Soil Salinity Assessment Using Saturated Paste and Mass Soil:Water 1:1 and 1:5 Ratios Extracts

: Soil salinization is directly related to the quantity and quality of food production, and often, to increased energy demands for high-quality irrigation water. Reliable monitoring of soil salinity based on a less laborious method than the soil saturated paste (SP) extract methodology is required. In the present study, an attempt is made to relate the electrical conductivity (EC) of the soil saturated paste (SP) extract (EC e ) with the EC determined in the 1:1 and 1:5 soil over water mass ratios, (soil:water) extracts (EC 1:1 and EC 1:5 ). EC e , EC 1:1 , and EC 1:5 values were obtained for 198 soil samples from ﬁve different locations in Greece. The results have shown that strong linear relationships exist between the EC e and the EC 1:1 and EC 1:5 values (R 2 > 0.93), and that the slopes of these linear relationships decreased from coarse to ﬁne soil types. For 123 soil samples, the concentrations of K + , Na + , Ca 2+ , Mg 2+ , and Cl − were also determined in the extracts of the three applied methodologies. Ion concentrations in the 1:1 and 1:5 extracts were highly correlated with the respective ion concentrations in the SP extracts. These ﬁndings strongly suggest that EC 1:1 and EC 1:5 values can be safely used for the estimation of EC e .


Introduction
All terrestrial life ultimately depends on soil and water. So commonplace and seemingly abundant are these ecosystem components that we tend to treat them with contempt [1]. Today, the explosive growth of human population makes it necessary to increase productivity. Intensification of irrigated agriculture is no longer the solution. The ability of natural resources (soil and water) to produce food is limited, and the exploitation of land and water resources beyond certain limits will result in soil degradation and lower productivity. Modern irrigated agriculture, exercised in arid or semi-arid places, depends to a large extent on water that is abstracted from underground aquifers. A direct consequence of this is the necessity of pumping water from deeper and deeper wells, which requires the use of larger and larger amounts of energy. Moreover, overexploitation of unconfined underground aquifers in coastal areas leads gradually to reversing the direction of the hydraulic head gradient, and inevitably, to sea-water intrusion, with its adverse effects on water quality manifesting in secondary soil salinization.
Soil salinity is a basic factor that, to a large extent, determines soil suitability for agricultural productivity. Apart from secondary soil salinization, another predominant mechanism for salt accumulation in irrigated agricultural soils is evapotranspiration, a process that promotes salts concentration in the remaining soil water. The problem of soil salinity is growing in arid and semi-arid regions. Approximately 995 million hectares of land around the world are estimated to suffer from salinity problems [2]. Adequate knowledge of the amount and distribution of salt is required for the management of saline soils. Soil salinity assessment is based on measurements of the electrical conductivity of saturated paste extracts (EC e ); this has been established as the standard method [3]. In addition, EC e simulates a naturally-occurring state of the soil solution, and can be related to plant-growth response. Unfortunately, this method is tedious, time consuming, and requires skills and expertise to reach saturation point, especially for clay soils [3]. EC e determination in SP extracts from a large number of soil samples, as in cases of salinity monitoring that involves repeated soil sampling from different parts of the field during the growing season, appears to be difficult and laborious [4].
For these reasons, instead of measuring EC e, many researchers have suggested that it would be easier to determine EC in various soil over water mass ratios (soil:water) extracts, such as 1:1, 1:2, 1:2.5, 1:5. The most widely-used soil over water mass ratios, (soil:water), are the 1:1 and the 1:5. The ratio of 1:5 is preferred for the assessment of soil salinity in Australia and China [5,6], while the ratio 1:1 is commonly used in the United States [6]. Predetermined and fixed soil over water mass ratios applied in various methodologies result in time reductions for the preparation and acquisition of the extracts, in comparison to the EC e methodology. However, due to the higher dilution of soil solutions, ion concentrations and EC 1:1 and EC 1:5 values are usually lower than those obtained by the EC e protocol. It is to be noted that soil over water mass ratios are weakly correlated with actual soil conditions. These methods can be very useful in practice when one is not interested in determining the absolute EC values or the absolute soil-salt concentration, but rather, is seeking to determine their relative changes. A serious disadvantage of methods measuring EC in the various soil over water mass ratios extracts is the effect of higher water quantities on the solubility of less soluble salts such as gypsum or lime. For gypsum, as the dilution increases, the concentration of all ions decreases, except of the Ca 2+ and the SO 4 2− concentrations, that remain relatively constant. In this respect, due to the presence of less soluble salts in soils containing gypsum or lime, as the degree of dilution increases, ions concentration changes considerably in relation to their respective concentrations in the natural soil solution [3,7,8].
Although strong linear relationships between EC e and EC 1:1 or EC 1:5 have been reported, the coefficients entering these relationships are not constant, but vary according to the area of interest. The causes leading to such variation are not yet clear. The relationship between EC e and EC of different soil-water extracts is affected by the soil texture and the presence of salts and gypsum in the soil [3]. The equilibration time and method are probably additional factors that have led to the observed differences among various models [9]. Thus, a better understanding of the transferability of these models would provide managers with more information about the accuracy of the EC e values derived from non-local EC conversion models. The respective EC e = f (EC 1:1 ) and EC e = f (EC 1:5 ) equations, together with the appropriate references, are given Table 1.
The relationship EC e = f (EC 1:1 ), as proposed by USDA [3], has the form EC e = 3 (EC 1:1 ). However, this model was not weighted for soil texture or organic matter-content effects on the composition and EC of soil extracts [10]. Sonmez et al. [8] and Franzen [10] studied the EC relationships in three different soil types and proposed a different equation for each soil type (Coarse, Medium, Fine).
The indices a,b,c refer to coarse, medium and fine soils respectively. The indices d and e refer to the presence or absence of gypsum, respectively. The equation of [18] refers to a gypsum mass percentage <0.2%. Chi and Wang [12] presented cases considering the range of θ SP variation. Their first equation corresponds to a range of θ SP between 20% and 45%, while their second to a range between 45% and 63%. The third equation corresponds to the full range of θ SP variation, i.e., between 20% and 63%. The index f refers to combined soil texture.
The possibility for the EC e prediction from EC 1:5 measurements has been investigated in a number of regions worldwide [4,8,9,[11][12][13][14]. In these studies, soil texture, specific salts presence, and organic matter content effects were taken into consideration [8,11,12,14,15]. Less examined is the subject of EC 1:5 measurement in relation to the methodology, followed for the acquisition of the soil over water mass ratio extract [7]. Slavich and Petterson [12] gave an expression for the multiplicative f factor in the EC e = f EC 1:5 relationship according to the Equation (1) below, where θ SP denotes the saturation percentage.
Moreover, these authors presented the range and the values of θ SP as a function of clay content. From Equation (1), the increase of θ SP leads to a decrease of f. In other words, the conversion rate increases as the soil becomes coarser.
Visconti et al. [18] presented EC e = f (EC 1:5 ) relationships for soils with gypsum mass percentages between 0.2-1.5% and >1.5%. They concluded that when the gypsum mass percentage is less than 0.2%, the relationship EC e = f (EC 1:5 ) is strongly linear.
Khorsandi and Yazdi [4], comparing EC e and EC 1:5 values for soils from Iran, suggested that gypsum concentration has by far a greater impact on the accuracy of EC e predicting models than soil texture.
He et al. [7,9] tested three agitation methods for the determination of the EC 1:5 ; for each method, nine agitation times were applied. The three agitation methods were (i) shaking plus centrifuging; (ii) shaking; and (iii) stirring. They report that different methods of 1:5 soil over water mass ratio preparation could yield different EC 1:5 values. These authors also found that agitation time depends on the EC e value, and proposed a higher agitation time if EC e < 4 dS m −1 . He et al. [9] presented EC e = f (EC 1:5 ) models for each different method of acquiring values of EC 1:5 . Their results indicate that for all the tested soil samples, the ln-transformed model is better than the non-transformed and the exponential models. Moreover, when the EC e data were separated at EC e = 4 dS m −1 , very good results were obtained for EC e < 4 dS m −1 from the quadratic curvilinear model. Aboukila and Norton [11] proposed a correlation equation EC e = f (EC 1:5 ) for EC e values up to 10.3 dS m −1 for the clay agricultural soils of north Egypt, while Aboukila and Abdelaty [15] presented the respective equation for coarse soils. It was observed from these two equations that the slope of the lines was higher for the coarse soils.
Very few works from those mentioned above studied simultaneously the relationships between the ion concentrations obtained by the different methodologies. USDA [3], Sonmez et al. [8], Hong and Henry [16], and Zhang et al. [17] presented relationships between the ion concentrations for the methods EC e and the EC 1:1 . Sonmez et al. [8] and Ozkan et al. [14] presented relationships between the ion concentrations for the methods EC e and the EC 1:5 . Sonmez et al. [8] presented the distinct relationships between the ion concentrations for the three methodologies (EC e , EC 1:1 and EC 1:5 ) for each soil type (sandy, loamy, clay).
To estimate ions concentration in EC e method extracts, from EC 1:1 method extracts data, USDA [3] proposed the conversion coefficients 2.78 and 1.67 for the monovalent and for the divalent ions respectively based on the chemical solubility in aqueous systems".
The lack of substantial research on the relationships between the various methods and the produced equations could lead to incorrect estimations of the ion concentrations in SP extracts, especially when these equations are to be applied in areas with different soil types [10].
In Greece, quite often, the EC 1:1 and EC 1:5 methods are used for soil salinity assessment. Nonetheless, no equations relating EC e and EC 1:1 or EC 1:5 , as well as ion concentrations, are proposed or used.
The present work aims to investigate (i) the relationships EC e = f (EC 1:1 ) and EC e = f (EC 1:5 ) for soil samples collected from five areas of Greece, and to compare the estimated EC e values with EC e values derived from models developed for other regions in the world; and (ii) the relationships between major cations and Cl anion concentrations of saturation paste extract and of the respective ion concentrations in 1:1 and 1:5 extracts.

Materials and Methods
A total of 198 surface soil samples (0-15 cm depth) presenting low organic carbon content (less than 1% for most cases) were collected from five areas over Greece, and more specifically, from the Prefectures of Evia (49 samples), Lakonia (12 samples), Preveza (7 samples), Argolida (90 samples), and from the island of Kos (40 samples) ( Figure 1). Most of the soils were under different crop cultivations, while some were non-cultivated. The selected soils represent irrigated soils of different soil salinity levels. Soil samples from Argolis were collected after the end of the irrigation period, i.e., August, and at the end of the rainy season, i.e., March of the next year. Soil sample collection from the other areas was performed during the irrigation season (June to August).
The mean value of the rainfall per year (mm) in each prefecture was: Argolida 500, Evia 500, Laconia 750, Preveza 1000, and Kos 550 mm, respectively.
After collection, the soil samples were transferred to the Agricultural Hydraulics Laboratory and left to air dry. The air-drying process, depending on the soil type of the sample and its initial soil moisture, could last for three to seven days. Afterwards, the samples were ground and passed through a 2 mm sieve. Using the standard method [19], for the preparation of the saturated pastes, 350 g of air-dried soil were used and the soil pastes were left for 24 h to reach equilibrium. Subsequently, the vacuum extracts were collected and electrical conductivity EC e was measured by a conductivity meter (WTW, Cond 315i). For the saturation percentage determination (SP%), a subsample of each paste was oven dried at 104 • C for 24 h. than 3% for AAS and flame photometer determinations. Potentiometric titration with silver nitrate was used to determine Cl − concentrations. Statistical analysis of the data concerning both the electrical conductivities ECe, EC1:1, EC1:5, as well as the ion concentrations of K + , Na + , Ca 2+ , Mg 2+ , and Cl − , as well as the SP, included their mean, median, and minimum-maximum values, and their standard error. For the relationships ECe = f (EC1: 1) and ECe = f (EC1:5), a least-squared linear regression was performed and the coefficient of determination R 2 was evaluated. The R 2 coefficient assesses how well a model (in our case the aforementioned relationships) explains and predicts future outcomes, and is used as a guideline to measure the accuracy of the model. Statistical analysis was performed using IBM SPSS Statistics 20 software.

Electrical Conductivity and Ions Concentration in the Extracts of the Three Methods
According to [20], the ECe, EC1:1, and EC1:5 values of the 198 soil samples were classified into three classes, i.e., 0-2, 2-4 και > 4 dS m −1 , presented in Table 2 along with their respective percentages. The soil sample electrical conductivities varied between 0.47 and 37.5 dS m −1 for the saturation paste extract, from 0.16 to 20.1 dS m −1 for the 1:1 extract, and from 0.10 to 5.08 for the 1:5 extract. From these findings, it is obvious that a wide range of EC values was used to compare the SP method with the EC1:1 and the EC1:5 methods.
According to the measured Saturation Percentage values (SP%), 30 samples (15.1%) showed SP% values ranging between 20 and 45%, and 168 samples (84.9%) exhibited SP% values > 45%. Thus, the great majority of the soil samples correspond to fine soil textures [12].  For the 1:1 soil over water ratio in 100 g of soil sample, 100 mL distilled water was added and the mixture was shaken for 1 min by hand, 4 times at 30 min-intervals, and soon thereafter, the extract was obtained [8,19]. For the 1:5 soil over water ratio in 50 g of soil, 250 mL distilled water was added and the same process was followed.
EC e , EC 1:1 , and EC 1:5 values were determined for all 198 samples. while for 123 soil samples, the concentrations of K + , Na + Ca 2+ , Mg 2+ and Cl − were also measured in the extracts of the three applied methods. In the various soil solution extracts, K + and Na + concentrations were determined by flame photometer, and Ca 2+ and Mg 2+ concentrations by an atomic absorption spectrometer (Varian AA-300). For quality control, internal standards provided by Merck were used, and a control sample was analyzed every 20 samples. Reproducibility was tested by re-analyzing 30% of the samples. The analytical precision, estimated as relative standard deviation (RSD) of three measurements, was less than 3% for AAS and flame photometer determinations. Potentiometric titration with silver nitrate was used to determine Cl − concentrations.
Statistical analysis of the data concerning both the electrical conductivities EC e , EC 1:1 , EC 1:5 , as well as the ion concentrations of K + , Na + , Ca 2+ , Mg 2+ , and Cl − , as well as the SP, included their mean, median, and minimum-maximum values, and their standard error. For the relationships EC e = f (EC 1:1 ) and EC e = f (EC 1:5 ), a least-squared linear regression was performed and the coefficient of determination R 2 was evaluated. The R 2 coefficient assesses how well a model (in our case the aforementioned relationships) explains and predicts future outcomes, and is used as a guideline to measure the accuracy of the model. Statistical analysis was performed using IBM SPSS Statistics 20 software.

Electrical Conductivity and Ions Concentration in the Extracts of the Three Methods
According to [20], the EC e , EC 1:1 , and EC 1:5 values of the 198 soil samples were classified into three classes, i.e., 0-2, 2-4 και > 4 dS m −1 , presented in Table 2 along with their respective percentages. The soil sample electrical conductivities varied between 0.47 and 37.5 dS m −1 for the saturation paste extract, from 0.16 to 20.1 dS m −1 for the 1:1 extract, and from 0.10 to 5.08 for the 1:5 extract. From these findings, it is obvious that a wide range of EC values was used to compare the SP method with the EC 1:1 and the EC 1:5 methods. Thus, the great majority of the soil samples correspond to fine soil textures [12].
The mean EC value for the SP extract was approximately 2 and 6.5 times higher than the EC values in the 1:1 and 1:5 extracts respectively ( Table 2). Our expression for the relationship EC e = f (EC 1:1 ) is almost identical to that of [8,17], who reported approximately twofold dilution when they compared the EC value of SP extract to that of 1:1 soil/water extract. For the relationship EC e = f (EC 1:5 ), the results of the present study are similar to those of [11], who reported that the mean EC e value was 5.7 times higher than EC 1:5 . In contrast, [8] reported a stronger dilution effect, since they found that the mean EC e value was 8 times higher than the mean EC 1:5 value.
Mean ion concentrations in the extracts of the different methodologies applied on the 123 soil samples showed similar trends to the relationships between the corresponding electrical conductivities (Table 3). Depending on the ion, the mean ion concentrations in the SP extract were higher, from 1.5 to 1.9 and from 4.11 to 7.5 times, compared to the respective ion concentrations in the EC 1:1 and EC 1:5 extracts.

The Relationship between EC e and 1:1 Method
For all studied soil samples, the linear relationship between EC e and EC 1:1 values is presented in Figure 2. The produced equation was EC e = 1.83 × EC 1:1 − 0.117 and the coefficient of determination value was close to unity (R 2 = 0.973).  Both the slope and the coefficient of determination values were higher for the soils with SP% values in the range 20-45%. Indeed, for SP% values between 20 and 45%, slope and R 2 values were 2.11 and 0.992, while for SP% > 45%, the respective values were 1.79 and 0.973. This outcome indicates that the ECe versus EC1:1 relationship was affected by the soil type, since the saturation percentage depends strongly on the clay content, as well as on the type of the clay [12,13]. When the soil texture changes from coarse to fine, a decreasing slope trend was observed in accordance with the results of [8,10,16]. The stronger ECe versus EC1:1 relationship for coarser soils suggests that for soils with values of SP% < 45%, ECe can be predicted accurately from EC1:1 data. Furthermore, in this study, the characteristics of ECe = f (EC1:1) equation for all soils (Figure 2) are almost identical to those of the ECe = f (EC1:1) equation for fine-textured soils (Figure 3 right). However, this is a reasonable result considering that most of the studied soil samples were of fine texture. These results are similar to the findings of other researchers, since strong linear relationships between EC e and EC 1:1 are reported in the literature. According to the findings of this study, the slope value of EC e = f (EC 1:1 ) relationship was 1.83, close to the slope values of 1.56 and 1.79 (for combined soil textures) reported by [16], and by [17] and to the slope value of 2.03 reported by [8], for fine textured soils. Nonetheless, significantly different slope values were produced by [3] and [10], who found slope values of 3 for the fine textured soils and 2.96 for combined soil textures. Further data processing indicated that neither the slope value (1.847) nor the coefficient of determination (R 2 = 0.97) changed significantly by fitting the data to linear correlation with an intercept equal to zero (i.e., the line passes from the origin), suggesting that the produced EC e = f (EC 1:1 ) equation can be reliably applied, even for soils with extremely low salinity levels.
The studied soil samples were grouped according to their Saturation Percentage (SP%) values, and two EC e = f (EC 1:1 ) linear curve fitting prediction equations were produced (Figure 3).  Both the slope and the coefficient of determination values were higher for the soils with SP% values in the range 20-45%. Indeed, for SP% values between 20 and 45%, slope and R 2 values were 2.11 and 0.992, while for SP% > 45%, the respective values were 1.79 and 0.973. This outcome indicates that the ECe versus EC1:1 relationship was affected by the soil type, since the saturation percentage depends strongly on the clay content, as well as on the type of the clay [12,13]. When the soil texture changes from coarse to fine, a decreasing slope trend was observed in accordance with the results of [8,10,16]. The stronger ECe versus EC1:1 relationship for coarser soils suggests that for soils with values of SP% < 45%, ECe can be predicted accurately from EC1:1 data. Furthermore, in this study, the characteristics of ECe = f (EC1:1) equation for all soils (Figure 2) are almost identical to those of the ECe = f (EC1:1) equation for fine-textured soils (Figure 3 right). However, this is a reasonable result considering that most of the studied soil samples were of fine texture. Both the slope and the coefficient of determination values were higher for the soils with SP% values in the range 20-45%. Indeed, for SP% values between 20 and 45%, slope and R 2 values were 2.11 and 0.992, while for SP% > 45%, the respective values were 1.79 and 0.973. This outcome indicates that the EC e versus EC 1:1 relationship was affected by the soil type, since the saturation percentage depends strongly on the clay content, as well as on the type of the clay [12,13]. When the soil texture changes from coarse to fine, a decreasing slope trend was observed in accordance with the results of [8,10,16]. The stronger EC e versus EC 1:1 relationship for coarser soils suggests that for soils with values of SP% < 45%, EC e can be predicted accurately from EC 1:1 data. Furthermore, in this study, the characteristics of EC e = f (EC 1:1 ) equation for all soils (Figure 2) are almost identical to those of the EC e = f (EC 1:1 ) equation for fine-textured soils (Figure 3 right). However, this is a reasonable result considering that most of the studied soil samples were of fine texture.
A strong linear relationship was also found between the ion concentrations in the SP and the 1:1 extracts (N = 123), with coefficients of determination (R 2 ) ranging from 0.88 to 0.973 (Table 4). The obtained relationships are shown with or without intercept to facilitate the comparison with similar published findings. In most cases, R 2 values suggest strong or sufficient linearity. However, stronger relations were observed for K + and Cl − than for Na + , Ca 2+ , and Mg 2+ , implying that further detailed characterization of the studied soils is needed to elucidate these results. The slope values of the ion concentration equations for monovalent ions (K + , Na + and Cl − ) were certainly lower than those reported by [3] (2.78) while those for divalent ions (Ca 2+ and Mg 2+ ) were very similar (1.67).

The Relationship between EC e and 1:5 Method
In Figure 2, the relationship between EC e and EC 1:5 is also shown. The EC e = f (EC 1:5 ) relationship is given by the expression EC e = 6.53 × EC 1:5 − 0.108, and the coefficient of determination (R 2 = 0.931) indicates a strong linearity. By imposing the line to pass from the origin, the slope value remained practically unaffected, while the respective equation is EC e = 6.47 × EC 1:5 . These findings are similar to those of other researchers [4,8,11,12,14] who also reported strong linearity for the EC e = f (EC 1:5 ) relationship. Nevertheless, our results do not match exactly with the findings of other studies but lie in between them, since our slope value was lower than that found by [4] (7.94), and higher than that obtained by [11] (5.04).
These differences may be attributed to the clay content and the clay type of the examined soils. However, the observed variation of the results among the various studies can be most likely attributed to the different methodologies used for the EC 1:5 determinations. Such differences seem to be a key factor that considerably affects the EC e and EC 1:5 relationship [9]. This is further supported by the fact that the soils examined in the present work presented similar characteristics, negligible gypsum contents, and medium to fine textures, as did those in the works used for comparison. Therefore, the different methodology applied in the present work for the acquisition of the EC 1:5 values appears to be the chief factor for the observed deviating results from those reported in other studies. Apart from this, another probable factor that could have affected the acquisition of EC 1:5 in this work is, compared to the other similar works, the broad range of the EC e values from which the EC e = f (EC 1:5 ) relationship was estimated. Thus, these two factors can be considered as being responsible for the fact that our findings produced slope values for the EC e = f (EC 1:5 ) expression that were close but not identical to similar findings presented in the literature. The predicted EC e values obtained by the ln-transformed (ln(EC e ) = f (ln(EC 1:5 )) and by the linear models (EC e = f (EC 1:5 ) were plotted against the actually measured EC e values ( Figure 4). In addition, the determination of the ECe = f (EC1:5) relationship according to SP% values of the tested soils samples produced higher slope values for SP% in the range of 20-45%, indicating that the finer the soil texture, the lower the slope of the estimating equation (data not shown).
The linear equations included in Table 5 show that the ion concentrations in the SP extracts are highly related to the respective ion concentrations obtained for the 1:5 extracts. The R 2 values for all ion equations, except Na + , are lower in comparison to the respective R 2 values of the 1:1 method (Table 4), indicating that ions concentrations in 1:1 extracts are better estimators for the actual ion concentrations in the SP extracts. The lowest coefficients οf determination were obtained for Ca 2+ and Mg 2+ . In all cases except Κ + , the slope values are lower than those mentioned by [8] either for combined soil texture or for fine textured soils.

Conclusions
The results of this study support that it is possible to accomplish a high degree of accuracy for ECe predictions from the more easily measured EC values in the 1:1 and 1:5 soil/water mass ratios extracts using the obtained relationships. Comparing ECe = f (EC1:1) and ECe = f (EC1:5) relationships, a higher coefficient of determination was found for ECe = f (EC1:1), suggesting that, under the experimental conditions of this work, EC values of 1:1 extracts appear to be better estimators for ECe. However, the ln-transformed model provided quite accurate results for the estimation of ECe from  As is shown in Figure 4, values predicted by the ln-transformed model EC e values are closer to the 1:1 line, and provide better results than the EC e values obtained by the linear model. This is in line with [9], who reported strong linear relations between the measured and the values predicted by ln-transformed model EC e values for the four cases of equilibrium they examined to determine EC 1:5 . It must be noted that the majority of the soil samples (67%) that these authors used in their work had SP% values in the range 20-45%, while in the present work, only the 15.1% of the soils are included in this range. Therefore, the ln-transformed model seems to have a general validity for all soil types, and in this sense, it is a reliable methodology for the estimation of EC e from EC 1:5 measurements.
In addition, the determination of the EC e = f (EC 1:5 ) relationship according to SP% values of the tested soils samples produced higher slope values for SP% in the range of 20-45%, indicating that the finer the soil texture, the lower the slope of the estimating equation (data not shown).
The linear equations included in Table 5 show that the ion concentrations in the SP extracts are highly related to the respective ion concentrations obtained for the 1:5 extracts. The R 2 values for all ion equations, except Na + , are lower in comparison to the respective R 2 values of the 1:1 method (Table 4), indicating that ions concentrations in 1:1 extracts are better estimators for the actual ion concentrations in the SP extracts. The lowest coefficients of determination were obtained for Ca 2+ and Mg 2+ . In all cases except K + , the slope values are lower than those mentioned by [8] either for combined soil texture or for fine textured soils.

Conclusions
The results of this study support that it is possible to accomplish a high degree of accuracy for EC e predictions from the more easily measured EC values in the 1:1 and 1:5 soil/water mass ratios extracts using the obtained relationships. Comparing EC e = f (EC 1:1 ) and EC e = f (EC 1:5 ) relationships, a higher coefficient of determination was found for EC e = f (EC 1:1 ), suggesting that, under the experimental conditions of this work, EC values of 1:1 extracts appear to be better estimators for EC e . However, the ln-transformed model provided quite accurate results for the estimation of EC e from the EC 1:5 measurements. The slope values in both 1:1 and 1:5 are higher for coarse (20% < SP < 45%) than for fine soils (SP > 45%).
Differences between the slope value of the relationship EC e = f (EC 1:5 ) and the slope values of similar relationships reported by other researchers could be attributed mainly to the different methodologies used for the EC 1:5 measurements, to diverse physicochemical soil characteristics, and to the wider range of the EC e values used in this work.
Based on the results of the highly-correlated equations obtained, it can be concluded that the 1:1 and 1:5 methods can be used to estimate the ion concentration in the SP extract.
No doubt, additional work is needed to further improve the accuracy of EC e predictions through the EC 1:1 or EC 1:5 methodologies by including more data for soil samples from other regions of the country.