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Nitrogen addition reduced carbon mineralization of aggregates in forest soils but enhanced in paddy soils in South China



Despite the crucial role of nitrogen (N) availability in carbon (C) cycling in terrestrial ecosystems, soil organic C (SOC) mineralization in different sizes of soil aggregates under various land use types and their responses to N addition is not well understood. To investigate the responses of soil C mineralization in different sized aggregates and land use types to N addition, an incubation experiment was conducted with three aggregate-size classes (2000, 250, and 53 μm) and two land use types (a Chinese fir plantation and a paddy land).


Cumulative C mineralization of the < 53-μm fractions was the highest and that of microaggregates was the lowest in both forest and paddy soils, indicating that soil aggregates enhanced soil C stability and reduced the loss of soil C. Cumulative C mineralization in all sizes of aggregates treated with N addition decreased in forest soils, but that in microaggregates and the < 53-μm fraction increased in paddy soils treated with 100 μg N g−1. Moreover, the effect sizes of N addition on C mineralization of forest soils were below zero, but those of paddy soils were above zero. These data indicated that N addition decreased SOC mineralization of forest soils but increased that of paddy soils.


Soil aggregates play an important role in soil C sequestration, and decrease soil C loss through the increase of soil C stability, regardless of land use types. N addition has different effects on soil C mineralization in different land use types. These results highlight the importance of soil aggregates and land use types in the effects of N deposition on the global terrestrial ecosystem C cycle.


Soils are the largest sink of the global carbon (C) cycle and hold 2500 Gt C that are 3.3 times the size of the atmospheric C pool and 4.5 times the size of the biotic C pool (Lal 2004). The maintenance of the soil C pool is critical to the global C cycle and climate change as even slight changes in the soil organic C (SOC) pool can seriously affect atmospheric CO2 concentration and global C budget (Schlesinger and Andrews 2000; Bellamy et al. 2005). Hence, the loss of SOC has received increasing attention in recent years (Liu et al. 2017; Qiu et al. 2018; Yanni et al. 2018; Wiesmeier et al. 2019). Approximately half of all SOC in managed ecosystems has been released to the atmosphere during the last two centuries, of which two-thirds is attributed to SOC mineralization (Lal 2004; Kirkby et al. 2013). Therefore, the study of the influencing factors and mechanisms of SOC mineralization could improve the understanding of the soil C cycle and their role in global climate change.

Except for soil temperature and moisture, which are the main factors controlling SOC mineralization (Contosta et al. 2013; Wang et al. 2016), soil nutrient availability, especially nitrogen (N) availability, greatly influences SOC mineralization through their impact on the decomposition and formation of soil organic matter (Reed et al. 2010; Poeplau et al. 2016; Soong et al. 2018; Zhu et al. 2018b). Moreover, N inputs from anthropogenic sources to biosphere, such as agricultural activities and fossil fuel combustion, are tenfold higher now than 100 years ago (Galloway et al. 2008), resulting in the continuous increase of soil N availability (Aber et al. 1998). Thus, the role of soil N availability in SOC mineralization is further highlighted. N addition is an important approach to change soil N availability, such as fertilization and N deposition. Although N addition is widely believed to reduce the rate of SOC mineralization (Mo et al. 2008; Fisk et al. 2015; Riggs et al. 2015; Guo et al. 2017; Hu et al. 2017; Zhu et al. 2018a), a few studies reported that N addition has no effects (Micks et al. 2004; Allison et al. 2008), even positive effects on SOC mineralization (Cleveland and Townsend 2006; Huang et al. 2011a; Zhao et al. 2019). This controversy may be because the level of N addition results in different responses of SOC mineralization (Allison et al. 2009; Zhu et al. 2016). However, why are there variable responses of SOC mineralization to N enrichment and what is the mechanism controlling these responses to N enrichment remain unknown.

The rate of SOC mineralization is controlled by SOC stability (Tian et al. 2016), and the protection of soil aggregates is proposed as one of the main mechanisms of SOC stabilization (Six et al. 1998; von Lützow et al. 2008; Chaplot and Cooper 2015). Soil aggregates, especially macroaggregates, can protect the SOC against microbial decomposition (Six and Paustian 2014) due to spatial inaccessibility to soil microorganism (Goebel et al. 2005; von Lützow et al. 2008). Different particle sizes of soil aggregates have distinct characteristics in the soil C turnover (Besnard et al. 1996). Many studies suggested that the rate of SOC mineralization was lower in macroaggregates than in microaggregates (Drury et al. 2004; Xie et al. 2017). However, no difference of SOC mineralization between macroaggreates and microaggregates (Razafimbelo et al. 2008) and even the opposite results (Wang et al. 2015; Bimüller et al. 2016; Yang et al. 2017) have been reported. Although no consistent conclusion exists about the SOC mineralization of different sizes of soil aggregates, SOC mineralization is widely believed to vary (Razafimbelo et al. 2008; Bimüller et al. 2016). The distinct compositions of soil aggregates with varying particle sizes in soils may result in the differences of SOC mineralization. Moreover, the responses of C mineralization of soil aggregates to N addition remain unclear, limiting the understanding of the influencing factors of SOC mineralization with N addition treatment. The differences in SOC stability of varying sizes of aggregates may cause the distinct responses of C mineralization of soil aggregates to N enrichment, resulting in the differences of C mineralization of bulk soil with N addition treatment. However, direct evidence of the effects of N addition on SOC mineralization of varying size aggregates is lacking (Riggs et al. 2015; Xie et al. 2017). Investigating the responses of C mineralization of soil aggregates to N addition can further explain the mechanism that controls the influence of N enrichment on SOC mineralization.

In addition, land use type can influence the soil aggregate distribution and aggregate stability index (Zhong et al. 2019; Okolo et al. 2020). For example, soil microaggregates were dominant under cultivated land, while soil macroaggregates were preponderant in grazing land (Okolo et al. 2020). Zhong et al. (2019) also suggested that the conversion from farmland to forest increased the proportions of soil macroaggregates and mesoaggregates and thus increased the organic carbon accumulation. The changes of soil aggregate distribution after land use change may alter the soil C mineralization. Moreover, different land use types have different management intensities, for example, more fertilization and tillage in farmland. Management intensity can affect the soil aggregate distribution (Sithole et al. 2019; González-Rosado et al. 2020) and then result in the change of soil C mineralization (Reeves et al. 2019). As forest and paddy are the main land use types in south China, the effects of N addition on their soil C mineralization are crucial to understanding the global C cycle. However, little is known on the difference of effects of fertilization on soil C mineralization among land use types.

In this study, we examined C mineralization over 3 months in macroaggregates, microaggregates, and the < 53-μm fraction in forest and paddy soils after the application of N fertilizer with a concentration gradient using a laboratory incubation experiment, to uncover the impacts of N addition on soil C mineralization in different aggregate sizes under different land use types. The specific objectives of our study are to (1) examine whether the SOC mineralization and their responses to N addition differ among aggregate sizes and (2) determine whether the effects of N addition on SOC mineralization are the same between different land use types (forest and paddy). We hypothesized that (i) the rates of C mineralization increase with decreasing size class of soil aggregates and (ii) the responses of C mineralization in forest and paddy soils to N addition are different.

Materials and methods

Study area

This study was conducted in the Huitong National Research Station of Forest Ecosystem (26° 40′–27° 09′ N and 109° 26′–110° 08′ E) (Huitong Station, hereafter) in Hunan Province in the south of China. The Huitong Station is located at the transition zone from the Yunnan–Guizhou Plateau to the low mountains and hills on the southern side of the Yangtze River. This region has a typical mid-subtropical monsoon climate with an annual mean rainfall of 1200 mm. The annual mean temperature is 16.5 °C with a mean minimum of 1.9 °C in January and a mean maximum of 29 °C in July. The soil derived from the Sinian Period gray–green slate was classified as Ultisol according to the United States Department of Agriculture (USDA) soil taxonomy (He et al. 2016).

Soil sampling

The composition of soil aggregates and the response of SOC mineralization to N addition may differ across land use types. To investigate the role of soil aggregate composition on the effects of N addition on SOC mineralization, two land use types—a typical forest ecosystem and a paddy land—were selected for soil sampling because these two types are the main land use types in the subtropical region in China. Forest soils were from Chinese fir (Cunninghamia lanceolata (Lamb.) Hook) plantations that were established in 1983, 1989, and 1990 after clear-cutting and slash-burning practices of the natural evergreen broadleaf trees. In the Chinese fir plantation, the dominant species in the shrub layer were Maesa japonica, Mussaenda esquirolli, and Rhus chinensis, and those in the herbaceous layer were Miscanthus floridulu, Dicranopteris linearis, Herba lophatheri, Carex tristachya, and Parathelypteris glanduligera. At each site of Chinese fir plantations, a 20 m × 20 m plot was selected. Crop rotation with Oryza sativa L. and Brassica campestris L. is typically applied for highly efficient utilization. O. sativa and B. campestris were planted in May and October in each year, respectively. Three sites of croplands were also selected. At each site, 10 soil cores at 0–10-cm depths were randomly collected using a stainless steel cylinder with 5-cm diameter and were composited into one soil sample. Soil samples from each land use type had three replicates. The forest soil samples were collected when the moisture content of the soil was 25–30% with cautious removal of floor residues. The paddy soil sampling was performed under the flooded condition because most of the growing season is under the flooded condition. A subsample (approximately 1 kg) was immediately placed in a sterile plastic bag on ice when transported to the laboratory and stored at 4 °C for inoculum preparation. The remaining soils were passed through an 8-mm sieve by gently breaking apart the soil, and air-dried in a laboratory for particle-size fractionation and subsequent C mineralization assays (Six et al. 2002). The plant residues including root and leaf litter, visible soil fauna, and stones were removed from the soil samples. The main properties of the forest and paddy soils in Huitong Station, subtropical China, are listed in Table 1.

Table 1 The main properties of forest and paddy soils in the Huitong National Research Station of Forest Ecosystem in Hunan Province, subtropical China

Soil particle-size separation

The aggregate separation was conducted by wet sieving the soil through a series of three sieves (2000, 250, and 53 μm) to obtain three aggregate-size classes (Six et al. 2002). Prior to wet sieving, all field moist samples were passed through an 8-mm sieve and air-dried in a laboratory. The aggregates were separated using an aggregate sieving machine (AS200, Germany) by the following procedure. A subsample of 100 g of air-dried soil was submersed in deionized water in a beaker of 500 mL for 10 min to loosen the soil sample and then poured into the top of a 2000-μm sieve. The aggregates were separated by moving the sieve up and down 50 times over a period of 2 min with an amplitude of 3 cm. The intact aggregates that remained on the 2000-μm sieve were scarce except the little rocks. The soil slurry that remained on the 250-μm and 53-μm sieves washed off the sieve and collected in an aluminum pan, considering as the macroaggregates and microaggregates, respectively. The < 53-μm fraction was separated by centrifuging (2500×g) the soil suspension that passed through the 53-μm sieve and collected in an aluminum pan. All fractions in the aluminum pan were oven dried at 50 °C and weighed to calculate the aggregate weight percentages. The procedure of aggregate separation was repeated until all fractions of the aggregates were sufficient for subsequent incubation. All fractions were stored at room temperature for future use. Soil C and total N (TN) of all sizes of soil aggregates and bulk soils were determined using an automated C/N analyzer (Vario MAX CN, Elementar Co. Hanau, Germany). The soil total phosphorus (TP) was extracted by wet microwave digestion procedure and determined using an inductively coupled plasma mass spectrometry (ICP-MS, Thermo Scientific iCAP Q, USA).

Laboratory incubation

This incubation experiment included two land use types, three sizes of soil aggregates and their bulk soils, and four N addition treatments. Two land use types included forest and paddy land. The three sizes of soil aggregates were macroaggregates, microaggregates, and the < 53-μm fraction. When the amount of N fertilizer applied to forest and paddy soils is 100 kg N ha−1, and the average soil bulk density is approximately 1 g cm−3, then the concentration of N added into soils through N fertilizer application is equivalent to 100 μg N g−1 soil. Generally, the amount of N fertilizer applied to forest and paddy soils is 100 kg N ha−1, and the N deposition is nearly 50 kg N ha−1 year−1 in Hunan Province (Zhao et al. 2017). Thus, four N addition treatments were established as follows: N0 (without N addition), N1 (50 μg N g−1), N2 (100 μg N g−1), and N3 (150 μg N g−1).

For each soil aggregate (macroaggregates, microaggregates, and the < 53-μm fraction) and bulk soils, a 25-g dried sample was placed into a 100-mL brown jar and treated with NH4NO3. Because the microorganisms were interfered by oven-drying during soil aggregate separation, all sizes of soil aggregates were inoculated with the inocula from bulk soils to simulate the microbial community composition in bulk soils. Prior to N treatment, the inoculum solution was prepared by shaking 100 g of fresh bulk soil from subsample with 1000 mL of deionized water for 10 min and leaving to stand overnight to simulate the actual microbial community composition in forest and paddy soils (Christensen 1987). Five milliliters of inoculum dissolved 3.6, 7.2, and 10.7 mg of NH4NO3 was added to each sample to obtain the concentrations of added N equal to 50, 100, and 150 μg N g−1. The sample added with 5 mL of inoculum without NH4NO3 was the control. To improve soil aeration and uniformly disperse the inoculum, the sample added by the inoculum was loosened, stirred, and leveled slightly. The soil moisture was adjusted to 60% of field capacity. The soil aggregates were incubated at 20 °C in an incubator for 90 days. This experiment had three replicates. Empty flasks were set as blank. The volume of head space (jar volume minus soil solid) was accurately measured after complementing the experiment by the method of water replacement. Since rewetting of dried sieved aggregates significantly increased C mineralization only during the early 3 days of the incubation experiment (Franzluebbers 1999), we preincubated the samples for 3 days to avoid the influence of disturbance (i.e., rewetting of dried soils and wet sieving) of field moist aggregates on soil C mineralization.

Soil respiration rates incubated at 20 °C were determined using a Li-820 infrared gas analyzer (Li-Cor Inc. Lincoln, NE, USA). The measurements were conducted in 1, 3, 5, 7, 10, 15, 20, 30, 45, 60, and 90 days after incubation. The measurement for each sample lasted 6 min until a stable respiration rate is reached. After each measurement, each sample was returned to ambient O2 level by leaving the incubation jars open for 1 h. The 100-mL incubation jars containing wetted soil aggregates (60% of field capacity) were weighed prior to the incubation. The weight decrease of incubation jars due to water loss from the aggregates during each of the incubation period was compensated by the slow addition of deionized water using a water spray.

Data analysis

The cumulative CO2-C mineralization of different aggregate-size ranges (or bulk soils) during 90-day incubation was calculated as the cumulative mineralized CO2-C divided by the soil C content of the aggregates (or bulk soils). The effect size of N addition on C mineralization in aggregates and bulk soils was calculated by comparing the cumulative CO2-C mineralization after 90-day incubation with and without N addition treatments in different particle-size aggregates and bulk soils as follows:

$$ \mathrm{Effect}\ \mathrm{size}=\left({\mathrm{C}}_{\min -\mathrm{N}}-{\mathrm{C}}_{\min -\mathrm{withoutN}}\right)/{\mathrm{C}}_{\min -\mathrm{withoutN}},\kern4.25em $$

where Cmin-N (mg CO2-C g−1 soil C) is the cumulative CO2-C mineralization in aggregates and bulk soils after 90-day incubation with N addition treatments and Cmin-withoutN (mg CO2-C g−1 soil C) is the cumulative CO2-C mineralization in aggregates and bulk soils after 90-day incubation without N addition treatments (the control). The results show a positive effect when the effect size is > 0 and a negative effect when the effect size is < 0.

The cumulative C mineralization values and their effect sizes of N addition on soil aggregate C mineralization were analyzed using two-way ANOVA. Significant differences between the various treatments were tested with the Tukey HSD test. Statistical analysis was performed using SPSS 17.0 software (SPSS, Chicago, IL, USA).


SOC, TN, and TP in different fractions

The mass fractions of different particle sizes of aggregates in forest and paddy soils displayed the same trend. The largest proportion was found in the < 53-μm fraction, followed by the microaggregates and the least in the macroaggregates (Table 2). No significance was found between the proportions of macroaggregates or microaggregates in forest and paddy soils, except that the < 53-μm fraction in forest soil was lower than that in the paddy soil.

Table 2 C, total N (TN), and total P (TP) contents in the different sizes of aggregates in forest and paddy soils

The SOC concentrations of aggregates in forest and paddy soils significantly increased with the increase in particle sizes (p < 0.05). The TN concentrations of different particle sizes of aggregates in forest soil did not vary, but the TN concentration of macroaggregates was 13.7% and 25.1% higher than that of the microaggregates and the < 53-μm fraction in paddy soil, respectively (p < 0.05). The TP concentrations did not vary among different particle sizes of aggregates in forest soil except that the TP concentration of macroaggregates was 28.7% and 21.6% higher than that of the microaggregates and the < 53-μm fraction in paddy soil (p < 0.05). The TP concentrations of all sizes of aggregates in forest soil were much lower than those in paddy soil (p < 0.05). However, the N and P ratio (N:P ratio) of all sizes of aggregates in forest soil was significantly higher than those in paddy soil (p < 0.05).

Differences in SOC mineralization rate among fractions

The rates of CO2-C evolution of aggregates decreased with the incubation time. The rate of CO2-C evolution of macroaggregates was higher than that of microaggregates and the < 53-μm fraction in forest and paddy soils (Fig. 1).

Fig. 1

Rate of CO2-C evolution from macroaggregates, microaggregate, and the < 53-μm fraction during 3 months of incubation in a 100-mL incubation jar. A and B are the forest and paddy soils, respectively. The amount of CO2-C evolved from samples was determined using a Li-820 infrared gas analyzer. A non-linear asymptotic regression model was fitted to the CO2-C evolution rate of soil aggregates. BS, MA, MI, and MF denote bulk soil, macroaggregate (2000–250 μm), microaggregate (250–53 μm), and the < 53-μm fraction. N0 (the control), N1 (50 μg N g–1), N2 (100 μg N g–1), and N3 (150 μg N g–1)

After 90-day incubation, the cumulative C mineralization (mg CO2-C g−1 soil C) in the < 53-μm fraction, microaggregates, and macroaggregates was 40.4%, 15.2%, and 16.0% higher than that of bulk soil in forest soil, respectively (Fig. 2A, p < 0.05). The cumulative C mineralization did not differ significantly between the macroaggregates and microaggregates, but was significantly lower than that of the < 53-μm fraction in forest soil (p < 0.05). The highest cumulative C mineralization was found in the < 53-μm fraction in paddy soil, followed by bulk soil and macroaggregates. However, the cumulative C mineralization of microaggregates in paddy soil was the lowest (Fig. 2B, p < 0.05).

Fig. 2

The response of cumulative C mineralization of aggregates to N addition in forest (A) and paddy (B) soils during the entire incubation period (90 days). BS, MA, MI, and MF denote bulk soil, macroaggregate (2000–250 μm), microaggregate (250–53 μm), and < 53-μm fraction. N0 (without N addition, the control), N1 (50 μg N g−1), N2 (100 μg N g−1), and N3 (150 μg N g−1). F is the forest soils and P is the paddy soils. A and N denote the soil aggregates and N addition

Effects of N addition on SOC mineralization rates

The rates of CO2-C evolution of aggregates were decreased in forest soil but were increased in paddy soil (Fig. 1). Compared with that in the control treatment, the cumulative C mineralization of forest soil treated with N1, N2, and N3 significantly decreased by 20.0%, 28.3%, and 30.3% (Fig. 2A, p < 0.001). There was an interaction effect between aggregate fractions and N addition on C mineralization of forest soil. Although N addition decreased the SOC mineralization of bulk soil and all sizes of aggregates, the reduction degree varied. The reduction of cumulative C mineralization of bulk soil was the least, and the reduction degree increased with decreasing particle size of aggregates in forest soil (Fig. 2A).

The cumulative C mineralization of paddy soil treated with N1, N2, and N3 significantly increased by 4.5%, 13.0%, and 2.8% compared with N0, respectively (Fig. 2B, p < 0.01). There was an interaction effect between aggregate fractions and N addition on C mineralization of paddy soil. The responses of SOC mineralization of different sizes of aggregates in paddy soil to N addition varied. Compared with N0, N1 significantly decreased the cumulative C mineralization of bulk soil, and N3 significantly decreased that of the macroaggregates, but N2 significantly increased that of the microaggregates and the < 53-μm fraction (Fig. 1B, p < 0.05).

The effect sizes of N addition on soil C mineralization of forest and paddy soils were quite different (Fig. 3). All effect sizes of forest soils treated with N addition were below zero, and the effect sizes decreased with the increasing N addition. However, most of effect sizes of paddy soils were above zero, in which the effect size of N2 was the highest.

Fig. 3

The effect sizes of cumulative C mineralization of forest and paddy soils by N addition. A and B are the forest and paddy soils, respectively. BS, MA, MI, and MF denote bulk soil, macroaggregate (2000–250 μm), microaggregate (250–53 μm), and < 53-μm fraction. N1, N2, and N3 are 50 μg N g−1, 100 μg N g−1, and 150 μg N g−1, respectively


Soil C mineralization differed among aggregates

Soil aggregate size significantly affected SOC mineralization of forest and paddy soils. Our results showed that the cumulative C mineralization of microaggregates and the < 53-μm fraction was higher than that of macroaggregates in forest soil, and it supported the hypothesis that the rates of C mineralization increase with decreasing class size of soil aggregates. This finding is consistent with the result reported by Xie et al. (2017). This pattern of SOC mineralization in aggregates in forest soil is due to the following causes. First, the physical protection of soil aggregates decreases SOC mineralization of macroaggregates. The formation of macroaggregates reduced the rate of soil aggregate turnover and protected the intra-aggregate particulate organic matter from microbial decomposition (Six et al. 2000; Blanco-Canqui and Lal 2004). During aggregate formation, organic particles were entrapped into macroaggregates and microaggregates, through the encrustation of SOM in the center of microaggregates, to prevent the accesses of microorganism (Golchin et al. 1994), resulting in the decreases of soil C mineralization in macroaggregates. The protection of soil aggregates against soil C mineralization supported the result of the highest cumulative C mineralization of the < 53-μm fraction in forest soils in this study. Second, the soil C:N ratios of different particle sizes of aggregates in forest soils vary. The soil C:N ratio can effectively predict soil C mineralization because it reflects the substrate quality for soil microorganism growth (Dai et al. 2017). SOM with higher C:N ratio persists for longer times and has a lower rate of decomposition (Blanco-Canqui and Lal 2004). The C:N ratio of macroaggregates was higher compared with the microaggregates and the < 53-μm fraction (Table 2), resulting in the lower rate of macroaggregate C mineralization in forest soils. Our results indicated again that soil aggregation plays an important role in forest soil C sequestration.

However, the cumulative C mineralization of soil aggregates in paddy soils differed from that in forest soils. The lowest cumulative C mineralization appeared in microaggregates and that in the < 53-μm fraction in paddy soils was the maximum probably due to the different biochemical properties of organic residues that bind mineral particles to form aggregates. The binding agents responsible for stabilizing the aggregates are classified as transient, temporary, and persistent agents (Tisdall and Oades 1982). The transient agents consist mainly of polysaccharides and organic mucilage, which can be rapidly decomposed by microbial processes (Blanco-Canqui and Lal 2004). They commonly bind 10-μm to 50-μm clay particles to form the < 53-μm fraction (Martin 1971). Temporary agents comprising large substances, such as plant roots, fungal, and mycorhizal hyphae, bacterial cells, and algae, are mainly associated with soil macroaggregates (Tisdall and Oades 1982). Moreover, most of the macroaggregates were newly formed due to the annual periodic severe disturbance in paddy soils with the rotation of O. sativa and B. campestris. Persistent agents include highly decomposed organic materials, such as humic compounds, polymers, and polyvalent cations, and are associated with the formation of microaggregates (Edwards and Bremner 1967). Compared with temporary agents binding in macroaggregates, persistent agents in microaggregates have the lowest decomposition rates and the longest decomposition time, and the transient agents in the < 53-μm fraction have the highest decomposition rates and the shortest decomposition time, resulting in the lowest and the highest cumulative C mineralization of microaggregates and the < 53-μm fraction in paddy soils, respectively. Our results showed that microaggregates play a better role in C sequestration of paddy soil.

Effects of N addition on SOC mineralization rates

N addition exhibited diverse effects on the cumulative C mineralization and different effect sizes of soil aggregates in forest and paddy soils, which was consistent with our second hypothesis. Added N decreased cumulative C mineralization and effect sizes in all aggregates and bulk soils of the forest. This result confirmed the hypothesis that N addition reduced soil C mineralization of aggregates in forest soils. This result was in line with the findings in subtropical forest soil (Wang et al. 2017), tropical forest soil (Mo et al. 2008), and temperate forest soil (Janssens et al. 2010). Although there is a debate on the effects of N addition on SOC mineralization, most previous findings support the opinion that N addition impedes organic matter decomposition and thus stimulates carbon sequestration in forest soils (Franklin et al. 2003; Chen et al. 2012; Fisk et al. 2015; Wang et al. 2017).

However, the impacts of N addition on soil aggregate C mineralization in paddy soils differed from that in forest soils. N addition enhanced the cumulative C mineralization and effect sizes of soil aggregates in paddy soils, especially N2 treatment. This result indicated that the added N enhanced the amount of potential mineralizable OC of soil aggregates and promoted soil aggregate C mineralization in paddy soils. This finding was inconsistent with our hypothesis but was consistent with the previous documents that reported that N addition has promoting effects on C mineralization of paddy soils (Zheng et al. 2007; Li et al. 2014; Zhou et al. 2014). These results indicated that added N has diverse effects on soil C mineralization in forest and paddy soils.

Several possible mechanisms can explain the relationship between N addition and SOC mineralization. The first possible mechanism is that added N can negatively impact soil microbial biomass, composition, and activity (Treseder 2008). A number of documents reported that N addition reduces microbial biomass and activity, such as fungal biomass (Frey et al. 2004; Högberg et al. 2007), bacterial biomass (Blǎsko et al. 2013), and microbial abundance (Treseder 2008). A review on the effects of N addition on microbial biomass showed that the microbial biomass declined by 15% on average under N fertilization and suggested that the reduction of microbial biomass caused a corresponding decline in soil CO2 emissions under N addition (Treseder 2008). Soil microbial biomass and community composition control the rates and dynamics of SOC decomposition. Thus, the reduction in soil microbial biomass by N addition may result in the decline of SOC mineralization of aggregates. However, this hypothesis is suitable for forest soils, not for paddy soils. The second possible mechanism is that the added N reacts with the breakdown products of lignin degradation to form recalcitrant complexes, such as melanoidins (Fog 1988). However, the results of our study showed that the reductions of C mineralization of all aggregate sizes in forest soils have similar range under the same levels of added N, despite the difference of OC concentrations in all aggregate sizes. Moreover, another document reported that only a small amount of added N is incorporated into the recalcitrant substrate (Clinton et al. 1995). Thus, this hypothesis is insufficient to support our findings. The third possible mechanism is “microbial N mining” theory (Moorhead and Sinsabaugh 2006). This theory assumes that the N-acquiring microbes use labile C as an energy source to decompose recalcitrant organic matter to obtain N. When N is added, the microorganism uses preferentially mineral N and has little incentive to break down the recalcitrant organic matter to acquire N, resulting in the reductions of C mineralization of all aggregates with N addition. Therefore, our result is consistent with the prediction of “microbial N mining” theory. However, this theory does not work in paddy soil.

The above possible mechanisms can explain the effects of added N on C mineralization of soil aggregates in forest soil, but are unsuitable for paddy soil. Few possible mechanisms can explain the difference in soil C mineralization by N addition in forest and paddy soils. First, the special microbial communities in paddy soils were already adapted to high N availability (Hagedorn et al. 2012), contrary to the microbial communities in forest soils. To increase crop yield, a large amount of N fertilizer was applied in croplands, resulting in the change of microbial community compositions that adapted to high N availability in paddy soils. In our study, soil microbial biomass carbon (MBC) in paddy soils was 1667 mg kg−1 and was 541% higher than that in forest soils (260 mg kg−1, Table 1). When N is added into the paddy soils, the microbial communities adapting to high N availability may proliferate rapidly and then speed up the rate of SOC turnover. Therefore, the added N can enhance the microbial biomass and promote C mineralization of aggregates in paddy soil (Li et al. 2014). Second, the responses of different soil carbon fractions to N addition varied. N addition significantly accelerates the decomposition of light fractions of soil organic carbon, but further decreases the C mineralization of heavy fractions through stabilization of soil C (Neff et al. 2002). The light fraction of soil organic matter is a labile OC characterized by rapid mineralization due to the labile nature of its chemical constituents, which have greater alkyl-to-O-alkyl ratio than the heavy fraction (Huang et al. 2011b). Labile OC is positively correlated to water-soluble SOC (Zhang et al. 2009). The water-soluble SOC of paddy soils (87.8 mg kg−1) was much higher than that of forest soils (39.1 mg kg−1), implying that more labile OC existed in paddy soils than that in forest soils. When N was added into paddy soils, the soil microorganisms preferred to use labile OC as energy and promoted soil microbial turnover, resulting in the accelerating effects of N addition on C mineralization of paddy soils.


The effects of N addition on soil C mineralization in aggregates in forest and paddy soils in subtropical China were investigated. Soil C mineralization decreased with the increasing sizes of soil aggregates in forest and paddy soils, implying that soil aggregates played an important role in the SOC stability and resulted in soil C sequestration. However, N addition exhibited diverse effects on soil C mineralization in forest and paddy soils in that it impeded soil C mineralization in forest soils but accelerated that in paddy soils. It indicated that land use type can affect the response of soil C mineralization to N addition. These results highlight the important role of soil aggregates and land use types in terrestrial ecosystem C cycle and sequestration under N enrichment. The heterogeneity of soil aggregates and the patch pattern of land use types in global landscape scales increase the uncertainty of soil C sequestration of terrestrial ecosystems with N deposition. Due to the role of soil aggregates and land use types in soil C sequestration, future soil C management should be focused on soil aggregates and land use types to alleviate global climate change.

Availability of data and materials

The datasets used and/or analyzed during the current study are available from the corresponding author on reasonable request.





Soil organic carbon




United States Department of Agriculture


Total nitrogen


Total phosphorus


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Thanks to two anonymous reviewers for their good comments. This study was supported by the National Natural Science Foundation of China (41630755 and 31971718).


The National Natural Science Foundation of China (41630755 and 31971718).

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LC has designed this experiment and written the manuscript. RC has conducted this experiment and analyzed the data. XH, XL, and HL reviewed the manuscript. All authors have read and agreed to the published version of the manuscript.

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Correspondence to Longchi Chen or Haimei Li.

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Cao, R., Chen, L., Hou, X. et al. Nitrogen addition reduced carbon mineralization of aggregates in forest soils but enhanced in paddy soils in South China. Ecol Process 10, 45 (2021).

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  • Ultisol
  • Land use type
  • Microaggregates
  • Soil organic carbon