The effects of early season soil temperatures on emergence of summer crops on the north-western plains of NSW

1971 ◽  
Vol 11 (48) ◽  
pp. 39 ◽  
Author(s):  
TE Launders
Keyword(s):  
Soil Temperature ◽  
Pearl Millet ◽  
Early Season ◽  
Related Data ◽  
The North ◽  
Temperature Requirement ◽  
Soil Temperatures ◽  
Emergence Percentage ◽  
Rate Of Emergence ◽  
Lower Temperature

The influence of early season soil temperatures on the extent and rate of emergence of five summer crops was examined using four sowings at weekly intervals between late September and late October. The crops were maize, grain sorghum, pearl millet, and two forage sorghums. Increasing soil temperature reduced the interval between sowing and first emergence, and gave variable results for the interval between first and final emergence. Percentage emergence of maize was high at all sowings, whereas that of all three sorghums was low at sowings with soil temperatures at 4 inches of below 65�F, but did not differ significantly between sowings at temperatures above 65�F. Emergence of pearl millet improved with each later sowing, but differences were not significant. Rate of emergence was accelerated by rising soil temperatures in the four days after first emergence, but subsequent effects after four days were generally minimal. Maize appeared to have a lower temperature requirement for emergence than grain and forage sorghums, which, in turn, showed a lower temperature requirement than pearl millet. From the results and other related data, it seems that maize can be sown with reasonable safety when four inch depth soil temperatures are 59� to 64�F (expected in late September), sorghums (both grain and forage) when this temperature is 65� to 69�F (expected in early- to mid-October), and pearl millet when it is 68� to 72�F (expected in early- to mid-November). The results support the concept of soil temperature being the best criterion to determine a safe time for early season sowing of summer crops.

EFFECT OF SOIL TEMPERATURE ON SEEDLING EMERGENCE

1962 ◽  
Vol 42 (3) ◽  
pp. 481-487 ◽  
Author(s):  
S. Dubetz ◽  
G. C. Russell ◽  
D. T. Anderson
Keyword(s):  
Soil Temperature ◽  
Seedling Emergence ◽  
Herbaceous Species ◽  
Sweet Clover ◽  
Sugar Beets ◽  
Red Fescue ◽  
Wild Oats ◽  
Soil Temperatures ◽  
Rate Of Emergence ◽  
Rough Fescue

Rate and percentage of emergence of 19 native and cultivated herbaceous species were studied at the following soil temperature: 6°, 13°, 18°, and 24 °C. The soil temperatures were held uniformly constant, and emergence data at the end of 5 weeks from four replications in time were obtained. The rate of emergence of all species was greater at 18 °C. than at 6 °C., and of all but five species was greater at 24 °C. than at 18 °C.The percentage of emergence of barley, bromegrass, crested wheatgrass, mustard, oats, peas, spring wheat, and wild oats was not significantly affected by soil temperature. Beans, corn, sugar beets, and sunflowers showed significantly lower emergence percentages at 6 °C. than at the three higher soil temperatures. Alfalfa, creeping red fescue, winter wheat, orchardgrass, rough fescue, sweet clover, and flax emerged best at moderate soil temperatures.

SUMMER TEMPERATURES OF CRYOSOLIC SOILS IN THE NORTH-CENTRAL KEEWATIN, N.W.T.

1980 ◽  
Vol 60 (2) ◽  
pp. 311-327 ◽  
Author(s):  
CHARLES TARNOCAI
Keyword(s):  
Soil Temperature ◽  
Slope Position ◽  
North Central ◽  
Soil Material ◽  
The North ◽  
Soil Temperatures ◽  
Summer Temperatures ◽  
The Mean

Soil temperatures were measured at six depths within 1 m of the surface on 10 Cryosolic soils in the north-central Keewatin area during the summer of 1976. The mean soil temperatures during the study period varied between 1.7 °C and 8.2 °C at a depth of 20 cm and −0.2 °C and 6.0 °C at a depth of 50 cm. The maximum and minimum soil temperatures at a depth of 20 cm ranged from 4.4 °C to 13.9 °C and from −0.6°C to 3.9 °C, respectively, while those at a depth of 50 cm ranged from −0.2 °C to 6.7 °C and from −1.1 °C to 2.2 °C, respectively. During the study period a freeze-back of 30 cm or more occurred from the permafrost on several sites. Soil temperatures were markedly higher where the soil material and vegetation were disturbed. The effects of drainage, soil materials, aspect, slope position, vegetation and peat cover on the soil temperature are discussed.

RELIEF AND MICROCLIMATE AS RELATED TO SOIL PROPERTIES

1978 ◽  
Vol 58 (3) ◽  
pp. 421-438 ◽  
Author(s):  
T. M. MACYK ◽  
J. D. LINDSAY ◽  
S. PAWLUK
Keyword(s):  
Redox Potential ◽  
Soil Temperature ◽  
Soil Properties ◽  
Exchange Capacity ◽  
Moisture Regime ◽  
X Ray Diffraction ◽  
The South ◽  
The North ◽  
Soil Moisture Regime ◽  
Soil Temperatures

This study was undertaken to determine the influence of relief and microclimate on soil properties. Seven sites were chosen at different positions on the north- and south-facing slopes of a moderately rolling till knob. Physical, chemical and mineralogical analyses were conducted to characterize the soils at each of the sites. The vegetation of the area was described and soil temperatures and moisture were monitored at four depths. Redox potential and pH were measured to detect seasonal variations. Data for oxalate and dithionite-extractable iron and aluminum, cation exchange capacity, and X-ray diffraction showed only minor differences among the seven pedons along the slope faces. Soil temperature was higher on the south-facing slope than on the north-facing slope and air temperature was usually higher than soil temperature at the 10-cm depth. Soil moisture regime varied with position in the landscape. The soil on the north-facing slope was generally more moist than the soil on the south-facing slope. Redox potential varied seasonally and appeared to be related to the moisture content of the soil.

scholarly journals Validation of Noah-Simulated Soil Temperature in the North American Land Data Assimilation System Phase 2

2013 ◽  
Vol 52 (2) ◽  
pp. 455-471 ◽  
Author(s):  
Youlong Xia ◽  
Michael Ek ◽  
Justin Sheffield ◽  
Ben Livneh ◽  
Maoyi Huang ◽  
...  
Keyword(s):  
Soil Temperature ◽  
Time Scales ◽  
Land Surface ◽  
Phase 2 ◽  
Soil Layers ◽  
The North ◽  
Weather And Climate ◽  
Soil Temperatures ◽  
Land Data Assimilation

AbstractSoil temperature can exhibit considerable memory from weather and climate signals and is among the most important initial conditions in numerical weather and climate models. Consequently, a more accurate long-term land surface soil temperature dataset is needed to improve weather and climate simulation and prediction, and is also important for the simulation of agricultural crop yield and ecological processes. The North American Land Data Assimilation phase 2 (NLDAS-2) has generated 31 years (1979–2009) of simulated hourly soil temperature data with a spatial resolution of ⅛°. This dataset has not been comprehensively evaluated to date. Thus, the purpose of this paper is to assess Noah-simulated soil temperature for different soil depths and time scales. The authors used long-term (1979–2001) observed monthly mean soil temperatures from 137 cooperative stations over the United States to evaluate simulated soil temperature for three soil layers (0–10, 10–40, and 40–100 cm) for annual and monthly time scales. Short-term (1997–99) observed soil temperatures from 72 Oklahoma Mesonet stations were used to validate simulated soil temperatures for three soil layers and for daily and hourly time scales. The results showed that the Noah land surface model generally matches observed soil temperature well for different soil layers and time scales. At greater depths, the simulation skill (anomaly correlation) decreased for all time scales. The monthly mean diurnal cycle difference between simulated and observed soil temperature revealed large midnight biases in the cold season that are due to small downward longwave radiation and issues related to model parameters.

scholarly journals Seasonal Changes in Soil and Air Temperature at Three Locations in Puerto Rico, 1963-67

1969 ◽  
Vol 56 (3) ◽  
pp. 307-317 ◽  
Author(s):  
M. A. Lugo-López ◽  
Modesto Capiel
Keyword(s):  
Soil Moisture ◽  
Soil Temperature ◽  
Air Temperature ◽  
Soil Cover ◽  
Bare Soil ◽  
Soil Conditions ◽  
Adequate Explanation ◽  
The North ◽  
Air Temperatures ◽  
Soil Temperatures

Soil temperature data at Río Piedras in the north, Lajas in the southwest, and Fortuna in the south, are given in this paper for the 5-year period 1963- 67. Seasonal variations in soil and air temperatures follow distinct patterns somewhat, depending on the nature of the soil cover and rainfall. Mean maximum and minimum temperatures at the 2-inch depth, respectively, are: Río Piedras, 96.2° F. and 79.6° F.; Lajas, 102.1° F. and 69.0° F.; and Fortuna, 93.2° F. and 79.1° F. The corresponding soil temperatures at the 8-inch depth, respectively, are: Río Piedras, 80.5° F. and 77.4° F.; Lajas, 83.4° F. and 77.8° F.; and Fortuna, 85.7° F. and 82.7° F. The differences and trends of soil temperature at 2-inch and 8-inch depths can find adequate explanation when soil moisture and soil cover are considered. However, the differences between maximum and minimum soil temperatures at 8 inches of depth are roughly one fifth of the corresponding ones at the 2-inch depth. The maximum and minimum air temperature at Lajas, Fortuna and Río Piedras are much more similar to each other than the corresponding soil temperature, especially at the 2-inch depth. This is mainly because air temperature is rather measured on a macro and integrating scale while soil temperature measurements exhibit localized effects of soil cover and soil moisture. It was found that highly significant 2-inch soil-air temperature relationships are evident under bare soil conditions. The same relationships were not significant under sod cover at Fortuna.

scholarly journals Simulation of Daily Mean Soil Temperatures for Agricultural Land Use Considering Limited Input Data

Atmosphere ◽  
2021 ◽  
Vol 12 (4) ◽  
pp. 441
Author(s):  
Philipp Grabenweger ◽  
Branislava Lalic ◽  
Miroslav Trnka ◽  
Jan Balek ◽  
Erwin Murer ◽  
...  
Keyword(s):  
Soil Temperature ◽  
Input Data ◽  
Agricultural Land ◽  
Soil Column ◽  
Soil Conditions ◽  
Snow Layer ◽  
Time Step ◽  
Soil Temperatures ◽  
Dimensional Simulation ◽  
Limited Input Data

A one-dimensional simulation model that simulates daily mean soil temperature on a daily time-step basis, named AGRISOTES (AGRIcultural SOil TEmperature Simulation), is described. It considers ground coverage by biomass or a snow layer and accounts for the freeze/thaw effect of soil water. The model is designed for use on agricultural land with limited (and mostly easily available) input data, for estimating soil temperature spatial patterns, for single sites (as a stand-alone version), or in context with agrometeorological and agronomic models. The calibration and validation of the model are carried out on measured soil temperatures in experimental fields and other measurement sites with various climates, agricultural land uses and soil conditions in Europe. The model validation shows good results, but they are determined strongly by the quality and representativeness of the measured or estimated input parameters to which the model is most sensitive, particularly soil cover dynamics (biomass and snow cover), soil pore volume, soil texture and water content over the soil column.

scholarly journals A simple model for predicting soil temperature in snow-covered and seasonally frozen soil: model description and testing

2004 ◽  
Vol 8 (4) ◽  
pp. 706-716 ◽  
Author(s):  
K. Rankinen ◽  
T. Karvonen ◽  
D. Butterfield
Keyword(s):  
Heat Capacity ◽  
Simple Model ◽  
Soil Temperature ◽  
Specific Heat ◽  
Specific Heat Capacity ◽  
Frozen Soil ◽  
Model Description ◽  
Freezing And Thawing ◽  
Catchment Scale ◽  
Soil Temperatures

Abstract. Microbial processes in soil are moisture, nutrient and temperature dependent and, consequently, accurate calculation of soil temperature is important for modelling nitrogen processes. Microbial activity in soil occurs even at sub-zero temperatures so that, in northern latitudes, a method to calculate soil temperature under snow cover and in frozen soils is required. This paper describes a new and simple model to calculate daily values for soil temperature at various depths in both frozen and unfrozen soils. The model requires four parameters: average soil thermal conductivity, specific heat capacity of soil, specific heat capacity due to freezing and thawing and an empirical snow parameter. Precipitation, air temperature and snow depth (measured or calculated) are needed as input variables. The proposed model was applied to five sites in different parts of Finland representing different climates and soil types. Observed soil temperatures at depths of 20 and 50 cm (September 1981–August 1990) were used for model calibration. The calibrated model was then tested using observed soil temperatures from September 1990 to August 2001. R2-values of the calibration period varied between 0.87 and 0.96 at a depth of 20 cm and between 0.78 and 0.97 at 50 cm. R2-values of the testing period were between 0.87 and 0.94 at a depth of 20cm, and between 0.80 and 0.98 at 50cm. Thus, despite the simplifications made, the model was able to simulate soil temperature at these study sites. This simple model simulates soil temperature well in the uppermost soil layers where most of the nitrogen processes occur. The small number of parameters required means that the model is suitable for addition to catchment scale models. Keywords: soil temperature, snow model

scholarly journals Quality control of 10-min soil temperatures data at RMI

2015 ◽  
Vol 12 (1) ◽  
pp. 23-30 ◽  
Author(s):  
C. Bertrand ◽  
L. González Sotelino ◽  
M. Journée
Keyword(s):  
Quality Control ◽  
Soil Temperature ◽  
Bare Soil ◽  
Climate Conditions ◽  
Air Temperatures ◽  
Temperature Observation ◽  
Soil Temperatures ◽  
Different Depths ◽  
Temperature Records ◽  
Energy Processes

Abstract. Soil temperatures at various depths are unique parameters useful to describe both the surface energy processes and regional environmental and climate conditions. To provide soil temperature observation in different regions across Belgium for agricultural management as well as for climate research, soil temperatures are recorded in 13 of the 20 automated weather stations operated by the Royal Meteorological Institute (RMI) of Belgium. At each station, soil temperature can be measured at up to 5 different depths (from 5 to 100 cm) in addition to the bare soil and grass temperature records. Although many methods have been developed to identify erroneous air temperatures, little attention has been paid to quality control of soil temperature data. This contribution describes the newly developed semi-automatic quality control of 10-min soil temperatures data at RMI.

THE DISTRIBUTION OF DERMACENTOR TICKS IN CANADA IN RELATION TO BIOCLIMATIC ZONES

1967 ◽  
Vol 45 (4) ◽  
pp. 517-537 ◽  
Author(s):  
P. R. Wilkinson
Keyword(s):  
British Columbia ◽  
Deciduous Forest ◽  
Strong Association ◽  
Eastern Deciduous Forest ◽  
Egg Development ◽  
The North ◽  
Winter Activity ◽  
Bioclimatic Zone ◽  
Soil Temperatures ◽  
Time Of Year

Dermacentor andersoni has been collected north of Jasper, Alberta, close to 54° N. and near 53° N. in British Columbia. Spread to the north and northwest is probably limited by low summer soil temperatures, which would act principally by slowing egg development, thus disrupting the seasonal cycle of the tick. To the southwest, mild winters may fail to release diapause at the correct time of year. Aspect and slope are important factors. Altitude spread of records is from 1000–7000 ft. The most generally applicable description of its distribution is the ecotone between western grassland and moister regions, including clearings and rocky outcrops m the montane and Columbia forests, and shrubby areas of the prairies. In British Columbia, a series of randomly selected transects indicated a strong association between the tick's presence and several species of shrubs growing without tree shade.Each bioclimatic zone tends to have a characteristic group of rodents as main hosts of the immature stages. The prairie and montane regions differ in the indigenous hosts available to the adult tick.East of 105° D. andersoni is replaced by D. variabilis, which is adapted to the more humid summers of the eastern deciduous forest zones, and differs considerably from D. andersoni in its phenology. There are no reliable records of indigenous D. variabilis north of 52° latitude.D. albipictus occurs from the east to the west coast. Because of the winter activity of its larvae, allowing the whole summer for egg development, it is able to penetrate much farther north than the other two species. There are two records close to 60° latitude.

Cover crop effects on soil temperature in a clay loam soil in southwestern Ontario

2021 ◽  
pp. 1-10
Author(s):  
X.M. Yang ◽  
W.D. Reynolds ◽  
C.F. Drury ◽  
M.D. Reeb
Keyword(s):  
Soil Temperature ◽  
Cover Crops ◽  
Environmental Performance ◽  
Cover Crop ◽  
Crop Production ◽  
Surface Soil ◽  
Clay Loam ◽  
Near Surface ◽  
Soil Temperatures ◽  
Surface Soil Temperature

Although it is well established that soil temperature has substantial effects on the agri-environmental performance of crop production, little is known of soil temperatures under living cover crops. Consequently, soil temperatures under a crimson clover and white clover mix, hairy vetch, and red clover were measured for a cool, humid Brookston clay loam under a corn–soybean–winter wheat/cover crop rotation. Measurements were collected from August (after cover crop seeding) to the following May (before cover crop termination) at 15, 30, 45, and 60 cm depths during 2018–2019 and 2019–2020. Average soil temperatures (August–May) were not affected by cover crop species at any depth, or by air temperature at 60 cm depth. During winter, soil temperatures at 15, 30, and 45 cm depths were greater under cover crops than under a no cover crop control (CK), with maximum increase occurring at 15 cm on 31 January 2019 (2.5–5.7 °C) and on 23 January 2020 (0.8–1.9 °C). In spring, soil temperatures under standing cover crops were cooler than the CK by 0.1–3.0 °C at 15 cm depth, by 0–2.4 °C at the 30 and 45 cm depths, and by 0–1.8 °C at 60 cm depth. In addition, springtime soil temperature at 15 cm depth decreased by about 0.24 °C for every 1 Mg·ha−1 increase in live cover crop biomass. Relative to bare soil, cover crops increased near-surface soil temperature during winter but decreased near-surface soil temperature during spring. These temperature changes may have both positive and negative effects on the agri-environmental performance of crop production.

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