The objective of this project was to use detailed soil profi le descriptions and soil carbon analyses to determine the soil C sequestration potential of tree planting across climatic gradients in the U.S. Great Plains. Tree windbreak age ranged from 19 to 70 years and age of cultivation from 22 to ~110 years. At each site, soil pits were prepared within the tree planting, the adjacent crop fi elds, and nearby undisturbed grassland. Windbreak soils had consistently thicker soil organic carbon (SOC)- enriched A or A+AB horizons when compared to the crop fi elds. The thickness of A or A+AB horizons in the windbreak soils were comparable to the undisturbed grassland soils. A linear relationship was detected between the difference in A+AB thickness of soils beneath windbreaks and undisturbed grasslands and a climate index (hydrothermal coeffi cient, HTC). These results indicate that tree windbreaks with more cool and moist climate conditions are more favorable for SOC accumulation in the surface soil. The relationship between SOC accumulation and climate factors enables the estimation of soil carbon stocks in existing windbreaks and the prediction of potential carbon sequestration of future plantings

G Hernandez-Ramirez

GT Selyaninov

JR Brandle

LA Sherrod

NJ Rosenberg

NT Mirov

OS Khokhlova

TJ Sauer

WH Droze

WR Schroeder

YG Chendev

The objective of this project was to use detailed soil profi le descriptions and soil carbon analyses to determine the soil C sequestration potential of tree planting across climatic gradients in the U.S. Great Plains. Tree windbreak age ranged from 19 to 70 years and age of cultivation from 22 to ~110 years. At each site, soil pits were prepared within the tree planting, the adjacent crop fi elds, and nearby undisturbed grassland. Windbreak soils had consistently thicker soil organic carbon (SOC)- enriched A or A+AB horizons when compared to the crop fi elds. The thickness of A or A+AB horizons in the windbreak soils were comparable to the undisturbed grassland soils. A linear relationship was detected between the difference in A+AB thickness of soils beneath windbreaks and undisturbed grasslands and a climate index (hydrothermal coeffi cient, HTC). These results indicate that tree windbreaks with more cool and moist climate conditions are more favorable for SOC accumulation in the surface soil. The relationship between SOC accumulation and climate factors enables the estimation of soil carbon stocks in existing windbreaks and the prediction of potential carbon sequestration of future plantings.This chapter is from Soil Carbon (2014): chapter 47, 475., doi:10.1007/978-3-319-04084-4_47.</p

Chendev, Yuri

Novykh, Larisa

Burras, C.

Sauer, Thomas

Petin, Aleksandr

Zazdravnykh, Evgeny

Burras, C. Lee

Digital Repository @ Iowa State University (ISU)

475A.E. Hartemink and K. McSweeney (eds.), Soil Carbon. Progress in Soil Science,DOI 10.1007/978-3-319-04084-4_47, © Springer International Publishing Switzerland 2014 Abstract  The objective of this project was to use detailed soil profi le descriptions and soil carbon analyses to determine the soil C sequestration potential of tree planting across climatic gradients in the U.S. Great Plains. Tree windbreak age ranged from 19 to 70 years and age of cultivation from 22 to ~110 years. At each site, soil pits were prepared within the tree planting, the adjacent crop fi elds, and nearby undisturbed grassland. Windbreak soils had consistently thicker soil organic carbon (SOC)-enriched A or A+AB horizons when compared to the crop fi elds. The thickness of A or A+AB horizons in the windbreak soils were comparable to the undisturbed grassland soils. A linear relationship was detected between the difference in A+AB thickness of soils beneath windbreaks and undisturbed grasslands and a climate index (hydrothermal coeffi cient, HTC). These results indicate that tree windbreaks with more cool and moist climate conditions are more favorable for SOC accumulation in the surface soil. The relationship between SOC accumulation and climate factors enables the estimation of soil carbon stocks in existing windbreaks and the prediction of potential carbon sequestration of future plantings.  Keywords  Soil organic carbon •  Afforestation •  Soil transformation  Chapter 47  Evolution of Soil Carbon Storage and Morphometric Properties of Afforested Soils in the U.S. Great Plains  Yury  G.  Chendev ,  Larisa  L.  Novykh ,  Thomas  J.  Sauer ,  Aleksandr  N.  Petin ,  Evgeny  A.  Zazdravnykh , and  C.  Lee  Burras  Y. G.  Chendev  •  L. L.  Novykh  •  A. N.  Petin  •  E. A.  Zazdravnykh  Belgorod State University ,  Belgorod ,  Russia  T. J.  Sauer  (*)  National Laboratory for Agriculture and the Environment ,  USDA-ARS ,  2110 University Boulevard ,  Ames ,  IA 50011 ,  USA  e-mail: tom.sauer@ars.usda.gov  C. L.  Burras  Iowa State University ,  Ames ,  IA ,  USA 476 Introduction  The Energy Independence and Security Act of 2007 mandating that 60.5 billion liters of liquid biofuels be produced annually in the U.S. from cellulosic feed stocks by 2022. To meet this production goal it is estimated that 6.5–7.7 million hectares of land will need to be dedicated to feedstock production (Biomass Research and Development Board  2008 ). In the U.S. Great Plains there is potential for the production of biofuels from grains, crop residues, and dedicated perennial crops, including woody biomass (Rosenberg and Smith  2009 ). The region has a history of forest plantations as single to multiple rows of trees and/or shrubs as windbreaks or shelterbelts (Brandle et al.  2004 ). Windbreak plantings have been often employed in sub-humid to semi-arid regions with extensive plantings in both the steppes of Russia (Mirov  1935 ; Schroeder and Kort  1989 ) and the U.S. Great Plains (Droze  1977 ).  Tree windbreaks represent a multiple-benefi t land use through their capacity to improve crop growth by modifying the local microclimate, sequester carbon in the soil and roots, and provide a renewable source of feedstock (above-ground biomass) for bioenergy production. Sauer et al. ( 2007 ) reported signifi cantly greater soil organic carbon (SOC) in the surface 15 cm of soil beneath a 35 year-old shelterbelt in Nebraska as compared to the adjacent cropped fi elds. Hernandez-Ramirez et al. ( 2011 ), using stable carbon isotope techniques, found that 54 % of the SOC in the 0–7.5 cm soil layer within the Nebraska shelterbelt was tree-derived. Minimizing site disturbance, improved microclimate, and the increased diversity of plant species in tree windbreaks have been credited with reducing C losses and increasing the stability of SOC stocks.  The objective of this research was to determine the soil carbon sequestration potential of tree plantings on marginal agricultural soils across a climatic gradient in the U.S. Great Plains. Here we report on the U.S. phase of a project regarding soil transformations at three U.S. sites. Details of the Russian phase of this project have been reported elsewhere (Chendev et al.  2013 ).  Study Sites  Three sites representing a gradient in mean annual precipitation (MAP) from 528 to 696 mm and mean annual temperature (MAT) of 4.35–9.56 °C were selected for study (Table  47.1 ). The hydrothermal coeffi cient (HTC) of Selyaninov ( 1928 ) was used as a climate index, calculated as HTC = ΣQ/0.1ΣT where Q is and T are precipitation (mm) and temperature (°C) during the growing season (defi ned as T > 10 °C). The Reynolds, North Dakota site is situated on a broad fl at landscape having less than 50 cm total relief. The site grades from the poorly drained upland of the glacial Lake Agassiz plain to the well drained stream terrace along Cole Creek. Parent mate-rials are silty and clayey lacustrine sediments over calcareous loamy glacial tills and similarly textured alluvium. Groundwater is at ~2.5 m. The crop fi eld has been cultivated approximately 110 years predominantly to small grains and more recently with some row crops including corn ( Zea mays , L.), soybean ( Glycine max (L.) Merr.), Y.G. Chendev et al.477or sunfl ower ( Helianthus annuus ). A six-row windbreak was planted in 1958 and now consists primarily of green ash ( Fraxinus pennsylvanica ), box elder ( Acer negundo ), red cedar ( Juniperus virginiana ), and caragana ( Caragana arborescens ). The adjacent grassland was formerly a pasture of primarily smooth brome grass ( Bromus iner-mis ). Soils at this site are mapped as Antler-Mustinka silt loams in the fi eld and windbreak and LaDelle silt loam in the grassland adjacent to the stream (Table  47.2 ). Soils at the Huron site were formed in loamy glacial till and meltwater sandy and loamy sand sediments and are moderately well or well drained. The soils are mapped as Hand-Bonilla loams and Carthage fi ne sandy loam (Table  47.2 ). The site had less than 3 % slope with groundwater at ~1.25 m. The entire site was in pasture until 1981 when it was plowed and cropped. In 1983 a 20+ row tree planting was established to evaluate different tree species and the grass area was returned to pasture. The fi eld continued to be cropped to corn, soybean, or grain sorghum ( Sorghum bicolor (L.) Moench).  Table 47.1  Sampling sites, elevation, mean annual temperature (MAT), mean annual precipitation (MAP), hydrothermal coeffi cient (HTC), and tree windbreak details  Site  Lat and long  Elev (m ASL)  MAT (°C)  MAP (mm)  HTC  Age of tree planting (years)  Tree species  Reynolds, ND  47° 42′ 13″ N  282  4.35  528  1.41  54  Green ash, red cedar and caragana  97° 10′ 59″ W  Huron, SD  44° 15′ 43″ N  397  7.71  582  1.31  19  Green ash  98° 15′ 12″ W  Norfolk, NE  42° 03′ 03″ N  492  9.56  696  1.47  70  Siberian elm, red mulberry, and cottonwood  97° 22′ 08″ W  Table 47.2  Soil series and taxonomic classifi cation for sampling sites  Site  Soil series a  Soil taxonomy  Reynolds, ND  Antler-Mustinka silt loam  Fine-loamy, mixed superactive, frigid Aeric Calciaquolls  LaDelle silt loam  Fine, smectitic, frigid Typic Argiaquolls  Fine-silty, mixed superactive, frigid Cumulic Hapludolls  Huron, SD  Carthage fi ne sandy loam  Coarse-loamy, mixed, superactive, mesic Pachic Haplustolls  Hand-Bonilla loams  Fine-loamy, mixed, superactive, mesic Typic Haplustolls &  Fine-loamy, mixed, superactive, mesic Pachic Haplustolls  Norfolk, NE  Thurman loamy fi ne sand  Sandy, mixed, mesic Udorthentic Haplustolls  Hadar loamy fi nd sand  Sandy over loamy, mixed, superactive, mesic Udic Haplustolls  a Series identifi ed from Soil Survey Geographic (SSURGO) database ( http://soils.usda.gov/survey/geography/ssurgo/description.html ) 47 Evolution of Soil Carbon Storage and Morphometric Properties of Afforested…478 The third site was located in Madison County, Nebraska northeast of the city of Norfolk. Soils at this site are very deep and somewhat excessively drained with sandy eolian parent material redeposited from glaciofl uvial sands and loamy sands from the Elkhorn River valley. The soils are mapped as Thurman loamy fi ne sand and Hadar loamy fi ne sand (Table  47.2 ). Soils at this site have been cultivated or grazed since European settlement in the 1880s. Irrigation is necessary for optimum crop yield although dryland row crop (corn and soybean), wheat ( Triticum aestivum , L.), and alfalfa ( Medicago sativa , L.) are also cultivated. A 5-row tree windbreak was planted in 1942. Dominant species currently include Siberian elm ( Ulmus pumila , L.), red mulberry ( Morus rubra , L.), and cottonwood ( Populus deltoides Marsh).  Methods  Soil profi le descriptions were prepared for one crop fi eld, tree, and grass site at each of the three sites in May of 2012. Two additional pits were prepared at the Norfolk site. As both sides of the windbreak at this site were cropped, pits were prepared in both fi elds. A second pit was also prepared in the windbreak as a 45–60 cm-tall ridge was observed in the middle of the windbreak. All soil pits were prepared by hand to a depth of 1.2–1.5 m. Horizon boundaries and profi le descriptions were prepared from observations of three exposed soil faces. Horizon boundaries were measured at fi ve sites on each exposed face. Presence of carbonates was determined by measuring the depth to effervescence following application of dilute acid to the pit sidewalls. Soil samples were taken from 0–15, 15–30, 30–45, 45–60, 60–80, and 80–100 cm depth increments. Visible roots were removed and a subsample passed through a 2 mm sieve, air dried, and roller-milled before total carbon and nitrogen analysis on a Fison NA 15,000 Elemental Analyzer (ThermoQuest Corp., Austin, TX). Soil inorganic carbon (SIC) was determined by modifi ed pressure calcimetry (Sherrod et al.  2002 ) and SOC calculated by difference. Triplicate horizontal cores (7.8 cm id × 5.15 cm long) were taken from one exposed soil face to determine soil bulk density. Two cores were collected with a Dutch auger approximately 5 m on each side of the pits. These samples were taken at the same depth increments and analyzed with the same methods as for the pit samples. Results are presented for the means of pit and cores samples.  Results  Topsoil thickness (A+AB horizons) of the uncultivated grass soils decreased from north-to-south; 52, 44, 41 cm thickness for the Reynolds, Huron, and Norfolk sites, respectively (Fig.  47.1 ). These soils were considered representative of the original, pre-cultivation soil properties. At each site, there were also signifi cantly greater thicknesses of the A+AB horizons in soils beneath tree plantings compared to the adjacent cultivated cropland soils. The difference in A+AB thickness between tree Y.G. Chendev et al.479and crop soils was 30.8, 15.5, and 11.2 cm for the Reynolds, Huron, and Norfolk sites, respectively, also following a north–south gradient. It is likely that these differences in thickness of the SOC-enriched surface horizons are due to both continued SOC loss from cropping practices, especially erosion and tillage, and SOC accumulation beneath the trees where there is both greater biomass input and  limited soil disturbance. Depth distributions of SOC and SIC content are consistent with the morphometric properties (topsoil thickness) and illustrate the contrasting effects of land use (Fig.  47.2 ). The Reynolds site had the greatest SOC and deepest humus-rich surface layers with the soil profi le in the grassland having the highest SOC content and stocks at all depths (Fig.  47.2a ). Also notable is the depletion of SOC in the cropland soil, especially from 15 to 60 cm. By contrast, the cropland soil had SIC present at all depths and SIC content from 30 to 60 cm represented almost 80 % of the total carbon in the profi le at these depths (Fig.  47.2b ). Neither grassland nor tree soil had SIC present above 45 cm but all three land uses had similar SIC below 60 cm. Land use effects on soil thermal and moisture regimes may be the driving forces behind soil carbon transformations when grassland soils are cultivated or planted to trees. When compared with grasslands, cultivated soils have bare soil surfaces for extended periods and increased evaporation from the soil surface may bring pedogenic carbonates upward from underlying parent materials. Lower SIC in the 80–100 cm layer of the Reynolds cropland soil may indicate loss of carbonate due to this upward movement. Under tree cover, soil conditions are cooler with less evapo-ration from the soil surface than in grasslands and croplands, and carbonates would be more likely to leach (Khokhlova et al.  2013 ).  The soil beneath trees at the Huron site had greater SOC at all depths than the cropland and grassland soils and, like for the Reynolds site, the cropland soil again 020406080Depth (cm)Tree Grass CropReynolds(Calciaquolls/Argiaquolls/Hapludolls)Huron(Haplustolls)Norfolk(Haplustolls) Fig. 47.1  Depth of A or A+AB horizons for U.S. sampling sites.  Error bars are one standard error (n = 15)  47 Evolution of Soil Carbon Storage and Morphometric Properties of Afforested…480100806040200a bcedDepth (cm)CropTreeGrass100806040200CropTreeGrass100806040200Depth (cm)100806040200Depth (cm)CropTreeGrass0 1000 2000 3000 4000 5000 6000 0 1000 2000 3000 4000 5000 60000 1000 2000 3000 4000 5000 6000 0 1000 2000 3000 4000 5000 6000100806040200CropTreeGrassCalciaquolls/Argiaquolls/HapludollsCalciaquolls/Argiaquolls/HapludollsHaplustolls HaplustollsCrop 1TreeTree RidgeCrop 2Grass0 1000 2000 3000 4000 5000 6000HaplustollsSOC (g m-2)SIC (g m-2) Fig. 47.2  Profi les of SOC and SIC for U.S. sampling sites. Note – no SIC was detected at the Norfolk site.  Error bars are one standard error (n = 3). ( a ) Reynolds SOC. ( b ) Reynolds SIC. ( c ) Huron SOC. ( d ) Huron SIC. ( e ) Norfolk SOC  Y.G. Chendev et al.481exhibited carbonate accumulation (Fig.  47.2c, d ). The soils of the Huron site exhibited the most distinct changes in SOC and SIC following tree planting yet this location had the youngest trees (19 year-old). The SOC profi les were very similar for the grassland and crop fi eld suggesting that cultivation had not led to signifi cant SOC loss via erosion or decomposition of organic matter accelerated by tillage.  The Norfolk site had the oldest trees (70 year-old) yet exhibited the smallest changes in SOC with land use (Fig.  47.2e ). The Tree Ridge profi le was collected from a narrow ridge of soil running parallel within the windbreak. This soil exhibited SOC accumulation throughout the profi le and is thought to be the result of deposition of topsoil from adjacent fi elds via wind erosion. The general low SOC and lack of carbonates at this site are likely due to the coarse-textured soils with low water-holding capacity limiting plant growth and warmer temperatures accelerating organic matter decomposition.  Differences of A+AB horizon thickness of tree and grassland soils when plotted versus HTC for the three U.S. sites and three sites in southern Russia using the same methodology (Chendev et al.  2013 ) exhibit a linear dependence with R 2 of 0.57 (Fig.  47.3 ). Thus, the effect of tree planting on grassland soils appears to follow the same rate of organic carbon accumulation in the U.S. Great Plains and Central Russian Upland and this rate is strongly linked to climate. The Reynolds site is an outlier to this trend and two factors may explain this fi nding. First, the soil under the windbreak had a dense layer of glacial origin coarse stone fragments at 38–56 cm. This restrictive layer could slow down the process of SOC accumulation by inhibiting root growth. Second, the grassland soil may have received external organic inputs from intermittent fl ooding that would increase SOC accumulation.-20-100102030400.9 1 1.1 1.2 1.3 1.4 1.5Hydrothermal CoefficientReynoldsHuronNorfolkStreletskayaYamskayaKamennaya(A+AB)diff = 62.625HTC – 69.873R2 = 0.57(A+AB) tree - (A+AB) grass (cm) Fig. 47.3  Plot of difference of A+AB horizon thickness of tree and grass soils versus HTC for all U.S. and Russian sites (Chendev et al.  2013 )  47 Evolution of Soil Carbon Storage and Morphometric Properties of Afforested…482 Conclusions  Mollisols of the Great Plains respond within decades to changes caused by human activity – changing virgin grasslands to arable lands, or arable lands to windbreaks. Tree cover seems to improve soil quality by increasing of A and A+AB horizons thickness, SOC content and stocks. The maximum effect of this soil development was found in more cool and moist conditions and was consistent with fi ndings at three sites in the Russian steppe. Аccumulation of carbon in windbreak biomass and soils indicates that afforestation is an effective measure to assimilate carbon from the atmosphere and convert it into ecosystem components. As such, tree planting in the Great Plains can improve or restore soil quality and is as an effective climate change mitigation practice.  Acknowledgements  The authors appreciate the assistance of Craig Stange, Martin Rosek, Lance Howe, Dan Mager, and Patrick Cowsert (Natural Resources Conservation Service), Steve Rasmussen (Nebraska Forest Service), Jim Marten (Northeast Community College), John Hinners (South Dakota Department of Agriculture), and Beadle Soil and Water Conservation District. This study was supported by U.S. Civilian Research and Development Foundation Grant RUG1-7024-BL-11.  References  Biomass Research and Development Board (2008) National Biofuels Action Plan. U.S. Department of Agriculture and U.S. Department of Energy.  http://www1.eere.energy.gov/biomass/pdfs/nbap.pdf  Brandle JR, Hodges L, Zhou XH (2004) Windbreaks in North American agricultural systems. Agrofor Syst 61:65–78  Chendev YG, Sauer TJ, Hall RB, Petin AN, Novykh LL, Zazdravnykh EA, Cheverdin YI, Tishchenko VV, Filatov KI (2013) Stock assessment and balance of organic carbon in the Eastern European steppe ecosystem tree windbreaks. Reg Environ Issue 4:9–19  Droze WH (1977) Trees, prairies, and people – a history of tree planting in the Plains States. Texas Woman’s University, Denton  Hernandez-Ramirez G, Sauer TJ, Cambardella CA, Brandle JR, James DE (2011) Carbon sources and dynamics in afforested and cultivated corn belt soils. Soil Sci Soc Am J 75:216–225  Khokhlova OS, Chendev YG, Myakshina TN, Shishkov VA (2013) The pool of pedogenic carbon in the soils of different types and durations of use as croplands in the forest-steppe of the Central Russian Upland. Eurasia Soil Sci 46:530–540  Mirov NT (1935) Two centuries of afforestation and shelterbelt planting on the Russian steppes. J For 33:971–973  Rosenberg NJ, Smith SJ (2009) A sustainable biomass industry for the North American Great Plains. Curr Opin Environ Sustain 1:121–132  Sauer TJ, Cambardella CA, Brandle JR (2007) Soil carbon and tree litter dynamics in a red cedar- scotch pine shelterbelt. Agrofor Syst 71:163–174  Schroeder WR, Kort J (1989) Shelterbelts in the Soviet Union. J Soil Water Conserv 44:130–134  Selyaninov GT (1928) On agricultural climate valuation. Proc Agric Meteorol 20:165–177 (in Russian)  Sherrod LA, Dunn G, Peterson GA, Kolberg RL (2002) Inorganic carbon analysis by modifi ed pressure-calcimeter method. Soil Sci Soc Am J 66:299–305 Y.G. Chendev et al.

Evolution of Soil Carbon Storage and Morphometric Properties of Afforested Soils in the U.S. Great Plains

The objective of this project was to use detailed soil profile descriptions and soil carbon analyses to determine the soil C sequestration potential of planting across climatic gradients in the U.S. Great Plains. The windbreak age ranged from 19to 70 years and age of cultivation from 22to-110 year

Chendev, Yu. G.

Novykh, L. L.

Sauer, T. J.

Petin, A. N.

Zazdravnykh, I. N.

DSpace at Belgorod State University

Yury G. Chendev

Larisa L. Novykh

Thomas J. Sauer

Aleksandr N. Petin

Evgeny A. Zazdravnykh

C. Lee Burras

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https://dr.lib.iastate.edu/handle/20.500.12876/4969

Evolution of Soil Carbon Storage and Morphometric Properties of Afforested Soils in the U.S. Great Plains

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