We present an intra-annual stable carbon isotope (δ13C) study based on a labeling experiment to illustrate differences in temporal patterns of recent carbon allocation to wood structures of two functional types of trees, Podocarpus falcatus (a late-successional evergreen conifer) and Croton macrostachyus (a deciduous broadleaved pioneer tree), in a tropical mountain forest in Ethiopia.
Dendrometer data, wood anatomical thin sections, and intra-annual δ13C analyses were applied.
Isotope data revealed a clear annual growth pattern in both studied species. For P. falcatus, it was possible to synchronize annual δ13C peaks, wood anatomical structures and monthly precipitation patterns. The labeling signature was evident for three consecutive years. For C. macrostachyus, isotope data illustrate a rapid decline of the labeling signal within half a year.
Our δ13C labeling study indicates a distinct difference in carryover effects between trees of different functional types. A proportion of the labeled δ13C is stored in reserves of wood parenchyma for up to 3 yr in P. falcatus. By contrast, C. macrostachyus shows a high turnover of assimilates and a carbon carryover effect is only detectable in the subsequent year.
If you can't find a tool you're looking for, please click the link at the top of the page to "Go to old article view". Alternatively, view our Knowledge Base articles for additional help. Your feedback is important to us, so please let us know if you have comments or ideas for improvement.
Fractionations of stable carbon and oxygen isotopes (δ13C and δ18O) in tree rings of many species in the temperate (Leavitt & Long, 1988; McCaroll & Loader, 2004; Etien et al., 2008; Esper et al., 2010; Kress et al., 2010), boreal (Kagawa et al., 2006a,b; Gagen et al., 2007) and Mediterranean (Battipaglia et al., 2010; De Micco et al., 2012; Szymczak et al., 2012) zones have been analyzed at inter- and intra-annual resolutions. Understanding of fixation, allocation and remobilization processes of δ13C within an annual cycle and various plant compartments is a prerequisite for isotope dendroclimatology (Damesin & Lelarge, 2003; Helle & Schleser, 2004; Augusti et al., 2006; Kagawa et al., 2006a,b). Helle & Schleser (2004) illustrated a ‘triphase seasonal δ13C pattern in broad-leaf deciduous trees’ with: δ13C increase at the beginning of the vegetation period owing to a carryover effect of stored carbohydrates assimilated during the previous vegetation period; δ13C decrease during the main vegetation period; and a slight increase of δ13C at the very end of the vegetation period as a result of the changed carbohydrate metabolism of senescent leaves. Furthermore, Helle & Schleser (2004) assumed that the mid-section of the seasonal δ13C variation is most affected by environmental factors and may be suitable for reconstruction of seasonal environmental changes. Kagawa et al. (2006a,b) investigated carbon translocation, storage, and remobilization in time and different plant compartments after 13CO2 pulse labeling of Larix gmelini growing in the boreal zone. The results show that earlywood of tree rings contains photoassimilates from the previous summer and autumn as well as from the current season. Usually, only latewood represents the photoassimilates of the current summer and autumn, although a contribution of stored material cannot be totally excluded. Hence, ‘carbon storage is a key mechanism behind autocorrelation in (isotope) dendroclimatology’ (Kagawa et al., 2006b). However, these results were obtained from tree saplings and the authors stress the necessity of carrying out respective experiments on adult trees, which might differ in their behavior (Kagawa et al., 2006b). As evident from a recent review article on pulse-labeling studies (Epron et al., 2012), comparable studies for tropical regions have not been assessed.
A number of studies have already successfully applied stable isotope approaches in tropical regions, most of them working on an annual resolution (Verheyden et al., 2004; Robertson et al., 2006; Gebrekirstos et al., 2009; Brienen et al., 2010; Fichtler et al., 2010; Wils et al., 2010; Gebrekirstos et al., 2011a, 2012; Williams et al., 2011). For instance, a significant negative correlation between annual precipitation and δ13C time series of tree rings was found for several broadleaved tree species in various tropical climates (Fichtler et al., 2010). Gebrekirstos et al. (2011b, 2012) found significant negative correlations of annual δ13C and δ18O variations in West African Sahel woodland species with precipitation amount, humidity, drought (Palmer drought severity index, PDSI), and positive correlations with temperature. Despite those encouraging correlations with climate parameters, physiologically based understanding of δ13C variations in different tree species and functional types is still incomplete.
Stable isotopes have also been used to prove the annual nature of tree rings, to verify visually indistinct growth ring boundaries, and to delineate annual growth layers when visible tree rings are not present in tropical wood (Evans & Schrag, 2004; Poussart & Schrag, 2005; Anchukaitis et al., 2008; Roden, 2008; Pons & Helle, 2011). Anatomically indistinct rings of two tree species growing in the tropical rainforest of central Guyana were identified as annual by Pons & Helle (2011). They used minima of intra-annual δ18O and δ13C variations as primary and secondary indicators of annual growth boundaries, verified by simultaneously measured diameter increment rates of the same trees. However, retrospective stable isotope analyses lack a precise time control when the respective part of the xylem was formed. High-resolution electronic dendrometers are a tool to register the dynamics of stem diameter incremental growth with great precision (Volland-Voigt et al., 2011; Krepkowski et al., 2011), thus providing a time control for the wood formed at a certain distance from the initial starting point of the measurements. Nevertheless, stem diameter increment alone cannot unambiguously be considered as an indicator of cambial growth (Krepkowski et al., 2011, 2012). Positive radial change may result from stem swelling as a result of water uptake and saturation of wood tissues after dry periods; cambial activity with formation of new cells; or enlargement of juvenile cells before lignification (Deslauriers et al., 2009; Krepkowski et al., 2011). Hence, wood anatomical indications of cell formation have to be included for determination of periods of active cambium.
Here, we study differences in carbon carryover effects between different tree functional types linked with dendrometer measurements and wood anatomy to expand our understanding of tropical dendrochronology. To this end, we studied two native tree species with contrasting physiological traits in a tropical mountain forest in Ethiopia. Podocarpus falcatus is a late-successional evergreen conifer, while Croton macrostachyus is an early-successional deciduous tree, but seedlings and saplings of both species compete on the same sites after forest disturbance (Tesfaye et al., 2010). In contrast to P. falcatus, C. macrostachyus shows a shorter life span, higher rates of photosynthesis and transpiration, a higher metabolic activity, and a higher transfer rate of phloem sugars to arbuscular mycorrhiza fungi in the soil (Seyoum et al., 2012; Shibistova et al., 2012). We hypothesize that in the case of the early-successional deciduous tree, the allocation of recently assimilated carbon from the tree canopy to wood will be faster than in the late-successional gymnosperm, and that as a result of the more conservative life strategy, the carryover effect will be more pronounced in the gymnosperm tree. In addition, we propose that intra-annual 13C allocation patterns are related to wood anatomical structures that might indicate annual growth boundaries.
The specific objectives of the study were to analyze the intra-annual patterns of recent 13C allocation in wood of tropical trees belonging to different functional types in order to detect differences in carbon carryover effects; to study differences in cambial dynamics and wood formation of the two studied tree species; and to investigate the relationships among intra-annual δ13C variations, wood anatomical structures and moisture availability.
Materials and Methods
The study site is located in the Munessa-Shashamene Forest, a tropical mountain forest located 240 km south of Addis Ababa at the eastern escarpment of the Main Ethiopian Rift Valley (7°26′N 38°53′E). The vegetation of the remnant natural forest is dominated mainly by the canopy species Croton macrostachyus Hochst. ex Del (143 trees ha−1) and Podocarpus falcatus (73 trees ha−1), but with the presence of other indigenous tree species (Celtis africana Burm.f., Syzygium guineense (Willd.) DC., and Prunus africana (Hook.f.) Kalkman (Tesfaye et al., 2010)).
The climate is subhumid with mean annual temperatures of 14.9°C (minimum 14.3°C, maximum 15.4°C) and the annual rainfall averages 1225 mm with a standard deviation of 217 mm. The precipitation distribution is characterized by a bimodal rainfall pattern (Fritzsche et al., 2006; Freier et al., 2010), with alternate rainy and dry seasons: a long and intense rainy season from July to October followed by a long dry season from November to February and an unreliable short rainy season from March to June delimited by a short dry period in June (Krepkowski et al., 2011). Recently, Strobl et al. (2011) reported that ‘the gap between the small and the long rains [the short dry season] has disappeared and the climate in general has become more humid’ during the last 9 yr.
Maximum air temperatures of 28.1°C occur at the end of the long dry season as a result of the rising position of the sun and low cloudiness accompanied by minimum air humidity. During the dry season, relative air humidity ranges between 45 and 75% and increases with the onset of the long rainy season to maximum values of 90%. The long-term climate data recorded c. 500 m from our study site indicated a high intra-annual precipitation variability with the occurrence of a distinct short dry season in April and May 2008 and 2009, as well as an indistinct long dry season in 2009–10 with many rain events during the period December 2009 to February 2010.
Soils in the area are derived from intermediate volcanic rocks that are present throughout the study area and are rich in clay and iron oxides. Plots under investigation are classified as Mollic Nitisol according to the World Reference Base of Soil Resources (FAO, ISRIC & ISSS, 1998).
Two indigenous tree species belonging to different functional types were selected for the study. The conifer P. falcatus (Podocarpaceae) can grow up to 40 m high and is characterized by a lobate stem form (Fig. 1a). P. falcatus is a shade-tolerant climax species constituting the dominant species in the upper story of the forest canopy (Tesfaye et al., 2010). P. falcatus continuously produces new leaves in moist conditions, with a life span of an individual leaf exceeding 2 yr (Seyoum et al., 2012).
By contrast, C. macrostachyus (Euphorbiaceae, Fig. 1d) is a shade-intolerant pioneer species growing in canopy gaps and occupying the middle and upper levels of the canopy (Tesfaye et al., 2010; Shibistova et al., 2012). Leaf fall of the deciduous C. macrostachyus begins at the end of the long dry season (January/February) and may extend until March/April, so that the leafless period lasts 3–4 months. Leaf flush occurs from March to June, followed by a vegetation period of 7 months (Tesfaye et al., 2011; Seyoum et al., 2012). Development of an individual Croton leaf requires up to 2 months, with a mean life span of only 3 months (Seyoum et al., 2012).
Fig. 1(b, c) illustrates the wood anatomical structures of P. falcatus and C. macrostachyus, following the terminology of Schweingruber et al. (2006). The conifer tree (Fig. 1b) shows distinct ring boundaries in the form of rather narrow bands of radially flattened tracheids with slightly thickened cell walls in the latewood. Additionally, intra-annual density fluctuations (IADFs) are found, but the occurrence of these false rings is irregular and varies among years as well as among tree individuals (Krepkowski et al., 2011). The cross-section of C. macrostachyus reveals wood structures typical for hardwoods with small and thick-walled fibers, a diffuse ring-porous structure with large vessels and wood rays one or two cell rows wide. Growth ring boundaries are marked by slightly thickened cells (Fig. 1c), but they are hard to identify. Occasionally, macroscopically visible tangential parenchyma bands occur and provide additional markers for growth ring boundaries.
Dendrometer measurements and wood anatomy
Electronic point dendrometers (Ecomatik, Germany) were installed in March and September 2008 at 1–1.5 m height on the stems of various-sized P. falcatus and C. macrostachyus (six per species). Before fixation of the dendrometers, the outer parts of the trees' bark were removed to avoid the influence of swelling or shrinking of bark material on the dendrometer curves. Radial stem diameter variations were registered automatically in 30 min intervals. Diurnal stem diameter changes result mainly from changes of the tree's water status. Furthermore, long-term growth trends are recorded that help in determining periods of cambial activity and wood formation (Biondi et al., 2005; Bräuning et al., 2008, 2009; Volland-Voigt et al., 2011; Krepkowski et al., 2011, 2012). In addition, from 2008, wood microcores were collected at intervals of 3–6 wk with a trephor microcorer (Costruzioni Meccaniche Carabin C., Belluno, Italy) to study cambial activity in more detail (Rossi et al., 2006). All microcores were stored in a solution of 50% ethanol in the field. In the laboratory, they were embedded in paraffin by means of dehydration (a mixture of ethanol and d-limonene) and successive infiltration of melted paraffin (Rossi et al., 2006). Thereafter, sections of thickness 10–30 μm were cut with a rotation microtome (Leica, Wetzlar, Germany), cleaned of the remaining paraffin and finally stained with solutions of astra blue and safranin red to distinguish living and nonlignified cells (in blue) from lignified structures (in red). Finally, the dried thin sections were photographed with a Leica microscope system at fourfold magnification and the pictures were edited using Adobe Photoshop software.
Short-term 13CO2 pulse labeling of the two target trees was carried out on two cloudless days (12 and 14 November 2008) at the start of the main rainy season. For the experiment, c. 6-m-high rectangular frames made of eucalyptus poles were constructed around the individual P. falcatus and C. macrostachyus trees, covering a surface of 12.7 and 16.7 m2 for the former and latter, respectively. Shortly before the labeling event, a plastic glasshouse cover (120 µm, 88% light transmission in photosynthetically active radiation (PAR); UVA Clear, Ginegar Plastics Products Ltd, Kibbutz Ginegar, Israel) was pulled over the frame and tightly sealed within 30 min. To prevent transport of 13CO2 from the chamber space into soil pores, the chamber was also sealed with the plastic film from the bottom side at 1.60 m distance from the forest floor. Corresponding chamber volumes were 58.4 m3 for C. macrostachyus and 71.1 m3 for P. falcatus. During the experiment, five electric fans (12 V, 0.21 A) circulated the air in the chambers and CO2 concentration, air temperature, and relative humidity were monitored continuously using a LI-8100 infrared gas analyzer (Li-Cor Inc., Lincoln, NE, USA). Fifteen minutes after the chambers were sealed, and the decline of the CO2 concentration inside the chambers clarified carbon dioxide uptake, 13C-labeled CO2 was generated by injecting diluted sulfuric acid into a flask containing isotopically enriched Na213CO3 solution (99 atom% 13C), and 12.5 mM of 13CO2 per 1 m3 was added to each chamber (0.73 mol 13CO2 for C. macrostachyus and 0.89 mol to P. falcatus) The labeling duration was 85 and 105 min for C. macrostachyus and P. falcatus, respectively, depending on the rate of the 12/13CO2 concentration decrease within the chamber, to prevent an unnoticed loss of the tracer by respiration.
Wood sample collection and isotopic measurements
Wood samples of the labeled trees and control trees of similar size were collected with an increment borer (0.5 cm diameter, Suunto, Vantaa, Finland) in March 2011 (P. falcatus control was sampled in March 2009). After drying, sanding and polishing, the cores were photographed with a Leica stereoscope and camera system. Increment cores were cut with a modified rotation microtome (Leica) in thin sections of 30–40 μm thickness. Each section was collected separately in Eppendorf tubes and they were numbered consecutively. Every third thin section was packed in tin capsules and the δ13C of whole wood was analyzed with a mass spectrometer (Delta V Advantage, Thermo Electron, Bremen, Germany). For high-resolution δ13C analyses we used whole wood instead of α-cellulose, because, during the α-cellulose extraction process, c. 60–70% (Loader et al., 1997) of the sample mass is lost, leading to insufficient amounts of remaining cellulose for mass spectrometry (Kagawa et al., 2006a,b; Pons & Helle, 2011). Numerous studies (Barbour et al., 2001; McCarroll & Loader, 2004; Helle & Schleser, 2004; English et al., 2011; Pons & Helle, 2011 and references therein) have used whole wood and have revealed a constant offset of δ13C of whole wood and cellulose for conifer wood of c. 1‰ (Warren et al., 2001; Pons & Helle, 2011), so that no bias in the measured isotope variations was expected, as the labeling effect that leads to isotope signals c. 30–140 ‰ above the normal fractionation signal by far exceeds the naturally occurring variability of carbon isotopes in wood. Isotope values were calibrated with a laboratory standard (Pepton II) and expressed in δ notation (‰), relative to the Vienna Pee Dee Belemnite (VPDB) standard.
Dendrometer data and microcores
The dendrometer curves of the six sampled P. falcatus (Fig. 2) show corresponding responses of fast or slow increment and stem shrinkage during wet and dry periods, respectively. Stem diameter increment occurs during the short rainy season after the first rainfall events at the end of the dry period (e.g. March and April 2009). The main growing period occurs during the long rainy season beginning around June. Despite the lack of dendrometer data at the end of the long rainy season in 2008, we delimit the growing period to the beginning of the dry season in November, as stem diameters before and after the data gap show almost identical values. By contrast, the main long rainy season of 2009 lasted until the end of October, followed by an indistinct long dry season with unusual rain events in December, inducing ongoing increment until a dryer period in February 2010.
A series of continuously sampled microcores of ‘Podo A01’ are shown in Fig. 3. All samples show growth ring boundaries formed during the long dry season of the years 2006, 2007 and 2008. The distinctness and width of the tree rings vary between the samples in the tangential direction as a result of lobate growth. The microcores illustrate periods of cambial activity in more detail. For example, in March 2009 the thin section depicts freshly formed cells, indicating an active cambium during the short rainy season (precipitation data are shown in Fig. 2). Hence, an IADF is visible in the following samples (IADF, 2009) caused by dormancy of the cambium during the short dry season in April and May 2009. Following the onset of the long rainy season in June 2009, the thin sections from June and September show bands of bluish-colored freshly formed unlignified cells. After a period of lower cambial activity or beginning dormancy in October 2009, the thin section from December 2009 again indicates an active cambium inducing a missing growth ring boundary in this year. Cambial activity continued until a drier period in June 2010 and a new IADF is visible in the samples of July 2010 and May 2011.
The dendrometer data of the six sampled C. macrostachyus (Fig. 4) indicate that all trees react synchronously to the local rainfall pattern. After a stem diameter minimum during the short dry season April–May 2009, increment started after complete refoliation and continued until November 2009. Owing to the ample rain events during the long dry season 2009–10, leaf flush of C. macrostachyus occurred earlier in 2010 and stem diameter increment had already started in the middle of March 2010.
Owing to the wood anatomy of C. macrostachyus, growth ring boundaries are hard to identify. Therefore, only similar wood structures of slightly thickened cells are marked in Fig. 5. The thin sections of May, June, and September 2009 indicate cambial activity by rows of new cells in blue. Corresponding to the dendrometer data and an earlier leaf flush in 2010, freshly formed cell rows are already visible in April 2010.
Intra-annual variations of tree-ring δ13C
High-resolution intra-annual δ13C analyses are illustrated in Table 1 and Figs 6 and 7. Before the labeling experiment, both P. falcatus trees showed similar average δ13C values and intra-annual ranges (unlabeled tree, −24.96 ± 0.99‰, range −26.80 to −22.97‰; labeled tree, −25.13 ± 0.83‰, range −27.06 to −22.90‰; P =0.15, not significant). An individual range in δ13C of 1–3‰ was also found in other species (Saurer et al., 1997; Gebrekirstos et al., 2009; Esper et al., 2010) and is influenced by site conditions (microclimate) and possibly tree age. After labeling, δ13C reaches extremely high positive values of up to 122.23‰ and stable isotope ratios in wood remain at elevated values for the following three annual cycles (Fig. 6). In labeled and control trees, peaks of δ13C can be aligned to distinct wood anatomical structures of tracheids with thickened cell walls. In Fig. 6, precipitation data of September 2008 to November 2009 were aligned to the isotope data of the labeled P. falcatus. The δ13C peak around the growth ring boundary of 2008 coincides with minimum precipitation during the long dry season 2008–09. Moreover, the dry conditions in May 2009 (short dry season 2009) induced a second peak of δ13C in the annual cycle. On the other hand, δ13C values decrease towards an annual minimum during the long rainy season (July–October 2009).
Table 1. Whole wood δ13C mean with standard deviation (SD), and maximum and minimum values of increment cores
δ13C (‰, VPDB)
Mean with SD
VPDB, Vienna Pee Dee Belemnite.
Podocarpus falcatus control
−24.96 ± 0.99
P. falcatus labeled
−25.13 ± 0.83
−8.75 ± 33.72
Croton macrostachyus control
−28.26 ± 0.55
C. macrostachyus labeled
−26.65 ± 0.56
−23.86 ± 7.29
The δ13C values of both C. macrostachyus samples show high intra-annual variations with a distinct peak and an annual amplitude of c. 2.5‰. The mean annual δ13C values of control and labeled C. macrostachyus before the labeling experiment were −28.26 ± 0.55‰ and −26.65 ± 0.56‰, respectively. Values of the unlabeled tree were higher, but show similar cyclic fluctuations as the labeled tree. After the labeling experiment, δ13C increased up to −1.51‰ and the labeling signature decayed during the following year (Fig. 7). No anatomical wood structures can be visually matched with the δ13C cycle. Precipitation data could not be reliably aligned to the δ13C data.
Cambial dynamics of different functional tree types
The wood anatomical thin sections demonstrate that P. falcatus can have repeated phases of cambial activity of different length within 1 yr. Cambium was active during the short rainy season (March 2009 and 2010), the long rainy season (June 2009 and September 2009), and occasionally even during the long dry season if there was sufficient rainfall (December 2009 and February 2010). On the other hand, phases of cambial dormancy are also implicated and result in distinct growth ring boundaries, but also in indistinct and multiple intra-annual density fluctuations (Krepkowski et al., 2012). By contrast, the broadleaved evergreen P. africana forms one growth ring boundary yr–1 (Krepkowski et al., 2011), indicating differences in cambial phenology between evergreen tree species.
In agreement with the leaf phenological studies of Tesfaye et al. (2010) and Seyoum et al. (2012), cambial activity in the broadleaved deciduous C. macrostachyus normally begins with the onset of the long rainy season around June (e.g. 2009). Generally, stem diameter increment before this date is the result of water re-saturation of wood tissues, except under humid conditions during the long dry season (e.g. in 2009–10), inducing an earlier leaf exchange and start of the growing season. Cambial dormancy and growth ring boundary formation at the end of the long rainy season are similar to the co-occurring deciduous C. africana (Krepkowski et al., 2011), but the growth boundary is more distinct in C. africana. It is worth noting that a detailed review of tree ring studies in the lowlands and highlands of Ethiopia (Wils et al., 2011) highlighted the complexity of ring formation and identified four major types of growth ring expression: anatomically not distinct rings, multiple rings yr–1, annual rings and multiple missing rings associated with the local precipitation regime (unimodal to multimodal) and species sensitivity to water availability.
Linking intra-annual stable isotope variation, wood anatomy and climate
Because of the wood anatomy of P. falcatus, with the formation of false rings, and C. macrostachyus, showing indistinct growth boundaries, the establishment of cross-dated ring-width chronologies from synchronized growth curves has not yet been successful. Our study of δ13C in whole wood indicates an annual pattern with a distinct peak of δ13C for both species and sampled individuals (labeled and control; Figs 6 and 7). Maxima of δ13C in P. falcatus can be visually correlated to latewood cells with higher cell wall thickness or to growth ring boundaries, and thus can be helpful for further dendrochronological studies. The annual peak of δ13C coincides with the beginning of the long dry season and thus with environmental conditions characterized by low relative humidity, high vapor pressure deficit or low soil moisture. In 2009, a second, smaller δ13C peak occurred in the labeled P. falcatus, which corresponds to the occurrence of a short dry season. Thus, primary and secondary maxima of δ13C reflect the tree's reaction to dry climate conditions by stomatal closure and decreased discrimination against 13C during photosynthesis. Although our sample size is not sufficient for statistical analysis, the visual correspondence between isotope variations and climate data in Fig. 6 encourages further dendroecological isotope studies, potentially verifying the negative correlation between moisture and δ13C discrimination.
In contrast to the conifer species, δ13C peaks of C. macrostachyus occur in the earlywood. This probably corre-sponds to the beginning of the growing season, as initial earlywood formation in broadleaved species is often accompanied by the mobilization of stored carbohydrates with a subsequent rise of δ13C (Hill et al., 1995; Barbour et al., 2002; Fichtler et al., 2010). After refoliation and the beginning of the growing season around June 2009, the downward trend of δ13C (Fig. 7) is more or less synchronous to increasing precipitation during the long rainy season from June to November 2009 (Fig. 7). Hence, this period of the annual δ13C cycle may correspond to the ‘mid-section of the seasonal δ13C variation’ sensu Helle & Schleser (2004). Owing to the indistinct formation of annual rings in the cores of C. macrostachyus, it was not possible to assign intra-annual stable isotope variations to distinct wood anatomical structures.
The cyclic intra-annual δ13C variations in the wood of P. falcatus may be used to identify annual growth ring boundaries. As has also been shown by Poussart & Schrag (2005) for other Podocarpus species from Thailand, intra-annual variations of δ13C can also help to distinguish tree-ring boundaries. By contrast, δ13C variations in the wood of C. macrostachyus did not allow a clear delimitation of growth rings, as was reported for other tropical broadleaved species by Pons & Helle (2011). In such cases, intra-annual δ18O variations may be used as additional evidence for the detection of annual growth layers (Evans & Schrag, 2004; Anchukaitis et al., 2008; Pons & Helle, 2011).
Carbon carry-over effects in different tree functional types
Both study species show a distinct reaction in the 13CO2-labeling experiment. Despite the comparable amount of 13C assimilated by C. macrostachyus and P. falcatus foliage during the labeling experiment (5.9 ± 0.3 and 6.9 ± 1.3 g, respectively; Shibistova et al., 2012), the proportion and temporal pattern of the tracer allocation to the wood tissues and carbohydrates in the phloem sap differed between the tree species. Phloem sap velocity was c. four times higher for C. macrostachyus. We found a rapid increase of δ13C in P. falcatus, with a maximum of 122‰ in thickened latewood cells of 2008, indicating a formation of latewood mainly from photoassimilates of the current growing season. Furthermore, earlywood and latewood of the two consecutive growing seasons show increased δ13C values, but with a gradual decline towards the natural value of c. −25‰ in spring 2011. The estimated life span of P. falcatus needles is up to 3 yr (Seyoum et al., 2012), which coincides with the decay of the labeling signal in the wood. On the other hand, Shibistova et al. (2012) found that the δ13C signal in labeled P. falcatus needles depleted and reached the value of the leaves of reference trees after 1 yr, whereas photosynthesis products (D-1-O-methyl-muco-inositol; OMMI) in phloem sap still showed isotopic enrichment of 2–10‰ after 1 yr. Hence, we assume that P. falcatus makes use of storage carbohydrates remobilized from reserves in the wood parenchyma to form new xylem cells.
Remobilization of 13C-enriched starch at the beginning of the growing period has been demonstrated for tropical tree species (Fichtler et al., 2010; Pons & Helle, 2011) as well as for species of the temperate and boreal climate zones (Helle & Schleser, 2004; Kagawa et al., 2006a,b; Gessler et al., 2009). Comparably, while carryover effects for the pioneer C. macrostachyus are similar to deciduous trees in temperate climate zones (Helle & Schleser, 2004), they extend over more than one vegetation period in the late-successional conifer P. falcatus, similar to evergreen trees in the boreal zone (Kagawa et al., 2006a,b). As the secondary metabolite OMMI, which is ubiquitous in gymnosperms, behaves more conservatively than the sucrose presented in angiosperm phloem sap (Shibistova et al., 2012), the observed differences in carryover effects might also partly reflect general evolutionary traits. The extended carryover effect in evergreen species might also influence the climatic signal strength contained in δ13C series. In eastern and western Africa, Gebrekirstos et al. (2009, 2012) found stronger climatic signals in deciduous species compared with co-occurring evergreen species.
We investigated a dominant late-successional evergreen conifer tree species and an early-successional deciduous broadleaved pioneer species in a tropical mountain forest in southern Ethiopia. Our study demonstrated that the functional types of tropical trees differ in their cambial phenology and use of stored carbohydrates for cell formation. The evergreen conifer is able to initiate wood formation at any time of the year when moisture conditions are sufficient, whereas cambial activity of the deciduous broadleaved species is restricted to the foliated period during the long rainy season.
Epron et al. (2012) reviewed 47 pulse-labeling studies mainly on beech and pine from temperate and boreal trees and concluded that the rate of transfer differs between broadleaved and coniferous species and generally decreases as temperature and soil water content decrease. Similarly, our δ13C labeling study, the first of its kind in a tropical ecosystem, suggests distinct differences in carryover effects in tropical tree functional types. Whole wood δ13C of C. macrostachyus shows a fast depletion of the isotope tracer within 1 yr. By contrast, the isotope signal can be detected over three vegetation periods in P. falcatus. This underlines the fact that a deeper knowledge of carbon storage strategies and ecophysiological processes is important to expand our understanding of tropical dendroclimatology. This difference in carbon allocation between early-successional deciduous pioneer species and late-successional conifers also has implications on plant–soil–atmosphere carbon balances of different forest successional stages, which have to be considered for carbon management of tropical forest landscapes. To gain a complete understanding of the different growth strategies and their ecological adaptations in the studied tropical mountain forest, the applied study approach should be extended to other tree functional types such as evergreen broadleaved trees.
We are indebted to the German Research Foundation for funding this project (BR 1895/15). We are grateful to the two anonymous reviewers for their constructive comments, which helped us to improve the quality of the paper.