This presentation was presented during the Plenary 1, GSOC17 – Setting the scientific scene for GSOC17 of the Global Symposium on Soil Organic Carbon that took place in Rome 21-23 March 2017. The presentation was made by Mr. Rattan Lal from Carbon Management and Sequestration Center – USA , in FAO Hq, Rome

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Carbon Management and
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Soil Organic Carbon Sequestration:
Importance and State of Science
Dr. Rattan Lal
Carbon Management and Sequestration Center
The Ohio State University
Columbus, Ohio

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CONSTITUENTS OF SOIL CARBON POOL
Soil Carbon Pool
Organic Inorganic
Pedogenic Lithogenic
Carbonates Bicarbonates
Live
- Fauna
- MBC
Undecomposed
(Detritus)
Decomposed
Protected Unprotected
DOC POC MOC

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THE SHORT-TERM GLOBAL CARBON CYCLE (2005-2014 DATA)
Anthropogenic
Activities
9.9 Pg/yr
Emissions
90 Pg/yr
Uptake
92.6 Pg/yr
ATMOSPHERE
800 Pg
+4.4 Pg/yr
OCEAN
The ultimate
graveyard
+2.6 Pg/yr
SOIL
6000 Pg to 3-m depth
(Organic & Inorganic)
+3.0±0.8 Pg/yr(Land)
VEGETATION
620 Pg
Live: 560 Pg
Detritus: 60 Pg
Le Quere et al. (2015); Lal (2004); Batjes (1996); Tarnocai et al. (2009); Jungkunst et al. (2012)
MRT = Pool ÷ Flux

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AGGREGATION (PHYSICAL PROTECTION) ENHANCES THE
MRT
Shaking and erosion lead to release of C and its oxidation by microbial processes
Clay particles Domains Micro-aggregates Aggregates Peds
Clay particles Domains Micro-aggregates Aggregates Peds

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SOIL EROSION AND THE GLOBAL CARBON BUDGET
• Transport and fate of soil organic carbon by erosional processes is an
integral component of the global C budget, but ignored.
• Soil erosion affects C budget directly and indirectly
Direct Effect
• Soil transport
• Topsoil truncation
Indirect Effects
• Plant growth/biomass production
• Soil water and temperature
• Soil aggregation
• Soil aeration and CO2, CH4, N2O
• SOC redistribution
• The Global Carbon Project must consider erosion-induced transport in its
annual assessment.

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CO2,N2O
CO2,CH4,N2O
GaseousEmissions
Stream
Top Soil
TRANSPORT, REDISTRIBUTION AND DEPOSITION OF SOIL ORGANIC CARBON ON AN
ERODED LANDSCAPE (LAL, 2016)
Delivery ratio is about 10%.
It decreases with increase in distance from the source.

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CUMULATIVE CO2 EMISSIONS AND SINKS BETWEEN 1750-2015
Le Quéré et al. (2016)
Source/Sink 1750-2015 (PgC)
Sources Fossil fuel and industry 410±20
Land use change 190±65
Total emissions 600±70
Sinks Atmosphere 260±5
Ocean 175±20
Residual terrestrial 165±70
With sources and sinks of landuse being uncertain, the global carbon
budget remains a work-in-progress.

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SOIL ORGANIC CARBON SEQUESTRATION
It is the process of transferring CO2 from the atmosphere into the soil of a
land unit plants, plant residues and other organic solids which are stored or
retained in the unit as a part of the soil organic matter with a long mean
residence time.
Thus , deposition/burial of C by erosion , land application of C-enriched
amendments( e.g., bio-char , compost , manure ,mulch etc.) and the burial of
biomass in deep mines or ocean floor brought in from outside the land units
are not sequestration.
Olson, Al-Kaisi, Lal, Lower (2014)

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Disease-
Suppressive soil
High Soil
Biodiversity
Mulch Cover crop
MANAGING SOIL HEALTH AND SOM
Mycorrhizae
Integrated Nutrient
Management
Rhizobium
Molecular-based signals
Integrated livestock-
tree systems
N, P, K, Zn, H2O
No-till

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PLANT FUNCTIONAL TRAITS AND SOC SEQUESTRATION
• The rate of C assimilation,
• C storage in belowground biomass (root architecture),
• Plant respiration rate,
• Recalcitrant aliphatic bio(macro) molecules
• Phytolith occluded carbon (PhytoC) especially in cereals, and
differences among genotype

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THE PRIMING EFFECTS
It refers to the enhanced or retarded soil organic matter
composition due to amendment of fresh biomass-C or mineral N.
Large amounts of C, N, and other nutrients can be released or
immobilized over a short-time by microbial activities.
• Interactions between different qualities of biomass,
• Interaction between living and dead organic matter,
• Mechanisms and the magnitude of effects depend on a
• Effects of macro-organisms on micro-flora
• Impact of INM

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SOIL FUNCTIONAL ATTRIBUTES FOR SOC SEQUESTRATION
• Clay + fine silt content
• Clay minerals
• Soil depth
• Water retention and internal drainage
• Nutrient reserves (N,P,S micronutrients)
• Slope aspect
• Slope shape

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MECHANISMS OF LONGER MRT OF ROOT VS. SHOOT-DERIVED SOC
• Chemical recalcitrance (cutin, suberins)
• Deep placement
• Interaction with mycorrhizae and root hairs
• Interaction with polyvalent cations
• Physico-chemical protection

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TOWARDS INCREASING CARBON STORAGE IN SOIL
1. Increasing the input of biomass-C and of Ca2+ and Mg2+
1. Decreasing losses by decomposition, erosion, leaching.
1. Enhancing stabilization of SOC by physical, chemical, biological
and ecological protection measures.
1. Enhancing the deep transport of C into the sub-soil.
1. Improving linkages between processes governing SOC and SIC
interactions of mutual enhancement.

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Elemental Ratio Cereal Residues Humus
C:N 100 12
C:P 200 50
C:S 500 70
Crop Residues
Humus
Biochemical Transformations
+ (N, P, S etc.)
NUTRIENTS REQUIRED TO CONVERT BIOMASS INTO HUMUS
There are hidden costs associated with the process of humification.

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Sustainableuseofsoil&waterresources
AND THE
ECOSYSTEM
SERVICES GENERATED
COUPLED CYCLING
OF H2O, C, N, P
Lal (2010)

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CONSEQUENCES OF THE COUPLED BIOGEOCHEMICAL CYCLING
Because of the coupled cycles of C, N, H2O, P, S, etc.,
management-induced changes in one can affect cycling of
others often with adverse environmental impacts or trade-offs:
• Gaseous emission of CH4, N2O
• Leaching of NO3, N2 or NH3
• Changes in soil inorganic C and N

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MECHANISMS OF STABILIZATION OF SOC
Mechanism Process Reference
Physical • Access to microbial processes Dungait et al. (2012)
• Stable microaggregates Vitro et al. (2008, 2010)
• Deep placement in sub-soil Lorenz and Lal (2005)
Chemical • Absorption on clay particles Theng et al. (2012, 2014)
• Formation of organo-mineral complexes Plaza et al. (2013), Chenu and
Plante (2006), Rumpel and Kögel-
Knaber (2011)
Biochemical • Supra-molecular structure Piccolo (2001)
• Formation and selective preservation of
molecules
Schnitzer and Monreal (2011)
• Recalcitrant substances Lorenz et al. (2007)
• Clay hutches Lündsdorf et al. (2000)
Ecological • Ecosystem property Schmidt et al. (2011)

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TEMPERATURE DEPENDENCE OF SOM DECOMPOSITION AND
FEEDBACK TO CLIMATE CHANGE
(Kinetic Theory, Arrhenius, 1889)
1. Decomposition rate increase with increase in temperature when substrate
availability and enzyme activity do not constrain the reaction rate
(Davidson and Janssens, 2006).
1. Increase in decomposition rate with the warming temperature is more in
colder than that in warmer climates (Del Grosso et al., 2005; Kirschbaum,
1995).
2. The decomposition reactions with high activation energies (i.e., slow rate)
will experience greater temperature sensitivity than those with low
activation energy (i.e., fast rate).

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THE DEBATE ABOUT TEMPERATURE-SENSITIVITY OF SOM
Assumption: Increased response in the rate of decomposition of recalcitrant
substrate with increase in temperature will result in large loss of SOC stock.
Argument: Such a rate increase may not be important because the
decomposition rate of recalcitrant materials, while being kinetically sensitive to
temperature, may be so slow that little SOM would decompose regardless of
the temperature (Conant et al., 2011).
Debate: Thus feedbacks to atmospheric CO2 concentrations from soil carbon
are uncertain (Zhou et al., 2009; Janssen and Vicca, 2010), the decomposition
rate (turnover) also depends on the accessibility (Dungait et al., 2012), the
physiology of soil microfauna (Lützow et al., 2009), and on the fact that the
persistence of SOM is an ecosystem property (Schmidt, 2011).

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SOM AS AN ECOSYSTEM PROPERTY
• Molecular structure alone does not control SOM stability.
• Environmental and biological controls predominate (Schmidt et al., 2011).
• The MRT of the fire-derived SOM (biochar), widely believed to be
recalcitrant, also depends on physical protection and interaction with soil
minerals (Brodowski et al., 2006), and the soil fertility trade-offs must also
be considered.
• Thus, management (soil, plant, animals, water, nutrients, tillage,
phytoengineering, cover crops, residues) can play an important role in SOM
persistence and in moderating feedback to climate change (Lal, 2004).

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THE CASE OF PERMAFROST
• Cryosols contain 1672 PgC (Tarnocai et al., 2009; Jungkunst et al., 2013)
• With stabilization due to low temperature, thawing may accentuate
mineralization (Nowinski et al., 2010) even of older SOM.
• However, formation of pedogenic carbonates (Strigel et al., 2005;
Kawahigashi et al., 2006) and enhanced aggregation in active layer
(Schmidt et al., 2001) may stabilize SOM.

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SOIL CARBON STOCKS
• SOC stock: prehistoric, 1750, 1800,
1900, 1950, 2000
• Gaseous emissions
• SIC stocks (3-m)
• SOC stock vs. yield

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OTHER RESEARCHABLE PRIORITIES
• Initiating long-term field experiments to assess
stabilization/destabilization processes and MRT,
• Evaluating global C budget with due consideration to the fate of
erosional processes, soil/water management,
• Mapping SOC stocks to 3-m depth, gaseous fluxes, productivity
effects and critical limits.
• Assessment of SIC and SOC stocks at landscape level.
• Developing new technologies for measurement of stocks (INS,
Mid-infrared reflectance spectroscopy-MIRS).

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CARBON PIE
Total C Pie = (560ppm-400ppm)  2Gt/1 ppm = 320 Gt

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2 – Food & Nutritional
Security
SOIL AS A
COMPONENT OF
THE NEXUS