Suñer L., J.A. Galantini. 2015.
Texture influence on soil phosphorus content and distribution in semiarid
Pampean grasslands. InternationalJournal of Plant & Soil Science (ISSN: 2320-7035) Vol.: 7, Issue.: 2 109-120, no.IJPSS.2015.136, PDF
Extended
Abstract
Soil
texture affects the soil environment and the mineralization of soil organic
matter (SOM) in several ways. It has been reported that a rich clay content in
the topsoil results in high levels of soil organic matter; at the same time, it
enhances nitrogen, phosphorus and sulphur availability (Galantini et al., 2004;
Duval et al., 2016). Soil P (phosphorus) equilibrium and availability can be modified
by soil texture as a consequence of changes in physicochemical properties, in phosphate
adsorption-desorption-diffusion processes, and in SOM mineralization-immobilization
processes.
Physical
fractionation methods based on SOM particle size have been developed to
separate organic fractions with different characteristics and dynamics
(Andriulo et al., 1990; Galantini et al., 1997). It is therefore now possible
to distinguish between SOM associated with the fine and with the coarse
fractions, which have different structures and roles. The fine soil fraction
(clay, silt) corresponds to a more humidified or mineral-associated organic
matter (MOM), and the coarse fraction (different sizes of sand) to less
transformed, labile, light or particulate organic matter (POM). Considering
that both fractions are crucial to soil fertility, it is important to determine
the organic (Po) and inorganic (Pi) phosphorus contents in each size fraction
and to relate them to soil texture. Differences in P content are expected to be
found in both particle size fractions: the fine fraction is likely to contain
the more stable Po (Po-MOM) and the more available Pi (Pi-clay and silt sizes);
the coarse fraction, instead, is assumed to contain the more labile Po (Po-POM)
and Pi (Pi-sand size) with low availability in the short term.
The
hypothesis is that soil texture affects the equilibrium of the different P-forms
in soils of the semiarid Pampas region, mainly through stabilization in the
resistant organic forms of fine-textured soils and accumulation in the labile
organic forms of sandy soils. The aim of the study is to determine the content
and distribution of the main P-forms in texturally different soils and to
relate them to the available P-index.
Soil
samples (0-0.15 m) were collected from 27 sites with different textures in a 25-year-old
pasture located in the Experimental Station of Bordenave, Argentina (63°01’20”W;
37°51’55”S). Soil particle size fractions were obtained through wet sieving by separating
the fine (0-100 µm) and coarse (100-2000 µm) fractions. Soil organic matter was
determined in both fractions, and thus mineral-associated (MOM) and particulate
organic matter (POM) were obtained, respectively. Extractable (Pe), organic
(Po), inorganic (Pi) and total extractable (Pt) phosphorus were determined. Occluded
P (Pocl) was calculated as the difference of [Pt - (Po+Pi)] applied to the
whole soil and the particle fractions.
In these
soils, texture determines P content and the equilibrium of its different forms.
Available P-forms (estimated by Pe) were related to the inorganic form present in
the fine fraction of the soil. Phosphorus content in its different forms was
closely associated with soil fractions. The level of Po was higher in the
coarse fraction of the soils containing more fine fractions. All the studied P-forms
were higher in fine-textured soils than in coarse ones. However, P-forms in
particle size fractions showed different tendencies. In coarse-textured soils,
Po in MOM was lower than in fine-textured ones, whereas P-content was higher in
MOM and lower in POM compared with fine-textured soils (Rosell et al., 2000).
Based on these results as well as previous ones, we propose a conceptual model to identify P changes in soils of different textures (Galantini et al.2005, 2007; Rosell et
al., 2000; Suñer & Galantini, 2012; Suñer et al., 1998, 2002, 2013, 2014;
Zalba & Galantini, 2007).
Soil
organic fractions and their P-content within the sand fraction are inside the
labile pool, whereas those within the silt and clay fractions are inside the
intermediate and passive pools. Inorganic minerals of the coarse fraction can
be considered a passive pool of P, while P in the fine fraction represents an
active pool. According to this finding, a conceptual model can be proposed
where P could be linked to SOM fractionation schemes. The principal flows in
this model are a) weathering and physico-chemical processes, which reduce the
size of coarse minerals until mineral particles reach a size below 50 µm and
are then included in the fine fraction; b) humification, by which organic
inputs are transformed into more complex molecules with a lower size; c) mineralization
of SOM fractions, which produce nutrient release and make P available for
plants; d) physico-chemical equilibrium, e) P-uptake by plants; f) recycled P, by
which crop residue returned to the soil can improve Po by a POM increase.
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