, 1964. Shaw, C.A. and McDonald, H.G., First record of Giant Anteater (Xenarthra, Myrmecophagidae) in North America, Science, 236, 186-188, 1987. Slate, J.L., Soil-Carbonate genesis in the Pinacate volcanic field, northwestern Sonora, Mexico, M.S. thesis, University of Arizona, Tucson, 85 p., 1985. Spaulding, W.G., Leopold, E.B. and Van Devender, T.R., Late Wisconsin paleoecology of the American Southwest, in, Wright, H.E., Jr., ed., Late Quaternary Environments of the United States, v. 1, Univ. of Minnesota Press, 259-293, 1983. Sykes, G., The Colorado Delta, Carnegie Institution/American Geographical Society, New York, 193 p., 1937a. Sykes, G., Delta, estuary, and lower portion of the channel of the Colorado River, 1933 to 1935, Carnegie Institution, New York, 76 p., 1937b. van Andel, T.H., Recent marine sediments of Gulf of California, in Marine Geology of the Gulf of California, van Andel, T.H. and Shor, G.G., eds., A.A.P .G., Memoir 3, 216-310, 1964. Van Devender, T.R. and Spaulding, W.G., Development of vegetation and climate in the southwestern United States, Science, 204, 701-710, 1979. Van Devender, T.R., Thompson, R.S. and Betancourt, J.L., Vegetation history of the deserts of southwestern North America; The nature and time of the late Wisconsin-Holocene transition, in Ruddiman, W.F. and Wright, H.E., Jr., eds., North America and adjacent oceans during the last deglaciation: Boulder, Colorado, The geology of North America, K-3, G.S.A., 323-351, 1987. Von der Haar, S. and Howard, J.H., Intersecting faults and sandstone stratigraphy at the Cerro Prieto geothermal field, Geothermics, 10, 145-167, 1981.

See also

Coordinates: 31°57′N 114°08′W / 31.95°N 114.14°W / 31.95; -114.14


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