Objectives Conclusions:conceptual model of OM stabilization  Evaluation of the relevance of stabilization mechanisms in different horizons  Relating.

Slides:



Advertisements
Similar presentations
The Carbon Farming Initiative and Agricultural Emissions This presentation was prepared by the University of Melbourne for the Regional Landcare Facilitator.
Advertisements

Soil Organic C, SON and SOP of Sandy Soils As Affected by Intensive Loblolly Pine Management in SE U.S. Deoyani V. Sarkhot.
Fundamentals of Soil Science
Soil Organic Matter Section C Soil Fertility and Plant Nutrition.
Shirley E. Clark, Ph.D., P.E., D. WRE Robert E. Pitt, Ph.D., P.E., BCEE, D. WRE.
Fate and Transport of Dissolved Organic Carbon in Soils from Two Contrasting Watersheds Oak Ridge National Laboratory, Environmental Sciences Division.
Class evaluations.
Formation and Characteristics of Hawaii’s Soils
The soil “Ewiger Roggenbau Halle (Germany) FYM I” pH (CaCl 2 ) 6 C org 19 mg/g  13 C -26,3 ‰ N tot 1 mg/g  15 N 19,9 ‰ microbial biomass 173 µg biomass.
Chemical Properties of Secondary Phyllosilicates Isomorphous substitution ‘replacement’ of an ion by another of similar size, but differing charge Creates.
Chapter 4: Soil Architecture and Physical Properties
LECTURE 10 Introduction to some chemical properties of soils : Factors affecting plant growth (2)
OM  humus 1º minerals  clays OM, clay, ions Transformations: runoff leaching Rain, OM capillary rise Four processes: Additions Losses Translocations.
The “Master” horizons O A E B C R organic horizon on the soil surface
Dynamics of the Northern Hardwood Ecosystem Yuqiong Hu, Jeff Plakke, Sharon Shattuck, Erin Wiley.
Ch 3 Soil Organic Matter continued.
Forest Soils & Site Productivity Soil Organic Matter and Organisms 1.
Soil Buffering and Management of Acid Soils. pH pH = - log (H + ) If (H + ) = 1 x mol/L (H + ) = mol/L pH = - log (1 x ) pH = - (-3)
Organic Matter. 1.Aluminosilcates are composed of two fundamental units: silica tetrahedra and aluminum octahedra to form sheet-like structures. 2. Cation.
Chemical Weathering. I. Introduction Chemical Weathering I. Introduction II. Process of Decomposition A. Overview: Decomposition alters minerals into.
Anyone who did not attend Lecture I, see me after class for materials and course basics.
Coupled Biogeochemical Cycles William H. Schlesinger Millbrook, New York.
Environmental Processes Partitioning of pollutants 3.i Sorption involving organic matter (between air/soil and water/soil)
Box 1 CO 2 mitigation potential of managed grassland: An example Franzluebbers et al. (2000; Soil Biol. Biochem. 32: ) quantified C sequestration.
Evaluation of a multisurface complexation reactive transport model on field data. Bert-Jan Groenenberg 1, Joris Dijkstra 2, Rob Comans 2,3 1 Alterra Wageningen.
Results of forest soil inventory implemented in within the scope of the demonstration project BioSoil Soil stability in ecologically and socially.
1 Waste Treatment, Chemical ENVE Why Treat Waste Have a RCRA Waste –TSDS –Treat instead of disposal, landfill –Treat before disposal Or treat in.
Soils Up Close: The Soil Profile and Horizon Characteristics.
Soils.
Effects of logging on soil organic carbon in the Coast Mountains of British Columbia, Canada Stephanie Grand and Les M. Lavkulich Soil Water Air Laboratory.
U6115: Populations & Land Use Tuesday, June Biogeochemical Cycling on Land A)Systems Analysis and Biotic Control B)Components of Terrestrial Ecosystems.
Environmental Factors Soils Earth’s Surface 770 % Water 330 % Land OOnly 10 % of land is arable (suitable for cultivation) OOf this arable land,
DOM-typical substrates ( 14 C-labeled):  glucose, fructose, glycine, alanine, oxalic acid, acetic acid, catechol  addition: 80 µg C g -1 sand or 400.
The geochemistry of Thai paddy soils
INFLUENCE OF LANDUSE ON ORGANIC MATTER DISTRIBUTION IN SOIL AGGREGATE SIZE FRACTIONS IN ILE-IFE, SOUTHWESTERN NIGERIA By Oyedele, D.J.; Pini, R.; Sparvolli,
Aquatic Chemistry 367 Civil and Environmental Engineering Meeting time: MWF 11:00-11:50am Meeting room: Abbott Auditorium in Pancoe Pavillion Instructor:
Soil forms when weathered parent material interacts with environment.
Ch. 4 continued Soil Properties.
Dru Yates Learning Objectives List and describe the 5 factors of soil formation List and describe the 4 soil forming processes.
Geologic Control of Soil Carbon Sequestration – Examples from Western Conifer Forests Craig Rasmussen Dept. of Soil, Water and Environmental Science The.
SOIL GENESIS, PHYSICAL, CHEMICAL AND COLLOIDAL PROPERTIES OF SOIL
Major research achievements DFG priority programme 1090 Final workshop Schloss Thurnau, Bayreuth, Germany March 2006 Soils as sink and source of.
Introduction to Soils Chapter 1. Air quality.
Table 1. Effect of no-till on the soil environment. Soil physical characteristics –Increased soil water –Moderation of soil temperature –Increased bulk.
Mixed Oak Ecosystem: Field and Lab Data Integration Deborah Hudleston Catherine Resler Mary Walton Chris Weber.
Bell Ringer In a short paragraph(3-5 sentences)….…describe what uses we have for soil and why it is important to our ecosystem.
Lecture 3a Naming Soil Horizons  Soil horizons (layers in the soil) are named so differences between soils can be identified.  Naming soil horizons takes.
SOIL: A RENEWABLE RESOURCE Soil is a slowly renewed resource that provides most of the nutrients needed for plant growth and also helps purify water. Soil.
Soil Acidity and Review of Colloid Charge. Mineral Charge.
Soil colloids. CHEMICAL PROPERTIES OF SOIL: Soil Colloids cat ion Exchange organic matter / Organic carbon Carbon –Nitroge ratio Soil fertility Soil reaction.
The Carbon Cycle. Carbon Dioxide and Carbonate system Why is it important? 1. Regulates temperature of the planet 2. Important for life in the ocean 3.
Fontaine S., Barot S., Barré P., Bdioui N., Mary B., Rumpel C. Nature (2007), Vol. 450,
What Is Soil? Chapter 1. Soil Analysis Ch Why Study Soil Science?  what we call soil is also known as the ‘lithosphere’  it plays an significant.
Soil minerals as mediators of nitrogen transformations in the rhizosphere Andrea Jilling1 and A. Stuart Grandy1 1Department of Natural Resources and.
Dynamics of aggregate stability and biological binding agents
Winfried E.H. Blum, Georg J. Lair & Jasmin Schiefer
Effects of water content fluctuations on organic matter transformation
David A. Ussiri and Chris E. Johnson; Syracuse University
Comparative simulative studies using PHREEQC-Interactive and Visual MINTEQ model for understanding metal-NOM complexation occurring in cooling and raw.
Department of Agronomy
Phosphatfractions in litter/soil
STABILIZATION MECHANISMS OF SOIL ORGANIC MATTER IN allophanic and non-allophanic VOLCANIC SOILs in the HIGHLAND area of Tenerife NATALIA RODRÍGUEZ1*, JOSE.
Soil Formation Soil is an important natural resource
Soils and their Significance
Figure 1. Long term annual precipitation received at Bird City, Kansas
Soil and Water Science Department, University of Florida
Chemical Weathering SAPROLITE.
Soils.
Semi-Recalcitrant Dissolved Organic Matter Particulate Organic Matter
Soils.
Presentation transcript:

Objectives Conclusions:conceptual model of OM stabilization  Evaluation of the relevance of stabilization mechanisms in different horizons  Relating time scales of stabilization mechanisms to conceptual pools Material and Methods Operational fractions: (abbreviations see Figure 1) LF <1.6 g cm -3 : LF <1.6 g cm -3 :controlled by recalcitrance & aggregation HF insoluble OM: HF insoluble OM: controlled by recalcitrance & spatial accessibility DF >1.6 g cm -3 : DF >1.6 g cm -3 : mineral associated fraction HF soluble fraction: HF soluble fraction:mineral associated fraction OM resistant to H 2 O 2 -oxidation: OM resistant to H 2 O 2 -oxidation: spatial inaccessible OM Results and Discussion Figure 1: Pool sizes and 14 C ages of soil OM fractions in different horizons of a Dystric Cambisol, Germany. SOC = bulk soil organic carbon, LF = Light fraction 1.6 g cm -3, H 2 O 2 = hydrogen peroxide oxidation, HF = demineralisation with hydrofluoric acid. Dates from Eusterhues et al. (2005) and (2006), Rumpel et al. (2002) and Kaiser and Guggenberger (in preparation). A horizon: 0.77 LF * 112,4 pMC = 77% of bulk soil pMC 0.90 HF insoluble * 113 pMC = 90% of bulk soil pMC 0.23 DF * 112 pMC = 23% of bulk soil pMC 0.10 HF soluble * 98 pMC = 10% of bulk soil pMC  Selective preservation & resynthesis and  Occlusion in aggregates are important as also indicated by a typically strong crumb structure.  Relevance of organo-mineral interactions is evaluated as low  Stabilization of OM within the active and intermediate pool (modern bulk soil age) in the surface soil  Pool sizes of not mineral associated fractions decrease in subsoils (HF insoluble fraction to 30% and LF to 12%). In B and C-horizons the HF insoluble fraction is even older than the mineral associated HF-soluble fraction.  Increasing importance of spatial inaccessibility in subsoils.  OM that is oxidized by H 2 O 2 decreases (from 90% to 70% SOC in A- to C-horizons). OM resistant to H 2 O 2 oxidation: hydrophobic OM - intercalated OM - OM in clay microstructures. H 2 O 2 has a low dispersing effect. Bw2 horizon: 0.55 HF soluble * 101 pMC = 60% of bulk soil age 0.8 DF * 84 pMC = 73% of bulk soil pMC 3C horizon: 0.7 HF soluble * 91 = 56 % of bulk soil pMC 0.8 DF * 70 pMC = 70% of bulk soil pMC  Increasing importance of organo-mineral interactions in subsoils. pH in B- and C-horizons is optimal for ligand exchange. Highest amounts of pedogenic oxides are found in the Bw horizon. M. v. L ü tzow a, I. K ö gel-Knabner a, E. Matzner b K. Ekschmitt c, G. Guggenberger d, B. Marschner e, H. Flessa f & B. Ludwig g a TUM, Lehrstuhl f ü r Bodenkunde, WZW, Department f ü r Ö kologie, TU M ü nchen,Germany; b Lehrstuhl f ü r Boden ö kologie, Universit ä t Bayreuth,Germany; c IFZ – Tier ö kologie, Justus Liebig Universit ä t, Giessen,Germany; d Institut f ü r Bodenkunde und Pflanzenern ä hrung, Universit ä t Halle, Germany; e Geographisches Institut, Ruhr-Universit ä t, Bochum, f Institut f ü r Bodenkunde und Waldern ä hrung, Universit ä t G ö ttingen, Germany; g Department of Environmental Chemistry, Kassel University, Witzenhausen, Germany A conceptual model of organic matter stabilization in soils Investigating pool sizes and turnover ( 14 C) of available operational fractions in relation to bulk soil organic matter (OM) LITERATURE: a Sollins, P., Homann, P. & Caldwell, B.A Stabilisation and destabilisation of soil organic matter: mechanisms and controls. Geoderma: Rumpel, C., Kögel-Knabner, I. & Bruhn, F Vertical distribution, age, and chemical composition of organic carbon in two forest soils of different pedogenesis,. Org. Geochem. 33: Eusterhues, K., Rumpel, C. & Kögel-Knabner, I Stabilisation of soil organic matter by oxidative degradation. Organic Geochem. In press. Eusterhues, K., Rumpel, C. & Kögel-Knabner, I Organo-mineral associations in sandy acid forest soils: importance of specific surface area, iron oxides and micropores. Eur. J. Soil Sci in press. Kaiser, K. & Guggenberger, G Long-term stabilisation of organic carbon in acid soil by association with the mineral matrix, in preparation. Poster of Eusterhues, K., Rumpel, C. & Kögel-Knabner, I Radiocarbon dating of soil organic matter fractions: How effective is stabilization by organo-mineral associations? Figure 2: Italic: mechanisms; 3 process groups of mechanisms according to Sollins et al. (1996) a : primary and secondary recalcitrance, spatial inaccessibility, organo-mineral interactions. Pools within broken lines indicate postulated pools but their existence is not verified by direct measurements. DOM = dissolved OM. Table 1: Selected properties of the Dystric Cambisol at Steinkreuz, Germany DepthC Oi+e+a3 - 0n.d. A Bw Bw Bw C n.d.0.1 3C HorizonpH 4C cm% CaCl SandClaySilt % Fe oxAl ox n.d g kg C age [years] Relative amount of SOC in different fractions [%] SOC:modern SOC: 655  25yr SOC: 1756  56yr A horizon Bw2 horizon 3C horizon 0 > > > > > >5000 LF HFinsoluble H2H2 O2O2 oxidable = 100 % HFsoluble resistant DF H2H2 O2O plant residues & exudates A C T I V E P O O L yr microbial / faunal biomass & residues decomposed residues I N T E R M E D I A T E P O O L yr Transport of DOM & colloids OM in clay microstructures P A S S I V E P O O L > 100 yr microbial / faunal biomass & residues Interactions with mineral surfaces Production of charcoal by fire intercalated OM humic polymers pseudo-macromolecules organo-mineral associations Selective preservation &resynthesis Biogenic aggregation organo-mineral associations Complexation with Fe 3+, Al 3+, Ca 2+ occluded particulate OM Formation of hydrophobic surfaces Polymerisatiation Intercalation Abiotic microaggregation Encapsulation charcoal Deutsche Forschungsgemeinschaft DFG Priority Programme 1090 Soils as sink and source of CO 2 - Mechanisms and regulation of organic matter stabilization in soils