SOILSOILSOILSOIL2199-398XCopernicus PublicationsGöttingen, Germany10.5194/soil-4-251-2018Effect of deforestation and subsequent land use management on soil carbon
stocks in the South American ChacoEffect of deforestation and subsequent land-use managementOsinagaNatalia AndreaÁlvarezCarina Rosaalvarezc@agro.uba.arTaboadaMiguel AngelCONICET, National Council of Scientific and Technical Research, Ciudad Autónoma de Buenos Aires, ArgentinaUniversity of Buenos Aires, School of Agronomy, Soil Fertility and
Fertilizer, Av. San Martín 4453, Ciudad Autónoma de Buenos Aires,
1417, ArgentinaSoil Institute, CIRN, INTA, Hurlingham, Buenos Aires, ArgentinaCarina Rosa Álvarez (alvarezc@agro.uba.ar)1November2018442512575December201712April201826September20186October2018This work is licensed under the Creative Commons Attribution 4.0 International License. To view a copy of this licence, visit https://creativecommons.org/licenses/by/4.0/This article is available from https://soil.copernicus.org/articles/4/251/2018/soil-4-251-2018.htmlThe full text article is available as a PDF file from https://soil.copernicus.org/articles/4/251/2018/soil-4-251-2018.pdf
The subhumid Chaco region of Argentina, originally covered by dry
sclerophyll forest, has been subjected to clearing since the end of the 1970s
and replacement of the forest by no-till farming. Land use changes produced a
decrease in aboveground carbon (C) stored in forests, but little is known
about the impact on soil organic C stocks. The aim of this study was to
evaluate soil C stocks and C fractions up to 1 m depth in soils under
different land use: <10-year continuous cropping, >20-year continuous
cropping, warm-season grass pasture and native forest in 32 sites distributed
over the Chaco region. The organic C stock content up to 1 m depth expressed
as equivalent mass varied as follows: forest
(119.3 Mg ha-1) > pasture (87.9 Mg ha-1) > continuous
cropping (71.9 and 77.3 Mg ha-1), with no impact of the number of
years under cropping. The coarse particle fraction (2000–212 µm) at
0–5 and 5–20 cm depth layers was the most sensitive organic carbon
fraction to land use change. Resistant carbon (<53µm) was the
main organic matter fraction in all sample categories except in the forest.
Organic C stock, its quality and its distribution in the profile were responsive
to land use change. The conversion of the Chaco forest to crops was
associated with a decrease of organic C stock up to 1 m depth and with the
decrease of the labile fraction. The permanent pastures of warm-season
grasses allowed higher C stocks to be sustained than cropping systems and so could
be considered a sustainable land use system in terms of soil C preservation.
As soil organic C losses were not restricted to the first few centimetres of the soil,
the development of models that would allow the estimation of soil organic C
changes in depth would be useful to evaluate the
impact of land use change on C stocks with greater precision.
Introduction
As one of the components of global change, land use change has a great
impact on terrestrial ecosystems, altering their structure and function
(Walker and Steffen, 1999). The most important land use change is due to
agriculturisation (Houghton, 1999), a process that involves replacement of
natural ecosystems, such as forests, by agricultural land (cropping or
grassland systems) as world food demand increases (Volante et al., 2012).
In Argentina, since the late 1970s, there has been an advance of the
agricultural frontier across the Chaco region native forests due to
conversion for production of annual crops (Gasparri et al., 2009). Thus, it
became one of the 10 countries with the greatest forest loss in the world
(FAO, 2015). The eastern subhumid Chaco is a large forest area that since
1997 has suffered a notable increase in forest-cleared area (Albanesi et
al., 2003; Grau et al., 2005; Volante et al., 2009). The average
deforestation rate is among the highest in the world and in the country,
mainly in the east of the province of Santiago del Estero, where Mollisols
are the predominant soil type (Volante et al., 2009).
Deforestation together with inadequate subsequent management leads to
acceleration of erosive processes, reduction of organic matter input,
decrease of soil aggregate stability (Cerdà, 2000; Cerdà et al.,
2009; García Orenes et al., 2010), changes in microclimate and
biodiversity loss, affects water basin functions and contributes to global
climate warming. These effects have been studied mostly in tropical and
temperate forests but have been poorly evaluated in South American
subtropical forests (Baccini et al., 2012; Harris et al., 2012; Hansen et
al., 2013).
In the subhumid Chaco, the intensity and seasonality of rainfall, the gently
undulating landscape, the fragility of the environment and the subtropical
climate predispose the soil to substantial physical degradation (Albanesi et
al., 2003). No-tillage was introduced in Argentina, including in the Chaco
region, in the mid-1990s. It was adopted due to its lower production
costs, the possibility it offered of incorporating areas with greater
limitations to crop yield (Satorre, 2005; Derpsch et al., 2010), to savings
in operating time and to lack of soil disturbance that reduces soil erosion,
recovers soil aggregate stability, conserves water and increases carbon
sequestration in the first few centimetres of soil (Díaz Zorita et al.,
2002). Despite its many advantages, no-tillage can negatively impact some
physical properties of the surface soil (bulk density, penetration
resistance), as mechanical formation of macropores is reduced and there is a
tendency to form laminar and massive structures (Strudley et al., 2008;
Álvarez et al., 2009, 2012). All these effects are increased by the
transit of heavy machinery that produces soil compaction of the first 40 centimetres of soil, especially when the soil is wet (Botta et al., 2004).
In the western part of the region, livestock production became important,
replacing native forests by megathermic pastures. This activity has negative
effects on soil physical properties and produces reduction of soil organic
carbon levels due to forest clearance and soil compaction caused by animal
transit (Caruso et al., 2012). However, it could have a smaller negative
impact than continuous agriculture on carbon sequestration and on soil
physical properties as animal trampling effects extend to a lesser depth and
live roots are present in the soil all year long.
The objective of the present study was to determine carbon stocks and soil
physical quality of subhumid Chaco soils under different land uses:
agriculture (less than 10 years and more than 20 years under cropping),
pastures and natural forests.
Materials and methods
The region of the subhumid Chaco is part of the Great American Chaco and
occupies the southern fringe of the eastern part of the semi-arid Chaco
(Vargas Gil, 1988, Fig. 1). In Argentina, it covers an area of
45 199.33 km2. Annual rainfall ranges from 700 mm in the west to
1000 mm on the limit with the humid Chaco (east) and it has a monsoon regime,
with periods of marked water deficit during the winter months and the
beginning of spring.
Location of the Gran Chaco, the subhumid Chaco and the study area.
Main characteristics of the soils of the study region.
The average annual temperature is 21 ∘C. The most representative soils
are Haplustolls and Argiustolls (Vargas Gil, 1988). Crop production is mainly
summer crops (soybean, corn, sorghum and cotton) sown in December and
January, with winter months generally as fallow periods, in order to store
soil water for the summer crop. In the west of the region, livestock
production on megathermic pastures predominates. The natural vegetation is a
xerophytic forest with dominance of various species of Schinopsis,
Prosopis nigra and Ziziphus mistol and shrubs of the genus
Acacia.
A total of 32 sites were selected in an area of 320 000 ha to the east of
the Santiago del Estero province (Fig. 1), which were representative of the
most common forms of land use of this region: native forest (reference),
continuous cropping (rotation of soybean–soybean–corn under no-till farming) during
different periods (6–9 and >20 years) and more than 10-year old
pastures (pasture, Gatton panic, Panicum maximum) on the most
representative soils (typical Haplustolls and Argiustolls) with silty and
clayey texture (Table 1). From each category, eight sites (n=8) located in
different farms were sampled. Mean values and standard errors of soil
particle size distribution in the 0–20 cm layer for different land uses are
presented in Table 2.
Mean values and standard errors of soil particle size distribution
in the 0–20 cm layer for different land uses.
Land useClaySiltSand(g kg-1)(g kg-1)(g kg-1)Forest240±11.1400±13.0360±12.4Pasture240±15.8390±26.2370±28.1Cropped 6–9 years290±39.3430±25.5280±44.1Cropped > 20 years300±22.4440±47.7260±52.1All land uses270±37.7410±34.5320±60.1
In each site, a composite sample built up of four subsamples was taken up to
1 m depth from the 0–5 cm layer, the 5–20 cm layer and then every 20 cm.
Soil organic carbon (SOC) was determined by wet combustion using the
Walkley–Black method (Nelson and Sommers, 1996). Coarse particulate organic
carbon (2000–212 µm, CPC), fine particulate organic carbon
(212–53 µm, FPC) and resistant organic carbon (<53µm, RC) were determined (Cambardela and Elliot, 1992). Bulk
density (BD) was determined using the cylinder method (Burke et al., 1986)
with 100 cm3 cylinders. Carbon content mass per unit area was estimated
using sample BD values. To compare soil total organic carbon stocks (Mg ha-1) a
correction was made to bring soil profiles to mass-equivalence up to 1 m
depth (Neill et al., 1997).
Additionally, four soil subsamples from the 0–20 cm layer were taken in
each site to determine the structural stability according to the methodology
described by Le Bissonnais (1996). Aggregates of 3 to 5 mm in diameter were
dried at 40 ∘C for 24 h and then subjected to three pretreatments:
fast wetting of air-dry aggregates with distilled water, wet agitation
(previously treated with ethanol) and low wetting (capillarity with distilled
water). After applying these pretreatments, the distribution of the
aggregates according to their size was determined using a series of sieves
(0.05, 0.1, 0.2, 0.5, 1 and 2 mm). The aggregate mean weight diameter (MWD)
for each pretreatment was calculated as an index of the structural stability
obtained as the algebraic sum of the percentage of the total mass of soil
retained in each sieve, multiplied by the opening of the adjacent sieves. The
MWD for each of the three pretreatments was estimated, and an integrated value
of MWD was also calculated. Penetration resistance was determined every 5 up
to 40 cm depth with a 30∘ conical tip dynamic penetrometer (Burke et
al., 1986), taking four determinations per site. At the same time soil water
content (SWC) was determined at two depths (0–20 and 20–40 cm), as penetration
resistance varies with it. As soil water content was only determined for the
0–20 and 20–40 cm layers, the relationship between soil penetration
resistance and water content was constructed by integrating soil penetration
resistance data for 0 to 20 and 20 to 40 cm layer depths. We measured MWD
and penetration resistance as erosion and compaction are the main soil
degradation processes in the studied region. The soil MWD index is conversely
related to soil susceptibility to erosion, and soil penetration resistance
allows soil compaction derived from machinery transit and
animal trampling to be characterised.
Variation of coarse particulate carbon (2000–212 µm,
CPC), fine particulate carbon (212–53 µm, FPC) and resistant
organic carbon (<53µm, RC) associated with land use. (a) Depth
0–5 cm. (b) Depth 5–20 cm. Different letters indicate significant differences
between land use categories within each depth interval (P<0.05).
Significance of differences was tested using analysis of variance (ANOVA)
after checking data normality (Shapiro–Wilks test) and variance homogeneity.
Soil organic carbon (SOC) and bulk density (BD) variation in depth
associated with land use: forest, pasture, 6–9-year and >20-year cropped soils. Different letters indicate significant differences between
land use categories within each depth layer.
SOC (Mg ha-1) Depth (cm)Forest Pasture Cropped 6–9 years >20 years 0–2057.97a32.07b32.54b31.84b20–4019.52a20.67a18.48a19.19a40–6018.90a18.54a11.62b10.83b60–8015.16a11.69b10.15bc7.89c80–1008.62bc11.60a9.03b6.74c0–100120.17a94.57b81.82bc76.49cBD (Mg m-3) Depth (cm)Forest Pasture Cropped 6–9 years >20 years 0–200.89c1.10b1.11b1.21a20–400.96c1.09b1.07b1.14a40–601.00d1.17a1.07c1.13b60–801.08a1.11a1.10a1.09a80–1001.14a1.15a1.15a1.16aResults and discussion
SOC was affected by land use up to a depth of 1 m (Table 3). As land use
produces changes in BD (Table 3), SOC content data have been corrected by BD.
Mean SOC content up to 1 m decreased as follows: forest, pasture and cropped
fields. The organic C stock content up to 1 m depth expressed as equivalent
mass showed the same tendency: forest (119.3 Mg ha-1) > pasture
(87.9 Mg ha-1) > continuous cropping (71.9 and
77.3 Mg ha-1), with no impact of the number of years under cropping.
There was a significant reduction in SOC in the cropped sites compared to the
forest in the first 20 cm and from 40 to 80 cm depth, while pastures showed
this decrease only in the surface layer. Between 34 % and 48 % of SOC
was found in the first 20 cm, while in the forest it presented greater
stratification. SOC vertical distribution tends to follow the distribution of
the root system (Jobbágy and Jackson, 2000); the reason why pastures have
a higher SOC is that roots are abundant down to a depth of 80–100 cm.
Functional relationships between soil penetration resistance and
gravimetric water content for different land uses at two depths
(a 0–20 cm; b 20–40 cm).
SOC content depended on the input of carbon contributed by the vegetation
that varied among vegetation types. Forest had the greatest content, due to
its higher net primary productivity, pastures represented the intermediate
situation and the lowest contribution corresponded to crops that in this
region consist of one summer crop per year (Follet et al., 2009). The most
important annual crops in the region are soybean, maize and cotton. Comparing
cropped and pristine soils in the Pampean region, Sainz Rozas et al. (2011)
found that SOC reduction for the 0–20 cm layer ranged between 36 % and
53 %, which placed our regional results in the middle of this range of
variation. This loss of SOC can be explained by the lower C input due to
harvesting, the greater mineralisation and the greater susceptibility to
erosion of these soils (Alvarez, 2001). Land use had different effects on SOC
fractions (Fig. 2). At both soil depths, coarse particulate carbon
(2000–212 µm, CPC) showed the greatest differences between land
uses. Resistant organic carbon (<53µm, RC) was the main
constituent of soil organic matter in all land uses except in the forest,
where CPC was the main fraction, with 65 % of total SOC in the 0–5 cm
layer and 55 % in the 5–20 cm layer. The SOC fraction most affected by
land use change was the most labile (CPC, 212–200 µm), which
represented 6 % of total SOC in cropped sites and 57 % in pastures
and forest sites. Our results are similar to those of Balesdent et al. (1998), who
found that the SOC of soils decreased rapidly in the first 7 years of
cultivation and more slowly after, and the decrease affected mostly the
coarse CPC fractions. The higher RC content in the cropped
sites (78 % of total SOC) showed that there is a shift towards more
humified fractions, which have a lower rate of nutrient mineralisation,
results that coincide with those obtained by Albanesi et al. (2003) and
Galantini and Suñer (2008).
In soils with native forest, BD increased with depth, from 0.88 Mg m-3
in the 0–20 cm layer to 1.14 Mg m-3 at 80–100 cm depth. The
cropped fields did not follow this trend. Their BD was highest in the surface
layer (0–20 cm) and in depth (80–100 cm) and lowest at 20 to 80 cm. The
pasture under 15 years of livestock production had similar values to the
fields cropped for 6–9 years. These higher surface BD values were a
consequence of the decrease in SOC and machinery transit in cropped fields
(Alvarez et al., 2012) and of the mechanical pressure exerted by livestock in
the pastures (Alvarez et al., 2012). Soils under more than 20 years of
cropping had a BD of 1.20 Mg m-3 in the first 20 cm, 8 % higher
than soils under 6–9 years cropping or pasture (1.11 Mg m-3) and
36 % higher than the values of the forest soil (0.88 Mg m-3).
Finally, soil BD in 0–20 cm was highly correlated with SOC (r=-0.9; p>0.0001) but not with soil particle size fractions.
The highest soil aggregate MWD values were measured in forest (1.61 mm) and
pasture (1.74 mm) soils, values that were not statistically different.
Cropped sites showed an average MWD of 0.76 mm, half that of forest and
pasture soils and significantly (P<0.05) different to that of those two
land use categories. In all land uses, fast wetting was the treatment that
reduced MWD most, reducing the size of aggregates by 40 % when compared
with the treatment of less stress (slow wetting by capillarity). MWD, which
characterises structural stability, was directly related to CPC (r=0.6,
p=<0.01) and to SOC (r=0.48, p<0.01). CPC loss of the first 20
cm largely explained the loss of MWD in cropped soils. Organic matter
influences soil structure, but at the same time the formation of stabilised
aggregates facilitates carbon sequestration and provides physical protection
to soil carbon (Onweremadu, 2007). In contrast, pastures, despite having a
lower amount of coarse particulate carbon (212–200 µm) than the
forest, had the same MWD values. This could respond to the presence of a fine
root network of the pasture grass (Gatton panic) that improved aggregate
resistance to stress.
Penetration resistance (PR) at 0–20 cm depth showed a negative correlation with
SWC (r=-0.72; p<0.0001; Fig. 3a). PR of cropped fields was 1.1 MPa
with 290 g kg-1 SWC; pastures had the same PR value at that depth but with
lower SWC (220 g kg-1). Forest showed higher PR values (1.5 MPa) as at
the moment of sampling, SWC was lower (130 g kg-1). At a greater depth
(20–40 cm), no correlation was found between those two variables (p=0.32; Fig. 3b). Fields under more than 20 years of cropping had an average
PR of 3 MPa with high SWC values (270 g kg-1). Soils with 6–9 years
continuous cropping and forests had a PR of 2.2 MPa, with a SWC of 250 g kg-1
and 140 g kg-1, respectively. The pasture had the lowest PR (0.9 MPa) with a
SWC of 210 g kg-1. Below 20 cm depth, there was soil hardening in
cropped sites; even with high SWC values (270 g kg-1), their PR values
were higher than 2 MPa, which could be critical for root development. This
would indicate soil compaction due to continuous machinery transit. Values lower
than 1.50 MPa at 0–20 cm depth could be attributed to the high
organic matter content at that depth (Table 3 and Fig. 3).
Conclusions
In the study region, SOC content, its quality and its distribution in the profile
were sensitive to the change in land use. The conversion of Chaco forests to
crop production was associated with SOC stock reductions up to 1 m depth and
with the decrease of the labile fraction, which mainly occurred in the first
years after deforestation. Permanent pastures proved to be a sustainable
practice to mitigate C stock loss compared with cropping systems. It is of
great interest to note that carbon losses are not restricted to the first few
centimetres of the soil, as is generally shown in organic carbon maps or in greenhouse
gas inventories. The development of models that would allow the estimation of
SOC changes in depth would be useful to evaluate the
impact of land use change on carbon stocks with greater precision. We recommend
that efforts are increased to minimise or stop deforestation in the South American Chaco, as
remaining native forests provide numerous essential ecosystem services such
as carbon sequestration, climate and flood regulation and preservation of
biodiversity. The change in land use also affected soil physical properties,
such as compaction, loss of structural stability in the first 20 cm and
hardening of the 20–40 cm depth layer in fields under no-till farming. Pastures,
despite their lower SOC and CPC contents than the pristine soils, had a
structural stability equal to that of the forest, showing that physical
properties are not only correlated with the level of carbon in a soil, but
also depend on the type of roots of the replacement vegetation and the
stresses applied to the soil (i.e. machinery transit).
The dataset is available at https://www.dropbox.com/s/i28ac8dl2dx1i3x/Datos.xlsx?dl=0,
last access: 29 October 2018.
NAO, CRÁ and MAT collected samples and wrote and edited the paper.
NAO did chemical soil analysis and processed the data.
CRÁ and MAT were responsible for the experimental design, funding acquisitions and project administration.
NAO was a doctoral student and CRÁ and MAT her advisors.
The authors declare that they have no conflict of
interest.
This article is part of the special issue “Regional
perspectives and challenges of soil organic carbon management and monitoring
– a special issue from the Global Symposium on Soil Organic Carbon 2017”.
It is a result of the Global Symposium on Soil Organic Carbon, Rome, Italy,
21–23 March 2017.
Acknowledgements
This work has been funded by UBACyT project no. 20020130100274BA. Farmers are
thanked for their help in carrying out this work on their
properties. Edited by: Viridiana
Alcéntara Reviewed by: Pia Gottschalk
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