Die Rolle der mikrobiellen Biomasse und des mineralisch fixierten Ammoniums bei den Stickstoff-Transformationen in niedersächsischen Löß-Ackerböden unter Winter-Weizen. I. Poolgrößenveränderungen

Significance of microbial biomass and non-exchangeable ammonium with respect to the nitrogen transformations in loess soils of Niedersachsen during the growing season of winter wheat. I. Change of pool sizes Nitrogen transformations in loess soils have been examined by laboratory and field experiments. After straw application (· 8 t · ha^?1), N in microbial biomass (N_mic) increased by about 20 mg · kg^?1 soil (· 90 kg N · ha^?1 · 30 cm^?1) after 9 days of incubation (20 °C). Another laboratory experiment yielded an increase of about 400 mg of NH₄+-N · kg^?1 fixed by minerals within 1 h after addition of 1 M NH₄+-acetate. Defixation of the recently fixed NH₄+ after addition of 1 M KCl amounted to only 60 mg · kg^?1 within 50 days. In a field experiment with winter wheat 1991, an increase in N_mic of about 80 kg N · ha^?1 · 30 cm^?1 was observed from March to June. After July, growth of the microbes was limited by decreased soluble carbon concentrations in the rhizosphere. Different levels of mineral N-fertilizer (0, 177 and 213 kg N · ha^?1) did not affect significantly the microbial biomass. The same field experiment yielded a decrease of non-exchangeable ammonium on the “zero”-fertilized plot in spring by 200 kg N · ha^?1 · 30 cm^?1. The pool of fixed ammonium increased significantly after harvest. After conventional mineral N-fertilizer application (213 kg N · ha^?1). NH₄+-defixation was only about 120 kg N · ha^?1 · 30 cm^?1 until July.     

Phytotoxic Effect of the Uranium on the Growing Up and Development the Plant of Corn

The aim of this article is the determination of uranium accumulation in plants tissue in shoots and roots of corn—maize (Zea mays), grown on two types of soils, pseudogley and chernozem, together with its phytotoxic effect on the plant growth and development. The soils was contaminated with different rates (10 to 1,000 mg U(VI) kg^?1) of uranyl nitrate (UO₂(NO₃)₂·6H₂O). Vegetative tests performed with maize indicated uranium phytotoxic effect on plant height, yield, and germination of seeds. This effect was stronger on the plants grown on pseudogley in comparison with those grown on chernozem. Soil properties determined the tolerance and accumulation of U in plants. A linear dependence between the content of uranium in soil and in plants tissue, including maximal content of 1,000 mg U?kg^?1, indicates that maize could be used for phytoremediation of uranium-contaminated soils.     

Die Rolle der mikrobiellen Biomasse und des mineralisch fixierten Ammoniums bei den Stickstoff-Transformationen in niedersächsischen Löß-Ackerböden unter Winter-Weizen. II. Umsetzung von 15N-markiertem Stickstoff

Significance of microbial biomass and mineral fixed ammonium with respect to the nitrogen transformations in loess soils of Niedersachsen during the growing season of winter wheat. II. ¹⁵N-turnover Field experiments 1988/89 on a fallow plot of the southern Niedersachsen loess area with straw application (δ 10 t · ha^?1, homogeneously incorporated by hand) yielded an increase in microbial biomass-N (N_mic) by 60 kg N · ha^?1 · 30 cm^?1 until March 1989 and further 40 kg N · ha^?1, till May which was almost completely remobilized until harvest. For a cropped plot (with winter wheat and 10 t · ha^?1 straw incorporation), N immobilization was of similar magnitude. Up to 18% of the applied ¹⁵N-fertilizer (185 kgN · ha^?1) were microbially immobilized. In contrast to 1988/89, no significant mass change of N_mic occurred in 1991 due to straw application (δ 10t · ha^?1). Variations in the amount of N_mic were nearly independent on the treatment (crop, with 140 kg fertilizer-N · ha^?1 or without N-fertilizer, respectively; fallow plot without fertilizer-N) within a range of 225-400 kg N · ha^?1 · 30 cm^?1. Directly after N-application (each 70 kg N · ha^?1 in March and in May), up to 100% of the fertilizer-N were assimilated by the microbes. Subsequently, remobilization of the immobilized nitrogen occurred within 2 (in March) or 6 weeks (in May), respectively. Simultaneously, organic soil-N was mineralized after each N-application and minerally fixed for us biggest part. Between March and June, the fixed NH₄+ decreased by about 112 kg · ha^?1 · 30 cm^?1.     

Solubility of a proto-imogolite sol in oxalate solutions

The amounts of aluminium liberated from a proto-imogolite (P-I) sol by 1–3 mM oxalate at pH 4·8–7·1 are found to be in excellent agreement with those calculated on the basis of the solubility product of the P-I sol, and the stability constants for aluminium oxalate complexes established earlier. Calculated solubility curves are presented for proto-imogolite sols in the presence of 10^?3, 10^?4 and 10^?5 M total oxalate over the pH range 4–8, and also for the case where oxalate concentrations are controlled by solid calcium oxalate in the presence of 0·05, 0·5 and 5 mM calcium ion. We conclude that the presence of a proto-imogolite allophane in podzol B horizons of pH 5·0 requires oxalate concentrations less than 10^?5 M. For fertile agricultural soils with typical calcium concentrations (approximately 5 mM) in the soil solution, aluminium oxalate concentrations would be limited by calcium oxalate solubility to less than 10^?6 M in the presence of proto-imogolite allophane at pH values exceeding 5·5. In leached podzolic soils calcium concentrations are generally less than 0·05 mM, and would not limit the formation of aluminium oxalate complexes.     

On the surface activity of humic acid

Humic acid, the principal component of soil organic matter, contains the surface active substances peptizable with alkali and non-lixiviable with benzene, ethanol and benzene-ethanol mixture. The surface tension of the decantate of suspension is below that of pure water being a few (< 10) erg cm^?2 before peptization, and up to 30 erg cm^?2 after peptization. According to the surface tension values of the decantates of suspensions, the soils can be in the following order: non-lixiviated < lixiviated with benzene < lixiviated with ethanol < lixiviated with benzene-ethanol mixture.     

Pentachlorophenol-decomposing and PCP-tolerant bacteria in field soil treated with PCP

Soil samples from field plots that had received annual applications of pentachlorophenol (PCP) for 3 consecutive years were analyzed each year for changes in microbial populations, particularly in PCP-decomposing microorganisms and PCP-tolerant bacteria. Within 6 weeks after an initial application of PCP, PCP-decomposing microorganisms increased by about 3 orders of magnitude; this increased population was still observed the following spring. The number of PCP-decomposing microorganisms in the soils that received PCP for 3 yr reached 10⁵· g^?1 soil or more, while that in soils without PCP was 10²· g^?1. The soils that received PCP were not enriched with tetrachlorophenoldecomposing microorganisms. The microbes enriched by PCP may have been bacterial in nature. In 1972 and 1974, the number of PCP-tolerant bacteria increased immediately after PCP application and continued to increase for 2 weeks, then declined. The 1973 data, however, showed no such decline. The number of PCP-tolerant and of crystal violet-tolerant (Gram-negative) bacteria correlated fairly well except at 2 weeks after PCP application (when PCP-tolerant bacteria were more numerous).     

AVAILABILITY OF POTASSIUM TO RYEGRASS FROM SCOTTISH SOILS II. UPTAKE OF INITIALLY NON-EXCHANGEABLE POTASSIUM

The stable desorption parts of soil Quantity/Intensity isotherms were used to determine the contributions of initially exchangeable and non-exchangeable potassium to plant uptake from ten soils. The activity ratio, AR^K= a_K/√^aC_a, Mg at which K was first taken up from non-exchangeable sources varied from 3 × 10^?3 to 8 × 10^?3 M^1/2 depending on the soil. Uptake rates of two categories of initially non-exchangeable K were linearly related to √times;. The first category appeared to be close to equilibrium with the initially exchangeable K, and gave effective diffusion coefficients of 10^?7 cm² s^?1 for four soils. The second category gave diffusion coefficients from 10^?20 to 10^?22 cm² s^?1, probably came from internal surfaces of micaceous clays, and began to be released at activity ratios below 3 × 10^?4 to 6 × 10^?4 M^1/2 depending on soil type. The soils fell into three groups, broadly consistent with soil series, on their ability to release the second category of potassium.     

Rhizobia in tropical legumes—X. Growth in coir-dust-soil compost

Conditions affecting the growth of two rhizobia (RRIM 968 isolated from Centrosema pubescens and CB 1809 from Glycine max) in the coir-dust-soil compost used in Malaysia were examined. Whilst differences in growth between the two isolates were observed, recommended conditions for rhizobial production are: compost—(coir-dust 8 g; Sungei Buloh series soil—25 g ; calcium carbonate—5 g; and distilled water—60 ml) incubation—at 25°C for 12d; storage—commercially for about 3 months at 20°C. Under these conditions more than 10⁹ viable rhizobial cells·g^?1 compost are obtainable, while more than 10⁸·g^?1 survive 5 months in storage.Addition of a “sticker” (methyl-ethyl cellulose) to the compost during incubation was encouraging.     

Interactions of ferricyanide with humic soils and charred straw

The iron‐cyanide complexes ferricyanide, [Fe^III(CN)₆]^3?, and ferrocyanide, [Fe^II(CN)₆]^4?, are anthropogenic contaminants in soil. We studied the interactions of ferricyanide with humic soils and charred straw (maize and rye, both charred at 300, 400 and 500°C) by batch experiments and Fourier transform infrared (FTIR) spectroscopy. All soil samples sorbed ferricyanide (up to 8.4 g kg^?1). Precipitation of a manganese ferrocyanide after reduction of ferricyanide in the moderately acidic to neutral soils was deduced from both FTIR spectroscopy (CN absorption bands at 2069–2065 cm^?1) and geochemical modelling. Ferricyanide was also adsorbed onto the charred straw. The amounts of iron‐cyanide complexes adsorbed increased with increasing charring temperature, with a maximum of 1.71 g kg^?1. An absorption band at 2083 cm^?1 indicated weakly adsorbed intermediates of the reduction of ferricyanide to ferrocyanide. This band disappeared in the samples charred at higher temperature, whereas a band at 2026 cm^?1 was present in all spectra and became intensified in the high‐temperature straw. We attribute this band to ferrocyanide forming inner‐sphere complexes, presumably with quinone species of the organic matter. The band at 2026 cm^?1 was also present in the spectra of the soils, indicating that soil organic matter also adsorbs ferrocyanide. However, in humic soils the main processes of ferricyanide interaction include reduction to ferrocyanide and precipitation as manganese ferrocyanide. Quantitatively, adsorption on highly aromatic substances plays only a less important role as compared with precipitation.     

Soil organic carbon stock for reclaimed minesoils in northeastern Ohio

Reclamation of disturbed soils is done with the primary objective of restoring the land for agronomic or forestry land use. Reclamation followed by sustainable management can restore the depleted soil organic carbon (SOC) stock over time. This study was designed to assess SOC stocks of reclaimed and undisturbed minesoils under different cropping systems in Dover Township, Tuscarawas County, Ohio (40°32·33′ N and 81°33·86′ W). Prior to reclamation, the soil was classified as Bethesda Soil Series (loamy‐skeletal, mixed, acid, mesic Typic Udorthent). The reclaimed and unmined sites were located side by side and were under forage (fescue—Festuca arundinacea Schreb. and alfa grass—Stipa tenacissima L.), and corn (Zea mays L.)—soybean (Glycine max (L.) Merr.) rotation. All fields were chisel plowed annually except unmined forage, and fertilized only when planted to corn. The manure was mostly applied on unmined fields planted to corn, and reclaimed fields planted to forage and corn. The variability in soil properties (i.e., soil bulk density, pH and soil organic carbon stock) ranged from moderate to low across all land uses in both reclaimed and unmined fields for 0–10 and 10–20 cm depths. The soil nitrogen stock ranged from low to moderate for unmined fields and moderate to high in some reclaimed fields. Soil pH was always less than 6·7 in both reclaimed and unmined fields. The mean soil bulk density was consistently lower in unmined (1·27 mg m⁻³ and 1·22 mg m⁻³) than reclaimed fields (1·39 mg m⁻³ and 1·34 mg m⁻³) planted to forage and corn, respectively. The SOC and total nitrogen (TN) concentrations were higher for reclaimed forage (33·30 g kg⁻¹; 3·23 g kg⁻¹) and cornfields (21·22 g kg⁻¹; 3·66 g kg⁻¹) than unmined forage (17·47 g kg⁻¹; 1·98 g kg⁻¹) and cornfield (17·70 g kg⁻¹; 2·76 g kg⁻¹). The SOC stocks in unmined soils did not differ among forage, corn or soybean fields but did so in reclaimed soils for 0–10 cm depth. The SOC stock for reclaimed forage (39·6 mg ha⁻¹ for 0–10 cm and 28·6 mg ha⁻¹ for 10–20 cm depths) and cornfields (28·3 mg ha⁻¹; 32·2 mg ha⁻¹) were higher than that for the unmined forage (22·7 mg ha⁻¹; 17·6 mg ha⁻¹) and corn (21·5 mg ha⁻¹; 26·8 mg ha⁻¹) fields for both depths. These results showed that the manure application increased SOC stocks in soil. Overall this study showed that if the reclamation is done properly, there is a large potential for SOC sequestration in reclaimed soils. Copyright © 2005 John Wiley & Sons, Ltd.     

Inorganic pyrophosphatase activity of soils

A simple method to assay inorganic pyrophosphatase activity in soils is described. It involves extraction and colorimetric determination of the orthophosphate (Pi) released when 1 g soil is incubated with buffered (pH 8) pyrophosphate (PPi) solution at 37°C for 5 h. The 1 n H₂SO₄ used to extract Pi gives quantitative recovery of Pi added to soils, and the colorimetric method used to determine the Pi extracted in the presence of PPi is specific for Pi. The inorganic pyrophosphatase activity of the six soils studied ranged from 50 to 450 μg Pi released·g^?1 soil·5 h^?1. Steam sterilization (121°C for l h), formaldehyde, fluoride, oxalate, and carbonate inhibited and toluene, Na⁺, K⁺, NH⁺₄, Cl^?, NO^?₃, NO^?₂, SO^2?₄, and EDTA had no effect on the activity of this enzyme in soils. The initial rates of Pi released obeyed zero-order kinetics. The temperature dependence of the rate constant conformed to the Arrhenius equation up to the point of enzyme inactivation (55°C). The activation energy of pyrophosphatase activity of the six soils studied ranged from 32.5 to 43.2 (av 36.1) kJ·mole^?1. Application of the three linear transformations of the Michaelis-Menten equation indicated that the K_m values of PPi for pyrophosphatase in four soils ranged from 20 to 51 (avg. 35) mM and that the V_max ranged from 130 to 830 (av 500) μg Pi released g^?1 soil·5 h^?1. Studies of other properties of inorganic pyrophosphatase activity in soils are reported.     

THE SURFACE TENSION OF SOIL WATER

Because of their organic matter content, the surface tension of water of soils is about 8 to 9 erg cm ^-2 (8 to 9 × 10 ^-7 J cm ^-2) less than that of pure water. It is estimated that the surface tension of soil solution is 63–64 erg cm ^-2 in the surface soils studied.     

Diffusion coefficients of nitrate, chloride, sulphate and water in cracked and uncracked Chalk

The rates of diffusion of chloride, sulphate and water, labelled respectively with ³⁶Cl, ³⁵S and ³H, and unlabelled nitrate, were measured in small cylindrical Chalk monoliths. Using a simple mathematical model, diffusion coefficients were calculated to provide a basis for comparing the movement of these substances through Chalk rock in the absence of hydrostatic pressure gradients. The diffusion coefficients of chloride and nitrate were similar, with a range of values (0.52–3.23 × 10^?6 cm² s^?1) and (0.53–3.20 × 10^?6 cm² s^?1) respectively. These were slightly less than for tritiated water (0.60–3.51 × 10^?6 cm² s^?1), while the coefficient for sulphate was about half that of the others (0.28–1.47 × 10^?6 cm² s^?1). The coefficients indicate the absence of any interaction with the Chalk surfaces.     

Soil Property Changes After Conversion from FOrest to Pasture in Mount Sacinka,Artvin, Turkey

Turkey's forests have been continuously facing conversion into both agriculture and pasturelands, causing not only degradation and fragmentation of forested lands but also negative changes in soil properties that have not been thoroughly investigated. In order to determine possible changes in some physical and hydrophysical soil parameters along with the dispersion ratio between natural coppice forests and the neighbouring forest‐to‐grassland converted areas, a foothill of Mount Sacinka in Artvin was chosen as a research area. Besides land use, possible effects of elevation change on soil properties due to the mountainous and moderately steep landscape of the region were also taken into consideration. The soil samples were analysed for soil texture, permeability, field capacity, bulk density, organic matter, pH and dispersion ratio. The results indicated that whereas permeability (43·05 mm h⁻¹ in forest and 18·82 mm h⁻¹ in pasture), field capacity (43·45% in forest and 38·08% in pasture) and organic matter (6·36% in forest and 5·34% in pasture) values turned out to be higher in forest soils, bulk density (0·91 g cm⁻³ in forest and 1·06 g cm⁻³ in pasture) and pH (5·89 in forest and 6·55 in pasture) values were low in grassland soils, meaning that conversion has negative effects on soil properties. Additionally, the mean dispersion ratios of 27·55% and 33·58% for forest and pastureland soils, respectively, indicated soil erosion problems in both land uses. In addition, as for elevation effect, forest soils especially showed better characteristics at higher elevations with high permeability, field capacity and organic matter and low pH and dispersion ratio. Copyright © 2015 John Wiley & Sons, Ltd.     

Zinc Diffusion and Self-Diffusion Coefficient in Alkaline Soils as Affected by Soil Properties and Zinc Carrier

The apparent diffusion coefficients, D_p/b+ø, of Zn and ZnEDTA were linear functions of added Zn, and were related to the adsorption and fixation capacities of soils rather than their pH. Lower apparent diffusion coefficient values were found in an Haplustoll soil that had higher clay and humus contents inspite of its lower pH. At comparable rates of added Zn, the apparent diffusion of ZnEDTA was 930–1010 (Bakyria), 700–1330 (Dirab), and 730–1880 (Baha) times that of Zn in the soils. The adsorbed Zn per cm³ of soil/Zn per cm³ of the equilibrium solution at the water content existing in the diffusion experiment approximated the capacity factor and was determined by extrapolation. The self-diffusion coefficient of Zn in Baha soil (5 × 10^?7 cm²sec^?1) of higher clay and water content was higher than in Bakyria or Dirab soil (2 × 10^?7 cm²sec^?1). These values were similar to the self-diffusion coefficient of P in soils of similar texture at similar water content.     

Least limiting water range for different soil management practices in dryland farming in Iran

Integrated evaluation of soil physical properties using the least limiting water range (LLWR) approach may allow a better knowledge of soil water availability. We determined the LLWR for four tillage practices consisted of conventional tillage (CT), reduced tillage (RT), no-tillage (NT) and fallow no-tillage (NT_f). In addition, LLWR was determined for abandoned soils (i.e. control), compacted soils, ploughed compacted soils and abandoned soils with super absorbent polymers (SAPs) application. Soil water retention, penetration resistance (PR), air-filled porosity and bulk density were determined for the 0–5 and 0–25-cm depths. Mean LLWR (0.07–0.08 cm³ cm^?3) was lower in compacted soils than the soils under CT, NT, NT_f, RT, tilled, abandoned and SAP practices but it was not different among tillage practices. The values of LLWR were 0.12 cm³ cm^?3 for NT and CT. LLWR for tilled plots (0.12 cm³ cm^?3) became greater than compacted soils by 1.3 times. Analysis of the lower and upper limits of the LLWR further indicated that PR was the only limiting factor for soil water content, but aeration was not a limiting factor. The LLWR was more dependent on soil water content at permanent wilting point and at PR.     

Pedobiochemical indicators for eutrophication and the development of ”︁black spots” in tidal flat soils on the North Sea coast

The increasing eutrophication of tidal flat soils on the North Sea coast and the appearance of ”︁black spots” gave rise to this study. The aim was to find pedobiochemical indicators for the development of ”︁black spots”. Artificially eutrophicated soils were compared with untreated soils in the field and laboratory. The pH values of the artificially eutrophicated and natural soils often differed by nearly one unit. The treated soils mostly showed lower redox potentials (˜ —300 mV) than the untreated samples (˜ —250 mV). The mean sulfate concentrations were 2.2 mM in the eutrophicated laboratory soils and 13.1 mM in the eutrophicated field soils, compared with 12.5 mM and 20.2 mM in the untreated ones. Consequently, the SO₄^2—:Cl^— ratios and SO₄^2— differences were lower in the treated soils. Non‐eutrophicated soils showed methane concentrations of < 5 nmol cm^—3, whereas the eutrophicated soils showed up to 217.0 nmol cm^—3 in the field and 479.1 nmol cm^—3 in the laboratory. Differences between field and laboratory data were mainly due to a continuous sulfate supply and reoxidation process only possible in the field. Although all parameters showed differences between the eutrophicated and untreated soils, only the methane data did not overlap with their interquartile ranges. Those of the untreated soils were 2—7 nmol cm^—3 and those of the treated were 12—360 nmol cm^—3. Thus, threshold values can be defined. Methane concentrations of approximately > 10 nmol cm^—3 refer to the beginning eutrophication process and those in the range of > 100 nmol cm^—3 to advanced processes, phenologically forming ”︁black spots”.     

Do earthworms (D. veneta) influence plant-available water in technogenic soil-like substrate from bricks and compost?

Purpose

Topsoil and peat are often taken from intact rural ecosystems to supply the urban demand for fertile soils and soil-like substrates. One way of reducing this exploitation is to recycle suitable urban wastes to produce Technosols and technogenic soil-like substrates. In this study, we investigate the role earthworms can play in impacting the hydraulic properties of such a soil-like substrate.

Materials and methods

In a 4-month microcosm experiment, the influence of the earthworm species D. veneta on the hydraulic properties of brick-compost mixture was examined. Of the ten boxes filled with ca. 11 dm³ of ground bricks (0.7 cm³ cm^?3) and green waste compost (0.3 cm³ cm^?3), five contained earthworms (W-boxes) and the remaining five were used as controls (C-boxes). The substrate was periodically irrigated and the weight of the boxes and of the drained water was monitored. At the same time, images were taken from the front of the boxes to quantify the activity of the earthworms by image analysis and soil aggregation was studied with micrographs. Before and after the experiment, water retention curves were determined from disturbed samples of the substrate using the simplified evaporation method.

Results and discussion

After 6 weeks, differences between the C- and the W-boxes were evident. Micrographs showed brick-compost aggregates only for the substrates processed by earthworms. The earthworm activity leads to reduced evaporation and an increased water content in the respective microcosms. The effect persists even after disturbing the substrate. The proportion of plant-available soil water is about 0.02 cm³ cm^?3 higher for the substrate processed by earthworms (0.250 ± 0.009 cm³ cm^?3) compared with the control (0.230 ± 0.008 cm³ cm^?3).

Conclusions

This study shows that earthworms are capable of ingesting and processing crushed bricks together with compost. The earthworms produced aggregates which persisted after disturbance and had a positive influence on the water retention capacity of such a soil-like substrate constructed from waste.

     

INORGANIC SOIL PHOSPHORUS

Sixteen soils and 4 soil preparations were cropped exhaustively with ryegrass in the glasshouse and monocalcium phosphate potentials (½pCa+pH₂PO₄=1) were measured after each of 6 consecutive harvests. The amounts of phosphorus (Q) removed from the soils by ryegrass accounted for 95·1–96·6 per cent of the variance in 1 for 3 soils and 2 soil preparations (P < 0·001), for 88·4–93·7 Per cent of the variance for 6 soils and 2 soil preparations (0·001 < P < 0·01), for 71·6–82·6 per cent of the variance for 3 soils (0·01 < P < 0·05) and for insignificant amounts of the variance for 4 soils. Values of ΔI/ΔQ ranged from 7 × 10^–4 to 431 × 10^–4½pCa+pH₂PO₄/ppm P removed from soil. ΔI/ΔQ tended to decrease (i.e. the soils were more buffered) with increasing clay contents and with increasing amounts of NaHCO₃-soluble P and to increase (i.e. the soils were less buffered) with increasing amounts of CaCO₃. Variations in organic C did not significantly affect ΔI/ΔQ. The following equation accounts for 81 per cent of the variance in ΔI/ΔQ for all soils except those in equilibrium with octacalcium phosphate: ΔI/ΔQ× (10⁴) = 225·9–4·17(% clay)+8·01(% CaCO₃)–1·38(ppm NaHCO₃-soluble P).     

Changes in Physical Properties of Soils with Land Use Time in the Brazilian Savanna Environment

Soils from central Brazil have been intensively used over the last decades because of the rapid conversion of savannas ( Cerrado ) into corn/soybean fields. The objective of this work is to study modifications in the physical properties of soils in the Rio Verde watershed, as a function of the land use time for agriculture, determined from classification of Landsat satellite images between 1980 and 2010. Soil samples were collected at surface (0–20 cm) and subsurface (20–40 cm) horizons for the different classes of land use time (<10, 10–20, 20–30, and >30 years). The following physical properties were measured: bulk density (BD), air permeability (K_a), penetration resistance (PR), microporosity (MI), macroporosity (MA), and total porosity (TP). Results showed a strong expansion with time of agriculture that occupied 35·3% (1980), 37·4% (1990), 51·3% (2000), and 60·9% (2010) of the watershed area. When properties were compared with those from the reference areas (preserved soils under native vegetation), significant differences were observed for all the physical attributes of soils for a land use time higher than 20 years. Overall, BD and PR increased with land use time, and the opposite was verified for K_a, MA, and TP. Some physical properties presented values (e.g., 1·54 g cm⁻³ for BD and 0.06 cm³ cm⁻³ for MA) close to the critical ones reported to affect crop development, but they were not still impacting on local soybean yield. Copyright © 2013 John Wiley & Sons, Ltd.