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Acta Amazonica

Print version ISSN 0044-5967

Acta Amaz. vol.41 no.4 Manaus  2011

http://dx.doi.org/10.1590/S0044-59672011000400017 

 

 

Does nitrogen availability have greater control over the formation of tropical heath forests than water stress? a hypothesis based on nitrogen isotope ratios

 

Tem a disponibilidade de nitrogênio maior controle sobre a formação de florestas tropicais de campinara do que o estresse hídrico? uma hipótese fundamentada nas razões isotópicas do nitrogênio

 

 

Francis Q. BrearleyI, II; Paul V. A. FineIII; Kristel PerreijnIV

ITrinity College, University of Dublin
IIManchester Metropolitan University E-mail: f.q.brearley@mmu.ac.uk
IIIUniversity of California, Berkeley E-mail: paulfine@berkeley.edu
IVUtrecht University E-mail: kristelperreijn@yahoo.com

 

 


ABSTRACT

Global scale analyses of soil and foliage δ15N have found positive relationships between δ15N and ecosystem N loss (suggesting an open N cycle) and a negative relationship between δ15N and water availability. We show here that soils and leaves from tropical heath forests are depleted in 15N relative to 'typical' forests suggesting that they have a tight N cycle and are therefore limited by N rather than by, often suggested, water availability.

Keywords: acid soils, kerangas, nitrous oxide, stable isotopes


RESUMO

Análises de δ15N solo e foliar, em escala global, encontraram relações positivas entre δ15N e a perda de N do ecossistema (sugerindo um ciclo aberto de N), e uma relação negativa entre o δ15N e a disponibilidade de água. Mostramosneste trabalho que os solos e a vegetação de florestas de campinarana são empobrecidas em 15N em relação a florestas 'típicas', sugerindo que elas têm um ciclo fechado de N e são, desta forma, limitadas pelo N, ao invés da disponibilidade de água, como frequentemente sugerido.

Palavras-Chave: solos ácidos, campinarana, óxido nitroso, isótopos estáveis.


 

 

Determining the factors that lead to differing species distributions in tropical forests, especially in relation to soil type, has been an important question in tropical ecology for many years and still remains a contemporary problem (Fine et al. 2004; Russo et al. 2005). Tropical heath forests (HFs) (also known as white sand forests in the Neotropics) are a formation that are very different to 'typical' lowland evergreen rain forests (LERFs) having more acidic soil, lower stature, a more even canopy, thicker smaller leaves and a greater proportion of trees in smaller size classes (Brünig 1974; Proctor 1999). There are a number of lines of evidence that suggest HFs have lower nitrogen (N) availability than LERFs. For example, Turner et al. (2000) found lower foliar N in a range of species from HFs in Brunei and Moran et al. (2000) found lower N in soil solutions and a reduction in N returned via litterfall fluxes in the same forests. In addition, Fine et al. (2005) found lower mineral N availability in Peruvian HFs. In contrast, Brünig (1971, 1974) considers that heath forests are formed due to water limitation which may be especially prevalent on sandy soils.

Examination of N stable isotopes is a powerful methodology that can assess N inputs, outputs and transformations in an ecosystem (Martinelli et al. 1999; Robinson 2001; Amundsen et al. 2003); N availability to plants and trees can be measured by determining stable N isotope abundance. As an example, tropical rain forest soils and leaves are 15N enriched compared to temperate forests (Martinelli et al. 1999). The reason for this difference is related to the nature of the greater loss of N from tropical forests: there is preferential leaching and gaseous loss of the lighter 14N isotope thereby leaving the soils enriched in 15N. However, another factor which leads to changes in δ15N between soils is a change in moisture regime as a decrease in δ15N with increasing rainfall has been found (Austin and Vitousek 1998; Handley et al. 1999; Schuur and Matson 2001). This is hypothesised to be because of a changing preference for organic forms of N in wetter soils (Handley et al. 1999).

The aim of this study was to compare δ15N values of soil and plant material from tropical HFs and LERFs and test the null hypothesis of no differences in δ15N signatures and hence minimal differences in N cycling between the two forest types.

Soil and leaf samples were taken from HF and LERF areas of six tropical sites (Table 1). From four of these sites soils (0-10 cm) were collected and from two of the sites leaves of the sub-canopy species Protium subserratum Engl. (Burseraceae) were collected; this species was chosen as it is one of the only species which is common in both HFs and LERFs (Fine et al. 2005).

 

 

Samples were analysed for δ15N using a ThermoFinnegan Deltaplus IRMS interfaced with a CE Instruments 1112 Flash elemental analyser via a Conflo III (or a Europa 20-20 IRMS interfaced with an ANCA-GSL elemental analyser for the Guyana samples). N isotope ratios are expressed as delta (δ) notation which is the per mille deviation from atmospheric N: δ15N (‰) = [(Rsample/Rstandard) - 1] x 1000 where R is 15N/14N. Precision (standard deviation) of duplicated measurement of sixteen samples on the Deltaplus IRMS was 0.38 ‰.

Soil δ15N values were significantly lower in the HFs when compared with LERF (F1,89 = 190, p < 0.001; Figure 1a). Leaf δ15N values of Protium subserratum were also significantly lower in the HF when compared with LERF (F1,20 = 118, p < 0.001; Figure 1b). There was a negative correlation between rainfall at each site and soil δ15N (r = -0.872) although this was not statistically significant (p = 0.128).

 

 

Numerous studies have shown that a climatic shift of increasing rain fall leads to a decrease in δ15N of soil and/or foliage (Austin and Vitousek 1998; Handley et al. 1999; Schuur and Matson 2001; Amundsen et al. 2003; Sah et al. 2006) both in temperate and tropical sites. Following this pattern, water limitation would be expected to lead to increases in δ15N. If, therefore, tropical HF soils were water limited over LERF soils we would expect an increase in δ15N, not the decrease which was actually seen. The change in δ15N values are most likely to result from an altered N cycle in the HFs and almost certainly from reduced losses of 15N depleted compounds.

Whilst there are often differences in available soil N between forest types there has been little evidence for differences in mineralisation rates. Can our isotopic results therefore be reconciled with those of Vernimmen et al. (2007) and Fine et al. (unpublished data) who found minimal differences in N mineralisation between HF and LERF soils at the Barito Ulu and Iquitos sites respectively? Yes, in so far that for isotopic fractionation to occur, there must be losses of 15N depleted compounds from soils. This can occur through nitrate leaching or denitrification to nitrous oxide. Indeed, we know that emissions of nitrous oxide can be very high from tropical forest soils (Houlton et al. 2006). At our Guyana study site, Perreijn (2002) found that denitrification rates were lower in HF than LERF and we therefore hypothesised that this, more generally, is the cause of the differences in soil δ15N between the two forest types as suggested by Houlton et al. (2006) to explain differences in soil δ15N in relation to climate.

This paper therefore suggests that nitrogen availability is more important in controlling the formation of HFs than water availability confirming the results of previous investigators who found little evidence for drought tolerance among HF trees (Becker 1996; Nagy and Proctor 2000; Sobrado 2010). Nagy and Proctor (2000) also showed that foliar δ13C values were not different between canopy trees in HF and LERF at Barito Ulu adding further support to our hypothesis that water limitation is not of over-riding importance in leading to the HF formation. We suggest that further examination of N cycling patterns in both forest types are continued to examine exactly where in this complex cycle differences between the forest types occur. However, whilst ruling out the over-riding importance of water stress it does not rule out that N cycling may be limited by extreme soil acidity as suggested by Proctor (1999).

 

ACKNOWLEDGEMENTS

Funding for this study was provided by the Department of Botany, Trinity College, Dublin. We thank the Guyanese, Indonesian, Malaysian and Peruvian authorities for permission to work and sample in their respective countries. Robert Bagchi and Ronald Vernimmen are thanked for their comments on the manuscript and Alexandra Gabaglia is thanked for the Portuguese translation.

 

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Recebido em 12/08/2010
Aceito em 13/03/2011

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