CARBON STOCK, CARBON POOLS, CARBON SEQUESTRATION

1. “BRIEF ASCEPTS IN CARBON STOCK, CARBON POOLS AND CARBON
SEQUESTRATION POTENTIAL UNDER DIFFERENT LAND USE OF
INDIAN SOIL”
Prepared by
TADI RAJA SEKHAR
M.Sc. (Agri.)
DEPARTMENT OF SOIL SCIENCE AND AGRICULTURAL CHEMISTRY,
COLLEGE OF AGRICULTURE,
VASANTRAO NAIK MARATHWADA KRISHI VIDYAPEETH, PARBHANI
MAHARASHTRA

2. INTRODUCTION
Cereal production in India increased from 50 million tonnes in 1947 to 219
million tonnes in 2000, though the requeriment is expected to increase to 300 million
tonnes by 2050. But there are several problems of degradation of soil and water
resources leading to reduction in productivity ,input use efficiency ( e.g fertilizer ,
irrigation ) ,pollution of surface and ground waters, and emission of greenhouse
gases (GHGS) From terrestrial and aquatic ecosystem into the atmosphere. Soil
organic carbon play multifunctional role into improve this degradation. Majority of
carbon is held in the form of soil organic carbon, having a major influence on soil
structure ,water holding capacity , Cation exchange capacity ,the soils ability to form
complexes with metal ions to store nutrient , improve productivity ,minimize soil
erosion etc. This organic carbon is highly sensitive to change due to land use
management practices such as increased tillage ,cropping systems, fertilization etc.
Sink of carbon from atmosphere to either plant or soil or directly from atmosphere
into soil is called as soil carbon sequestration. Excluding carbonate rocks ( inorganic
carbon path ), the soil represents the largest terrestrial stock carbon ,holding 1500 P g
=10^15 g). which is approximately twice the amount held in the atmosphere and three
time the amount held in the terrestrial vegetation is reported to contain 600 P g C
.Atmospheric concentration of carbon dioxide and other green house gases is changing
rapidly because of anthropogenic activities including fossil fuel combustion , biomass
burning , cement manufacturing , drainage of wetlands and soil cultivation. The
current level of carbon dioxide concentration in the atmosphere which was at 370 ppm
in 2004 ,is increasing at the rate of 1.5 ppm per year or 3.3 p g C per year.
Researchers predicted that unless drastic measure are taken to reduce net emission of
carbon dioxide ,atmosphere carbon dioxide may increase to 800 to 900 ppm by end of
the 21st
century .
Climatic sensitivity to atmospheric enrichment of carbon dioxide may be 1.5 to
4.5 ◦ C increase in mean global temperature , with attendant increase in sea level. A
bout 20% of earths land area is used for growing crops and thus farming practices
have a major influence on C storage in the soil and its release into the atmosphere as

3. CO2 . With cropping /farming system , the equilibrium levels of soil organic carbon (
SOC ) can be related linearly to the amount of crop residue returned /applied to soil.
The rate of accumulation of SOC depends on the extent to which the soil is already
filled by SOC i.e., the size and capacity of the reservoir. Mechanical disturbance of
soil tillage increases the decomposition rate of SOC. Practices , which increase residue
, and /or plant growth result in enhancing SOC sequestration. The beneficial effect of
SOC is more than improving soil quality and fertility. Total geographical area of
India is 328.9 million hectares (m ha) or about 2.5% of the total land area of the
world. The principal land uses include 161.8 m ha of arable land (11.8% of the world )
of which 57.0 m ha (21.3% of the world ) is irrigated 68.5 m ha of forest and
woodland ( 1.6 % of the world ) 11.5 m ha of permanent pasture (0.3% of the world ).
And 7.95 m ha of permanent crops (6.0% of the world). The large base ,similar to that
of the U.S.A and china , has a potential to sequester C and enhance productivity while
improving environmental quality . The green Revolution of the 1970s need to be
revisited to enhance production once again and to again and to address environmental
issues of the 21st
century including climate change. Thus we need to understand how
land land use and management practices such as fertilization ,tillage, cropping systems
etc. can potential enhance SOC storage and improve environmental quality .The
sequestration mechanism, total carbon stocks in Indian soils ,possible way to enhance
SOC have been discussed in this chapter.
Soils are the largest carbon reservoirs of the terrestrial carbon cycle. Soil if
managed properly ,can serve as sink for atmospheric carbon dioxide .As the
atmosphere CO2 concentration continue to increase globally ,more attention is being
focused on the soil as a possible sink for atmosphere Co2 .There is every possibility
that atmospheric carbon dioxide concentration would be increase in near future. Under
such circumstances ,soil will remain a potent sink for atmospheric carbon-dioxide.
The global soil organic carbon storage corresponds to 615 Gt C in the top 0.2 m depth
and 2344 Gt C in depth of up to 3 m, which is more than the combined C content of
biomass and atmospheric CO2. Soils constitute the largest pool of actively cycling
carbon (c ) in terrestrial ecosystem and stock about 1500-2000 Gt C ( to depth of 1m)
in various organic forms ranging from recent plant litter to charcoal , to very old,

4. humfied compounds and 800 to 1000 Gt C yr as in organic carbon or carbonate
carbon. The total quantity of CO2-C exchanged annually between the land and
atmosphere as gross primary productivity is estimated at 120 Gt C yr and about half of
it is released by plant respiration. Soil are the largest carbon reservoirs of the
terrestrial carbon. Soil contains 3.5% earth’s carbon reserves, compared with 1.7 % in
the atmosphere, 8.9% in fossil fuel ,1.0% in biota and 84.9% in the oceans (Lal 1995).
Mean residence time of soil organic carbon pools have slowest turnover rate in
terrestrial ecosystem and thus C sequestration in soil has the potential to mitigate CO2
emission to the atmosphere. Furthermore, higher carbon stabilization in soil is
benefitting the other ecosystem functioning like improvement in soil structure, water
holding capacity, nutrient retention, buffering capacity and greater availability of
substrate for soil organisms. However, little is known about the actual achievable
carbon level in soil under different Agro-ecological regions of the country.
The amount of organic carbon stored in various soil pools is the balance
between the rate of soil organic carbon input and the rate of mineralization in each of
the organic carbon pools. However, the storage of carbon in soil profile is governed by
soil type, topography, soil organisms and other unknown factors. Carbon sequestration
potential of different soils also vary with the clay content. It is suggested that if a soil
has a very silt +clay content, the potential for soil carbon sequestration would be very
high. But, in true sense, the potential for soil carbon sequestration is generally limited
by the climate (rainfall and temperature) and the net primary productivity of the
region. For example, the soils of dryland (vertisol) which contains appreciable amount
of silt+clay contents had high carbon sequestration potential but in reality, it would be
difficult to attain the true level because of other limiting factors like rainfall,
temperature, and net primary productivity of the region. It means, a soil may be high
carbon sequestration potential that would be achieved only if other factors are non –
limiting. In the subsequent sections, we are trying to high light some of recent
development in soil carbon research and terminology, which will help in developing
sound strategy for carbon sequestration in agricultural soils.
Concepts of soil carbon saturation and related implications-:

5. The soil carbon saturation suggests a limit to the whole soil organic carbon (SOC)
accumulation determined by the physicochemical characteristics of four soil C pools:
unprotected, physically protected ,chemically, and bio-chemically protected ( Stewart,
2007) The relationship between soil structure and the ability of soil to stabilize soil
organic matter (SOM) is the key element in soil C dynamics but very few models have
taken cognizance of this fact (Six et al ., 2002).Native soils C levels reflect the balance
of C inputs and C losses under native condition (i.e. productivity .moisture and
temperature regimes ) , but do not necessarily represent an upper limits in soil C
stocks . Most SOC model assume a linear increase in C content with C input, and thus
C sequestration can continue regardless of the amount of organic carbon already
contained in each SOC pools. Contrary to this, in many long-term experiments, soils
rich in C did not show any further increase in SOC following an enhanced C input.
These finding suggest that there exists a soil carbon saturation limit. The difference
between a soil’s theoretical saturation level and the current carbon content of the soil
is defined as saturation deficit (Stewart et.al 2007)Hassink (1997) reported C
saturation of the silt + clay protective capacity ,but not the whole soil. This occurs
because C is retained in the labile (unprotected) state, which is subject to a faster rate
of decomposition as the recalcitrant pool approaches saturation. This report clearly
suggests that soil has a definite capacity to capture or sequester organic carbon,
beyond which the added carbon would be escape to the atmosphere. However, the
proposed theory has few implications in soil carbon management. Because the true
soil C level may be of small practical importance, as large organic C inputs must be
maintained over long time periods to sequester large quantities of C (Stewart et
al.,2007). Because of the limitations placed on plant dry matter production and
decomposition rates by climate and soil properties, there are specific levels of SOM
that can be reached for any system in particular geographical and soil type. Hence
maximum attainable level of soil carbon under different agro-ecological regions of the
country would be the pragmatic approach rather than determining carbon
sequestration potential.
Comprehensive Studies on distribution of OC in Indian soils-:

6. Jenny and Raychaudhuri conducted one of the first comprehensive studies on the
distribution of OC in Indian soils in relation to the prevailing climate. but they are not
provided estimates of the total soil C reserves. Dadhwal and Nayak Using ecosystem
areas and representative global average C density and estimated organic C at 23.4 -
27.1 Pg in Indian soil. Chhabra et al estimated organic C pool at 6.8 pg C in the top
1.0 m using estimated SOC density and remote sensing-based area under forest. Gupta
and Rao reported SOC stock as 24.3 Pg for the soil ranging from surface to an average
sub surface depth of 44-186 cm. These data however based on only 48 soil series.
Based on a much broader national data base, Velayutham et al. reported on total mass
of SOC stock followed by Bhattacharya et al who reported on both organic and
inorganic C stocks. India has 5 distinct bioclimatic systems with varying MAR. they
are cold and hot (MAR <550mm), semi-arid (MAR 550-1000mm), sub-humid (MAR
1000-1,500), humid to per humid (MAR 1,200-3,200 mm) and coastal (MAR 900-
3000mm) . The major soils of India are vertisols, Mollisols, Alfisols , Ultisols
,Aridisols, Utisols , Aridisols , Inceptisols , and Entisols covering 8.1 , 0.5 , 12.8 ,
2.6 , 4.1, 39.4 , and 23.9 % respectively of the total geographical area (TGA) of the
country. Although soils of India in 5 bioclimatic systems, but only a few soil orders
are spread in more than one bioclimate. Vetisols belong to arid hot, semi –arid, sub
humid and humid to per humid climatic environments. Mollisols belong to sub-humid
and also humid climates. Alfisols belong to semi-arid, sub-humid and also in humid to
per humid climates. Whereas Ultisols belong to only humid to per humid climates.
Both Entisols and Inceptisols belong to all the 5 bio climate zones of India, and arid
sols belong to mainly to arid climate environments. This baseline information
indicates that expect for the ultisols and aridisols , the rest of 5 soil orders exit in more
than one climate zone of India. The absence of Oxisols and the Ultisols ,occupying
only 2,56% of TGA of the country , suggest that soil diversity in the geographic
tropics in general and in India in particular , is at least as large as in the temperate
zone .Therefore any generalizations about tropical soil are unlikely to have wider
applicability because of the diversity of soil are unlikely to have wider applicability
because of the diversity of soil and the factor affecting organic matter (OM) dynamics
.As the tropics comprises 40% of the land surface of the earth , more than one- third

7. of the soil of the world is of tropical type . Global extent of such soil suggest that any
is developed in India for enhancing crop productivity and maintain soil health through
C sequestration might also have application in similar soils occurring elsewhere in the
tropical and sub- tropical part of the world. A review of Indian soils and their capacity
to sequester organic and inorganic carbon in seven soil orders and the factors
favouring C sequestration amidst nuances of pedo- genesis and poly genesis due to
tectonic, climate and geomorphic episodes during the Holocene. Soil captures and
store both organic and inorganic carbon (SIC), In developing appropriate management
for SOC sequestration, basic information on SOC and SIC stocks needed. The SOC,
SIC and the total carbon stock in seven orders indicate that the SOC stock (in first 0-
150 cm) of Indian soil is less (29.92 Pg ) than that of SIC ( 33.98 Pg ) . The SOC and
SIC stocks in the 0-30 cm depth of in five bio-climatic zones of India. It indicates that
SOC stocks are two times more than SIC stocks. Although the presence of caco3 in
the humid and per humid region is due to its inheritance from strongly calcareous
parent material the SIC stock in dry climate is relatively large. In all soli orders,
expect the Ultisols, the SIC stock increase with depth, indicating are affected by dry
climatic condition that cause more calcareous in the sub soil.
Soils of India and their carbon pool-: In accord with a wide range of eco-regions (
sehgal et al .,1991) India is also endowed with diverse soil of varying characteristics
out of the total land area of 297.3Mha of Alfisols (27.3%) , 60.4 Mha of vertisols (
20.3%) ,51.7 Mha of Inceptisols ( 17.4%) ,36.6Mha of Ultisols (12.3%) ,24.8 Mha of
Entisols (8.3%) , 18.3 Mha of Aridisols (6.2%) ,1.8 Mha of mollisols (0.6%) ,and 0.8
Mha of Gelisols (0.27%) .These diverse soils are also characterized by a wide range of
SOC concentration ,which is generally related to clay content (Ali et al.,1966) and
climate (Jenny and Raychaudhary,1960) .In general SOC concentration increase with
clay content and rainfall ,and decrease with increase in mean annual temperature
.Some of these soils have been cultivated for centuries, and often with low off-farm
input ,based on systems that involve removal of crop residue and dung for fuel and
other purposes. Consequently, SOC concentration of most soils low that SOC
concentration of moist soil is less than 10g/Kg, and is generally less than 5g/kg.
Because of the clay contents, the SOC concentration is especially low in alluvial soils

8. of Indo-Gangetic plains, coarse –textured soils of southern India, and arid zone soils
of north western India (Dhir et al .,1991).
The prevalent low levels of SOC concentration are attributed to soil-mining practices
of excessive tillage, imbalance in fertilizer use, little or no crop residue returned to the
soil, and severe soil degradation. Consequently, even the well –established
relationship between climate (temperature and precipitation) (Jenny and
Raychaudhary ,1960) and SOC concentration does not exit. the low SOC
concentration in soils with rainfall regime of 500-1000 mm/y. Under native system
and undisturbed soils, however, the SOC concentration of most soils is high (jenny
and Raychadhuri ,1961). Total SOC pool in soils of India is estimated at 21Pg to 30
cm depth and 63pg to 150 cm depth. The SOC pools in soils India is 2.2% of the
world pool for 1 m depth and 2.6% to 2 m depth. The decline in SOC concentration of
cultivated soils by 30-60% compared with the antecedent level in undisturbed
ecosystems even by 1960. The total soil C pool also comprises the soil inorganic
carbon (SIC), which is generally high in calcareous soils of arid semi-arid regions.
Calcareous soil are widely distributed covering 54% of the geographical area of India,
but especially occur in Rajasthan, Gujrat, Punjab, Haryana, Uttata Pradesh,
Maharashtra, Karnataka, Tamilnadu, Andhra Pradesh and part of Madhya Pradesh and
Bihar (Pal et al 2000). The SIC pool in world is estimated at 196 Pg to 1-m depth
(batjes,1996) therefore, the SIC pool in soils of India comprises about 27% of the
world total. Pedogenic or secondary carbonates play a significant role in C
sequestration through formation of Caco3 or Mgco3 and leaching Ca (Hco3)2
especially in irrigated systems. The rate of formation of secondary carbonates may be
range from 30-130 kg/ ha/y (Pal et al ., 2000) . The principal cause of decline in SOC
pool in degraded soils is a related in biomass productivity and low amount of the crop
residue and root returned to the soil. A typical example of the low SOC pool is in salt-
affected soil of Haryana, Andhra Pradesh and west Bengal. Even in the surface 0 to 10
cm layer, the SOC pool may be lower than 5g/kg (Singh and Badyopadhyay ,1996).
Accelerated soil erosion depletes the SOC pools severely and rapidly. The SOC
fraction is preferentially removed by surface runoff and wind because it is
concentrated in the vicinity of the soil surface has low density (1.2 to 1.5 Mg/m3

9. compared with 2.5 to 2.7 M g/m3 for the mineral fraction). Consequently, eroded
sediments are enriched with SOC pool compared with the field soil with an
enrichment ratio of 1.5 to 5.0 (Lal,1999). The SOC loss by erosion and runoff can be
high even on gentle slope of 0.5 to 3.0 % (Banerjee et al., 1991). Soil erosion is four
step process .it involves detachment, breakdown, transport, and deposition of soil
particles. soil detachment and breakdown are caused by soil slaking or disruption of
aggregate by raindrop impact, shearing force of flowing water or blowing wind, and
collision among particles. Break down of aggregates exposes SOC hitherto
encapsulated and physically protected to microbial process. Although the fate of SOC
displaced along with eroded sediments is governed by a series of complex and
interacting processes, a considerable part of it is mineralized leading to release of CO2
under aerobic conditions CH4 under anaerobic environments. Lal (1995) assumed that
20% of the SOC displaced by erosion is mineralized. Assuming that 20% of the
eroded SOC is mineralized, erosion-with erosion emission of C in India is estimated at
6 T g C /y. This compares with erosion-induced emission of 15 Tg C /y. This
compares with erosion –induced emission of 15 Tg C/Y in the Us (Lal et al 1998) and
1.1 pg C /y in the world (Lal ,1995) therefore, adaption of conservation –effective
measures that reduce erosion may lead to reduction of carbon emission from erosion –
prone ecosystems.
Carbon stock of Indian soil-: Lal et al (2004) computed carbon sequestration
potential of Indian soils by assuming converting degraded soil to restorative land use
and estimated total potential of 39-49 T g C y. Indian soil have considerable potential
of terrestrial / soil carbon sequestration. They estimated the soil organic carbon (SOC)
pool of 21 pg in 30cm depth and 63 pg in 150 cm depth. The restoration of wasteland,
degraded lands /desertified soils and ecosystems (e.g., afforestation, improved
pastures) and adoption of improved farm management practices can be enhancing soil
organic carbon and improve soil quality and soil health. The organic carbon pool in
soils india and the world is presented below the table. All these estimates by are based
on Walkley and Black C measurement. However, there is problem of computing soil
carbon content by Walkley-Black method which give only an approximation soil
carbon content. The walkley and Black method gives variable recovery of soil organic

10. C. A general standard conversion factor of 1.32 for in complete oxidation of organic
carbon is commonly used to convert Walkley –black carbon to the total carbon –C
content ,although true factor vary greatly between and within soils because of
difference in the nature of organic matter in different soil depth and vegetation type.
Soil organic Carbon ( SOC) Concentration of some soils in India -;
LOCATION SOIL TYPE TEXTURE SOC CONTENT (
g/kg)
Bangalore, KT Haplustalf Sandy loam 5.5
Barrackpore, WB Eutrochrept Sandy loam 7.1
Bhubaneswar, O Haplustalf Sandy 2.7
Coimbatore, T N Vertic Ustochrept Clay loam 3.0
Delhi Ustocherpt Sandy loam 4.4
Hydrabad, T Tropaquept Sandy clay loam 5.1
Jabalpur,MP Chromustert clayey 5.7
Ludhina ,Pb Ustochrept Loamy sand 2.1
Palmpur, HP Hapludalf Silty clay loam 7.9
Pantnagar,UP Hapludoll Silty clay loam 14.8
Rauchi, B Haplustalf Silty clay 4.5
(Source: Adapted from Nambiar,)
Inference -: According to the Nambiar the soil SOC content report in different
locations major cities in India. The highest SOC content reported in Pantnagar U. P is
14.8 g/kg, this soil texture is silty clay loam and soil types is Haplodoll. the climate of
these soils humid and high vegetation good rainfall condition and temperature high
forest coverge good clay content area causes good SOC content in the soil. The lowest
SOC content reported at Ludhina PUNJAB is 2.1 g/kg. These state soils texture is
loamy sand and soil type is Ustochrept . The low SOC content is due to high burning

11. crop residues and low soil and water conservative practices , high temperature , low
clay content , Indiscriminate use of fertilizers and low rainfall
Organic carbon pool in soils of India and the world -:
SOIL ORDER INDIAN
SOIL (0-30
CM) (Pg)
INDIAN
SOIL (0-
150CM) ( pg)
WORLD
SOIL ( 0-
25CM ) (Pg)
WORLD
SOIL (0-
150CM) ( Pg)
Alfisols 4.22 13.54 73 136
Andisols - - 38 69
Aridisols 7.67 20.3 57 110
Entosols 1.36 4.17 37 106
Histosols - - 26 390
Inceptisols 4.67 15.07 162 267
Mollisols 0.12 0.5 41 72
Oxisols 0.19 0.49 88 150
Spodosols - - 39 98
Ultisols 0.14 0.34 74 101
Vertisols 2.62 8.78 17 38
Total 20.99 63.19 652 1555
(Source : Adopted from Lal et al )
(Source: Adopted from Batjes , ( world soil) )
Inference-: In the above the table, we display the soil organic pools in the India and
world. In that table we know the SOC pool in different depths of soil order. They are
taken soil 0-30 cm in different soil orders contains total SOC content is 20.99
petagrams. But the highest SOC contained soil order is ARIDISOL 7.67 petagrams at
the soil depth 30cm but lowest SOC contained soil order in India recorded as
MOLLISOL 0.12 petagrams . The SOC content in different soil orders in India at soil
depth 0-150 cm is recorded total SOC is 63.99 petagrams but the highest contain soil

12. order Is Inceptiol 15.07 petagrams and the lowest SOC contained soil order is
ULTISOLS 0.34 petagrams
Soil organic carbon (SOC) concentration of soils of India in relation to rainfall
regime and temperature-;
Rainfall (mm/y) Mean annual
temperature (◦c)
SOC content of
surface soil(g/kg)
SOC content of
sub surface soil (
g/kg)
<500 25.9-26.7 1.2-8.0 1.2-4.0
500-1000 23.6-27.9 1.8-12.5 0.7-11.7
>1000 24.4-27.2 2.6-9.0 2.3-8.4
(Source: Adopted from Sekhon and Meelu ,)
Inference -: the presented above table talks about relation between temperature and
rainfall on SOC content in the surface and sub surface soil. According jenny,
Rayachaudhaury the rainfall increases the SOC content in the soil, At the same time
high temperature cause soil SOC loss occurs due to decomposition. the low rainfall
<500 and MAP cause 25.9-26.7 causes lot of SOC decomposition losses occur due to
temperature. but good rainfall 500-1000mm and optimum MAP causes The SOC in
the soil increase due low decomposition and high infiltration of carbon. The high
rainfall >1000 and MAR cause lot of SOC losses occur due to soil erosion but if can
fallow AGROFORESTRY, Social forestry can reduce the soil SOC losses
Soil Carbon Stocks and Their Distribution in the Soil Profile in Agro Ecological
Sub Regions (AERS)-: Using broad soil data, total C in Indian soil was estimated in
60 AESRs. The SOC and SIC stock in Indian soil based on point data of bench mark
(BM) Soils and from other reported in the literature in 60 AESRs were estimate stocks
to different soil depth namely 0-30 ,0-50, 0-100, and 100-150 cm. This estimate
indicates 29.97 Pg SOC in the 0-150 cm depth of the soil. The first ever estimate of
total SIC stock of Indian soils indicates 34.03 Pg in the first 0-150 cm depth. The TC
stock (SOC plus SIC) is 64 .0 Pg . however, the content of SOC and SIC follow a
reverse trend with depth. The relative contribution of SOC and SIC stock to the total

13. stock in 0-30 cm depth is 70 and 29% respectively. However, in the 0-150 cm soil
depth, the contribution of SOC and SIC is 47 and 53% respectively. The enrichment
of SOC in the Upper horizon (0-30cm) is due to the accumulation of organic C in
various agriculture land uses, where as that of SIC in deeper layer (beyond 30 cm) is a
result of accumulation of pedogenic caco3 (PC) due to regressive pedogenesis in the
arid and semi-arid climates of the Holocene. The SOC stock of Indian soils stored in
the upper 30 and 150 cm depth when compared to the stock for tropical regions and
the world shows that the share of Indian soil is not substantial because in India there
are very few OM rich soil like Histosols, Spodosols, Andosols, and Gelisols and the
area under Mollisol is relatively small. Moreover, the soils of India cover only 11% of
the total area of the world. Even under unfavourable environmental condition for OC
rich soils, the SOC in Indian soils demonstrate in SOC in Indian soils, is largely due to
less accumulation of organic C in soil of the arid and semi-arid and dry sub-humid
climatic region, which cover nearly 50% of the TGA of India.
Carbon stock ( pg) distribution by order in Indian soils-;
Soil order Soil depth
range (cm)
Carbon stock
(pg.) (SOC)
Carbon stock
(pg.) ( SIC)
Carbon stock
(p g) (T C)
Entisols 0-30
0-150
0.62
2.56
0.89
2.86
1.51
5.42
Vertisols 0-30
0-150
2.56
8.77
1.07
6.14
3.66
14.90
Inceptisols 0-30
0-150
2.17
5.81
0.62
7.04
2.79
12.85
Aridisols 0-30
0-150
0.74
2.02
1.40
13.40
2.14
15.42
Mollisols 0-30
0-150
0.09
0.49
0.00
0.07
0.09
0.56
Alfisols 0-30
0-150
3.14
9.72
0.16
4.48
3.30
14.20

14. Ultisols 0-30
0-150
0.20
0.55
0.00
0.00
0.20
0.55
Total 0-30
0-150
9.55
29.92
4.14
33.98
13.69
63.90
(Source; Adopted from Bhattacharya et al)
Inference -: In the above the table, we know the Soil organic carbon SOC and soil
inorganic carbon SOC at different soil depth in different soil orders in India. The soil
organic carbon in the ALFISOLS recorded as highest soil organic carbon content soil
that is 3.14 pg at 30cm soil depth and 9.74 Pg at 0-150cm soil depth .The lowest soil
organic carbon recorded in MOLLISOL that is 0.20 pg at 0-30 depth and 0.49 pg at 0-
150cm.The soil inorganic carbon pool recorded highest in ARIDISOLS that is 1.40 pg
at 30 cm soil depth and 13.40 at 0-150 cm depth , the lowest value of soil inorganic
carbon is recorded in ULTISOLS , but Total carbon content High in
VERTISOLS that is 3.66pg at 0-30 cm depth and 14.90 pg at 0-150 cm depth . The
total soil organic carbon recorded in India soil orders is 9.55pg at 0-30cm and 29.92
pg at 150cm at the same time soil inorganic carbon in India soil orders is 4.14 pg at 0-
30cm soil depth and 33.98 Pg at 150cm soil depth. The total carbon content recorded
is 13.69 Pg at 0-30cm depth and 63.90 pg at 150 cm. The soil organic carbon and soil
inorganic carbon in India reported by Bhattacharya
SOC Stocks in Relation to AESRs-;
SOC stocks of different AESRs do not help identifying areas for OC sequestration
because C stocks in soil depend largely on the areal extent of the soil besides other
factors such as C content, depth and bulky density of soils. Even with a relatively
small SOC content (0.2-0.3%), the SOC stocks of arid and semi- arid soils indicates a
high value due to large area under dry region. The concept of C stock per unit area
(Pg/m ha) to realize the influence of soil was therefore, advocated. They set a
threshold value of 0.03 Pg SOC /m ha, as an effective approach in determining a
system (agriculture, horticulture, forestry) that can sequester substantial amount of OC
in the soil.

15. Soil organic and inorganic carbon stock ( Pg ,0-30) in different zones in India-:
Bioclimatic
zone
Area
coverage
(m ha)
% of
TGA
SOC
stock
% of
SOC
stock
SIC
stock
% of
SIC
stock
TC
stock
% of
TC
stock
Stock
per
unit
area (
Pg/m
ha)
SOC
Stock
per unit
area
(Pg/m
ha) SIC
Cold arid 15.2 4.6 0.6 6 0.7 17 1.3 10 0.39 0.046
Hot arid 36.8 11.2 0.4 4 1.0 25 1.4 10 0.011 0.27
Semi-arid 116.4 35.4 2.8 30 2.0 47 4.8 35 0.025 0.016
Sub humid 105 31.9 2.4 26 0.33 8 2.7 2.0 0.024 0.003
Humid to
perhumid
34.9 10.6 2.0 26 0.04 1 2.04
- 15
0.060 0.001
Coastal 20.4 6.2 1.3 13 0.07 2 1.37
--- 10
0.064 0.033
( Source; Adapted from Bhattacharya et al )
Inference-: In the above table we know the soil organic carbon and soil inorganic
carbon in different bioclimate zones in India.in that table SOC soil organic carbon and
soil inorganic stock and percentages of stock occupied in bioclimatic zones. And total
carbon stock present bioclimate zone and total carbon stock percentage, stock per unit
area of organic carbon and stock per unit area of soil inorganic carbon present in
bioclimatic zones of India. The highest SOC stock and percentage of SOC stock
recorded in semi-arid bioclimate zone is 2.8pg and 30 % and lowest values recorded
in hot arid 0.4 pg SOC stock and 4 %. The SIC stock and percentage of SIC highest
recorded in semi- arid bioclimate zone and lowest SIC stocks and percentage recorded
in humid and perhumid. The total carbon stock located highest in semi-arid
bioclimate 4.8 pg and 35%. The lowest Total carbon stock present in cold-arid
bioclimate zone. The stock per unit area SOC highest in cold arid bioclimate zone and
the least soil organic low in hot arid bioclimate zone. The stock per unit area soil

16. inorganic SOC pool highest hot arid climate and lowest inorganic SOC in humid to
perhumid
Changes in SOC and CaCo3 with depth in representative Soils from different
ecosystems-:
Soil depth (cm) pH (water) CEC cmol(+)
kg
OC (% ) CaCo3 (% )
Kibber series:
Typic Crothid –
jammu &
Kashmir –Arid
(cold) AESR 1.1
0-25
25-50
50-100
7.8
8.2
8.1
9
6.1
4.5
1.4
0.66
0.57
13.8
13.8
17.3
Shobsar series:
Typic
Camborthid-
Rajastan-Arid
(hot) AESR 2.1
0-25
25-50
50-100
8.5
8.6
8.5
2.8
3.8
2.9
0.01
0.01
0.3
1.4
8.2
10.7
Bhola series:
Vertic
Ustochrept –
Gujarat Semi-
arid (hot, dry )-
AESR 5.1

17. 0-25
25-50
50-100
8.4
8.6
8.7
38.5
43.6
38.9
0.65
0.37
0.25
17.5
20.7
26.6
Nimone series:
Typic Haplustert
– Maharashtra-
Semi arid (dry) –
AESR 6.1
0-25
0-50
50-100 8.1
8.3
8.7
56.9
56.1
35
0.6
0.4
0.4
3
8.8
10.2
Channasandra
series: Typic
Oxic Rhodustalf
– Karnataka –
semi arid (hot,
moist) –AESR
8.2
0-25
25-50
50-100
6.7
6.5
6.8
4.4
10.3
6.3
0.65
0.4
0.2
Nil
Nil
Nil
Itwa series: Aeric
Ochraqualf –
Uttar Pradesh-

18. Subhumid
(hot,dry ) –AESR
9.2
0-25
25-50
50-100 6.6
6.7
7.8
12
14.7
15.1
0.32
0.21
0.19
0.1
6.4
16.5
Gogji Pather
series: Typic
Haplustalf –
Jammu&Kashmir
–subhumid
(warm, moist,
dry) AESR 14.2
0-25
0-50
50-100
7.9
7.8
8.3
11.6
14.3
14.2
0.35
0.25
0.2
0.2
0.23
7.7
Mahimbar series
–Aeric
Hapluquept-
Assam –Humid –
per-humid (hot)-
AESR 15.2
0-25
25-50
50-100
5.8
6.4
7.8
10
9.2
4.5
0.85
0.11
0.11
Nil
Nil
Nil
Sagar series:
Typic
Haplaquept –

19. West Bengal
Coastal –AESR
18.5
0-25
25-50
50-100
6.6
7.5
7.8
22
25.7
26.1
0.69
0.24
0.2
Nil
Nil
Nil
(Source: Adapted from Velayutham et al and Bhattacharya)
Inference-: In the above the table represent the changes in SOC and caco3 with depth
in representative soils from different ecosystems. In that table we taken kibber series
from Kashmir, Shobsar series from rajasthan , Bhole series from Gujarath , Nimone
series from Maharashtra , Channasandra series from Karnataka , Itwa series from
Uttara Pradesh, Gogi Pather series from Jammu Kashmir , Mahimbar series from
Assam, Sagar series from West Bengal. All of the series Kibber Series : Typic
Cryorthid – jammu kashir recorded high OC content at the 0-25,25-50,50-100 cm
depths is 1.4 , 0.66, 0.57 at the same time caco3 % 13.8 %, 13.8% 17.3 %, the shobar
series : typic Camborthid – Rajastan (hot arid ) climate recorded very low organic
carbon 0.01 %,0.01% 0.3% caco3 content is 1.4 % , 8.2% , Bhola series : vertic
Ustochrept – gujarath semi-arid contain low OC values 0.65%, 0.37%, 0.25% but
caco3 recorded high valuecompared to other series that is 17.5% 20.7%, 26.6% .
Nimone series : typic Haplustert –Maharashtra semi-arid dry condition contain OC
0.6% ,0.4%, 0.4% and caco3 3% 8.8%10.2%. Channasandra series :Oxic Rhodustalf
Karnataka contain semi-arid contain OC 0.65%, 0.4% 0.2% but caco3 are nil in the
series .Itwa series : Aeric Ochraqualf uttara Pradesh –sub humid (hot dry) contained
OC% 0.32%, 0.21%,0.19% caco3 contained 0.1 % 6.4% 16.5% , Gogji Pather series :
typic Haplustalf -jammu Kashmir contained 0.35%, 0.25%,0.2% but Caco3 0.2 %,
0.23% 7.7%, Mahambari series : Aeric Haplaquept assam contained OC% 0.85%,
0.11%, 0.11% and caco3 nil , Sagar series :Typic Hapluaquept west Bengal coastal
contained OC % 0.69%, 0,24%.0.2% but nil caco3

20. SOC Concentration in BM soils of india-:
Horizon Depth (cm) pH CEC C mol
(+) kg
OC (%) SOC (%)
Typic
Dystrochrept:
Tripura
A1
B1
B2
B3
B4
0-10
10-37
37-73
73-120
120-155
5.0
4.7
4.9
4.8
4.8
5.3
5.6
5.8
7.4
7.4
1.6
1.0
1.2
0.8
0.6
0.012
Ustic
Kandihumult:
Keral
Ap
Bt1
Bt2
Bt3
Bt4
0-15
15-39
39-119
119-162
162-205
5.1
5.2
5.3
5.2
5.4
6.5
6.2
6.6
5.9
5.3
1.2
1.0
0.9
0.6
0.5
0.059
Kanhaplic
Haplustult:
Karnataka
Ap
AB1
AB2
Bt1
Bt2
0-14
14-34
34-50
50-83
83-107
6.4
6.3
6.3
5.9
5.2
6.3
5.7
5.3
4.9
5.1
1.2
1.1
0.6
0.3
0.2
0.004
Typic Vertic
Argiudoll :
Maharashtra

21. A1
Bw
Bt1
Bt2
Bt3
Bc1
Bc2
0-15
15-40
40-74
74-108
108-146
146-175
175-180
5.7
5.7
6.1
6.1
18.7
6.1
6.1
18.6
18.5
18.7
18.6
0.3
20.0
18.5
2.0
1.2
0.7
0.4
0.1
0.1
-
Vertic
Haplustroll:
Madhya
Pradesh
A1
A2
B1
B2
B3
B4
0-6
6-16
16-37
37-74
74-106
106-120
5.9
5.8
5.8
5.9
5.6
5.5
52.2
59.8
59.8
67.4
71.7
73.9
3.5
3.0
2.0
1.2
0.8
0.5
-
Typic
Haplustalf:
Madhya
Pradesh
Ap
Bt1
Bt2
C1
C2
0-10
10-30
30-59
59-94
94-131
6.2
5.9
5.9
6.5
6.7
25.5
29.1
28.8
28.8
36.4
1.9
1.8
1.0
0.4
0.4
-
Aquic
Natrustalf:
Punjab
A1
BA
0-6
6-24
10.3
9.8
8.2
11.8
0.2
0.2

22. Bt1
Bt2
Bt3
Bc
Ck
24-48
48-73
73-97
97-124
124-145
9.6
9.4
9.4
9.4
9.3
13.6
14.2
13.8
9.8
9.0
0.1
0.14
0.1
0.1
0.1
-
(Source: Adapted from velayutham et at )
A bove the table we know the SOC concentration in benchmark soils of India in
different states. In Tripura state Typic Dystrochtept soils recorded different soil
horizons the soil organic carbon values 1.6.1.0,1.2, 0.8, 0.6 % and SOC percentage is
0.012 %. In Kerala State Ustic Kandihumult benchmark soils in different soil horizons
the organic carbon content was 1.2, 1.0, 0.9, 0.6, 0.5% and SOC concentration was
0.059 % . The Karnataka state Kanhaplic Haplustult bench mark soils in different soil
horizons the soil organic carbon values are 1.2, 1.1, 0.6, 0.3, 0.2% and SOC
concentration was 0.004 . The Maharashtra states benchmark soils Typic Argiidoll in
different soil horizons the organic carbon was 2.0,1.2,0.7,0.4, 0.1,0.1.% , The Madhya
Pradesh vertic Haplustalf benchmark soils in different soil horizons soil organic
carbon 3.5, 3.0, 2.0, 1.2, 0.8,0.5% at the same state Typic Haplustalf bench mark soils
in different horizons the soil organic carbon was 1.9, 1.8,1.0,0.4,0.4%. The Punjab
state Aquic Natrustalf benchmark in different soil horizons was recorcded soil organic
carbon valus 0.2. 0.2, 0.1, 0.14, 0.1, 0.1,0.1 %
Changes in soil organic carbon stock as an effect of land use system in Gondia
district of Maharashtra
Soil carbon stock (ton/ha) for 30 cm depth in land use system
Profile no Land use SOC SIC TC
TRANSECT -1
(Goregaon)
P1(Assalpani) Open forest 15.86 0.81 16.67
P2(Bagarban) More than 10
years of paddy
8.60 0.67 9.27

23. cultivation
(Rainfed)
P3(Assalapani) More than 50
years of paddy
cultivation
(Rainfed )
11.63 0.68 12.31
P4(Bagarban) More than 100
years paddy
cultivation
(Rainfed)
11.57 0.0 11.57
Transect -2
(Aamgaon)
P5
(waghdongari)
Open forest 12.99 0.48 13.48
P6(waghdongari) More than 10
years paddy
cultivation
(Rainfed)
6.29 1.93 8.22
P7 (pauldauna) More than 50
years paddy
(irrigated)
12.59 0.0 12.59
P8(Pauldauna) More than 100
years of paddy
cultivation
12.51 0.0 12.51
Transect-3
(Salekasa)
P9(Salekasa) Dense forest 50.19 0.0 50.19
P10(Nimba) More than 10
years paddy
cultivation
9.29 0.18 9.46

24. (Rainfed)
P11(Nimba) More than 50
years paddy
cultivation
(Rainfed)
12.92 0.0 12.92
P12(Nimkanaa) More than 100
years paddy
cultivation
(irrigated)
13.34 0.0 13.34
Source: - International journal of Environment sciences volume
Author -: Sarika D.patil et al
Inference-:
As The area is homogenous, the difference in estimated SOC stock were caused by
different land use system and 0r land use pattern and the management practices. Soil
in forest showed higher soil orgnic carbon than rice cultivated land. SOC increased as
the duration increased from 10 years to 50 years and then no further because it
reached to a new equillirium value.Therefore further increase in SOC stock after 50
years is very rate.
In view of beginning soil resource, this study demonstrates that conversion from
natural to agricultural ecosysytem brings in a considerable loss in SOC stock.
Moreover, since most soils in the present investigation are much below their potential
level in SOC stock. (because of huge carbon losses), the scope of sequestering organic
carbon in these soils is immense. Further, the stabilization of SOC stock in soils that
remained under paddy cultivation for a period of more than 50 years under existing
condition point at the maximum sequestration potential of these soils. Any endeavour
to further sequester carbon beyond this limit will call for improved management
strategies and hence the regional government should be emphasis and policy priority
toward sequestering carbon stock in the efforts of improving environmental
degradation

25. Estimated biomass carbon and carbon sequestered by tree in agroforestry in
selected districts of Maharashtra
Parameter Type of
carbon
Latur Wardha Thane Nashik
Total biomass
(tree+crop)
Baseline
Simulated
Biomass 14.69
17.69
23.92
42.18
26.91
39.89
28.22
44.44
soil carbon
(Mg C /ha)
Baseline
Simulated
18.65
19.2
16.87
20.80
17.60
19.23
14.82
17.63
Biomass
carbon (Mg
C/ha)
Baseline
Simulated
Carbon 6.76
8.14
11.00
19.23
12.39
18.35
12.98
20.44
Total carbon
(biomass+soil)
(Mg C/ha)
Baseline
Simulated
25.41
27.34
27.34
40.20
29.99
37.58
27.80
38.07
Net carbon
sequestrated
in AFS over
the simulated
period of
thirty years
(Mg C/ha)
------------
---
------------- 1.93 12.33 7.59 10.27
Estimated
annual carbon
sequestered
potential of
AFS in
different
districts (Mg
C/ha/yr)
Carbon
sequestered
0.06 0.41 0.25 0.34

26. Inference: - Total biomass (tree+crop) for baseline come out to be 23.92, 28.22,
26.91 and 14.69 Mg/DM/ha in Wardha, Nasik, Thane, and Latur districts respectively.
the soil carbon is expected to increase from 16.87, 14.82, 17.60, and 18.65 Mg C/ha in
wardha, Nasik, Thane, and Latur districts in thirty years simulation. Total carbon
(biomass+ soil) in baseline was estimated to be 27.87, 27.80, 29.99, and 25.41 Mg
C/ha. both total biomass and total carbon was lowest in latur district because number
of trees/ha in this district very less (2.11) as compared to other three districts. Highest
total biomass (42.18 Mg DM/ha) and total (40.20 MgC/ha) was found in Wardha
district due to highest tree density (13.53 tree/ha). Net carbon sequestrered was
estimated to be 12.33, 10,27, 7.59, and 1.93 Mg C/ha with average of 8.03 Mg C/ha in
four didstricts considering an agroforestry area of 167754.19 ha, net carbon
sequestered in 30 years would be 1.347 million tonnes. Annual CSP of existing
Agroforestry area system in wardha, Nasik, Thane, and Latur districts come out to be
0.41, 0.34, 0.25, and 0.06 Mg C/ha, respectively. the CSP can be increased
considerably by increasing tree density from present 2-14 t0 40-50 tree/ha. In this
way, long term storage of carbon in tree biomass as well as in soils by agroforestry
systems have significant contribution in reducing atmospheric CO2 and mitigation of
climate change. Agroforestry provides the silence to the agricultural production under
climate variability as well as long term climate change through intensification.
Agroforestry systems whether traditional or commercial have potential of carbon
sequestration in the form of tree biomass and soil carbon. They can play a vital role in
mitigating the effects of climatic change through sequestration of atmospheric CO2.
Present Study demonstrated how agroforestry system have significant contribution in
reduction of Atmospheric Co2 through carbon sequestration in selected districts of of
Maharashtra. With suitable agroforestry interventions like planting fruit trees with
crop any loss in crop yield can be compensated by Fruit production. Hence with the
adoption of agroforestry on farmers’ fields, the climatic vagaries like drought may be
tolerated.
Source: - Indian journal of Agricultural sciences
Authors; -R H Rizvi, Ram Newaj , O.P chadurvathi et al

27. SOC IN Forest and Horticultural Systems-:
By and large, black soils ( Vertisols and vertic integrades) under agricultural system in
In dia show QEV of 0.5-0.6% SOC In the surface layer .Naitam and Bhattacharya
made an attempt to provide QE value of SOC of Vertisols under various land use
system (horticulture ,Cotton, cotton plus pigeon pea and forest. Naitam and
Bhattacharyya in moist sub-humid central peninsular India observed that the SOC
sequestration with in the first 100 cm was higher in soils under forest, followed by
horticulture and agriculture system. The QEV of SOC in the first 50 cm depth of soil
under horticultural system was 0.71% over the past 30 years orange cultivation. A
among the three systems, the soil under forest showed the highest value (0.76%) and
the soil under cotton showed the lowest (0.43%) in the first 50 cm depth, which was
increased to 0.50% with the introduction of Pigeon pea in the system. Thus, The
variation in QEV in the clayey and smectitic soils is primarily due to the difference in
land use systems. This was further confirmed by Chandran et al who studied
ferruginous red soil (Rhodostalfs) with mixed mineralogy class in southern India
under various lands uses under forest , agriculture and horticulture .The QEV of SOC
under different systems indicated that agriculture system at 30 cm depth had the
lowest value of OC (0.68%) after 40 years of agricultural land use ,and forest system
had the highest QEV (1.78%) .However ,the maximum threshold limit of 2.04% SOC
at 30 cm depth was reported to be similar for soil in forest ecosystem in a sub humid
climate under high vegetation ,and minimum threshold of 0.63% was reported for the
shrink –swell soil under agricultural land use. The QEV of SOC in the horticulture
system on ferruginous soil was 0.81%, suggesting that this system with greater crop
canopy cover, leaf litter and favourable micro-environment increased SOC content.
Observation made on shrink-swell and ferruginous Alfisols indicate that irrespective
of soil types, the highest QEV is obtained in forest system followed by horticulture,
and lowest value is obtained in the agricultural system. Therefore, for C sequestration,
horticultural system is a better option if forestry is not feasible. The soil under
agriculture system in the sub-humid tropical climate has the potential to attain higher
QEV of 1.0% even under tropical humid climate provide OM is added.

28. Soil carbon stock and pool in Acid sulphate soils of Kerala -:
Total organic carbon content (%) of acid sulphate soils Kerala-
Soil series Rice Coconut Rice-fish Mean
S1-
Ambalapuza
3.34 3.17 3.51 3.34
S2-Purkkad 2.84 3.47 3.23 3.18
S3-Thakazhi 3.44 2.89 6.21 4.18
S4-Thuravur 6.58 2.50 2.11 3.73
S5-Thottapalli 2.59 1.97 2.80 2.46
S6- Kallara 9.38 8.67 8.61 8.89
Mean 4.69 3.78 4.41
Water soluble carbon (mg kg ) of acid sulphate soils of Kerala-:
Soil series Rice Coconut Rice –fish Mean
S1-
Ambalapuza
72.19 59.15 117.77 83.04
S2-Purkkad 56.57 56.57 86.05 66.04
S3-Thakazhi 51.81 62.09 104.12 72.67
S4-Thuravur 201.9 126.98 179.47 169.45
S5-Thottapalli 49.52 44.38 60.24 51.38
S6-Kallara 208.68 202.60 146.25 185.84
Mean 106.78 91.96 115.65
Labile carbon (mg kg ) of acid sulphate soils of Kerala -:
Soil series Rice Coconut Rice-fish Mean

29. S1-
Ambalapuza
5.60 4.64 7.94 6.06
S2- Purkkad 5.33 4.76 8.62 6.24
S3- Thakazhi 9.70 9.59 5.85 8.38
S4-Thuravur 11.24 10.19 9.05 10.16
S5- Thottapalli 4.89 5.05 4.36 4.77
S6-Kallara 13.06 12.55 11.09 12.23
Mean 8.30 7.80 7.82
The result of present study revealed a significant difference in total organic among
the soil series and land use with the maximum value for Riceland use in kallara series
and the minimum value for coconut in thottapalli series. The highest value of water-
soluble carbon was observed from rice in kallara series and the lowest from coconut in
thottapalli series. With respect to labile carbon, the highest value was noted from rice-
based system in kallara series and the lowest from rice –fish in thottapalli series the
mean values of particulate organic carbon was the highest in kallara series under rice
and the lowest in Purkkad series under coconut. the mineralizable carbon was found to
be highest in thottapalli series (rice-fish) and the lowest in thuravur series (rice). The
highest active carbon pools were noted from coconut based kallar and lowest in from
rice-fish in thuravur. The passive pools of were highest in kallara series of acid
sulphate soils. A among the different land uses, rice and rice-fish contributed to
maximum soil organic pools showing the prevalence of conducive environment in
these ecosystems for the build of organic carbon. The proportion of POC and SOC
was highest in kallara series under rice land use indicating it as a potential carbon sink
. The carbon turnover rate was found to be the highest in Thottapalli series under
coconut land use indicating it as a potential carbon source. The emphasizes the need to
conserve the wet land eco system of Kuttanad in kerala to sequester more carbon into
the soil
Carbon sequestration in dominant soil series under Different Land uses of Tamil
Nadu -:, India
Soil organic carbon stock (Mg ha) in Arasanatham series (250-2000 µm)

30. Land use Soil depth
(cm) 0-30
soil depth
(cm) 30-50
Soil depth
(cm) 50-80
Soil depth
(cm) 80-100
Mean
Agriculture 15.4 14.3 12.8 15.4 14.5
Plantation 17.4 16.3 15.9 12.2 15.5
Agroforesty 35.4 36.5 33.3 21.7 31.7
Forest 76.0 63.1 55.1 51.3 61.4
Mean 36.1 32.6 29.3 25.2
Soil organic carbon stock (Mg ha) in Arasanatham series (53-250µm)
Landuse Soil depth
(cm) 0-30
Soil depth
(cm) 30-50
Soil depth
(cm) 50-80
Soil depth
(cm) 80-100
mean
Agriculture 16.5 15.8 14.0 13.7 15.0
Plantation 18.7 16.9 16.3 9.0 15.2
Agro-
forestry
40.1 38.5 34.4 23.7 34.2
Forest 76.8 67.8 53.8 52.0 62.6
Mean 38.0 34.8 29.6 24.6
Soil organic carbon stock (Mg ha ) Arasanatham series (<53 µm)
Land use Soil depth
(cm) 0-30
Soil depth
(cm) 30-50
Soil depth
(cm) 50-80
Soil depth
(cm) 80-100
Mean
Agriculture 21.3 18.4 20.4 20.6 20.2
Plantation 21.2 18.8 17.8 13.9 17.9
Agro
forestry
50.6 40.1 33.5 26.8 38.3
Forest 78.3 69.3 56.7 55.8 65.0

31. Mean 42.6 36.7 32.6 29.3
Soil organic carbon (SOC) is one of the largest and most dynamic reservoirs of carbon
in the global carbon cycle. Soil organic carbon stock under different land uses in
Macro-sized fractions, micro sized fractions and silt+clay sized fractions is presented
above the tables. The variation of SOC stock under different land uses was
significantly prominent at different soil depth and the soil organic carbon (soc) stock
varied significantly among the selected land use types. In Arasanatham series, the
highest SOC stock was recorded under forest land use (78.3 Mg ha) in the silt + clay
sized fractions (<53 µm) and the agriculture land use (21.3 Mg ha) the lowest SOC
stock at 0-30 cm soil depth
With increasing soil depth, SOC stock was found to decrease. similar trend was
observed in Kadambady series also where maximum soil organic carbon stock was
registered under forest land use (56.2Mg ha) in macro –sized fraction, micro sized
fractions (58.2Mg ha) at 0-30 cm depth followed by agro-forestry and plantation.
while comparing the different soil fractions, maximum SOC was retained in the
silt+clay sized fractions, maximum SOC was retained in the silt+clay sized fractions
in all the land uses. Soil organic carbon in the silt +clay sized fraxtions was highest
under forest soil followed by plantations, agro forestry and agriculture land use. The
amount of organic carbon in forest system may be because of high litter content and
extensive root system of forest trees (Mandal et al). The total amount of organic
carbon in the soil can be considered as a measure of stored organic matter. Agriculture
system stored the lowest soil organic carbon content and stocks.
Seasonal wise SOC pool in all the three different sites of Jhimil Jheel wetland,
Haridwar – Uttarakhand, India -:
Seasonal wise SOC pool under grassland and Natural forest of jhilmil jheel
wetland -:
SI NO Seasons Sites SOC Std Std. Error

32. POOL
(t/ha)
deviation
1 Autumn Grassland 81.38 ±20.957 4.68
2 Autumn Natural
forest
76.85 ±17.268 3.86
3 Autumn Plantation 55.95 ±16.759 3.74
4 Winter Natural
forest
131.25 ±23.803 5.32
5 Winter Plantation 123.78 ±22.093 4.94
6 Winter Grassland 72.92 ±20.093 4.64
7 Spring Natural
forestry
170.46 ±31.518 7.04
8 Spring Plantation 155.13 ±37.223 8.32
9 Spring Grassland 73.17 ±19.616 4.38
10 Summer Natural
forest
123.89 ±19.093 4.26
11 Summer Plantation 114.61 ±18.130 4.05
12 Summer Grassland 64.73 ±19.829 4.43
The SOC Pool under different land use of jhimili jheel wetland was estimated and
result were present in above the table 1. The result indicated that during autumn
season the SOC pool was maximum in grassland (81.38 t ha) followed by natural
forest (76.85 t ha) and minimum was under plantation (55.95 t ha) , in winter season
the SOC pool was maximum in under forest (131.25 t ha) followed by plantation
(123.78 t ha) followed by plantation (114.61 t ha) and minimum was grass land
(64.73 t ha) . overall, it was observed that the maximum SOC pool was spring under
the natural forest (170.46 t ha) and the minimum SOC pool was observed in autumn
season and decreased in winter followed by spring and then least was in summer. it
may be because the above ground herbaceous biomass die in autumn and regenerate in
spring in the perennial grassland and that their root systems also have a rapid turnover
but on a longer time scale an estimated 55% of temperate grassland root biomass turn
over annually . The natural grassland locked in a significant amount of SOC and the

33. presence of extensive root biomass of grass community may be one of the reason for
higher SOC pool content
Soil organic carbon stocks and fractions in different orchards of easte rn plateau
and hill region of India -:
Total global carbon in soils between 1500 and 2000 Gtons : The majority of it stored
in forest biomes (Janzen 2004: Smith 2004). Carbon stock in soil depend largely on
the aerial extent of the soil besides other factors such as carbon content, depth, and
bulky density of soils. The Eastern plateau and hill region cover 13% of the total
geographic area of the country and contributes 9, 1, and 7, of the soil organic carbon
(SOC), soil inorganic carbon ( SIC) and total carbon ( TC) stocks of the country
,respectively ( Bhattacharyya et al 2008) .Cropping system and management practices
that ensure greater amount of crop residue returned to the soil are expected to cause
net build-up of the SOC stock. Identifying such system or practices is priority for
sustaining crop productivity. The soils of tropical ,sub-tropical, and arid and semi-
arid regions are reported to be contributing more oxidative product ( particular Co2)
per unit SOC to the atmosphere vis-à-vis the soils of temperate and cooler regions.
Again ,crop species that are cultivated may also play an important role in maintaining
the stock because both quantity and quality of their residues that are returned to the
soil vary greatly affecting their residues that returned to the soil vary greatly affected
their turnover or residence time in soil.( Chan et al (2001) suggest that certain
fractions of soil organic matter are more important in maintaining soil quality and are
therefore , more sensitive indicator of the impact of management practices, Change in
SOC due to management practices are difficult to quantify as these occur slowly are
relatively small compared to the vast SOC pool size, vary both spatially and
temporally (Russell et al 2004). Upon application of organic amendment, a part of
their carbon is stabilized into SOC and distributed among different pools. To better

34. understand the mechanisms by which carbon is lost or stabilized in soil, the soil
organic carbon (TSOC) stock is separated into labile or actively cycling pool, a slow
pool, and a stable or passive, recalcitrant pool with varying residence times (Parton
and Rasmussen 1994). The labile carbon pool is the fraction of TSOC with the most
turnover rates, the labile pool consists of living microbes and their products besides
soil organic matter. At the same time, this pool is important from the point of view of
crop production It fuels the soil food web and therefore greatly influences nutrient
cycling for maintaining soil quality and its productivity (Janzen 1987, chan et al 2001;
Majiumder et al 2007). Highly recalcitrant or passive pool is only very slowly altered
by microbial activities (Sherrod et al 2005). The passive pool is comparatively more
stable than active pool and is slowly decomposable having a larger turnover time. In
this investigation, they hypothesized that different orchard system would be have
influence on the soil carbon pools in the acidic alfisols. They examined the soils of 6-
year- old orchard of mango, litchi, and guava, in an alfisols of the eastern plateau and
hill region with respect to soil carbon pool, soil carbon stock management indices and
carbon sequestration.
Soil organic carbon and its fraction-:
Significant variation (p≤0.05) in total soil organic carbon (C tot) was observed a mong
the different orchard throughout depth (0-0.60 m) of the soil profile. The C tot
gradually decreased with increasing depth of soil up to 0.60 m. Earlier studies also
reported that fallowing reduces soil organic carbon (SOC) by decreasing the amount
of non- harvested plant residue returned to the soil (Calegari et al 2008) while
increasing the cropping intensity increased SOC (Hutchinson et al 2007). The
maximum C tot was recorded in the surface soil as compared with lower depth due to
the addition of roots and plant biomass in surface layer and lack of nutrient and
biological activity in deeper layers, which ultimately constraints the rooting depth
(Ingram and Fernandes 2001). The maximum C tot in 0-0.60 m depth was 62.47 Mg
ha in mango orchard and resulted in 17.2% increase over control. Similarly, the guava
and litchi orchard recorded significantly (P ≤ 0.05) higher C tot and resulted in 12.6
and 11% increase over control, respectively. The higher C tot in mango orchard may

35. be attributed to the different quantities and quality of organic matter input through
fresh litter fall, living organisms and root activity (e.g .turnover and exudates ) (
Vasterdal et al 2008) . On an average, the total C left over in soil through leaf litter
biomass and FYM in 6 –year –old litchi, guava and mango orchard was 5.89, 6.72 and
9.19 t ha, respectively in fact, the confinement of C tot in the orchard subsoil is
essential for long term storage of carbon due to reduced biological decomposition. It
was also thought that the exposed soil surface and breaking of aggregates due to lack
of vegetation which high precipitation could be the reason for lowest C tot content
control plot (Conant and Paustian 2002). The Oxidizable organic carbon (C oc ) varied
40.1 to 46.94 Mg C ha soil among the different orchard was due to significant among
the orchard but when compared with control ,it varied significantly (P≤0.05). This
increase in C oc in different orchard was due to significant (P ≤0.05) increase in
carbon input with organic manure and leaf litter of orchard system ( Purakayastha et al
2008; Gong et al 2009 ; Ma et al 2011) . Similar increase in SOC after manure
application were also reported in long term experiment at Rothamsted (UK) (
powlson et al 1998) .The mango orchard registered as much as 4 and 17% higher C
oc over that of the guava orchard and control ,respectively .The relative
preponderance of C oc under different orchard system was in the following order :
mango orchard ≥guava orchard ≥ litchi orchard ≥ control .Similar to C tot there was a
sharp decrease in its content along depth with 0.15-0.30, 0.30-0.45, and 0.45-0.60 m
depth layers maintaining only 80,64.8 and 51.7% ,respectively ,of the amount in
surface layer.
The different orchard system increased the very labile fraction of carbon (C frac1) as
compared with control. Maximum and significant (P≤0.05) increase in the C frac1 was
observed under guava orchard followed by mango in surface soil (0.05) highest
mango orchard (21.88 Mg ha) throughout the depth of soil profile and resulted in
20,7% increase over control. The guava and litchi orchard resulted in 17% and 14.2%
increase in total C frac1 over control and were statistically at par. Similarly, the labile
carbon fraction (Cfrac2) varied significantly (p≤0.05) among the orchard at the
surface soil. The mango orchard resulted in greater accumulation of C frac2 in the
surface layer. The total C frac2 in mango orchard (14.31Mg ha) was significantly

36. (p≤0.05) highest over control resulting in 13.5% increase. The guava and litchi
orchard registered 6 and 5.4% increase in total C frac2 over control respectively.
Fresh litter fall and root residues are the primary source of SOC leading toward
increased amount of C frac1 and c frac2 in different orchards (vesterdal et al 2008).
The less labile carbon fraction (Cfrac3) and non –labile carbon fraction (Cfrac4) did
not significantly (p>0.05) throughout the depth of the soil profile among the orchard.
The distribution of different carbon fraction followed the order C frac1>C frac4>
Cfrac2>Cfrac3 throughout the depth of soil profile of different orchard was attributed
to the rapid conversion of organic inputs and labile C fraction to recalcitrant forms,
and its persistence under favourable condition of moisture , thick canopy cover and
minimal soil disturbance (sreekanth et al 2013) Lefroy et al (1994) also found similar
variation in Cfrac1,Cfra2,Cfrac3,C which indicated that these fractions were mainly
responding to cropping .Among the orchards, a relatively higher proportion of the
carbon fraction was found in surface soil whereas it was found to decrease with
increasing soil depth. This was found to decrease with increasing soil depth. This was
due to supply and the availability of additional mineralisable and readily hydrolysable
carbon resulting in higher microbial activity in surface layers (Kaur et al 2008)
Active and Passive carbon pool in EPH region of Indian soils-:
The active carbon pool corresponding to very labile and labile pool of oxidisable
organic carbon and varied significantly (P ≤0.05) a mong the different orchard in
surface soil (0-0.30 m), whereas it was non-significant (p >0.05) in the sub-surface of
the soil (0.30-0.60m). The mango and guava orchard recorded significantly (p≤0.05)
higher active carbon pool over control in 0-0.30 m depth. Irrespective of orchard
systems, the maximum active carbon pool was recorded in the 0-0.15 m layer being
highest in guava orchard (12.06Mg ha), and lowest in control (10.57 Mg ha). The
data showed that the total active carbon pool in 0-0.60m depth among soils of
different orchard did not show considerable variation ,however when compared to
control ,it varied significantly (p≤0.05) .The maximum total active carbon pool was
recorded under mango orchard (36.2Mg ha) followed by (34.57Mg ha). Minimum
total active carbon pool was detected under control (30.72 Mg ha) which is nearly 1.2

37. times smaller than the highest value recorded. The higher active carbon pool in
different orchard compared to control may be attributed to the tannin and lignin
constituents formed from the decomposition of leaf litter and root biomass of the
orchard systems protected the carbon from rapid decomposition and thus preserved it
in the aggregates (Kalambukattu et ai 2013
Active Carbon pools in soil different layer (m) of 6-year-old at plandu in EPH
region of India-: active carbon pool (Mg ha)
Orchard Active
carbon pool
soil depth
(0-0.15
Active
carbon pool
soil depth
(0.15-0.30)
Active
carbon pool
soil depth
(0.30-0.45)
Active
carbon pool
soil depth
(0.45-0.60)
Active
carbon pool
total
Control 10.57 7.67 7.08 5.38 30.72
Litchi 10.94 8.96 7.96 6.10 33.97
Guava 12.06 9.30 7.53 5.68 34.57
Mango 11.88 10.66 7.89 6.36 36.20
Mean 11.35 9.00 7.62 5.88 33.87
The passive carbon pool corresponds to less labile and non –labile pool of oxidisable
organic carbon. The maximum passive pool in 0-0.15 m depth was recorded in mango
orchard (8.60 Mg ha) and minimum in control (7.92Mg ha). The passive carbon pool
gradually decreased with increasing depth of soil profile. The results confirmed that
the total passive carbon pool in 0-0.60 m depth a mong soil of different orchard did
not show considerable variation, however, when compared to control, it varied
significantly (P≤0.0.5). The maximum total passive carbon pool was recorded under
mango orchard (26.27Mg ha) followed by guava orchard (25.52Mg ha)

38. Passive carbon pool in soil in different layers (m) of 6-year-old orchard at Plandu
in EPH Region of India-: passive carbon pool (Mg ha)
Orchard Passive
carbon pool
soil depth
(0-0.15)
Passive
carbon pool
soil depth
(0.15-0.30)
Passive
carbon pool
soil depth
(0.30-0.45)
Passive
carbon pool
soil depth
(0.45-0.60)
Passive
carbon pool
total
Control 7.92 5.77 4.77 4.15 22.56
Litchi 8.28 6.96 5.64 4.31 25.20
Guava 8.21 6.94 5.74 4.63 25.52
Mango 8.25 7.26 5.72 4.69 26.27
Mean 8.25 6.73 5.46 4.45 24.89
Soil microbial biomass and microbial quotient-:
The soil microbial biomass (C mic), which normally constitutes about 1-5% of the C
tot can provide an early warning for a possible degrading and / or aggrading effect of
different management practices on soil quality (powlson 1994; Mandal 2005). The C
mic in surface varied significantly (P≤0.05) a mong the orchards. The maximum and
significant (p≤0.05) C mic was 370 mg kg recorded in guava orchard followed by
mango orchard (343 mg kg ) and resulted in 63.7% increase over control .The lower
value C mic in the control seemed to be related to its unfavourable environment
arising out of depletion of nutrient following without any fertilization and surface
runoff , while a higher value in the orchard systems was due to its congenial
environment for microbial growth for C enrichment through FYM and leaf litter
addition (Grego et al 1998) . The cumulative leaf litter biomass added in 6 – year –oid
litchi, guava , and mango orchard was 11.6, 11.9, 12.2 ,t ha ,corresponding to total C
content of 41.5 ,39.1, and 38.5 % respectively .Further ,the higher C mic in guava and
mango orchard was attributed to the quantity and quality of litter with high rate of
decomposition, greater availability of nutrient due to the addition of higher plant
quality ( Ramesh et al 2013) .The microbial quotient ( MQ, C mic as a proportion of C

39. tot ) ranged from 2.79 to 4.26 with the mean value of 3.62% .The MQ between guava
and mango orchard was non-significant (p>0.05) ,when compared with litchi and
control it varied significantly (p≤0.05) .The value of MQ for the soils of the present
study were within the range of of1-5% as advocated by number of researchers
(powlson 1994; Carter 2002) .The higher value of MQ in guava and mango orchard
suggested a greater stability of organic carbon under the Orchard system ( sparling et
al 1992 ) . The lowest value of MQ IN the control under indicated lower soil microbial
biomass carbon and a poor-quality soil with impairment of its capacity for C cycling
(Chaudhury et al 2005). The better nutritional environment to microbial population in
the soils guava and mango orchard increased the quotient (Ruddrappa et al 2005) .
Total fungal and bacterial count varied widely a mong the different orchard system.
The mango and guava orchard significantly (P ≤0.05) highest microbial count over
litchi and control orchard in the surface soil suggesting higher decomposition rate of
leaf litter over litchi resulted in higher labile carbon fraction. Further, the fungal count
was more in mango orchard compared to guava whereas the bacterial count was more
in guava orchard compared to mango. The bacterial and fungal count between mango
and guava orchard was non- significant (p> 0.05). however, a general range of the
count showed an improvement in mango, guava, litchi, orchard over control.
Carbon management index (CMI), Carbon pool index (CPI) and Carbon build
up -: CMI provides an integrated measure of quantity and quality of SOC. Compared
to a single measure such as total SOC concentration, CMI can be used as a more
sensitive indicator of the rate of change of SOC in response to soil management
changes, and was suggested by whitbread et al (1998) to be +a useful technique for
describing soil fertility. The CPI value was higher in mango orchard throughout depth
of soil profile highlighting the high potential of mango orchard in restoring the
original C stock s. The highest CPI value of 1.29 recorded in mango in 0.15-0.30 m
depth. AS a whole, CPI increased in all the orchard over control. There is not much
variation of lability index among the orchard throughout the depth of soil profile. The
guava orchard recorded higher lability index (1.72) followed by mango orchard (1.68)
in 0.015 m depth. This pattern showed that guava orchard provide a less oxidative
environment, giving greater physical protection to the SOM favouring a higher

40. proportion of labile C compared to TSOC by increasing the rate of C lability in the
soil (Blair et al 1995).
The CMI values of mango and guava orchards were significantly (P
≤0.05) higher over litchi orchard and control in 0-0.15 m depth. The highest CMI
values was 228.34 recorded in mango orchard in 0.15-0.30 m depth and resulted in 1.2
–fold better than control. The orchard system promoted higher CMI values, possibly
not only due to the enhancement in the formation of organic matter as a consequence
of the increase in annual C addition, but also due to changes in organic matter quality,
such as C/N ratio, content of lignin, cellulose, hemicellulose, protein, and
carbohydrates, thus modifying the lability of C to move to an oxidized from (Tirol-
Padre and Ladha 2004). The mean CMI ranked as mango orchard (204.18) > litchi
orchard (192.48) = guava orchard (192.41) > control (169.47) due to different litter
stocks and decomposition characteristics of the biomass. The results of the present
investigation are in agreement with the finding of Lakaria et al (2012), who reported
higher CMI of 402 in mango orchard. In the present study, there is net build of TSOC
in soils in all the orchards over control. The carbon build up was highest in mango
orchard (17.3%) followed by guava orchard (11%). The carbon build-up rate is more
important for a long –term perspective, which was found more (1.53 Mg C ha Soil
year) in mango orchard as against lowest of 0.98 Mg C ha soil year in litchi orchard in
0-0.60 m depth of soil. The carbon build up was less in litchi orchard soil compared to
mango and guava, which was attributed to high N content in leaf litter of litchi
(0.52%) associated with resistant lignolytic products slowly down their decomposition
resulted in less carbon build-up (Gundersen et al 2006). The orchard like mango and
guava which have leaf litter of low N content of 0.28-0.31%, respectively, are likely to
be more efficient in C sequestration in soil than the litchi orchard, which give leaf
litter of higher N content.
Carbon management index of soil organic matter in different layers (m ) of 6-
year –old orchard at plandu in EPH region of India -:
Orchard CMI at soil CMI at soil CMI at soil CMI at soil MEAN

41. depth 0-
0.25
depth 0.15-
0.30
depth 0.30-
0.45
depth 0.45-
0.65
Control 161.31 170.17 181.63 164.75 169.47
Litchi 172.53 203.83 203.91 189.65 192.48
Guava 185.71 207.67 193.93 182.35 192.41
Mango 186.21 228.34 205.65 196.53 204.18
Indigenous carbon management practice in NER -:
Number of Indigenous farming system are being practiced in NER and production is
maintaining only through organic nutrition. There are Zabo systems practiced in phek
district of Nagaland which have a combination of forest ,agriculture ,livestock and
fisheries .Rice based farming systems of Apatani plateau occupying a stretch of 26 sq
km area in subansiri districts of Arunachal Pradesh is inhabited by ‘Apatani’tribe ,
bamboo drip irrigation system of jaintia and Nagaland ,Manipur ,and Sikkim ,
Taungya system which is a method of establishing forest species in temporary
combination with field crops are some of the systems which have inbuilt mechanism
of resource conservation .Homested Agroforestry where farmers of Tripura ans Assam
grow number of tree species along with livestock ,poultry and fish mainly purpose of
meeting their own needs is also a low inut hut popular system
GIS mapping of soil organic carbon across NE region-:
Soil carbon density of surface layer was estimated from the soil depth, bulk density
and the corresponding SOC content for the six states of NE region. On interpolation
spatially (using kriging ) In GIS environment ,wide variability among the within each
states of NE region was observed that Average SOC density varied from 10 t ha to 60
t ha across NE states ,with more than half of the area (52% of TGA :15.61 Mha) fall
under medium category SOC density (20-30 t ha) .Nearly one fourth of the area
(23.30% of TGA ) fall under high category SOC density ( 30-40 t ha) while only
8.0% area falls under very high category SOC density (>40-60 t ha) Among the six

42. states Sikkim had maximum area (81.98%) falls under very high SOC density (40-50 t
ha) followed by Manipur (13.03t ha) and Nagaland (4.06%) . Similarly, Sikkim, was
the only state having considerable area (>10%) registed very high SOC density (50-60
t ha) next to Sikkim, Nagaland has 57.5% area falls under SOC density of 30-40 t ha
while 40.4% area recorded 20-30 t ha. Nearly half of the area in Meghalaya (49.51%)
registered 20-30 t ha while in 42.56% area, SOC density was 30-40 t ha. Similarly, in
Among the NE states, Tripura recorded highest percentage of area (81.8%) under very
low category SOC density (10-20 t ha). Assam also registered 1/5 th of the total area
under low SOC density (10-20 t ha) while in 2/3 rd of the area (65.3%), SOC density
was 20-30 t ha
GIS based spatial distribution of different classes of SOC density across NE
region of India
STATE GEOGRAPHIC
AL AREA (M
ha)
Carbon
density (t
ha) in
percent of
total
geographic
al area (10-
20)
Carbo
n
densit
y in %
TGA
(20-
30)
Carbo
n
densit
y in %
of
TGA
(30-
40)
Carbo
n
densit
y in %
of
TGA
(40-
50)
Carbo
n
densit
y in %
of
TGA
(50-
60)
Carbo
n
densit
y in %
of
TGA
(60-
80)
Assam 7.70 19.40 65.31 13.26 1.86 0.17 -
Manipur 2.218 - 49.39 36.51 13.03 1.07 -
Meghalay
a
2.238 1.42 49.51 42.56 4.06 1.72 0.73
Nagaland 1.649 1.71 40.43 57.51 0.35 - -
Sikkim 0.6999 - - 7.17 81.98 10.86 -
Tripura 1.017 81.80 18.20 - - - -
Total 15.611 15.39 52.16 24.30 7.07 0.97 0.13

43. The significant influence of land use practices on surface SOC content across NE
region was affirmed by Choudhury et al they reported that surface soil under grass
land and dense forest contain very high SOC content (<2%) compared to settled
agriculture including low land paddy (SOC -1.45-1.69%) as well as shifting
cultivation (1.70 %). Next to SOC content, it was sampling depth which also reflected
a positive correlation with SOC density (r=+32 to +0.67) and then soil bulk density.
This was also affirmed from the result revealed in considerable variation of SOC
content among the six studied states of NE region, which varied from 1.23% to 2.99%
compared to marginal variation in sampling depth (14. 6 cm to 18. 6 cm) and soil BD
values (0.88 to 1.32 M g m3). variation in parent material, more particularly particle
size distribution climatic factors, more particularly, amount and distribution pattern of
rainfall in luxuriant growth and regeneration rate of phyto- biomass also exert
consideble influence on SOC content and bulk density values. therefore, integrated
effects of host of factor ranging from SOC content to land use practices resulted in
variation of SOC stock –density NE region of India.
AESR (Agro-ecological sub- regions) soil and Crop biomass, carbon stocks in
Madhya Pradesh -: The cropping pattern in the state was much diversified and
dependent on soil type, rainfall, water resources development, and socio- economic
status. Millet and wheat were the major crops in the central and northern regions,
paddy in eastern and southwestern parts of Madhya Pradesh. The introduction of
soybean during the 1980s enhanced the oilseed production. The state contributed
nearly 75% of soybean production and 36% of gram production to the national
production. Food grain production of the state has increased from 8.9 Mt in 1964-65
to 14.1 Mt in 2004-2005. As a result of adoption of high yielding crops and varieties
and intensification of agriculture in the state the total crop biomass has increased.
Crop distribution and intensity pattern play a dominant role in deciding the total crop
biomass and density. District crop biomass carbon stock, respectively. The result
indicated that total estimated crop biomass C for the state is 34.94 Tg and AESR 5 had
maximum crop biomass carbon (2.71 Tg) , The Maximum ( 3.95 Mg C /ha ) and
minimum (0.50 Mg C ha ) crop biomass C density were recorded in Indore and
Shahdol districts respectively .

44. AESR soil and crop biomass, carbon stocks in M.P -:
AESR NBSS&
LUP
CODE
NET
SOWN
AREA
(M ha)
AGRIL.C
DENSITY
IN SOIL
(Mg/ha)
AGRIL.
C
DENSITY
IN CROP
(Mg/ha)
AGRIL.
C Stock
in soil
(T g C)
AGRIL
C Stock
in Crop
(T g C)
TOTAL
1 4.4 2.27 42.35 1.30 96.13 2.95 99.08
2 5.2 5.90 37.00 1.23 218.32 7.23 225.56
3 10.1 6.99 37.66 2.01 263.23 14.12 277.35
4 10.3 3.92 35.26 1.99 138.23 7.93 146.16
5 10.4 1.99 37.45 1.36 74.70 2.71 825.56
Soil organic carbon density and stock-:
Soil organic carbon hold a very important role in global carbon cycle; as it is the
largest terrestrial carbon pool. Soil can be a source (C02, CH4 and N2o) or sink (CO2
and CH4) of greenhouse gases depending on land use and management (Lal 2002).
The high diversity of soil type in M.P resulted in high variation in soil organic carbon
distribution both spatially and in profile. The total estimated soil C pool of the state is
790.61 Tg AESR 1 had the maximum SOC density (42.3 Mg C ha) and AESR 4 had
maximum SOC density (35.3Mg C ha) This was likely caused by climate and
agriculture development; AESR 1 is the moist and semi-arid uplands with irrigation
facilities and AESR 4 is the dry, sub –humid plateau region. The estimated AESR soil
organic carbon stock varied from widely with maximum SOC stock observed in
AESR 3 (263.2 Tg) and minimum in AESR 5 (74. 7 Tg) followed by 96.13 Tg in
AESR 1 . The wide difference is mainly because of larger area of AESR 3 and deep to
moderate clay soils. Bhattacharya et al (2007) studied changes in carbon levels in soils
up to a depth 150 cm from 1980 to 2005 of two important food production zones of
India, the Indo-Gangetic Plains and the black soil region in semi –arid tropics, and
reported that soils in Kheri (bench mark location in Jabalpur district of Madhya

45. Pradesh) showed an increase of 87% of SOC stock over 1980. It was also observed
that the non- calcareous during 1980, is now calcareous. This suggested that although
intensive agriculture increased the SOC, simultaneously it caused an increase in soil
CaCo3.
Total agriculture carbon pool-: The total estimated crop biomass stocks of Madhya
Pradesh was 34.94 Tg and 790.6 Tg, respectively. Soil C stocks which were
approximately 25 times higher than biomass C stock which underlines the role of soil
in sequestrating atmospheric Co2. Similarly, conclusions were also drawn by Dadhwal
& Chhabra (2002). Total agricultural C stock was estimated to be 825.56 Tg with
AESR 3 recording the highest C stock and 5 the lowest C stock. In case of total
agricultural carbon density AESR 1 recorded the highest agricultural C density and
AESR 4 recorded the lowest agricultural C density. The estimated crop biomass
density (2.1 Mg C ha) for the state of Madhya Pradesh is less than the crop NPP (2.9
Mg C ha) estimated by Dadhwal et al (1995) as the state was divided into
Chhattisgarh and Madhya Pradesh in 2000 and the rain-fed /low productivity western
region included in Madhya Pradesh. It can be concluded that crop biomass C and SOC
pool varies with intensity and type of cropping, soil type, and climatic regions.
Soil organic carbon in Rice soils of India-:
Rice is an important crop in India. Out of a total area of 99.5 Mha under cereal
cultivation ,42.3 Mha or 42.5% is under rice cultivation (FAO,2001). of this 10 M ha
is grown as a rice-wheat system in Indo-Gangetic Plains (Ladha et al 2000) Out of a
total cereal production of 219 million Mg, rice constitutes 122 million Mg or 56% of
the total production. Rice cultivation differ from upland crops. It is grown under
flooded condition and the seedbed preparation involves Puddling or Ploughing when
the soil is wet to destroy aggregate and reduce the infiltration rate of water. Anaerobic
condition lead to emission of methane (CH4) and possibly nitrous oxide (N20)
through inefficient fertilizer use (Bronson and Singh,1994) Emission of CH4 from
rice paddies in India is estimated at 2.4 to 6 Tg out of the world total emission of 25.4

46. to 54 Tg from all sources and 16 to 34 Tg from rice cultivation (Sass ,1994) .The
average CH4 flux from rice paddies ranges from 9 to 46 g/m over a 120-150 day
growing season (Prashar et al 1994) .Because of a favourable water regime during the
rice season ,the SOC concentration in rice soils is more than in upland soils .however
,rice straw ,similar to those of other crops, is removed for fodder and other uses ,and it
reduces the input of C into the system. Swarup (1998) reported that integrated nutrient
management to enhanced SOC concentration of rice soils from <5 g/kg in 1973 to
about 8g/kg 1994. Research is being done to find ways growing rice without puddling
so that emission of greenhouse gases can be minimized and use of fossil fuel reduced
(Duxbury et al.,2003). conservation tillage, rapidly being adopted in Indo-Gangetic
plains (Hobbs and Gupta 2003 >; Malik et al 2003) may enhance SOC concentration
these soils. In addition, it will also reduce fossil fuel use for plowing and puddling.
Sequestration of SOC in Submerged Rice soil system-: In temperate soils, low rate
of OM decomposition leads to almost invariably to the accumulation of organic matter
in soils that are poorly drained. In the tropics, this may not be always hold at a
temperature above 30◦c the rate of decomposition of OM by anaerobic organisms is
sufficiency rapid so that poor drainage did not necessarily lead to accumulation of
OM. Jenny and Rayachaudhuri noted that Indian soils under paddy (or) low land Rice
cultivation generally had greater SOC and N than those under upland systems. The
observation of jenny and Raychaudhuri on relatively high OM status of wet land rice
soils fine support with those recently reported by Sahrawat. Sahrawat, based on a
detailed review of global literature on the accumulation of OM in submerged soil and
sediment. The inclusion of an upland crop in the crop sequence with low Rice system
caused a decrease in OC and Total N due to low C sequestration in soil. The
mechanism involved in Prefrential accumulation of OM in wet land soil are mainly
associated with anaerobioss-related chemical –biochemical changes in submerged
soil. Decomposition of added OM is relatively fast complete and inefficient in the soil
under aerobic condition where oxygen act as electron acceptor but decomposition OM
in the absence of oxygen in submerged soils is completely incomplete and inefficient.
The lignin and polyphenol content in compost rice crop residue favour the formation
of biochemical complexes with protein plant origin under submergence. The resistant

47. to microbial decomposition resulting in a comparatively high proportion of total C in
passive pools.
Soil degradation and soil organic carbon pool-:
Soil degradation, decline in soil quality with an attendant reduction in biomass
productivity and environment moderating capacity, has severe adverse impact on the
SOC pool. In other words, the low SOC pool in soil of India is partly due to the severe
problem of soil degradation. Estimates of soil degradation by different process vary
widely (Biswas et al 1991:). The GLASOD estimates (FAO ,1994) Show that land
area affected is 32.8 Mha by water erosion ,10.8 Mha by wind erosion ,29.4 Mha by
fertility decline ,4.1 Mha by salinization and 3.1Mha by Indution. The total area
affected by diverse degradative process is 45 Mha. There is also a severe problem of
desertification because 102 Mha out of the 162 Mha or 63% of the dryland area is
prone to some degree of desertification. The principal cause of decline in SOC pool in
degraded soils is a reduction in biomass productivity and the low amount of crop
residue and root returned in biomass productivity low amount of crop residue and
roots returned to the soil. A typically example of the low SOC pool is in salt- affected
soils of Haryana, Andra Pradesh and west Bengal. Even in the surface 0-10 cm layer,
the SOC pool may be lower than 5g/kg (Singh and Bandyopadhya ,1996). Accelarated
soil erosion depletes the SOC pool severely and rapidly. The SOC fraction is
preferentially removed by surface has low density (1.2 to 1.5 Mg /m3 compared
with2.5 to 2.7 Mg/m3 for the mineral fraction) Consequently, eroded sediment are
enriched with SOC pool compared with the field soil with an enrichment ratio of 1.5
to 5.0 (Lal 1999). The SOC loss by erosion and runoff can be high even on gentle
slopes of 0.5-0.3% (Banerjee et al 1991). soil erosion is a four –step process. It
Involve detachment, breakdown, transport, and deposition of soil particles. Soil
detachment break down are caused by soil slaking or disruption of aggregate by
raindrop impact, shearing force of flowing water or blowing wind, and collision
among particles. Breakdown of aggregate exposes SOC hitherto, encapsulated and
physically protected to microbial processes. Although the fate of SOC displaced along
with eroded sediment is governed by a series of complex and interacting process. A

48. considerable part of it is mineralized leading to release of CO2 under aerobic
condition and CH4 under anaerobic environments. Lal (1995) assumed that 20% of
the SOC displaced by erosion mineralized. Assuming SOC concentration of 8 to 12
g/kg (1%) in eroded sediments, total C displaced by erosion process is 29.8 Tg /C/y.
Assuming that 20% of the eroded SOC is mineralized, erosion –induced emission of C
in India is estimated at 6 Tg C/ y. This compares with erosion –induced emission of
15 Tg C/y In U. S (Lal et al 1998) and 1.1 Pg C /y in the world (Lal ,1995). Therefore,
adoption, of conservation- effective measure that reduce may lead to reduction of
carbon emission from erosion –prone ecosystems.
Soil erosion and C emission in India
Process Flux
Total soil erosion 2.98 Pg sediments/yr (2979 Tg
sediments/yr)
Total C loss at 8-12 g/kg 23.8-35.8 Tg C /yr
C emission at 20% of displaced C 4.8-7.2 Tg C/yr
The soil erosion and C emission in India recorded that Total soil erosion process in
India soil flux carbon was 2.98 pg sedimenys /yr (2979 Tg sediment/yr) and Total C
loss at 8-12g/kg the carbon flux value was 23.8-35.8 C/yr then C emission at 20% of
displaced C causes 4.8-7.2 Tg/C/y Carbon flux developed
Soil Quality and Soil Organic Carbon Concentration -;
Soil organic matter is an important component necessary to the formation of both
micro-and macro-aggregates. The SOC thus encapsulated is protected from the
microbial process, and is sequestered until aggregate are broken or disrupted by
flowing and other disruptive process such as raindrop impact and shearing force of
running water. The degree of aggregation and the stability of aggregates is directly
proportional to SOC concentration. Because of high aggregation, soils with high SOC
concentration have high available water holding capacity, low susceptibility to soil
erosion, and have low losses of plant nutrient into the ground water. Use efficiency of

49. fertilizer, irrigation, and other input high in soils with high SOC concentration. All
other factors remaining the same, soil with high SOC concentration have more
agronomic, / biomass productivity than those with low SOC concentration (Sandhu et
al 1996). High crop yield in coarse –textured soils of Punjab are due to high input of
water and fertilizer. Therefore, enhancement and management of SOC concentration
are important to sustainable management of soil and water resources.
Technological Options for Soil Carbon Sequestration -: The overall strategy is to
increase SOC intensity, distribution of SOC density can be enhanced by increasing C
input into the soil and decreasing losses by erosion, mineralization and leaching. The
depth distribution of SOC can be achieved by planting deep-rooted species with high
below – ground biomass production. Using biosolids and improving earthworm
activity can enhance aggregation (Singh and Singh 1996; Sharma et al 1995). These
strategies can be achieved through a wide range of land use and soil and ecosystem ,
erosion control and conversion of agriculturally marginal soils to a restorative land use
are important options of SOC sequestration (Moench, 1991 ;Agarwal et al 1997
;Singh 1996 ; Kaur et al 2000,2002 ) Restoring eroded soil can enhance biomass
production and improve SOC concentration .Similarly , restoration of Salt –affected
soils can lead to a drastic increase in SOC pool .Garg (1998) observed a drastic
increase in SOC pool of Sodic soil planted to perennials (e.g., mesquite ) . The SOC
pool increased from about 10 Mg /ha to 30-45 Mg /ha over an 8-year period of
establishing tree species. Bhojvaid and Timmer (1998) also reported a substantial
increase in SOC pool by restoration of salt –affected soils. A similar potential exists in
restoring vast tract of waste lands throughout India (Gupta and Rao ,1994). The
potential of SOC sequestration is 2.6 to 3.9 Tg C/y for water erosion ,3.5 to 4.4 Tg
C/y for restoring soils prone to wind erosion, 0.4 to 0.7 Tg C/y for water logged soils,
and 0.5 to 0.6 Tg C /y for salinized soils. The total potential of restoring degraded
soils in India is 7to 10 Tg C/Y. Similarly, a large potential of SOC sequestration exists
for desertification control (Lal)

50. The potential of soil organic carbon sequestration in different ecoregions of India
-:
Region Temperature Area (M ha) Rate of soc Total
potential
Arid Cold 15.2 20-40 0.30-0.60
Hot 36.8 10-20 0.37-0.74
Semi-arid Hot 116.4 20-40 2.33-4.66
Sub-humid Hot 86.4 40-60 3.46-5.18
Sub-humid
/humid
Warm 21.2 40-60 0.85-1.27
Moist 12.1 100-120 1.21-1.45
Per humid Moist 20.2 120-150 2.42-0.30
Sub-humid
/semi arid
Hot 8.5 40-60 0.34-0.51
(source: Pal et al)
The potential of soil organic carbon sequestration in different ecoregions of India.
The total highest soil organic carbon sequestration occur in sub-humid/humid rate of
S0C 100-120 tg and total potential soc is 1.21-1.45 tg/c/y.in arid hot regions the rate
of SOC 10-20 Tg and total potential 0.37-0.74 Tg /C/y .Arid cold region rate SOC is
20-40 Tg and SOC potential is 0.30-0.60 Tg/C/y. semi-arid hot soc sequestration was
20-40 Tg and carbon potential was 2.33-4.66 in perhumd condition SOC sequestration
rate was 120-150 Tg and carbon potential 2.42-0.30 Tg/C/y and Sub-humid hot
condition soc rate is 40-60 Tg and carbon potential was 0.34-0.51 tg/C/y
Potential of sequestration of secondary carbonates in India-:

51. SOIL AREA (Mha) Rate of SIC
Sequestration
(kg/ha/y)
Total potential (
Tg C /y)
Vertsols 60.4 35-40 2.11-2.42
Alluvial 94.8 125-133 11.85-12.61
Ferriginous 116.5 28-32 3.26-3.73
Irrigated 57.0 80-120 4.56-6.84
(source; Pal et al)
Above the tells us about secondary carbonates potential in Indian soils, In vertisols the
rate of SOIL inorganic sequestration is (kg /ha/y) and potential total carbon is 2.11-
2.42 Tg/c/y) , In alluvial soils rate of SOIL inorganic sequestration is about 125-133
(kg/ha/y) and total potential carbon 11.85-12.61 (Tg /C/y) In ferriginous soils Rate of
Soil inorganic sequestration is 28-32 (kg/ha/y) vary low and Total potential carbon
(Tg/C/y) in Irrigated soils the rate of soil inorganic sequestration 80-120 (kg/ha/y) and
total potential 9(Tg/C/y)
Total potential of carbon sequestration in soils of India -:
Process Potential
1. Soil organic carbon (SOC) by
erosion control
4.8-7.2
Restoration of degraded soils 7.2-9.8
Agricultural intensification 5.5-6.7
Secondary carbonates 21.8-25.6
Total potential of carbon sequestration in Indian soil by varies process that are
soil organic carbon stored by erosion control measures by 4.8 -7.9 Tg and restoration
of degraded soils was improve soil organic carbon potential is 7.2-9.8 Tg, Agricultural
intensification causes in India soils 5.5-6.7 tg soil carbon will developed in soil,

52. Secondary carbonates causes highest amount of carbon sequestration 21.8-25.6 Tg
established in soil
Growing stock and biomass and soil carbon in Kolli hills by forestry in Tamil
Nadu
FORES
T type
Volum
e
Timb
er
bioma
ss
(tons/
ha)
Brach
and
foliag
e
(ton/h
a)
Stum
ps
and
root
(ton/h
a)
Bioma
ss
(tons/h
a)
Area
of
each
forest
(ha)
Total
bioma
ss (M
tons)
TO
C
(T
G)
SO
C
stoc
k
(Tg
)
Evergre
en
foresty
428.22
9
196.98
8
47.27
7
63.03
6
307.30
2
3962.2
3
1.22 0.60 1.01
Decidou
s
forestry
316.06
0
161.31
6
38.71
6
51.62
1
251.65
3
12684.
74
3.19 1.57 1.63
Seconda
ry
deciduo
us
216.67
3
154.98
3
37.19
6
49.59
5
241.77
3
2960.2
8
0.72 0.35 0.35
Souther
n Thorn
73.025 42.282 10.14
8
13.53
0
65.960 6676.1
5
0.44 0.22 0.47
Euphor
bia
scrub
52.72 36.859 8.846 11.79
5
57.500 304.40 0.02 0.01 0.03
Total 1086.7
07
592.42
8
142.1
83
189.5
77
924.18
8
26587.
80
5.58 2.74 3.48
In kolli hills, the reserve forests (RF) occupy about 27,103 ha and there are five
forests types, namely Tropical broadleaved hill forest, southern dry mixed deciduous
forest, secondary deciduous foresty , Southern thorn forest and Euphorbia scrub forest

53. . The total area under the semi –ever-green forest type is about 3962 ha comprises
15% of the total area under the semi-ever green forest area. This forest type has been
classified further into Four sub classes based on the crown density, viz. Very dense
(>70%), dense (40-70%), open (10-40%) and degraded (<10%), the very dense semi-
ever green forest occupies 1984 ha which is 50% of the total semi- ever green forest.
About 25 and 21% of the semi-ever green forest are under dense and open
respectively only 4% is under degrade semi-ever green. The deciduous forest
comprises 46% of the total forest area. The total Biomass carbon of Kolli hills was
2.74 T g and total SOC was 3.48 Tg . The ratio between SOC and biomass carbon was
1.18 Post et al reported that ratio between SOC and Biomass carbon is 2.5 to 3 times
in the terrestrial ecosystem. However, in tropical forest, the carbon in the soil is
roughly equivalent or lesser than the above ground biomass due to degradation. In
case of kolli hills, the carbon content in the soil was the higher than the above –ground
biomass carbon due to heavy exploitation of timber and sandal wood. higher content
of SOC than the above ground biomass carbon indicates that the sequestered SOC was
the result of its original vegetation in the past exploitation.
Sequestered standing carbon stock in selective tree species grown in university
campus at Aurangabad, Maharashtra, India
SR.No Scientific name Mean above
ground
organic
carbon (t/tree)
Mean below
ground
organic
carbon (
t/tree)
Mean organic
carbon (t/tree)
1 Acacia nilotica 0.60 0.09 0.69
2 Albizia lebbeck 1.18 0.17 1.35
3 Azadirachta
indica
1.91 0.26 2.08
4 Bauhinia 0.31 0.04 0.35

54. raemosa
5 Butea
monosperma
2.10 0.31 2.41
6 Cassia fistula 0.55 0.08 0.63
7. Dalbergia sisso 0.46 0.06 0.53
8 Delonix regia 2.12 0.31 2.44
9 Eucalyptus
citridora
0.88 0.12 1.01
10. Ficus
bengalensis
3.89 0.57 4.46
11 Ficus religosa 4.27 0.641 4.91
12 Hyphorbe
americaulismort
1.53 0.23 1.76
13 Leucaena
latisiliqua
0.72 0.18 0.90
14. Mangifera
inidica
3.13 0.46 3.59
15 Peltoforum
pterocarpum
2.01 0.29 2.30
16 Pithecellobium
dulce
0.84 0.12 0.96
17 Polyalthia
longifolia
1.20 0.18 0.90
18 Pongamia
pinnata
1.57 0.23 1.80
19 Tamarindus
indica
1.25 0.18 1.43
20 Terminalia
catappa
0.15 0.02 0.17
(Source;- B.L Chavan )

55. The 1658 number of 20 species of trees present on University campus of Dr. B.A.M.
University the mean organic carbon (t/tree) in the trees studied is Summarized for
comparison Above Ground Carbon (AGC) Below Ground Carbon (BGC) Mean
Organic Carbon (MOC) in Ficus religiosa is 4.27 , 0.641, and 4.91 t/tree respectively
it is followed by Ficus bengalensis (3.89,0.57,4.46 t/tree) Mangifera
indica(3.13,0.46,3.59t/ tree ) Delonix regia(2.12,0.31,2,44 t/tree) Betea monosperma
(2.10,0.31,2.44t/tree) Peltaforum Pterocarpum (2.01,0.29,2.30 t/tree) Azadirachta
indica (1.91, 0.26,2.08 t/ tree) , Pongium pinnata (1.57,0.23,1.80t/tree) and
Hyophorbe amercaulismort (1.53,0.23,1.76 t/tree) respectively .Remaining all trees is
having carbon below 1.5/t/tree
The present study has calculated total organic carbon stock in 20 trees species in
Dr.B.A.M University, Aurangabad. The average standing stock of organic carbon in
20 well grown trees in Dr.B.A.M University campus is about 1.65 t /tree. the study is
helpful to estimate the Organic carbon stock (OCS)present in Aurangabad city and
other cities or forest cover by using non- destructive method
Case studies on carbon sequestration in India-:
Depletion of soil organic soil organic carbon content of cultivated soil compared
to with that of in Undisturbed soils -:
Region SOC content (%)
in cultivated soil
(g kg)
SOC content (%)
in native soils (g
kg)
Percent reduction
(%)
1.North west India
Indo-gangetic
Plains
Northern
Himalaya
4.2±0.9
24.3±8.7
104±3.6
34.5±11.6
59.6
29.6

56. 2.Northeast India 23.2±10.4 38.3±23.3 39.4
3.Southeast India 29.6±30.1 43.7±23.4 32.3
4. West coast 13.2±8.1 18.6±2.1 29.1
Deccan plateau 7.7±4.1 17.9±7.6 57.0
Inference-: Above the study we know the relationship between SOC content in
Cultivated Soil and SOC content in Native soils in different regions of India. In the
different regions of India, The SOC content more in native soils compared to
cultivated soils because the native soil are high covered vegetation and no tillage
operation that’s way there is no Carbon losses at the Native soils at the same time the
SOC content in cultivated soil decrease due to high tillage operations and no cover
vegetation causes lot Carbon losses occurs in the surface soil
Effect of farmyard and green manure on soil organic carbon under different
land use systems -:
Land use Treatment T ha Organic C
(%)
Reference
Alluvial maize-
wheat (15
years)
Control
FYM
-
69.7
0.51
2.49
Biswas et al
Medium black
cotton –
Sorghum (45
years)
Control
FYM
-
6.2
0.56
1.14
Khaiani &
more
Black soil
ragee- cow pea
– maize (3
Control
FYM
-
25
0.64
0.43
Mathan et al

57. years)
Red soil-rice-
rice (10 years)
control
50% from
inorganic+
50% through
green manure
(Sesbania
aculeate)
-
-
0.43
0.93
Hegde
Sodic soil rice
– wheat (3
years)
Control
FYM
-
16
0.44
0.54
Manna
Sodic soil rice
Wheat (7
years)
Fallow –rice-
wheat
Green manure
(Sesbania
Aculeate) rice-
wheat
-
-
0.23
0.37
Swarup
Inference-: In the above table we study about the Effect of green manure and farm
yard manure on SOC under different crop use systems. Above the table alluvial
wheat-maize systems (15 years) their maintain control and farm yard manure. The
following of farm yard manure 15 years causes the organic carbon increase 2.49% .
The next land use system medium black cotton sorghum land use system (45 years)
farm yard manure causes the soil organic carbon increases 1.49%. Black soil ragee –
cowpea and maize land use systems (3 years) farm yard manure can be increase
0.43% soil carbon. In the red soil rice-rice land use system (10 years) following 50%
inorganic from and 50% through green manure cropping (sesbania aculeate) causes
the soil carbon in the soil increase 0.93%. In the sodic soil rice –wheat land use
system (3 years) following Farm yard manure can be increase 0.54% carbon in the
soil. In the sodic soil rice-wheat (7 years) land use system following green manure

58. I(sesbania aculeate) causes soil organic carbon increase 0.37 % compared to fallow
rice –wheat system.
Case study one -: Biomass and carbon stocks of Different tree plantations in
Entisol soil Eastern Chhattisgarh India
s.n
o
Species AGB
(Q/TREE
)
AGB
(Q/TREE
)
TOTAL
BIOMAS
S (Q/tree)
CARBON
STOCK
(Q/TREE
)
YEARLY
CARBON
STORAG
E (t/ha)
1 Albizia
lebbeck
23.93 6.23 30.16 15.08 37.70
2 Azadiracta
indica
2.71 0.71 3.42 1.71 4.275
3 Dalbergeia
sissoo
2.16 0.57 2.73 1.36 3.375
4 Emblica
officinalis
2.57 0.67 3.24 1.62 4.050
5 Eucalyptus
globulus
13.23 3.43 16.66 8.33 20.825
6 Deris indica 1.37 0.35 1.72 0.86 2.150
7 Peltophoru
m ferrugium
2.18 0.57 2.75 1.37 3.425
8 Terminalia
arjuna
3.64 0.95 4.59 2.29 5.72
9 CD p <0.05 0.77 0.18 1.85 0.33 0.45
(source; BHARDWAJ &CHANDRA)
Data showed C in tree species in different plantation is revealed that C storage was
strongly was strongly correlated with the diameter height and biomass of the tree
species and strongly positive R₂=0.98 ,0.786 and 1 respectively. higher biomass, C
storage would be more in wood. As in present study biomass of tree varied greatly in