Open access peer-reviewed chapter

Time Domain Reflectometry: Temperature-dependent Measurements of Soil Dielectric Permittivity

By Wojciech Skierucha

Submitted: October 19th 2010Reviewed: March 2nd 2011Published: June 21st 2011

DOI: 10.5772/17162

Downloaded: 3659

1. Introduction

The purpose of this study is to determine the temperature influence on the soil bulk dielectric permittivity, εb, calculated from the measurement of the electromagnetic wave velocity of propagation along the parallel waveguide in a TDR probe, i.e. a probe working in Time Domain Reflectometry technique. The experimental evidence shows that the existing models do not completely describe the temperature effect. However, it has been confirmed that the observed temperature effect is the result of two competing phenomena; εb increases with temperature following the release of bound water from soil solid particles and εb decreases with temperature increase following the temperature effect of free water molecules. It has been found that there is a soil type characteristic moisture value, θeq, named the equilibrium water content, having the specific temperature property. The temperature effect for this moisture is not present, which means that for soils with the moisture value equal to θeq the both competing phenomena mentioned earlier compensate each other. The equilibrium water content, θeq, decrease is correlated with the soil specific surface area. The temperature correction formula adjusting the soil moisture determined by TDR, θTDR, at various temperatures to the corresponding value at 25 C, based on knowledge of θeq, decreases the standard deviation of the absolute measurement error of soil moisture θTDR by the factor of two as compared to the uncorrected values.

The majority of measurements of physical, chemical and biological properties of porous materials including soil should be accompanied with the measurement of soil water content and temperature. These parameters determine almost all processes in natural environment. It seems obvious to accompany the sensors for the measurement of soil salinity, oxygenation, content of nutrients, soil water potential, and others with the temperature and moisture sensors having the same measurement volume and performing measurements at the same time. Temperature sensors of various accuracy and size are easily available and together with the necessary electronics they can fit into the desired sensor enclosure. More problems are encountered with moisture sensors of porous materials because they do not measure water content directly, but use other parameters of the measured matter that indirectly and selectively determine its moisture. Such a property of porous materials accompanied with moisture is dielectric permittivity.

Measurement of soil moisture using time domain reflectometry (TDR) has become increasingly popular because of simplicity of operation, satisfactory accuracy and fast result available, the process of measurement is non-destructive, portable systems are available and the method gives ability for measurement automation and probes multiplexing (Dirksen & Dasberg, 1993; Malicki et al., 1996; Topp et al., 1980). Beside above advantages there are some drawbacks of this measurement technique including the requirement of excellent contact of the probe to soil and the dependence of dielectric permittivity of soil on temperature affecting the TDR soil moisture readout.

In first applications of the TDR technique for soil moisture determination, the influence of temperature on the TDR determined soil bulk dielectric permittivity, εb, was neglected. The significant fluctuation of measured data, which was obviously correlated with soil temperature, was noticed with the introduction of soil moisture field monitoring systems based on reflectometric meters. Also, it was found (Pepin et al., 1995; Halbertsma et al., 1995) that εb decreased with temperature increase for sandy, silt and peat soils and it did not change for the tested clay soil.

The text below uses two terms that need explanation: (i) soil free water – composed from water particles that rotation in the electric filed is not hampered, and (ii) soil bound water – composed from water particles so close to solid phase that their rotation in the electric field is hampered by surface charge on the solids. The real part of the complex dielectric permittivity of free water is about 80 at room temperature and is much smaller for bound water (Boyarskii et al., 2002) reaching the minimal value of ice (about 3.2) for the first layer of water particles adsorbed on the clay soil surface.

2. Basics of TDR technique

Time Domain Reflectometry (TDR) technique for the measurement of water content of isotropic and homogenous media becomes popular for the simplicity of operation, accuracy and the non-destructive, as compared to other methods, way of measurement (Malicki, 1999; O’Connor & Dowding, 1999). This measurement technique takes advantage of four physical phenomena characteristic to the porous materials including soil:

  1. for soils with negligible magnetic properties and electrical conductivity, which is true for the majority of arable soils, and in the frequency range of about 1 GHz, the complex dielectric permittivity of the soil can be approximated by its real value and the electromagnetic wave propagation velocity, v, in the soil can be calculated from:

  2. vc[ε(θ)]1/2=cn=2LΔtE1
  3. where: c is a velocity of light in free space, ε(θ) is a real part of the complex dielectric permittivity dependent on its water content, θ; n = [ε(θ)]1/2 is the medium refractive index; L is the length of TDR probe rods inserted into the soil; Δt is the time distance between the reflections of TDR pulse from the beginning and the end of the probe rods, inserted into the medium,

  4. the dielectric permittivity of the medium liquid phase has much higher value than the other medium phases, i.e. about 80 against 2÷4 for the solid and 1 for the gas phase,

  5. the relation between the water content of the medium and its dielectric permittivity is highly correlated for the majority of the porous media (Davis et al, 1977; Malicki & Skierucha, 1989; Topp et al., 1980),

the attenuation of the amplitude of electromagnetic wave traveling along the parallel transmission line inserted into the medium, measured from the amplitudes of the pulse before (Uin) and after (Uout) attenuation caused by the pulse travel twice a distance of the probe length, L (Fig. 1) depends on its bulk electrical conductivity, ECb (Dalton et al., 1984):

ECb(Sm1)=(ε)1/2120πLln(UinUout)E2

Therefore, water content of the soil, which is assumed to be an isotropic and homogenous medium, is the main reason determining its bulk dielectric permittivity.

The simplified formula (1) for the determination of the electric pulse propagation velocity in porous medium is derived from more general one:

v=c(ε'2(1+(1+tg2δ)1/2))1/2E3

where: c is the light velocity of propagation in free space, ε′ is the real value of the complex dielectric permittivity of the medium, tgδ is the dielectric loss defined as:

tgδ=ε"+ECb2πfε0ε'E4

The complex dielectric permittivity of the medium, ε, is:

ε=ε'j(ε"+ECb2πfε0)E5

where: ε″ represents dielectric loss connected with the dielectric polarization of soil particles, EC is the medium electrical conductivity, f is the frequency of the electromagnetic field, ε0 is dielectric permittivity of free space, j jest equal to (-1)1/2.

The idea of simultaneous measurement soil water content and electrical conductivity as well as the respective hardware setup are presented in Fig. 1.

The TDR probe consists of two waveguides connected together: a coaxial one, called the feeder, and a parallel one, called the sensor, made of two or more parallel metal rods, one of which is connected to the cable hot wire the others to the shield. The sensor should be fully inserted into the measured medium, that by definition should be homogeneous. The initial needle pulse travels from the generator by the feeder towards the sensor. A fast sampling oscilloscope registers this pulse in time. In the junction between the feeder and the sensor, there is a rapid change in geometry of the electromagnetic wave travel path. At this point some energy of the pulse is reflected back to the generator, like in radar, and the remaining travels along the parallel waveguide to be reflected completely from the rods ending. The

Figure 1.

Hardware setup for simultaneous measurement of soil water content and electrical conductivity using Time Domain Reflectometry technique

successive reflections are recorded for the calculation of the time distance between the two reflections (a) and (b). Three reflectograms representing pictures from the oscilloscope screen (voltage as a function of time at the chosen point in the feeder) are drawn in Fig. 1. They represent cases when the sensor was placed in dry, wet and water saturated soil. The time Δti necessary for the pulse to cover the distance equal to the double length of the metal rods in the soil increases with the soil dielectric permittivity, thus water content. The reason for that is the change of electromagnetic propagation velocity in media of different dielectric permittivity, according to (1). Also, the amplitude of the pulse at the point (b) decreases with the increase of soil electrical conductivity, according to (2).

2.1. Temperature effect of soil free water and electrical conductivity

Corrections of the TDR determined moisture data related to the temperature effect of dielectric permittivity of free water was examined by Pepin et al. (1995) and Halbertsma et al. (1995) and the influence of soil texture on the observed temperature effect was reported. Temperature dependence of dielectric permittivity of free water can be described as (Wheast, 1979):

nfw(T)=nfwd(T)=8.851d(T)E6
[d(T)]2=10.4536102(T25)+0.9319107(T25)2E7

where nfw = (εfw)1/2 = 8.851 is free water refractive index at 25ºC for the frequency in the range of 108 Hz, εfw is dielectric permittivity of free water at 25ºC, and T is the temperature in ºC.

If bulk soil dielectric permittivity had a temperature dependence related solely to free water, measurements of soil εb would show a negative correlation with temperature that would increase with water content. Results from Pepin et al. (1995) show this negative correlation, but the overall changes are smaller than predicted from a dielectric mixing model that integrated the temperature change in dielectric permittivity of water. The same was observed by Halbertsma et al. (1995) who made measurements of sand and silt soil samples. Also, he reported the lack of the discussed temperature effect for clay soil. It was obvious that the physical processes involving other soil phases beside the liquid phase should be taken into account when interpreting the temperature effect on the soil εb.

Literature reports (Nadler et al., 1999; Or & Wraith, 1999 ) show that soil electrical conductivity does not influence the TDR determined soil bulk dielectric permittivity, εb, in the soil salinity range where the majority of plants are growing, i.e. up to the corresponding values of soil solution from 1600 to 2600 mSm-1. Following the discussion in Or & Wraith (1999 ) it is possible to present the frequency dependence of the real and imaginary parts of a salt-water mixture’s dielectric permittivity, ε’ and ε”, as well as the velocity of propagation, v, of electromagnetic wave along the TDR probe rods inserted in this mixture for different temperatures and electrical conductivities, σdc. The increase of temperature of the salt-water mixture increases the frequency range around the frequency 1 GHz, where the velocity of propagation of an electromagnetic wave along the waveguide, used in TDR technique, does not change. Therefore the temperature effect on the electrical conductivity of soil, resulting mainly from ionic conductivity of soil electrolyte should not influence the bulk temperature effect of soil dielectric permittivity.

2.2. Temperature effect of soil bound water

The discussion of the release of bound water from the solids with the temperature is presented by Or & Wraith (1999 ), where the authors applied the Debye model for polar liquids and liquid viscosity dependence on temperature, T, for bound water molecules at the distance x from the solid surface to describe their relaxation frequency. They reported that εb increased with temperature for a silt loam soil for all soil moisture, however another silt loam soil showed the increase of εb for relatively low water contents, whereas it decreased with temperature at higher water contents. The change of εb with temperature is not fully explained yet but they discuss its two reasons: εb decreases with temperature because the real part of soil complex dielectric permittivity decreases following the temperature effect of soil free water and εb increases with temperature following the release of bound water molecules.

Water molecules that are adsorbed to the solid surface are less mobile in the imposed EM (electromagnetic) field as the not adsorbed ones. For a given temperature, the more distant the water molecules are from the solids, the higher is their relaxation frequency. The increase of temperature increases their kinetic energy that raises the relaxation frequency and they become more mobile in the imposed EM field. Bound water molecules released from the solid surface become now free with higher value of the real part of the complex dielectric permittivity.

The release of water molecules from the solids results in the increase of the real part of the soil dielectric permittivity and decreases its imaginary part describing the loss tangent of dielectric material. This phenomenon leads to a new equilibrium with more free water molecules and less bound water ones.

According to recent studies (Or and Wraith, 1999 ; Boyarskii et al., 2002), only a few layers of water covering soil particles are subjected to the change of relaxation time in relation to relaxation time of free water. The analysis of nuclear resonance spectra of bound water films in clay shows the approximated relation between relaxation time of bound water, and thickness of the film covering soil particles (Boyarskii et al., 2002). The resonant frequency of hydrogen in water particles, measured by NMR, is different for various layers of water films on the solids and consequently different frequency response of their dielectric permittivity. The relaxation time of bound water drops rapidly with the number of layers covering the particles and it seems that only one or two layers have significantly longer relaxation times than that of free water.

On the base of Debye model (Debye, 1929; Hasted, 1973) for polar liquids and using relations showing dependence of viscosity of liquid molecules on temperature T and distance x from the solid phase, the relaxation frequency frel of water molecules can be expressed as (Or & Wraith, 1999 ):

frel(x,T)=kTexp(1T(ax+d))8π2r3cE8

where: k is Boltzman constant (1.38∙10-23 JK-1), T is temperature in Kelvin degrees, a = 1621∙10-10 mK, d = 2.047∙103 K and c = 9.5 10-7 Pas are constants as the consequences of applied simplifications, r = 1.8÷2.5 ×10-10 m is the radius of water molecule.

The equation (8) shows that moving closer to solid phase, water particles are increasingly hampered to rotate in the electromagnetic field of high frequency, which is manifested by decreasing relaxation frequency for these molecules. Also, the temperature of water particles will have some effect on the frel, which is simulated in Fig. 2A.

The dependence of dielectric permittivity (real part) for free and bound water particles on the frequency can be described by Cole-Cole formula (9), where ω=2πf is the angular frequency of the external electrical field, εlow= 81 and εhi= 4.23 are relative dielectric permittivity values for free and bound water particles in the frequency values lower and higher, respectively, from 18 GHz (relaxation frequency of free water particles), τ=1/(2πfrel) is the relaxation time of water particles, h=0.013 is a parameter describing interaction of water dipoles (Hasted, 1973).

ε=εhi+(εlowεhi)[1+(ωτ)1hsinhπ2]1+(ωτ)2(1h)+2(ωτ)1hsinhπ2E9

Three curves in Fig. 2B represent water particles located at various distances from solid phase and the highest one relates to free water with relaxation frequency of 18 GHz, while the lowest to bound water particles close to solid phase.

The frequency range of an electric field, for which the values of ε determined from equation (9) are fixed at about 81, is the largest for free water. Adsorbed water molecules, by virtue of proximity to the solid phase are characterized by lower relaxation frequency and are less mobile in an external electric field. Consequently, according to the formula of Cole-Cole (9), the value of ε for frequencies below the relaxation frequencies are lower than for free water. The decreasing number of adsorbed water molecules, due to increasing temperature, increases the amount of free water molecules. Fig. 2A shows that moist soil temperature increase from 278 K to 338 K increases the relaxation frequency of water molecules located 2 10-10 m away from the solid phase from 0.1 GHz to 0.7 GHz. As a result, this temperature increase also increases the effective value of the dielectric permittivity of adsorbed water. Or and Wraith (1999) recognized the frequency limit of 1 GHz of the TDR method as the cut-off frequency, f*, that distinguishes water molecules between free and bound. Water layers having dielectric relaxation frequencies lower than the cut-off frequency were considered as bound water having smaller dielectric permittivity than for free water. It was shown (Dirksen & Dasberg, 1993) that the quantity of bound water increases with the volume of clay fraction in the soil due to large specific surface area of clay.

Figure 2.

A - relaxation frequency for water particles bound to solids according to (8) and related to its distance x from the solid phase; B - example relation between dielectric permittivity of water molecules and relaxation frequency for bound and free water particles

3. Materials and methods

TDR measurements were performed in the laboratory on mineral soils with negligible organic content, collected from Lublin region, Poland (Table 1) mainly from the topsoil layer. The soils were spread in layers of about 1 cm thickness on a flat surface in laboratory for drying at room temperature and then they were grinded to destroy big aggregates and passed through 2 mm sieve.

Dry soils were mixed with appropriate amount of distilled water to obtain five soil samples for each analyzed soil, with moisture values from air dry to saturation with regular differences in moisture content, taking care to get homogeneous distribution of water in the soil samples. Eight containers with soil samples covered with plastic foil to minimize evaporation were placed in a specially constructed rack. The volume of the soil containers was 0.5 dm2 and their shape assured that the TDR probes sphere of influence was in the measured soil samples. The gravimetric moisture content, θg, and bulk density, ρ, were determined for each soil sample directly after completion of the TDR measurements. The values of ρin Table 1 are the mean for all applied moistures for each tested soil. Soil texture was determined by standard Bouyoucos method (Pansu & Gautheyrou, 2006). The values of soil specific surface area, S, were measured by water vapor adsorption method (Oscik, 1983).

Soil No.Soil typeSpecific surface S
× 103 m2kg-1
Bulk density ρ
× 103 kgm-3
ISSS soil texture
sandsiltclay
2-0.02 mm0.02-0.002 mm< 0.002 mm
611brown soil91.599451
566rendsina101.459271
589soil lessive101.7088111
605brown soil101.699541
597soil lessive111.539451
604brown soil121.659721
593brown soil191.3577203
560rendsina201.4687112
569brown soil211.3373234
606muck soil231.429721
591brown soil251.4070273
601chernozem311.3864315
568brown soil341.35603010
570brown soil351.40632611
623chernozem361.39622513
622chernozem371.4061336
621chernozem421.3360346
562rendsina651.44523513
619chernozem691.1687121
565rendsina831.0477185

Table 1.

Selected physical parameters of the tested soils

The applied TDR probes had two parallel metal rods of 10 cm length and they were enhanced with the electronics (microcontroller, digital output temperature sensor, analog-to-digital converter and serial interface) for independent measurement of the probe temperature and soil electrical conductivity. The construction of such a “smart sensor” is presented in Fig. 3.

The electrical conductivity of the soil sample, ECb, is measured from the voltage drop on the reference resistor R1 connected in series with the soil equivalent resistor R2. Low frequency conductivity, ECb, of the soil samples were determined from the formula: ECb =C/R2, where C is a calibration constant determined individually for each TDR probe by the measurement in NaCl solution of known conductivities.

The source voltage for electrical conductivity measurement was a square wave, generated by the microcontroller, of 100 kHz frequency that does not polarize the electrode-soil system, the inductance L is for separation of high frequency TDR signal from much lower frequencies.

Reflectometric measurements for determination of the change of soil samples bulk dielectric permittivity with temperature, moisture and electrical conductivity were performed using the setup that is shortly described below as well as in Fig. 4 and Fig. 5.

It consists of three functional modules controlled by a program running on a PC compatible computer: (i) oscilloscope frame HP54120B with the TDR test set HP54121A, (ii) self-designed and manufactured interface connecting TDR probes (two wire waveguide, 10 cm long and spaced 1.5 cm) to the TDR unit by eight position 0.01-2.4 GHz multiplexer and reading selected temperature sensors and controlling the temperature chamber, (iii) temperature chamber consisting of a freezer, a fan-heater inside it and an additional fan to minimize temperature gradients inside the chamber.

Figure 3.

Block diagram of the TDR probe with the electronics for soil electrical conductivity and temperature measurements

Figure 4.

Laboratory setup for the determination of the temperature variability of the soil dielectric permittivity

Figure 5.

Block diagram of the laboratory setup for the determination of temperature effect on soil dielectric permittivity

PC compatible computer controlling the dedicated interface by means of the serial RS232C interface and the oscilloscope by universal GPIB link, was connected to Internet to monitor remotely the performance of the experiment. The application software provides a user friendly interface for the operator. Temperature of the soil samples was controlled by switching on and off the fan-heater located at the bottom of the temperature chamber and the freezer, only one working at a time. For security reasons, an independent temperature sensor connected to the main security switch was applied to disconnect all power devices in the system in case of reaching upper limit temperature, Tz=65ºC, inside the chamber.

The complete measurement cycle at six temperature values, from 5ºC to55ºC in 10ºC (±1 C) increments, for the set of eight soil samples took about 12 hours. Starting from the 4th cycle, the measurable decrease of TDR moisture values of soil samples was noticed, which was attributed to the loss of water evaporating from the not perfectly sealed holes of plastic foil where the TDR probe rods entered the soil samples.

The collected data in ASCII format representing reflectograms were processed by proprietary software to calculate travel times along the TDR probe rods, and soil bulk dielectric permittivity, εb, according to the “flat tangent” approach (Fig. 6) described by Wraith & Or (1999).

The bound water volume fraction of the soil θbw is the product of solid phase specific surface S, temperature dependent thickness of bound water layer x(T) and bulk density ρ:

θbw(T)=x(T)SρE10
(

and x(T) can be presented after Or & Wraith (1999) from reorganizing (8) as:

x(T)=ad+Tln(kT8π2r3cf*)E11

where f * = 1 GHz is the cut-off frequency, that distinguishes water molecules between free and bound. Having determined the dependence of bound water volume fraction of soil, θbw(T), on temperature using (10), it was possible to find the overall temperature dependence of bulk soil dielectric permittivity, εb, by application of dielectric mixing models. Among many dielectric mixing models describing soil as the mixture of solids, liquid, gas and also bound water phase, there are two applied in the presented study: alpha model (Birchak et al., 1974) and the model of de Loor (1990), given by the (12) and (13), respectively:

εbα=(1ϕ)εsα+(ϕθ)εaα+(θθbw)εfwα+θbwεbwαE12
εb=3εs+2θfw(εfwεs)+2θbw(εbwεs)+2θa(εaεs)3+θfw(εsεfw1)+θbw(εsεbw1)+θa(εsεa1)E13

where: εb – bulk dielectric permittivity determined by TDR method; ϕ - soil porosity (m3m-3); εs, εa, εfw and εbw are dielectric permittivity of dry soil, air, free water and bound water, respectively; θ, θbw and θa (m3m-3) are volume fractions of water in the soil (free and bound water), only bound water, and air, respectively.

To perform analysis of the models (12) and (13) the following values were assumed: εbw = 3.2 (the same as for ice), εs = 5 as used by Or & Wraith (1999), εa = 1.

4. Results and discussion

The experimental setup described earlier produced reflectograms like in Fig. 6 – upper curves, which after processing by dedicated software were converted to data pairs (εb,T) representing bulk dielectric permittivity and temperature of respective soil samples. Lower curve in Fig. 6 is produced by analysing software application software and it represents one differentiated curve, which local maxima localize inclination points in reflectograms for application the “flat tangent” algorithm.

All tested soils were divided into three groups with the soil specific surface areas below 12∙103 m2kg-1, between 20 and 35∙103 m2kg-1 and above 37∙103 m2kg-1. The calibration curves taken for the tested soils are trend lines of 2nd degree polynomials fitted to the data pairs (θ, εb(T)) collected experimentally at six applied temperature values. The first group of soils had TDR calibration curves close to the equation given by Topp et al. (1980).

With the increase of the soil specific surface area, S, as well as the decrease of bulk density, ρ, the bulk dielectric permittivity values, εb, were below the Topp’s calibration. This is in agreement with other reports (Dirksen & Dasberg, 1983) showing the influence of S and ρ on the calibration of the TDR method for soil moisture determination. The biggest temperature effect on εb was observed for the soil 569 at its highest moisture content; with the temperature increase of 50ºC its value decreased by 3.49. This temperature change of the TDR determined bulk dielectric permittivity corresponds to a decrease of the calculated soil moisture of 0.037 m3m-3, using the calibration from Topp et al. (1980).

Figure 6.

Set of reflectograms registered by the measurement setup for the same soil sample in different temperatures

The calibration curves for each soil taken for different soil temperatures meet at a characteristic moisture content value θeq, where the physical phenomena responsible for the temperature effect of soil dielectric permittivity equalize (Fig. 7). This moisture content is named the "equilibrium water content" in this study. For water contents below θeq, soil bulk dielectric permittivity εb measured at 5 C is smaller than the one measured at 55 C and for water contents above θeq the change of εb with temperature is opposite. The observed temperature effect of soil dielectric permittivity confirms the theory of Or & Wraith (1999 ), which explains it by the temperature caused exchange of water particles between free and bound phases.

The value of εb for air-dry soils does not depend on temperature. With the increase of soil moisture from air dry, there is an increase of εb with temperature. All soils except one (soil 562) have higher values of εb for 5 C than 55 C at high water contents, and the biggest difference is observed for the soils having medium values of S (Table 1). For the soil 562, there was no equilibrium water content observed in the analysed temperature range, although this soil does not have the highest value of specific surface area from all the tested soils. The bulk dielectric permittivity for this soil is higher at 55 C than for 5 C in the whole range of moisture from air dry state to almost saturation. The soil bulk electrical conductivity in low frequency range, σdc, for the soil 562 and for example the soil 565 at different temperatures and high moisture was compared.

Bulk electrical conductivity for the soil 562 ranged from 47 mSm-1 at 5 C to 192 mSm-1 at 55 C for θ = 0.3 m3m-3, while for the soil 565 the respective values were even bigger, i.e. they ranged from 50 mSm-1 at 5 C to 221 mSm-1 at 55 C for θ = 0.4 m3m-3, and still the temperature behaviour of the soil 565 dielectric permittivity was typical. This confirms the literature reports (Nadler et al., 1999; Or & Wraith, 1999) that the increase of soil bulk electric conductivity does not increase the TDR readout of εb in the presented variability range of σdc. Further studies are needed to diagnose the temperature effect of the soil 562.

Figure 7.

TDR calibration curves for three tested soils at different temperatures, S is the soil specific surface area, θeq is the equilibrium moisture where the temperature effect caused by the described two competing physical phenomena is compensated

The value of soil moisture at the equilibrium point, θeq, depends on the amount of bound water attracted by the soil, which is described by equation (10). The relation between the equilibrium water content, θeq, and the specific surface for the tested 19 soils, except the soil 562, is presented in Fig. 8.

Figure 8.

Empirical relation between the equilibrium water content, θeq, and soil specific surface, S, for the tested soils

The good correlation between the soil specific surface S and θeq confirms the assumed physical description of the processes involving the temperature effect of soil dielectric permittivity.

The temperature dependence of the soil bulk dielectric permittivity, εb, of the selected soils is presented in Fig. 9. The majority of tested soils show similar trends that confirm other experimental data (Pepin et al., 1995; Or & Wraith, 1999). For small and medium moisture values there is a negligible temperature effect and the linear trend lines in Fig. 9 are almost in parallel to the horizontal axis representing no or a small positive temperature change.

This is especially evident for the two trend lines representing the lowest moisture values in εb(T) relations for all soils in Fig. 9. For higher moisture values there is a tendency to decrease εb with temperature proving that the dominant reason for this behaviour is the decrease of free water dielectric permittivity with the temperature increase. However, as expected for the soils with large specific surface area this tendency is much smaller or has the opposite direction, as for the soil no. 562.

Figure 9.

Bulk dielectric permittivity temperature dependence of selected soils bulk dielectric permittivity for different soil volumetric water contents (θg stands for thermo-gravimetrically determined soil water content)

Other soils from the same group as the soil no. 562, i.e. no. 619 and no. 565 having larger values of soil specific surface area, 69∙103 m2∙kg-1 and 83∙103 m2∙kg-1 respectively, show typical temperature effect of soil dielectric permittivity, i.e. for moisture below θeq, εb increases with increasing temperature, and for moisture above θeq, εb decreases with increasing temperature. For all tested soils, except the soil no. 562, the slope was small and positive for low and negative for high soil moisture.

The applied models: 4-phase alpha and de Loor models do not follow the measured data εb(T) for all soils and for all moisture values. The examples of the performance of these models are presented in Fig. 10, for the soil no. 562 (S = 65∙103 m2kg-1).

Figure 10.

Performance of applied 4-phase soil dielectric mixing models for the soil no. 562. The assumed values for dielectric permittivity for soil solid phase εs=5 and bound water εbw=3.2

The alpha model has a fitting parameter representing the geometry of modelled medium (Roth et al., 1990) and enabling to adjust model data to the measured ones, as it was done in Fig. 10. The values of εb from the model data are generally higher than the TDR determined from the measurement. Therefore the applied correction of the temperature effect on the soil dielectric permittivity is based on empirical data and it accounts for the observed property of θeq. The applied correction turns the slope of the linear trend lines of the measured values of εb(T) to zero. The turning centre is the soil temperature of 25ºC (Fig. 9).

For each soil sample the temperature dependent value of soil moisture θTDR(T) was determined basing on the individual TDR soil calibration function giving the bulk dielectric permittivity values at different temperatures. Temperature corrected values of volumetric water contentθTDRcorr, were determined from the relationship between θTDR(T)and θeq, as follows:

For: θTDR(T)θeq:θTDRcorr=θTDR(T)[1A(θeqθTDR(T))(T25)]E14
For:θTDR(T)θeq:θTDRcorr=θeq+θTDR(T)θeq1+n25B[d(T)1]θTDRnE15

where: n = (εb)1/2 is the soil refractive index, n25 is its value at 25ºC, ∂θTDR/∂n is the slope of TDR calibration, for example the one taken from Topp et al. (1980) is 0.127.

Formula (14) refers to TDR determined soil moisture values not exceeding equilibrium water content, θeq, for which the temperature effect of the soil bulk dielectric permittivity increases its value, which is due to release of water molecules adsorbed by the surface of the soil solid phase. Formula (15) applies TDR determined soil moisture values exceeding equilibrium water content, θeq, when the temperature effect of the soil bulk dielectric permittivity is mainly from the temperature effect on free water, resulting in declining soil bulk dielectric permittivity with increasing temperature.

Parameters A = 0.008 and B = 0.55 are empirically adjusted to minimize the slope Δεb/ΔT for all examined soils. Because of good correlation between soil specific surface, S, and θeq (Fig. 8), the former can be applied from the fitted line.

Figure 11.

Errors of TDR determined soil moisture at various temperature values referenced to the respective values at 25 C: A - without temperature corrections, B - with temperature corrections based on (14) and (15)

The comparison of mean values and standard deviations of absolute errors for measured data, ΔθTDR, and temperature corrected data, ΔθTDRcorr, according to the temperature corrections (14) and (15) is presented in Fig. 11. The mean values for the both errors are calculated for 20 tested soils at six values of temperature from 5 C to 55 C with 10 C steps between.

The mean values of TDR determined soil moistures at tested soil temperatures are below the respective values at 25 C. The absolute measurement error of soil moisture measured by TDR, defined as double the standard deviation from the mean value does not exceed 1.5% of measured value. After applying the empirical correction given by (14) and (15) the absolute measurement error decreased almost three times to the value not exceeding 0.54%.

5. Summary

The temperature effect of the examined mineral soils’ bulk dielectric permittivity, εb, determined by TDR method, confirms the theory presented by Or and Wraith (1999), describing it as the result of two competing phenomena; εb increases with temperature increase following the release of bound water from soil solid particles and εb decreases with temperature increase following the temperature effect of free water molecules.

It has been found that there is a soil type characteristic moisture value, θeq, named the equilibrium water content, having the specific temperature property. The temperature effect for this soil water content value is not present, which means that at θeq the both competing phenomena mentioned earlier compensate each other. The equilibrium water content, θeq, is correlated with the soil specific surface area. For soils with water content below θeq, the temperature effect of soil dielectric permittivity is positive, i.e. it increases with temperature, and for soils with water content above θeq, the temperature effect of soil dielectric permittivity is negative, i.e. it decreases with temperature.

The temperature correction formula adjusting the soil moisture determined by TDR at various temperature values to the corresponding value at 25 C, based on knowledge of θeq, decreases the standard deviation almost three times as compared to uncorrected values of θTDR. The electrical conductivity of the examined soils does not show any influence on the observed temperature effect of soil dielectric permittivity.

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Wojciech Skierucha (June 21st 2011). Time Domain Reflectometry: Temperature-dependent Measurements of Soil Dielectric Permittivity, Electromagnetic Waves, Vitaliy Zhurbenko, IntechOpen, DOI: 10.5772/17162. Available from:

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