Temperatures of the Soil and Air in a Desert

Sinclair, John G.

doi:10.1175/1520-0493(1922)50<142b:totsaa>2.0.co;2

Cited by 26 publications

(13 citation statements)

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“…Temperatures at the lowest recorded depth (20 em) still fluctuated 6°C during a 24-hour period. Earlier studies reported that a depth of 45 em must be reached before temperature fluctuations become negligible (Sinclair 1922;Guild 1950). A similar temperature gradient occurred above the desert surface, although during hotter portions of the day a very small increase in height above the surface ( 1 em) resulted in a greater decrease in temperature than observed for an equivalent depth below the surface.…”

Section: Resultsmentioning

confidence: 66%

“…Exploitation of such habitats is particularly critical for many desert organisms that require this temporary escape from climatic extremes which otherwise would be lethal. Sinclair ( 1922), Buxton ( 1924), Guild ( 1950), and Williams ( 1954) have reported on the severity of the desert climate on or near the ground, and general discussions of arid-zone microclimate and arthropod fauna are contained in two UNESCO symposia ( 1958,1962). A comprehensive review of microclimate and arthropod distribution by Cloudsley-Thompson (1962) includes several references to studies concerning desert species as well as investigations applicable to desert regions (Parry 1951, Edney 1953.…”

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confidence: 99%

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Micrometeorology and Energy Exchange in Two Desert Arthropods

Hadley

1970

Ecology

100

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Incoming solar, net, and reflected radiation, wind velocity, relative humidity, and temperatures at various levels above and below an open desert surface were recorded simultaneously at 30—minute intervals for a 3—day period. Concurrent measurements were also made of arthropod burrow temperatures and relative humidities, scorpion body temperatures, and body and subelytral temperatures of tenebrionid beetles. The burrowing habit enabled arthropods to escape the hot, desiccating conditions recorded on the desert surface during the day. Temperatures and humidities to which scorpions were subjected while in their subterranean retreats depended upon the burrow's depth and subsequent movements in the burrow. Vertical movements between the surface and maximum burrow depths during a 24—hour period provided arthropods with a wide choice of micro— environments. Tenebrionid beetles on the surface were able to achieve a temperature equilibrium only under low temperature and radiation loads. Subelytral cavity temperatures in black Eleodes armata were generally 2—7°C warmer than body temperatures after exposure to direct sunlight. Temperature differences between subelytral cavities of black beetles and beetles with their elytra painted white were small, but suggested that a white dorsal surface was, at least, paritally effective in reducing absorption of solar radiation. The subelytral cavity, in addition to reducing transpiratory water loss, apparently provides a mechanism for increasing convective cooling, and may serve as a temperature “buffer zone” against heat conduction resulting from high intensity solar radiation. A heat exchange budget was estimated for E. armata on the desrt surface. Major contributing factors were heat gained from incoming radiation versus heat lost from convection and reradiation. Contributions from evaporation and metabolism, as determined by laboratory experiments, were very small in comparison, while the role of conduction in energy exchange was assumed to be negligible. Inherent problems in the estimation of contributing factors to net energy exchange, and comparison of similar budgets for mesic arthropods are discussed.

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Section: Resultsmentioning

confidence: 66%

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confidence: 99%

Micrometeorology and Energy Exchange in Two Desert Arthropods

Hadley

1970

Ecology

100

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“…Field studies also corroborate these results. In an analysis of the temperature conditions of air and soil conducted in the desert near Tucson, Arizona, a maximum soil temperature of 71.5°C (160.7°F) was measured 0.4 cm below the soil surface at 1:00PM on June 21, 1915 [ Sinclair , 1922]. The corresponding air temperature measured 4 ft above the ground was 42.5°C (108.5°F) [ Sinclair , 1922].…”

Section: Resultsmentioning

confidence: 99%

“…In an analysis of the temperature conditions of air and soil conducted in the desert near Tucson, Arizona, a maximum soil temperature of 71.5°C (160.7°F) was measured 0.4 cm below the soil surface at 1:00PM on June 21, 1915 [ Sinclair , 1922]. The corresponding air temperature measured 4 ft above the ground was 42.5°C (108.5°F) [ Sinclair , 1922]. Other studies that have observed extreme maximum surface temperatures and air temperatures near the time of the observed surface temperature have found differences of even greater magnitude [ Peel , 1974].…”

Section: Resultsmentioning

confidence: 99%

A global comparison between station air temperatures and MODIS land surface temperatures reveals the cooling role of forests

Mildrexler¹,

Zhao²,

Running³

2011

J. Geophys. Res.

251

199

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[1] Most global temperature analyses are based on station air temperatures. This study presents a global analysis of the relationship between remotely sensed annual maximum LST (LST max ) from the Aqua/Moderate Resolution Imaging Spectroradiometer (MODIS) sensor and the corresponding site-based maximum air temperature (T amax ) for every World Meteorological Organization station on Earth. The relationship is analyzed for different land cover types. We observed a strong positive correlation between LST max and T amax . As temperature increases, LST max increases faster than T amax and captures additional information on the concentration of thermal energy at the Earth's surface, and biophysical controls on surface temperature, such as surface roughness and transpirational cooling. For hot conditions and in nonforested cover types, LST is more closely coupled to the radiative and thermodynamic characteristics of the Earth than the air temperature (T air ). Barren areas, shrublands, grasslands, savannas, and croplands have LST max values between 10°C and 20°C hotter than the corresponding T amax at higher temperatures. Forest cover types are the exception with a near 1:1 relationship between LST max and T amax across the temperature range and 38°C as the approximate upper limit of LST max with the exception of subtropical deciduous forest types where LST max occurs after canopy senescence. The study shows a complex interaction between land cover and surface energy balances. This global, semiautomated annual analysis could provide a new, unique, monitoring metric for integrating land cover change and energy balance changes.

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“…The instru- ment, however, is unsuitable for measurements at places where the temperature gradient is very strong. Measurements under desert conditions were taken by SINCLAIR (1922) and by HAUDE (1934). They show a very rapid fall of the air temperature in the first few milimeters above the surface.…”

Section: Air Temperatures In Cases If Strong Insolationmentioning

confidence: 99%

Heaths and Inland Dunes of the Veluwe

Stoutjesdijk¹

1959

Wentia

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Temperatures of the Soil and Air in a Desert

Cited by 26 publications

References 0 publications

Micrometeorology and Energy Exchange in Two Desert Arthropods

Micrometeorology and Energy Exchange in Two Desert Arthropods

A global comparison between station air temperatures and MODIS land surface temperatures reveals the cooling role of forests

Heaths and Inland Dunes of the Veluwe

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