DOCSLIB.ORG

Soil Respiration Across Scales: the Importance of a Model-Data

Total Page：16

File Type：pdf, Size：1020Kb

Download full-text PDF Read full-text
Soil Respiration Across Scales: the Importance of a Model-Data 344 DOI: 10.1002/jpln.200700075 J. Plant Nutr. Soil Sci. 2008, 171, 344–354 Soil respiration across scales: The importance of a model–data integration framework for data interpretation§ Markus Reichstein1* and Christian Beer1 1 Max-Planck Institute for Biogeochemistry, Biogeochemical Model-Data Integration Group, Hans-Knöll-Str. 10, 07745 Jena, Germany Abstract Soil respiration represents the second largest CO2 flux of the terrestrial biosphere and amounts 10 times higher than the current rate of fossil-fuel combustion. Thus, even a small change in soil respiration could significantly intensify—or mitigate—current atmospheric increases of CO2, with potential feedbacks to climate change. Consequently, to understand future dynamics of the earth system, it is mandatory to precisely understand the response of soil respiration to chan- ging environmental factors. Among those changing factors, temperature is the one with clearest and most certain future trend. The relationship of soil respiration to environmental factors and particular temperature has been tackled at a variety of scales—from laboratory via field scale to global, with each of the approaches having its particular problems, where results from different scales are sometimes contradictory. Here, we give an overview of modeling approaches to soil respiration, discuss the dependencies of soil respiration on various environmental factors, and summarize the most important pitfalls to consider when analyzing soil respiration at the respec- tive scale. We then introduce a model–data synthesis framework that should be able to reconcile and finally integrate apparently contradictory results from the various scales. Key words: soil respiration / modeling / upscaling / Bayesian / temperature dependence Accepted January 26, 2008 1 Introduction With globally 68–120 Pg C y–1 soil respiration represents the In this study, methods and problems analyzing soil-respira- second largest C flux between ecosystems and the atmo- tion data from different scales are reviewed and jointly inter- sphere (Schimel et al., 1996). This is more than 10 times the preted with emphasis on the temperature and moisture de- current rate of fossil-fuel combustion and indicates that each pendence of soil respiration. The application of an ecosystem year approx. 10% of the atmosphere’s CO2 cycles through model–data integration framework which is developed in a the soil. Thus, even a small change in soil respiration could cascade from fine scale to landscape scale, and parameter- significantly intensify—or mitigate—current atmospheric ized by using observations across these scales, is proposed increases of CO2, with potential feedbacks to climate change. to provide additional insights into the factors controlling tem- Despite this global significance as well as considerable scien- poral and across-ecosystem variability of soil respiration and tific commitment to its study over the last decades, there is C content. still limited understanding of the factors controlling temporal and across-ecosystem variability of soil respiration. 2 Environmental factors controlling soil This understanding is largely hampered by the fact that stud- respiration ies are often conducted and compared at different temporal and spatial scales that are not compatible. Since particularly 2.1 Abiotic factors in large-scale studies factors influencing soil respiration often correlate with each other, responses of soil respiration to Temperature is virtually influencing all biological and physico- those factors are confounded by other factors, and only chemical processes. This has been empirically observed in apparent relationships are obtained. the 19th century (van’t Hoff, 1898) and later formalized by * Correspondence: Dr. M. Reichstein; e-mail: [email protected] § Paper presented at the Workshop “Upscaling – Soil organisms and soil ecological processes up to the landscape scale”, February 23–24, 2006 at the University of Vechta, Germany. The workshop was organized by the Soil Ecology Working Groups of the German Soil Science Society (DBG) and the Ecological Society of Germany, Austria, and Switzerland (GfÖ), convenor Gabriele Broll and co-con- venors Volkmar Wolters and Anton Hartmann. 2008 WILEY-VCH Verlag GmbH & Co. KGaA, Weinheim www.plant-soil.com J. Plant Nutr. Soil Sci. 2008, 171, 344–354 Soil respiration across scales 345 Arrhenius (1889). Not surprisingly, temperature has also perature. Since enzymes act in a certain temperature inter- been the most obvious and most often studied factor influen- val, all biological processes exhibit optimum temperatures. cing soil respiration, one of the first studies dating back to the Hence, the optimum function (Kirschbaum, 1995) may be 1920s (Waksman and Gerretsen, 1931). All studies confirm a considered as the most appropriate description. However, nonlinear positive direct relationship between temperature soil temperatures rarely reach such high values, so that with- and soil respiration. A number of shapes have been pro- in the normal range of temperatures, the monotonic exponen- posed, but the most commonly used are reviewed by Kätterer tial function may be as valid. et al. (1998), Kirschbaum (1995) as well as by Lloyd and Tay- lor (1994). The simplest, but theoretically not justified function The effect of soil water status on soil respiration has been de- is the so-called exponential Q10 relationship (Tab. 1), where scribed empirically via absolute or relative measures of volu- the parameter Q10 is the factor by which soil respiration in- metric water content and soil water potential as reviewed by creases with a 10°C temperature increase. The Arrhenius Rodrigo et al. (1997) (see examples in Tab. 2). It is usually function is theoretically justified from first physicochemical assumed, that both very low and very high water contents principles of the underlying biochemical reactions and pre- reduce soil respiration, via direct inhibition of biological activ- dicts an increasing Q10 towards lower temperatures. How- ity or inhibition of O2 diffusion, respectively. The relationship ever, the validity of a simple transfer from physicochemical between soil water status and soil-respiratory processes is reactions to complex processes controlling soil respiration complex, since many individual processes vary with soil has not been proved yet. Instead, more flexible exponential water content, in particular gas and solute diffusion, enzyme relationships have been derived from empirical field data, activities, and growth and mortality of microorganisms (Kill- which imply an even stronger variation of the Q10 with tem- ham, 1994; Marshall and Holmes, 1988). Soil water potential Table 1: Typical functions used for describing soil respiration in relation to temperature. Author Function Background Properties dfa À = van't Hoff (1898) Á T Tref 10 emprical always above 0 2 f T a Q10 2 Ratkowsky et al. (1982) f T a Á T À Tmin empirical studies on zero respiration at T = Tmin 2 microbial growth ÀE0= RÁT Arrhenius (1989) f T a Á e physical chemistry always >0, very similar to Q10, 2 ÀEa = T ÀTmin Lloyd and Taylor (1994) f T a Á e Arrhenius + study on zero respiration at T = Tmin,no 3 field respiration optimum Á À : = O'Connell (1990); f T a Á eb T 1 0 5T Topt empirical studies on optimum function 3 Kirschbaum (1995) soil respiration in lab a degrees of freedom (i.e., number of free parameters) Table 2: Typical model formulations used for soil-drought effects on soil respiration. Formulationa References Dependency on volumetric soil moisture f a Á b (plain linear) Stanford and Epstein (1974) À f a Á b (scaled linear) Myers et al. (1982) opt Àb f (hyperbolic) Bunnell et al. (1977) a1 Dependency on soil water potential É É Á log ÀÉ f m 10 c Sommers et al. (1981); Orchard and Cook (1983); Andrén and Paustian log ÀÉÀlog ÀÉ (log-linear) (1987) É 10 10 min f log ÀÉ Àlog ÀÉ 10 opt 10 min f Éa Á ebÁÉ (exponential) Davidson et al. (1998) Dependency on proportion of water-holding capacity P À À 2 f Pe a P Pref b P Pref (exponential) Howard and Howard (1993) a symbols a, b, hopt, hb, a1, m, c, Wmin, Wopt, Pref are model parameters determining the shape and scale of the functions. 2008 WILEY-VCH Verlag GmbH & Co. KGaA, Weinheim www.plant-soil.com 346 Reichstein, Beer J. Plant Nutr. Soil Sci. 2008, 171, 344–354 has often been considered the physiologically more appropri- optimally under neutral conditions while fungi prefer slightly ate predictor of activities in soil, because it expresses the acidic soil pH. A recent study has shown that such optimum actual availability of water independent of texture (Davidson curve can be found through analysis of field data of respira- et al., 1998; Miller and Johnson, 1964). However, plausible tion (Reth et al., 2005), although confounding factors have to arguments for soil water content as a predictor have also be considered. been presented, based on the reasoning that the number and extent of microenvironments where microbial activity may Also in the temporal domain, processes from various time- take place is a function of the volume of the water in the soil scales overlap and superimpose on the resulting soil biologi- (Fang and Moncrieff, 1999; Orchard and Cook, 1983). cal activity and soil respiration (Fig. 1). Consequently, a cur- Furthermore, nutrient and O2 diffusion seem to be better de- rently observed soil respiration can be the result of processes scribed as dependent on soil water content (Skopp et al., that have occurred a long time
Load more

Recommended publications
  • Fact Sheet 3: Organic Matter Decline
    Sustainable agriculture and soil conservation Soil degradation processes Fact sheet no. 3 Organic matter decline What is organic matter decline? Soil organic matter includes all living soil organisms together with the remains of dead organisms in their various degrees of decomposition. The organic carbon content of a soil is made up of heterogeneous mixtures of both simple and complex substances containing carbon. The sources for organic matter are crop residues, animal and green manures, compost and other organic materials. A decline in organic matter is caused by the reduced presence of decaying organisms, or an increased rate of decay as a result of changes in natural or anthropogenic factors. Organic matter is regarded as a vital component of a healthy soil; its decline results in a soil that is degraded. A soil that is rich in organic matter (Source: Soil Atlas of Europe) Why is soil organic matter/carbon important? Soil organic matter is a source of food for soil fauna, and contributes to soil biodiversity by acting as a reservoir of soil nutrients such as nitrogen, phosphorus and sulphur; it is the main contributor to soil fertility. Soil organic carbon supports the soil’s structure, improving the physical environment for roots to penetrate through the soil. Organic matter absorbs water – it is able to hold about six times its weight in water – making it a lifeline for vegetation in naturally dry and sandy soils. Soils containing organic matter have a better structure that improves water infiltration, and reduces the soil’s susceptibility to compaction, erosion, desertification and landslides. On a global scale, soils contain around twice the amount of carbon held in the atmosphere and three times the amount found in vegetation.
    [Show full text]
  • Soils and Fertilizers for Master Gardeners: Soil Organic Matter and Organic Amendments1 Gurpal S
    SL273 Soils and Fertilizers for Master Gardeners: Soil Organic Matter and Organic Amendments1 Gurpal S. Toor, Amy L. Shober, and Alexander J. Reisinger2 This article is part of a series entitled Soils and Fertilizers for Master Gardeners. The rest of the series can be found at http://edis.ifas.ufl.edu/topic_series_soils_and_fertil- izers_for_master_gardeners. A glossary can also be found at http://edis.ifas.ufl.edu/MG457. Introduction and Purpose Organic matter normally occupies the smallest portion of the soil physical makeup (approximately 5% of total soil volume on average, and usually 1 to 3% for Florida’s sandy soils) but is the most dynamic soil component (Figure Figure 1. Typical components of soil. 1). The primary sources of soil organic matter are plant Credits: Gurpal Toor and animal residues. Soil organic matter is important for maintaining good soil structure, which enhances the What is the composition of soil movement of air and water in soil. Organic matter also organic matter? plays an important role in nutrient cycling. This publication is designed to educate homeowners about the importance Soil organic matter contains (i) living biomass: plant, of soil organic matter and provide suggestions about how to animal tissues, and microorganisms; (ii) dead tissues: partly build the organic matter in garden and landscape soils. decomposed materials; and (iii) non-living materials: stable portion formed from decomposed materials, also known as humus. Soil organic matter typically contains about 50% carbon. The remainder of soil organic matter consists of about 40% oxygen, 5% hydrogen, 4% nitrogen, and 1% sulfur. The amount of organic matter in soils varies widely, from 1 to 10% (total dry weight) in most soils to more than 90% in organic (muck) soils.
    [Show full text]
  • Agricultural Soil Compaction: Causes and Management
    October 2010 Agdex 510-1 Agricultural Soil Compaction: Causes and Management oil compaction can be a serious and unnecessary soil aggregates, which has a negative affect on soil S form of soil degradation that can result in increased aggregate structure. soil erosion and decreased crop production. Soil compaction can have a number of negative effects on Compaction of soil is the compression of soil particles into soil quality and crop production including the following: a smaller volume, which reduces the size of pore space available for air and water. Most soils are composed of • causes soil pore spaces to become smaller about 50 per cent solids (sand, silt, clay and organic • reduces water infiltration rate into soil matter) and about 50 per cent pore spaces. • decreases the rate that water will penetrate into the soil root zone and subsoil • increases the potential for surface Compaction concerns water ponding, water runoff, surface soil waterlogging and soil erosion Soil compaction can impair water Soil compaction infiltration into soil, crop emergence, • reduces the ability of a soil to hold root penetration and crop nutrient and can be a serious water and air, which are necessary for water uptake, all of which result in form of soil plant root growth and function depressed crop yield. • reduces crop emergence as a result of soil crusting Human-induced compaction of degradation. • impedes root growth and limits the agricultural soil can be the result of using volume of soil explored by roots tillage equipment during soil cultivation or result from the heavy weight of field equipment. • limits soil exploration by roots and Compacted soils can also be the result of natural soil- decreases the ability of crops to take up nutrients and forming processes.
    [Show full text]
  • Dynamics of Carbon 14 in Soils: a Review C
    Radioprotection, Suppl. 1, vol. 40 (2005) S465-S470 © EDP Sciences, 2005 DOI: 10.1051/radiopro:2005s1-068 Dynamics of Carbon 14 in soils: A review C. Tamponnet Institute of Radioprotection and Nuclear Safety, DEI/SECRE, CADARACHE, BP. 1, 13108 Saint-Paul-lez-Durance Cedex, France, e-mail: [email protected] Abstract. In terrestrial ecosystems, soil is the main interface between atmosphere, hydrosphere, lithosphere and biosphere. Its interactions with carbon cycle are primordial. Information about carbon 14 dynamics in soils is quite dispersed and an up-to-date status is therefore presented in this paper. Carbon 14 dynamics in soils are governed by physical processes (soil structure, soil aggregation, soil erosion) chemical processes (sequestration by soil components either mineral or organic), and soil biological processes (soil microbes, soil fauna, soil biochemistry). The relative importance of such processes varied remarkably among the various biomes (tropical forest, temperate forest, boreal forest, tropical savannah, temperate pastures, deserts, tundra, marshlands, agro ecosystems) encountered in the terrestrial ecosphere. Moreover, application for a simplified modelling of carbon 14 dynamics in soils is proposed. 1. INTRODUCTION The importance of carbon 14 of anthropic origin in the environment has been quite early a matter of concern for the authorities [1]. When the behaviour of carbon 14 in the environment is to be modelled, it is an absolute necessity to understand the biogeochemical cycles of carbon. One can distinguish indeed, a global cycle of carbon from different local cycles. As far as the biosphere is concerned, pedosphere is considered as a primordial exchange zone. Pedosphere, which will be named from now on as soils, is mainly located at the interface between atmosphere and lithosphere.
    [Show full text]
  • The Nature and Dynamics of Soil Organic Matter: Plant Inputs, Microbial Transformations, and Organic Matter Stabilization
    Soil Biology & Biochemistry 98 (2016) 109e126 Contents lists available at ScienceDirect Soil Biology & Biochemistry journal homepage: www.elsevier.com/locate/soilbio Review paper The nature and dynamics of soil organic matter: Plant inputs, microbial transformations, and organic matter stabilization Eldor A. Paul Natural Resource Ecology Laboratory and Department of Soil and Crop Sciences, Colorado State University, Fort Collins, CO 80523-1499, USA article info abstract Article history: This review covers historical perspectives, the role of plant inputs, and the nature and dynamics of soil Received 19 November 2015 organic matter (SOM), often known as humus. Information on turnover of organic matter components, Received in revised form the role of microbial products, and modeling of SOM, and tracer research should help us to anticipate 31 March 2016 what future research may answer today's challenges. Our globe's most important natural resource is best Accepted 1 April 2016 studied relative to its chemistry, dynamics, matrix interactions, and microbial transformations. Humus has similar, worldwide characteristics, but varies with abiotic controls, soil type, vegetation inputs and composition, and the soil biota. It contains carbohydrates, proteins, lipids, phenol-aromatics, protein- Keywords: Soil organic matter derived and cyclic nitrogenous compounds, and some still unknown compounds. Protection of trans- 13C formed plant residues and microbial products occurs through spatial inaccessibility-resource availability, 14C aggregation of mineral and organic constituents, and interactions with sesquioxides, cations, silts, and Plant residue decomposition clays. Tracers that became available in the mid-20th century made the study of SOM dynamics possible. Soil carbon dynamics Carbon dating identified resistant, often mineral-associated, materials to be thousands of years old, 13 Humus especially at depth in the profile.
    [Show full text]
  • Unit 2.3, Soil Biology and Ecology
    2.3 Soil Biology and Ecology Introduction 85 Lecture 1: Soil Biology and Ecology 87 Demonstration 1: Organic Matter Decomposition in Litter Bags Instructor’s Demonstration Outline 101 Step-by-Step Instructions for Students 103 Demonstration 2: Soil Respiration Instructor’s Demonstration Outline 105 Step-by-Step Instructions for Students 107 Demonstration 3: Assessing Earthworm Populations as Indicators of Soil Quality Instructor’s Demonstration Outline 111 Step-by-Step Instructions for Students 113 Demonstration 4: Soil Arthropods Instructor’s Demonstration Outline 115 Assessment Questions and Key 117 Resources 119 Appendices 1. Major Organic Components of Typical Decomposer 121 Food Sources 2. Litter Bag Data Sheet 122 3. Litter Bag Data Sheet Example 123 4. Soil Respiration Data Sheet 124 5. Earthworm Data Sheet 125 6. Arthropod Data Sheet 126 Part 2 – 84 | Unit 2.3 Soil Biology & Ecology Introduction: Soil Biology & Ecology UNIT OVERVIEW MODES OF INSTRUCTION This unit introduces students to the > LECTURE (1 LECTURE, 1.5 HOURS) biological properties and ecosystem The lecture covers the basic biology and ecosystem pro- processes of agricultural soils. cesses of soils, focusing on ways to improve soil quality for organic farming and gardening systems. The lecture reviews the constituents of soils > DEMONSTRATION 1: ORGANIC MATTER DECOMPOSITION and the physical characteristics and soil (1.5 HOURS) ecosystem processes that can be managed to In Demonstration 1, students will learn how to assess the improve soil quality. Demonstrations and capacity of different soils to decompose organic matter. exercises introduce students to techniques Discussion questions ask students to reflect on what envi- used to assess the biological properties of ronmental and management factors might have influenced soils.
    [Show full text]
  • Age of Soil Organic Matter and Soil Respiration: Radiocarbon Constraints on Belowground C Dynamics
    April 2000 BELOWGROUND PROCESSES AND GLOBAL CHANGE 399 Ecological Applications, 10(2), 2000, pp. 399±411 q 2000 by the Ecological Society of America AGE OF SOIL ORGANIC MATTER AND SOIL RESPIRATION: RADIOCARBON CONSTRAINTS ON BELOWGROUND C DYNAMICS SUSAN TRUMBORE Department of Earth System Science, University of California, Irvine, California 92697-3100 USA Abstract. Radiocarbon data from soil organic matter and soil respiration provide pow- erful constraints for determining carbon dynamics and thereby the magnitude and timing of soil carbon response to global change. In this paper, data from three sites representing well-drained soils in boreal, temperate, and tropical forests are used to illustrate the methods for using radiocarbon to determine the turnover times of soil organic matter and to partition soil respiration. For these sites, the average age of bulk carbon in detrital and Oh/A-horizon organic carbon ranges from 200 to 1200 yr. In each case, this mass-weighted average includes components such as relatively undecomposed leaf, root, and moss litter with much shorter turnover times, and humi®ed or mineral-associated organic matter with much longer turnover times. The average age of carbon in organic matter is greater than the average age predicted for CO2 produced by its decomposition (30, 8, and 3 yr for boreal, temperate, and tropical soil), or measured in total soil respiration (16, 3, and 1 yr). Most of the CO2 produced during decomposition is derived from relatively short-lived soil organic matter (SOM) components that do not represent a large component of the standing stock of soil organic matter. Estimates of soil carbon turnover obtained by dividing C stocks by hetero- trophic respiration ¯uxes, or from radiocarbon measurements of bulk SOM, are biased to longer time scales of C cycling.
    [Show full text]
  • Soil Carbon Losses Due to Increased Cloudiness in a High Arctic Tundra Watershed (Western Spitsbergen)
    SOIL CARBON LOSSES DUE TO INCREASED CLOUDINESS IN A HIGH ARCTIC TUNDRA WATERSHED (WESTERN SPITSBERGEN) Christoph WŸthrich 1, Ingo Mšller 2 and Dietbert Thannheiser2 1. Department of Geography, University of Basel, Spalenring 145, CH-4055 Basel, Switzerland; e-mail: [email protected]. 2. Department of Geography, University of Hamburg, Bundesstr. 55, D-20146 Hamburg, Germany. Abstract Carbon pool and carbon flux measurements of different habitats were made in the high Arctic coastal tundra of Spitsbergen. The studied catchment was situated on the exposed west coast, where westerly winds produce daily precipitation in form of rain, drizzle and fog. The storage of organic carbon in the catchment of Eidembukta amounts to 5.98 kg C m-2, mainly within the lower horizons of deep soils. Between 5.2 - 23.6 % of the carbon pool is stored in plant material. During the cold and cloudy summer of 1996, net CO2 flux measure- ments showed carbon fluxes from soil to atmosphere even during the brightest hours of the day. We estimate -2 -1 that the coastal tundra of Spitsbergen lost carbon at a rate of 0.581 g C m d predominantly as CO2-C. Carbon loss (7.625 mg C m-2 d-1) as TOC in small tundra rivers accounts only for a small proportion (1.31 %) of the total carbon loss. Introduction tetragona, Betula nana, and Empetrum hermaphroditum might accompany warming on Spitsbergen (WŸthrich, Large terrestrial carbon pools are found in the peat- 1991; Thannheiser, 1994; Elvebakk and Spjelkavik, lands of the boreal and subpolar zones that cover in 1995).
    [Show full text]
  • Interpreting, Measuring, and Modeling Soil Respiration
    Biogeochemistry (2005) 73: 3–27 Ó Springer 2005 DOI 10.1007/s10533-004-5167-7 -1 Interpreting, measuring, and modeling soil respiration MICHAEL G. RYAN1,2,* and BEVERLY E. LAW3 1US Department of Agriculture-Forest Service, Rocky Mountain Research Station, 240 West Pros- pect Street, Fort Collins, CO 80526, USA; 2Affiliate Faculty, Department of Forest, Rangeland and Watershed Stewardship and Graduate Degree Program in Ecology, Colorado State University Fort Collins, CO 80523, USA; 3Department of Forest Science, Oregon State University, 328 Richardson Hall, Corvallis, OR 97331, USA; *Author for correspondence (e-mail: [email protected]) Key words: Belowground carbon allocation, Carbon cycling, Carbon dioxide, CO2, Infrared gas analyzers, Methods, Soil carbon, Terrestrial ecosystems Abstract. This paper reviews the role of soil respiration in determining ecosystem carbon balance, and the conceptual basis for measuring and modeling soil respiration. We developed it to provide background and context for this special issue on soil respiration and to synthesize the presentations and discussions at the workshop. Soil respiration is the largest component of ecosystem respiration. Because autotrophic and heterotrophic activity belowground is controlled by substrate availability, soil respiration is strongly linked to plant metabolism, photosynthesis and litterfall. This link dominates both base rates and short-term fluctuations in soil respiration and suggests many roles for soil respiration as an indicator of ecosystem metabolism. However, the strong links between above and belowground processes complicate using soil respiration to understand changes in ecosystem carbon storage. Root and associated mycorrhizal respiration produce roughly half of soil respiration, with much of the remainder derived from decomposition of recently produced root and leaf litter.
    [Show full text]
  • Soil Organic Carbon in a Changing World
    Pedosphere 27(5): 789{791, 2017 doi:10.1016/S1002-0160(17)60489-2 ISSN 1002-0160/CN 32-1315/P ⃝c 2017 Soil Science Society of China Published by Elsevier B.V. and Science Press Preface Soil Organic Carbon in a Changing World JIA Zhongjun1, Yakov KUZYAKOV2;3, David MYROLD4 and James TIEDJE5 1State Key Laboratory of Soil and Sustainable Agriculture, Institute of Soil Science, Chinese Academy of Sciences, Nanjing 210008 (China). E-mail: [email protected] 2Agro-Technology Institute, RUDN University, Moscow 115419 (Russia). E-mail: [email protected] 3Institute of Physicochemical and Biological Problems in Soil Science, RAS, Pushchino 142290 (Russia) 4Department of Crop and Soil Science, Oregon State University, Corvallis OR 97331 (USA). E-mail: [email protected] 5Center for Microbial Ecology, Michigan State University, East Lansing MI 48824-1325 (USA). E-mail: [email protected] Soil contains more than three times as much carbon like compounds. By characterizing soil organic matter (C) as either the atmosphere or terrestrial vegetation. species using solid-state 13C cross polarization magic Soil organic C (SOC) is essentially derived from in- angle spinning (CPMAS) nuclear magnetic resonance puts of plant and animal residues, which are processed (NMR) (13C CPMAS-NMR) spectroscopy of humic by the microbiota (bacteria, archaea, protists, fungi substances and density-based fractions in a forest eco- and viruses) that dominates SOC transformation and system, Ranatunga et al. observed greater fractions of turnover in complex terrestrial environments. A tiny alkyl C, O-alkyl C, and carbohydrate functional gro- change in the SOC pool would have profound impacts ups in response to burning.
    [Show full text]
  • Inherent Factors Affecting Soil Organic Matter
    Soil organic matter (SOM) is the organic component of soil, consisting of three primary parts including small (fresh) plant residues and small living soil organisms, decomposing (active) organic matter, and stable organic matter (humus). Soil organic matter serves as a reservoir of nutrients for crops, provides soil aggregation, increases nutrient exchange, retains moisture, reduces compaction, reduces surface crusting, and increases water infiltration into soil. Components vary in proportion and have many intermediate stages (Figure 1). Plant residues on the soil surface such as leaves, manure, or crop residue are not considered SOM and are usually removed from soil samples by sieving through a 2 mm wire mesh before analysis. Soil organic matter content can be estimated in the field and tested in a lab to provide estimates for Nitrogen, Phosphorus and Sulfur mineralized available for crop production and adjust fertilizer recommendations. Soil organic matter impacts the rate of surface applied herbicides along with soil pH necessary to effectively control weeds. Soil organic matter impacts the potential for herbicide carryover for future crops, and amount of lime necessary to raise pH. Figure 1. Major soil organic matter components (Source: The Soil Food Web, USDA-NRCS). Inherent Factors Affecting Soil Organic Matter Inherent factors affecting soil organic matter such warm and humid and slower in cool, dry climates. as climate and soil texture cannot be changed. Organic matter also decomposes faster when soil is Climatic conditions, such as rainfall, temperature, well aerated (higher oxygen levels) and much moisture, and soil aeration (oxygen levels) affect slower on saturated wet soils (refer to soil the rate of organic matter decomposition.
    [Show full text]
  • The Importance of Soil Organic Matter in Cropping Systems of the Northern Great Plains
    The Importance of Soil Organic Matter in Cropping Systems of the Northern Great Plains Laura F. Overstreet, North Dakota State University Jodi DeJong-Hughes, University of Minnesota 1. Introduction a. Soil Organic Matter (SOM): chemical nature & fractions b. SOM levels in the Northern Great Plains Soil organic matter (SOM) has been called “the most complex and least understood component of soils” (22). The Soil Science Society of America defines SOM as the organic fraction of soil after removing undecayed plant and animal residues (27). However, organizations and individual researchers differ in their opinion about whether undecayed plant and animal tissues (e.g. stover, dead bugs, earthworms, etc.) should be included in the definition of SOM. In this chapter, we will adopt a broader definition of SOM proposed by Magdoff (1992), which consider SOM to be the diverse organic materials, such as living organisms, slightly altered plant and animal organic residues, and well-decomposed plant and animal tissues that vary considerably in their stability and susceptibility to further degradation. Simply put, soil organic matter is any soil material that comes from the tissues of organisms (plants, animals, or microorganisms) that are currently or were once living. Soil organic matter is rich in nutrients such as nitrogen (N), phosphorus (P), sulfur (S), and micronutrients, and is comprised of approximately 50% carbon (C). Soil organic matter is complex because it is heterogeneous (non-uniform) and, due to the biological factors under which it was formed, does not have a defined chemical or physical structure. Soil organic matter is not distributed evenly throughout the soil and breaks down at various rates by multiple agents that are influenced by the unique environmental conditions in which they are found.
    [Show full text]