Cemented Horizons and Hardpans in the Coastal Tablelands of Northeastern Brazil

: Horizons with varying degrees of cementation are a common feature of the soils from the coastal tablelands of Northeastern Brazil. In most cases, these horizons are represented by the following subsurface horizons: fragipan, duripan, ortstein, and placic. The aims of this study were to analyze differences regarding the development and the degree of expression of cementation in soils from the coastal


INTRODUCTION
Horizons with varying degrees of cementation are a common feature of soils from the coastal tablelands of Northeastern Brazil (Araújo Filho, 2003).In most cases, these horizons are represented by the following subsurface horizons: fragipan, duripan (duric character), ortstein (cemented spodic horizon), and placic (Soil Survey Staff, 1999;Santos et al., 2013).Moreover, detailed soil maps (1:100,000 or greater) have shown that the geographic expression of such horizons in the coastal tableland soils is greater than that represented on more generalized maps of the region (Araújo Filho et al., 1999;Araújo Filho, 2003;Curi and Ker, 2004).The cemented horizons usually occur in Argissolos Amarelos (Udults and Ustults), Argissolos Acinzentados (Udults and Ustults), and Espodossolos (Spodosols), but they are also found in Neossolos Quartzarênicos (Quartzipsamments), Planossolos Háplicos (Quartzipsamments), and other soil classes from the Brazilian System of Soil Classification (Santos et al., 2013).The ortstein is a cemented spodic horizon, which is typically influenced by organometallic complexes.The placic horizon is a thin pan of black to dark-red color, cemented by Fe (or Fe and Mn) and organic matter.This horizon may or may not be associated with the spodic horizon (Soil Survey Staff, 1999;Santos et al., 2013).
Whether the presence of cementing agents is necessary for a horizon to be diagnosed as a fragipan is still disputed (Aide and Marshaus, 2002;Weisenborn and Schaetzl, 2005), or not very relevant (Certini et al., 2007).The development of fragipans by the compression of particles has been explained by different theories, which are not mutually exclusive: past periglacial conditions (Bryant, 1989;Payton, 1992) and water-driven collapse deposits (Assallay et al., 1998), including the effect of earthquakes in the liquefaction of waterlogged deposits (Green et al., 2005).Several studies, along with Soil Taxonomy (Soil Survey Staff, 1999), report the relevance of low-crystallinity materials, such as Si, Fe, and Al compounds, regarding expression of two of the most singular properties of a fragic material: breakability under moist conditions, due to sudden rupture of aggregates under pressure (the air is vigorously expelled as the pores are saturated with water); and the soil aggregate slaking after a relatively short time period of water immersion (Norfleet and Karathanasis, 1996;Duncan and Franzmeier, 1999).
Unlike the concept of the fragipan, which does not require the presence of a quantity of Si that characterizes it as a cementing agent, the duripan is necessarily cemented by a silification process (Norton, 1994;Schaetzl and Anderson, 2013).Such a process predominantly occurs in the small pores and in the grain-to-grain contacts, without a total filling of the spaces between grains (Chadwick et al., 1987).
In the coastal tablelands, cemented horizons occur in sandy loam, sandy clay loam, and loamy sand textured soils (their occurrence is uncommon in soils with a texture which approximates sandy clay).They occur in spodic and textural B horizons located in the extensive plateaus with flat relief, mainly when associated with closed depressions (Filizola et al., 2001).The associated climate is humid tropical.However, the occurrence of cemented horizons tends to increase in dry summer conditions, on latitudes north of the city of Salvador, BA (Ribeiro, 1998).
In order to contribute to understanding the processes that regulate the cementation of pedogenetic horizons in the coastal tablelands of Northeastern Brazil, the aim of this study was to analyze the different development conditions of such horizons, and to evaluate the degree of cementation in these soil materials, which were sampled in four pedons.Expression of the degree of cementation was verified according to field morphology and through immersion of parts of the cemented materials in water, as well as in acid and basic solutions.The soil horizons were characterized through morphological, physical, micromorphological, mineralogical, and chemical properties in order to understand the genesis of these cementations.
Tertiary sediments from the Barreiras Formation compose the parent material of all the pedons analyzed.The sites sampled were located from the shoulders to the summits of the landscape, under flat relief, with 0-1 % slope.The soil drainage ranges from moderate to imperfect.
These sediments are mineralogically homogeneous in the clay fraction (extremely kaolinitic, very little oxidic), yet highly variable in particle size (Resende et al., 2011).The areas of Coruripe, Umbaúba, and Acajutiba (p-EK, p-PAC, and p-SX) have a humid tropical climate with dry summers, whereas Nova Viçosa (p-ESK) has a humid tropical climate with no dry season, i.e., the lowest average monthly rainfall is above 60 mm.The coastal tablelands comprise an area of approximately 52,811 km 2 within three states (Alagoas, Sergipe, and Bahia) where the pedons were described and sampled (Silva et al., 1993).The Coruripe site (p-EK) is the only area studied under primary forest (Silva et al., 1993).The Acajutiba (p-SX) and Nova Viçosa (p-ESK) areas are under areas planted to eucalyptus, whereas the Umbaúba area (p-PAC) is located in an area planted to 'Pera' orange.

Soil description, sampling and analysis
Pits were dug for morphological description, sampling the horizons of each pedon, and soil classification, which was complemented by laboratory analysis (Santos et al., 2013).Undisturbed soil samples were collected in the horizons selected for micromorphological analysis.Duplicates of disturbed soil samples were also collected, and one sample was kept under refrigeration for extraction of the soil solution.Soil clods were collected from the cemented horizons for immersion tests.In such horizons, as well as in other horizons with hard to extremely hard soil consistency, in which Kopecky ring samples of known volume could not be collected, soil clod samples were also gathered for analysis of bulk density (BD).The disturbed and unrefrigerated soil samples were air-dried, crushed, and sieved (2 mm mesh), in order to obtain Air-Dried Fine Earth (ADFE).Clay samples were separated from the ADFE by sedimentation after chemical dispersion (1 mol L -1 NaOH) and were used for X ray diffraction studies (35 kV, 25 mA, and CoKα radiation).Bulk density was determined using the volumetric ring method or the clod method, depending on the sample type (Archer and Smith, 1972).Particle size distribution was determined according to the pipette method (Gee and Bauder, 1986) using a NaOH solution as a chemical dispersant; pH was measured in water and KCl; organic C was determined according to the Walkley and Black method (Walkley, 1946).Ca, Mg, and Al were determined through KCl extraction (McLean et al., 1958); K and Na, through HCl extraction (Mehlich, 1953); H+Al, through a calcium acetate extraction at pH 7 (Shaw, 1959); and P, through extraction by Mehlich-1 (Mehlich, 1953).Iron and Al contents were determined by atomic absorption, using the ADFE after sieving through a 100 mesh, according to the following extraction processes: dithionite-citrate-bicarbonate (Mehra and Jackson, 1960;Jackson, 1974); acid ammonium oxalate (according to the Tamn method); and sodium pyrophosphate, the last two adapted from Wang (1978).Silica was determined in acid ammonium oxalate (Wang, 1978) through plasma spectrometry produced by inductive coupling (ICP-AES).Thin sections were prepared from the undisturbed samples for micromorphological characterization (Murphy et al., 1977;Ringrose-Voase, 1991;Castro et al., 2003).Images were acquired using a Sony ® digital camera (DFW-X700 model) coupled to a Zeis ® polarizing petrographic microscope.Interpretations followed the terminology defined by Brewer (1976), Bullock et al. (1985), and Lima et al. (1985).
The aqueous solution was extracted from the refrigerated samples through shaking, centrifugation, and extract filtering (soil: water ratio of 1:0.5) (Rhoades, 1982).The extract was used for determining dissolved organic C in a carbon analyzer, and Fe and Al were determined by atomic absorption.For Si analysis, 5 mL of the aqueous extract was mixed with 0.5 mL of 7.5 % sulphomolybdic acid solution (7.5 g of ammonium molybdate + 10 mL of 9 mol L -1 sulfuric acid completed to 100 mL with distilled water.After a 10 min resting period, 1 mL of a 20 % tartaric acid solution was added, and after a 5 min resting period, 5 mL of 0.3 % ascorbic acid was added.After 1 h, Si was read in a 600 nm wavelength spectrophotometer.

Immersion test of cemented materials in water and in acid and base solutions
Fragments of seven cemented horizons of 0.05 to 0.1 m in size were immersed in water (8 h) and in solutions of HCl (1, 3, and 6 mol L -1 ; evaluations at 4, 6, 7, and 8 days) and NaOH (1 and 4 mol L -1 ; evaluations at 4, 6, 7, and 8 days) and were evaluated according to Araújo Filho (2003).

Soil morphology and physical properties
All the pedons studied had features which relate to drainage impediments.They are located on predominantly flat relief, with some degree of concavity.Features associated with redoximorphic conditions are present, expressed in pale colors, mottlings, and bands of Fe oxide segregation (Table 1, Figure 2).The cemented and/or hardened horizons (apparently cemented) are located in the lower parts of the sequa, coinciding with illuvial horizons.
Of the four soils studied, three had features indicating podzolization in the upper portion of the sequum, with spodic horizons or spodic character beneath the eluvial horizons (Silva et al., 2013).The podzolization process is intense in p-EK and p-ESK and only incipient in the p-SX (not enough to classify it as a Spodosol).The p-PAC presented argilluviation as the main pedogenesis process.The p-SX, p-EK, and p-ESK, which exhibited podzolization, had, below the A horizon, an eluvial E horizon of relatively paler colors in relation to its neighboring horizons, single-grained structure, loose or very friable consistency, and clay contents always below 100 g kg -1 (Tables 1 and 2, and Figure 2).
The cemented horizons of p-SX and p-EK (identified as Btgm) displayed both duric character and gleying features.These features occurred beneath the horizons with podzolization in each pedon, acting as an impervious layer at the subsurface and favoring the occurrence of podzolization, which is also favored by other conditions, such as flat relief, concave topography, and sandy-quartzous parent material (Oliveira et al., 2010;Silva et al., 2013).The p-ESK also had flat relief conditions and sandy-quartzous material from p-SX and p-EK, showing, in its lower portion, a C horizon with massive structure and particle size distribution that suggests a lithological discontinuity in relation to the Bsm horizon (Table 2).The podzolization process in p-ESK is of such magnitude that it resulted in cementation of the spodic horizons, both characterized as ortsteins (Bhsx and Bsm), but with a different magnitude of cementation.
The Btgm horizon of the p-EK had thin, cemented, red-colored (10R), and discontinuous plates of a placic horizon within it, which distinguishes it from the Btgm horizon of p-SX, which had only mottles (Table 1).
The p-PAC, a Grayish Argisol, was developed from sediments with quite different clay contents in relation to the other pedons studied (Table 2), and it did not have an eluvial horizon.Cementation occurs in two placic horizons and in the Btx/Bt horizon and is also present in parts of the Bt/Btx horizon.The structure of the non-cemented B horizons (BA1, BA2, Bt, and parts of the Bt/Btx) is typical of Argisols from the coastal tablelands (Ferreira et al., 1999), which are weak, of medium to small size class, subangular, and blocky.
The clay content of the cemented horizons ranged from 90 to 260 g kg -1 (Table 2).Variations in the clay content of these horizons have also been recorded in other studies of coastal tableland soils (Figure 3).However, silt content ranged from 10 to 160 g kg -1 (Table 2).Some of the results found in other studies (Figure 3) showed silt contents that were quite higher, reaching values above 60 %.Considering the pre-weathered parent material of the coastal tableland soils, it is likely that the high values of silt content found in other studies are related to problems of adequate soil dispersion.In the cemented horizons, in addition to the variation in clay contents, the textural gradient also varied greatly between the horizon immediately above and the cemented horizon (Table 2), reaching a maximum in the p-SX (textural gradient between EBh and Btgm of 3.7).
The cemented horizons, mainly those with a duric character, had higher values of BD than the overlying horizons (Table 2), corroborating the findings from other studies with soils of the coastal tablelands (Filizola et al., 2001;Araújo Filho, 2003;Moreau et al., 2006) and with fragipans formed in glacial deposits (Habecker et al., 1990;Weisenborn and   Placic: occurs in an irregular and wavy form, with 1.0-15 mm thickness.They are very discontinuous in the EK profile (see figure 2). (2) BA1 and BA2 horizons of the PAC profile have a cohesive character of intermediate expression.Schaetzl, 2005).The horizons with duric character had the highest values of BD.In the p-PAC, BD values in the BA1 and BA2 horizons (of 1.69 and 1.67 Mg m -3 , respectively) were greater than in the horizons with fragic materials (Btx and Bt/Btx, of 1.56 and 1.49 Mg m -3 respectively).These higher BD values in the horizons with cohesive character, as in the BA1 and BA2 horizons of the p-PAC, are typical of soils from the coastal tablelands, regardless of the presence of cemented horizons (Jacomine, 2001;Araújo Filho, 2003).

Micromorphological properties
The skeleton of all the cemented horizons is dominated by quartz grains.Analysis of the micrographs from these horizons showed the predominance of a low porosity matrix, in accordance with the BD values (Table 2).Porosity is relatively greater in the horizons with the "x" subscript (the Btx/Bt horizon from p-PAC and the Bhsx horizon from p-ESK) than in the horizons with a duric character (the Btgm horizon from p-SX and p-EK).
The horizons with a duric character had several micromorphological features in common: porphyric distribution, with some portions more open and others more closed; predominance Rev Bras Cienc Solo 2017;41:e0150453 of massive microstructure (apedal features); segregation of Fe oxides; planes pores; and argilluviation features, as seen in the microlamination of the clay coatings (Figures 4a, 4b, and 4c).
The two horizons with milder cementation ("x" subscript) differed from each other in texture and in the major pedogenetic process type, podzolization in the Bhsh horizon from p-ESK, and argilluviation in the Btx/Bt horizon from p-PAC.The fragipan from p-PAC (Btx/Bt horizon) had both harder and softer portions.In its hardest parts, it had porphyric distribution with simple spaces and distinct lines of Fe oxide segregation, with portions coinciding with limits of voids (Figure 5a).The ortstein from p-ESK (Bhsx horizon) had enaulic distribution with chitonic portions and skeleton (which predominates over the matrix) with strong organic matter coatings (Figures 5b and 5c), in addition to a partial filling of the inter-grain space with microaggregates of fine material rich in organic matter.The fragipans from p-ESK and p-PAC have features common to the fragipans of the northern hemisphere: both have a well-distributed fabric, without pore interruptions; coated pores without fillings are common in the Btx/Bt horizon from p-PAC; and in the Bhsx horizon from p-ESK, bridges between grains are common (Miller et al., 1993;James et al., 1995;Weisenborn and Schaetzl, 2005).
No features indicating silica were found in the micrographs.Observation of micromorphological evidence for silica cementation, even in duripans, can be impeded by the close relationship of silica with ferriargillans and clays of these horizons (Torrent et al., 1980).However, this evidence is commonly described in micrographs and in electron microscopy images of horizons with duripans or with some degree of silica cementation (Chadwick et al., 1987;  Boettinger and Southard, 1990;Creutzberg et al., 1990;Hollingsworth and Fitzpatrick, 1994;Moody and Graham, 1997;Gutiérrez-Castorena and Effland, 2010).
Iron segregation bands were conspicuous in the cemented horizons from p-EK and p-PAC (Figures 4a and 5a), corroborating the diagnosis of the placic horizons in these pedons (Figure 2 and Table 1).Fe segregation features were found in a lower degree in the micrograph of the Btgm horizon from p-SX (Figure 4c), confirming the mottling identified in the morphological description made in the field (Table 1).(Filizola et al., 2001;Araújo Filho, 2003;Moreau et al., 2006).

Clay mineralogy
Except in the placic horizons from p-PAC, the clay fraction mineralogy of the cemented horizons studied was widely dominated by kaolinite, in agreement with data from the literature on coastal tableland soils (Moreau et al., 2006;Gomes et al., 2008Gomes et al., , 2012) ) and also for the cemented horizons which occur there (Filizola et al., 2001;Araújo Filho, 2003;Moreau et al., 2006).Both placic horizons from p-PAC had a more complex assemblage, with detection of quartz, kaolinite, goethite, hematite, and ilmenite (Figure 6).In the cemented horizons (except for the placic horizons from p-PAC), a background could be noted in the clay fraction diffractograms, which can be associated with the presence of minerals with a low degree of crystallinity (Klug and Alexander, 1974) and, consequently, with the contents of Fe, Al, and Si extracted by acid ammonium oxalate (Table 3).

Immersion tests of cemented materials in water and in acid and basic solutions
Immersion tests in water were the criterion used to define the duric character in the Btgm horizons from p-SX and p-EK and in the Bsm horizon from p-ESK, and they served to confirm the field soil morphology description (Table 4).
In the acid solution immersion, the greatest resistance to slaking occurred in the fragments of the Btgm horizon from p-EK and in the Bsm horizon from p-ESK.The fragments of the Btgm horizon from p-EK were the only ones in which the slaking did not occur completely after 8 days of immersion in 4 mol L -1 NaOH solution.
From the immersion tests, the cemented horizons studied exhibited the following descending order regarding their degree of cementation: Btgm -p-EK > Bsm -p-ESK> Btgm -p-SX > deeper placic -p-PAC = shallower placic -p-PAC = Btx/Bt -p-PAC > Bhsx -p-ESK.These results are similar to those observed by Araújo Filho (2003) in the immersion tests of cemented materials of soils from the coastal tablelands of Alagoas.

pH and contents of Fe, Al, and Si in different extractions and in aqueous solution
The variations of pH were small, between 4.7 and 5.9 for all the horizons and between 4.7 and 5.5 for the cemented horizons (Table 3); pH values were relatively lower in the cemented horizons in relation to the overlying horizons, which differs from the data reported for soils with fragipan in glacial deposits by Miller et al. (1993) and Weisenborn and Schaetzl (2005).
Most often, maximum values of Fe, Al, and Si in the different extractions occurred in the cemented horizons, whether spodic or not.This trend is very clear in p-SX, p-ESK, and p-PAC and quite subtle in p-EK (Table 3).In the aqueous solution extracts, only the values of Si (Sih) showed a noticeable accumulation in the cemented horizons, excluding the fragipan horizon from p-PAC.It is important to notice that in p-SX, p-EK, and p-ESK, the spodic or transitional to spodic horizons, which are overlying the cemented horizons, are also accumulating Fe and Al, mainly associated with organic matter, which also occurs in the cemented and spodic horizons from p-ESK (Table 3).These results indicate the current condition of the podzolization process in those sites.Not only should the relative accumulation in the cemented horizon be considered, but also the absolute values from the extraction, especially in p-SX, p-EK, and p-ESK formed in sandy-quartzous sediments and with the simultaneous podzolization process.In any case, in the cemented Btgm horizon, p-EK has higher values for Fe and Si in relation to the overlying Bh1and Bh2 horizons, in addition to a significant absolute value of Al o (13.96 g kg -1 ), very close to the values from Bh1 and Bh2.
The absolute Al o contents were high in all the cemented horizons, while the contents of Fe o and Si o variable; for Fe o , contents decreased in the following order: p-ESK > p-PAC > p-EK > p-SX; and for Si o , they decreased in the following order: p-ESK > p-SX > p-PAC > p-EK.Therefore, the results observed reinforce the generalized importance of Al compounds with a low degree of crystallinity in the genesis of ortstein, fragipan, and duripan horizons in coastal tableland soils (Araújo Filho, 2003;Lima Neto et al., 2010;Corrêa et al., 2015).However, they also demonstrate that Fe and Si compounds with a low degree of crystallinity also take part in the process to a varied extent, an aspect which was also pointed out by Corrêa et al. (2015).Some hypothesis can explain the origin of Si acting in the genesis of these horizons: dissolution (by hydrolysis) of kaolinite, which is accelerated by the local redoximorphic conditions, being translocated downwards into the pedon (Duncan and Franzmeier, 1999); lateral transport, originating from soils (mainly Argissolos Amarelos and Latossolos Amarelos) that occur in the surroundings of the gentle depressions of the landscape (Moreau et al., 2006;Oliveira et al., 2010); and weathering of very small size quartz (Resende et al., 1988).

Processes of formation of cemented horizons
Three conditions favor or are even required for the development of pans and/or other cementations in soils from the Brazilian coastal tablelands, and they have already been discussed in previous studies (Boulet et al., 1998;Filizola et al., 2001;Moreau et al., 2006): flat or almost flat relief, with a tendency to form depressions; a water regime with seasonal periods of water excess in the pedon (redoximorphic conditions); and a sedimentary substrate with low clay contents (or the relief and the water regime conditions favor kaolinite hydrolysis).The well-defined dry period seems to increase the incidence or degree of the pans/cementations in these ecosystems.In the case of coastal tablelands under forest vegetation,(in which a shrub-like vegetation, known locally as "restinga", can also occur), the dry season often coincides with the summer and repeats one of the conditions stated by Franzmeier et al. (1989) as favorable to the formation process of fragipans in the mid-western United States.Podzolization can occur, favored by cementation in the lower parts of the pedons, or it can also be simultaneous, with the spodic horizon being cemented (Silva et al., 2012).The redoximorphic conditions cause strong dissolution and migration of Fe oxides, often forming iron bands.Soil development in sedimentary deposits with higher clay contents tends to decrease the effectiveness of the cementation process by compounds with a low degree of crystallinity in two ways: through the larger surface area of the sediment to be cemented and through the greater occurrence of expansion and contraction events (Smeck et al., 1989).
Opposing some studies about fragipans developed under periglacial conditions (Payton, 1992(Payton, , 1993;;Weisenborn and Schaetzl, 2005), the values of Fe, Al, and Si obtained in this study from different extractions increased in the fragipan (p-PAC) in relation to the horizon overlying it.Some micromorphologial features are common to these soil profiles, such as the constant presence of coated and unfilled pores, ferri-argillans, and matrix with intense Fe diffusion resulting from redoximorphic conditions, which form the placic horizons.
The p-SX and p-EK exhibited a horizon with duric and gleyed characters.In these horizons, pale colors and argilluviation cutans predominated, and Fe diffusion zones were common (Figure 4).In the p-EK, as well as in the p-PAC, these Fe diffusion zones constituted Fe segregation lines, which are in fact pieces of the placic horizon.In the horizons with a duric character from both profiles, the cementing action of Al (formed with a low degree of crystallinity) and, to a lesser extent, of Si, was evident (Table 3).Horizons with some degree of podzolization occurred, overlaying the horizons with duric character.
In p-ESK, the massive structure (coherent) horizon 2C must have favored podzolization, and this process culminated in the formation of cemented spodic horizons (ortsteins).
The deepest spodic horizon of this pedon still has a duric character.The values from different extractions of Fe, Al, and Si in these horizons indicate the occurrence of both the podzolization and cementation process (Table 3).

Practical Applications
The pans and the other forms of cementation in the four pedons studied were found below the cultivated soil layer (Table 1).Therefore, the soil limitations which can be associated with these features will generally be related to seasonal water excess.The extent of the limitation caused by water excess (oxygen deficiency) in the soil will depend on the degree of cementation, the depth of the cemented horizon, and the relief.
The p-EK site is located in a gentle depression, under forest vegetation, and with a seasonal water excess that is strong enough to restrict agricultural use in the area.The combination of a strong degree of cementation (duric character) with the small depth of the cemented horizon (0.95 m) and the flat and concave topography imposes a greater oxygen deficiency restriction (water excess) on the p-EK in comparison to the other soils studied, regardless of the fact that the primary vegetation found in the area is protected by law.In most cases, soils with a subsurface pan layer that are located on closed depressions, or on depressions associated with headwaters, are restricted from any agricultural activity, either by law or by suitability.
The p-SX and p-ESK are cultivated with eucalyptus.The presence of diffuse mottles in the EA1 and EA2 horizons of p-SX indicates a slight seasonal water excess during the rainy season.The aspect of the area planted to eucalyptus during the survey period and the greater depth of the Btgm cemented horizon (which starts at 1.75 m) indicate that limitations associated with water excess are only moderate in the area.Given that the soil texture is sandy up to the depth of the Btgm horizon, agricultural restriction of the p-SX is mostly linked to water deficiency in the soil.This restriction is attenuated by the water conservation environment provided by the system, due to flat relief and the presence of the cemented horizon, especially for forests (such as the areas planted to eucalyptus), which have a deep root system.In comparison to the p-SX, the p-ESK has the disadvantage of a shallower cemented horizon, located at a depth of 0.54 cm.Therefore, the latter pedon may induce antagonistic forms of plant stress due to water excess or water deficiency, depending on the annual rainfall distribution.During the period under study, the areas planted to eucalyptus in the p-ESK area displayed gaps and nonuniform development.
The p-PAC has two main differences in relation to the other soils studied: a clayier texture on the whole soil profile and a lighter degree of cementation (placic horizons and fragipan, both discontinuous).The area is located in an area planted to 'Pera' orange, and the plants are in the adult phase.Flat relief combined with the presence of subsurface obstructive layers generates an environment which tends to conserve soil moisture, particularly considering the clayier texture starting from the soil surface.The yield and the quality of the area planted to 'Pera' orange in the region are limited by intense water deficit during the summer, typical of the local climate.However, seasonal water excess also leads to plant anoxia, with the placic and fragipan (Btx) horizons beginning at a depth of 0.66 m.

Figure 4 .
Figure 4. Micrographs (under planar polarized light) of selected micromorphological features from Btgm cemented horizons.(a) EK profile: predominance of single-spaced porphyric distribution, with closed porphyric parts (right side, above); low porosity (planes pores); and matrix with segregation of Fe oxides (central part of the photo).(b) EK profile: pore with oriented clay (argilluviation process).(c) SX profile: single-spaced porphyric distribution; segregation of Fe oxides in several parts of the thin section; low porosity (planes pores).

Figure 5 .
Figure 5. Micrographs (under planar polarized light) of selected micromorphological features from cemented horizons with "x" subscript (fragipan and ortstein).(a) PAC profile, Btx/Bt horizon (cemented part) -single-spaced porphyric distribution; vughs pores; and Fe oxides segregation line, including the border of pores.(b) ESK profile, Bhsx horizon -enaulic distribution with chitonic parts; quartz grains with continuous dark coating (organic matter).(c) ESK profile, Bhsx horizon -strong filling of the space between grains with microaggregates of fine material rich in organic matter.

Table 1 .
Morphological properties of the horizons from the studied pedons Horizon

Table 2 .
Soil texture and bulk density of the horizons from the studied pedons

Table 4 .
Evaluation of crumbling of cemented materials in water and in acid and basic solutions

Table 3 .
Chemical analyses of the genetic horizons from the soil profiles Fe d and Al d : Fe and Al extracted by Na citrate-dithionite-bicarbonate. (2) o , Al o and Si o : Fe, Al, and Si extracted by acid ammonium oxalate.(3)Fep and Al p : Fe and Al extracted by Na-pyrophosphate.(4)Fe h , Al h and Si h : Fe, Al, and Si in aqueous solution.