ORIGINAL RESEARCH article
Sec. Terrestrial Microbiology
volume 2 - 2011 | https://doi.org/10.3389/fmicb.2011.00274
Production of branched tetraether lipids in the lower Pearl River and estuary: effects of extraction methods and impact on bGDGT proxies
- 1 State Key Laboratory of Marine Geology, Tongji University, Shanghai, China
- 2 Department of Marine Sciences, University of Georgia, Athens, GA, USA
- 3 School of Earth Resources, China University of Geosciences-Wuhan, Wuhan, China
- 4 MARUM – Centre for Marine Environmental Sciences, University of Bremen, Bremen, Germany
- 5 Geomicrobiology Laboratory, State Key Laboratory of Geological Processes and Mineral Resources, China University of Geosciences, Beijing, China
- 6 Department of Geology, Miami University, Oxford, OH, USA
Branched glycerol dibiphytanyl glycerol tetraethers (bGDGTs) are known as bacterial lipids that occur widely in terrestrial environments, particularly in anaerobic peat bogs and soil. We examined the abundance and distribution of bGDGTs in both core (C) and polar (P) lipid fractions from the water column and surface sediments in the lower Pearl River (PR) and its estuary using two extraction methods (sonication vs. Bligh and Dyer). A number of soil samples in the lower PR drainage basin were also collected and extracted for bGDGTs using the sonication method. The results showed aquatic production of bGDGTs as supported by substantial abundances of P-bGDGTs in the water column and sediment samples. The bGDGT-based proxies (BIT, CBT, and MBT) were not affected by the method of extraction when C-bGDGTs were analyzed; in such case, the pHCBT of the sediments reflected the soil pH of the lower PR drainage basin, and the temperature close to the annual mean air temperature (MAT) in the lower PR basin. On the other hand, the P-bGDGT-derived proxies were inconsistent between the two methods. The P-bGDGTs (particularly those extracted using the sonication method) may not be reliable indicators of annual MATs.
Rivers and coastal regions play a key role in the global biogeochemical cycle of carbon because they represent a fundamental, multi-faceted link between the atmosphere, land, and ocean (Raymond and Cole, 2003; Cole et al., 2007; Mayorga, 2008). Rivers are known to be the main channels delivering terrestrial particulate- and dissolved organic matter into the ocean as the majority of the global burial of organic carbon in the ocean is found in margins adjacent to rivers (e.g., Hedges and Keil, 1995; Goni et al., 2006). Increasing evidence further indicates that rivers may constitute a moving bioreactor with interactions occurring between microbial communities and the river organic and/or inorganic constituents (e.g., Dagg et al., 2005; Duan and Bianchi, 2006).
Estuaries are dynamic environments where the transportation of terrestrial organic matter from rivers to oceans occurs, and water chemistry changes dramatically between ocean and river environments. The composition of organic matter can also change in the estuary as a result of mixing and enhanced physical, chemical, and microbial reworking of the organic matter (Hedges et al., 1988; Zimmerman and Canuel, 2001; Zhu et al., 2011a).
Recently a number of novel proxies have been developed that are thought to reflect terrestrial environmental signals because biomarkers constituting these novel proxies are known to be ubiquitously and predominantly produced in soil and peat bogs (Hopmans et al., 2004; Weijers et al., 2006a, 2007a). These include methylation index of branched tetraethers (MBT), cyclization ratio of branched tetraethers (CBT) and branched and isoprenoid tetraethers (BIT), which all consist of glycerol dialkyl glycerol tetraethers (GDGTs; Hopmans et al., 2004; Weijers et al., 2007a). CBT and MBT utilize compounds produced by organisms of unknown origin but appear to be from bacteria found in terrestrial environments (Weijers et al., 2006b; Sinninghe Damsté et al., 2011). In particular, CBT is known to reflect soil pH (Weijers et al., 2007a; Peterse et al., 2009) and CBT and MBT in combination can reflect annual mean air temperature (MAT; Weijers et al., 2007a; Sun et al., 2011). These proxies have been increasingly used for past continental temperature (Weijers et al., 2007b,c, 2011; Ballantyne et al., 2010; Peterse et al., 2011; Zhou et al., 2011) or pH (Weijers et al., 2007b; Tyler et al., 2010; Fawcett et al., 2011; Zhou et al., 2011) determinations as well as for paleotemperature determinations in continental margins (Weijers et al., 2007b,c; Schouten et al., 2008; Rueda et al., 2009; Bendle et al., 2010) or lakes (Tyler et al., 2010; Zink et al., 2010).
The BIT index was originally developed to reflect the relative abundances of marine crenarchaeol and terrestrial branched tetraethers in a marine setting, which serves as a unique proxy for transport of terrestrial carbon to marine environments (Hopmans et al., 2004). An increasing number of studies have used BIT to address transport of terrestrial organic matter from rivers into the marine system (Herfort et al., 2006; Kim et al., 2006, 2007, 2009, 2010; Huguet et al., 2007; van Dongen et al., 2008; Walsh et al., 2008; Belicka and Harvey, 2009; Schmidt et al., 2010; Smith et al., 2010; Zhu et al., 2011b). A general observation of these studies is that the terrestrial organic matter preserved in marine sediments as estimated by BIT reflects mostly soil origin (Walsh et al., 2008; Belicka and Harvey, 2009; Weijers et al., 2009). On the other hand, crenarchaeol is known to be present in soil (e.g., Leininger et al., 2006), lakes (e.g., Powers et al., 2004), rivers (e.g., Herfort et al., 2006), and terrestrial hot springs (Pearson et al., 2004; Zhang et al., 2006), which can complicate the interpretation of BIT in certain geological settings.
All of those studies focused on the core lipids of bGDGTs. Recently, intact polar lipids (IPL) of bGDGTs have been examined in soil or peat bogs (Liu et al., 2010; Peterse et al., 2010; Weijers et al., 2011) and a lake (Tierney et al., 2011). The IPL of bGDGTs are lower in abundance than the core lipids of bGDGTs in soil (Peterse et al., 2010; Weijers et al., 2011) or peat (Liu et al., 2010) but respond similarly to pH variations as do the core lipids in soil (Peterse et al., 2010). Mounting evidence indicates that branched tetraether lipids can be produced in situ in aquatic environments including fjords (Peterse et al., 2009), lakes (Sinninghe Damsté et al., 2009; Tierney and Russell, 2009; Sun et al., 2011; Tierney et al., 2011; Wang et al., 2012), and estuaries (Zhu et al., 2011b). These observations warn that cautions should be exercised when using BIT, CBT, or MBT as proxies for soil input into marine or lacustrine sediments or for estimating changes in paleo-air temperatures of continental settings.
The Pearl River is the second largest river in China and together with the Mekong River it provides the largest inflow of fresh water to the South China Sea (Hu et al., 2006a, 2009). It discharges ∼3.26 × 1011 m3 of fresh water and ∼7 × 107 tons of sediment annually to the South China Sea. However, 80% of the sediment is estimated to be deposited within the Pearl River estuary (Wai et al., 2004). A number of studies have examined the terrestrial inputs of organic matter to the Pearl River estuary and adjacent South China Sea by looking at dissolved organic carbon (e.g., Callahan et al., 2004; Chen et al., 2004; Hu et al., 2006a), particulate organic carbon (e.g., Chen et al., 2003), or sedimentary organic matter (He et al., 2010; Yu et al., 2010). Molecular biomarker studies show increased terrestrial signals from the Pearl River mouth to the inner estuary and enhanced marine conditions further offshore (Hu et al., 2006b, 2009).
Here we present initial measurements of both core lipids and polar lipids (PL; see the definition of PLs in Material and Methods) of branched GDGTs from the lower Pearl River to the estuary. Our goal was to delineate the sources of bGDGTs in estuary environments and evaluate the potential use of these biomarkers for paleo-continental climate studies in the region. In particular, the PLs can add additional insight into the sources of the in situ production of bGDGTs in these systems. We chose the Pearl River for examining the sources and distribution of bGDGTs because this system has been well characterized in terms of the distribution and degradation of terrestrial organic matter, which would provide a good context for studying the bGDGT-dynamics at the land-sea interface. Our results show in situ production of bGDGTs in the lower Pearl River and the estuary, with a significant decrease in the abundance of core lipids from fresh water to brackish water. The pH of the sediments as calculated from core (C)-bGDGTs-derived CBT reflects the soil environment of the lower Pearl River drainage basin, and the temperatures recorded by the C-bGDGTs in the sediments reflect the annual MATs of the lower Pearl River drainage basin. On the other hand, temperatures calculated from the polar (P)-bGDGTs are significantly lower than those from the C-bGDGTs, suggesting that P-bGDGTs (particularly those extracted using the sonication method) may not be reliable indicators of annual MATs.
Materials and Methods
Description of Field Site
The lower Pearl River is a complex water system that consists of three main tributaries: Beijing (North River), Dongjiang (East River) and Xijiang (West River; Figure 1). Discharge of freshwater by the Pearl River goes through three sub-estuaries: Lingdingyang, Modaomen and Huangmaohai (Figure 1). Nearly half of the freshwater flows through Lingdingyang, which is a North–South bell-shaped area with a length of about 49 km and a width varying from 4 to 48 km (Hu et al., 2006a, 2009). The average water depth of the Lingdingyang is 4.8 m, increasing from north to south and west to east (Hu et al., 2009). The average tidal range is 1–2 m and the tidal current is 1–2 m/s (Hu et al., 2009). The sedimentation rates vary in the estuary/shelf system, with 1.13–2.34 cm/year in the coastal regions (Jia and Peng, 2003) and 0.2–1.0 cm/year on the shelf (Owen and Lee, 2004). The age of the surface sediment (the top 10 cm) is estimated to be 5–10 years in the estuary/shelf system (Hu et al., 2006a).
Figure 1. Map of the lower Pearl River and estuary. Insert “A” shows filter samples from water column (solid circles, PR1–PR10) in the lower PR. Insert “B” shows filter samples in the estuary (solid circles, PR11–PR14). Soil samples in the lower PR drainage basin and estuary are shown in white squares. The sediment samples were collected at the same locations at which filter samples were collected.
The lower Pearl River region is characterized by humid subtropical weather with annual MAT of about 22°C and annual precipitation of 1200–2200 mm (Zhang et al., 2008). Vegetation in this tropical region is dominated by C3 plants with C4 grasses being a minor component; however, sugarcane (a C4 plant) is one of the major agricultural products in the region today (Yu et al., 2010). Soil pH in this region ranges from 4.07 to 7.22 (Wong et al., 2002).
Collection of Water, Sediment, and Soil Samples
A cruise in July 2010 collected samples in the Beijing tributary and the Lingdingyang estuary (Figure 1). Water samples were collected at 14 stations, which included 10 in the lower Pearl River and 4 in the estuary (Table 1). The river stations included both main channel and sub-tributary samples. Samples from the estuary were collected from both surface and bottom water layers.
Table 1. Water depth, temperature (Temp), salinity (Sal.), suspended particulate matter (SPM), and abundances of lipids in the water column.
At each station in the river, water at a depth of 1–3 m was collected into a 200-L plastic barrel using a submersible pump. The barrel was rinsed with the river water three times before being filled. The pump was then connected to a filtration system that held three 142-mm glass-fiber filters in parallel. The filters had been combusted at 450°C overnight and weighed individually at room temperature prior to the cruise. The total volume of water for all three filters was recorded and the filters were then carefully transferred to sterile 50-mL centrifuge tubes, which were immediately stored in a liquid nitrogen container. Finally, suspended particulate matter was collected using 0.45-μm filters by filtering 10–20 L of water. Before water was collected using the submersible pump, a Horiba instrument (Model W-20XD, Kyoto, Japan) was used for in situ determination of water depth, salinity, and temperature.
Surface sediment (0–10 cm) in the river and estuary was collected using a portable device. The sediment was collected into 50-mL centrifuge tubes and stored in the liquid nitrogen container upon collection (exception was samples for grain size analyses, which were stored under ambient temperature conditions).
Soil samples (from the top 5–10 cm) were collected at 20 locations along the bank of the Beijing tributary and local drainage basin (Figure 1) because this tributary contributes the vast majority of sediments in the estuary. The surface soil samples were collected in 50-mL centrifuge tubes and immediately stored in the liquid nitrogen container. Additional soil material was collected into plastic bags for analysis of grain sizes.
Analyses of Organic Carbon from Sediments and Soil
In the laboratory, aliquots of freeze-dried sediment or soil samples were homogenized for acidification in 10% HCl, washed with deionized water to remove chloride, and subsequently dried at 80°C overnight for analysis of total organic carbon (TOC) using an organic element analyzer EA1110 (Carlo Erba). The carbon isotopes of the TOC were then determined on the GV-Isoprime EA IRMS with a precision of 0.1% for δ13C, which is defined as [(13C/12C)sa/(13C/12C)std − 1] × 1000 (where sa, sample, and std, standard).
Measurements of PH, Salinity, and Grain Sizes of Sediments and Soil
The pH of soil and sediment was determined by drying the samples, which were then pulverized and prepared for each as slurry by adding ultrapure water to the sample powder in a ratio of 1:2.5 (g/mL). The pH of the slurry was determined in the upper solution using a pH meter (Mettler Toledo, USA) after homogenization of the slurry and settling of particles to the bottom of the container.
Pore water salinity was measured using a salinity refractometer (Sino Science and Technology Co., China) after sediment pore water was collected through centrifugation (4000 rpm) and filtered through 0.45-μm cellulose acetate membranes.
Grain size analysis followed Xiao et al. (2009). Briefly, about 0.15 g of sediment or soil material was pretreated with 10-mL of 30% H2O2 to remove organic matter and then with 15 mL of 25% acetic acid to remove carbonates. NaOH was used under boiling conditions to remove biogenic silicate. The residue (in 50 mL solution) was dispersed with 300 mg of (NaPO3)6 and boiled for 1 min, then cooled down and ultrasonicated for about 3 min before grain size analysis. The grain size distribution was determined using a laser diffraction size analyzer (Beckman Co., USA), which had a mechanical reproducibility of better than ±1% for the median diameter.
Lipid Extraction and LC–MS Analysis
The freeze-dried sediments and soil were homogenized with a mortar and pestle and frozen filters were cut into pieces before lipid extraction. One of the serial filters or 5-g dry sediment/soil was extracted by sonication (10 min, 3× each) with methanol, dichloromethane (DCM)/methanol (1:1, v/v), and DCM, respectively, with centrifugation being used after each extraction. The supernatants were pooled, carefully evaporated to dryness under a nitrogen stream at 40°C, re-dissolved in a small amount of n-hexane/DCM (9:1, v/v), and separated into apolar and polar fractions by sequential elution of the total lipids through an activated silica column using n-hexane/DCM (9:1, v/v) and DCM/methanol (1:1, v/v), respectively. Half of the polar fraction was condensed, dissolved in n-hexane/isopropanol (99:1, v/v), and filtered through a 0.45-μm PTFE filter prior to analysis. The other half of the polar fraction was hydrolyzed (4 h, 70°C) in 5% HCl/methanol (v/v). DCM and MilliQ water were added and the DCM fraction was collected (repeated 4×). The DCM fraction was washed (6×) with MilliQ water in order to remove acid, and dried under N2. The hydrolyzed fraction was also re-dissolved in n-hexane/isopropanol (99:1, v/v) and filtered through 0.45 μm PTFE filters prior to analysis on the LC–MS. The difference in LC–MS results between the hydrolyzed and non-hydrolyzed polar fractions is considered to be the IPLs (Huguet et al., 2010b). However, because we did not identify the head groups of the IPLs, the hydrolyzed product may include other fractions not in the form of the IPLs. Thus in this study we consider this difference to be the PL.
A modified Bligh and Dyer extraction procedure (White et al., 1979) is preferred for evaluation of intact polar GDGTs from natural environments (Pitcher et al., 2009; Peterse et al., 2010; Tierney et al., 2011; Weijers et al., 2011). This method was also used for extraction of GDGTs from the filter and sediment samples.
The GDGTs were analyzed on an Agilent 1200 liquid chromatography equipped with an automatic injector coupled to QQQ 6460 MS and Mass Hunter LC–MS manager software using a procedure modified from Hopmans et al. (2004) and Schouten et al. (2007). Separation of peaks was achieved using a Prevail Cyano column (2.1 mm × 150 mm, 3 μm; Alltech Deerifled, IL, USA) maintained at a temperature of 40°C. Injection volume was 5 μL. GDGTs were first eluted isocratically with 90% A and 10% B for 5 min, followed by a linear gradient to 18% B in 45 min. Solvent was held for 10 min in 100% B and was then allowed to re-equilibrate in a mixture of A:B (9:1, v/v) for 10 min. A represents n-hexane and B is a mixture of 90% n-hexane and 10% isopropanol.
Detection of GDGTs was performed using the Agilent 6460 triple-quadrupole mass spectrometer (MS) with an atmospheric pressure chemical ionization (APCI) ion source. The scanning type used was single ion monitoring mode of protonated molecules. The conditions for APCI/MS were as follows: nebulizer pressure 40 psi, vaporizer temperature 350°C, drying gas (N2) flow 5 L/min and temperature 250°C, capillary voltage 3 kV, and corona 4 μA. All samples were quantified by adding a known amount of an internal C46 standard with a detection limit of 0.8 pg.
Definition of the BGDGT Proxies
The structures of bGDGTs and crenarchaeol (Cren) are presented in Appendix.
Mean air temperatures and soil or sediment pH derived from CBT and MBT were calculated using Weijers et al. (2007a):
Results and Discussion
Production of BGDGTs in Water Column and Surface Sediments
Concentrations of P-bGDGTs obtained from the sonication and Bligh and Dyer methods showed large variations and an overall decrease from the lower PR to the estuary (Figure 2A). When using the sonication method, P-bGDGTs had a range of 0.24–2.0 μg/g SPM (average = 1.04 ± 0.56 μg/g SPM, n = 9) in the lower PR and a range of 0.05–0.76 μg/g SPM (average = 0.34 ± 0.30 μg/g SPM, n = 7) in the estuary (Figures 3A,B; Table 1). The Bligh and Dyer method yielded lower concentrations of P-bGDGTs, which had a range of 0.23–1.64 μg/g SPM (average = 0.75 ± 0.46 μg/g SPM, n = 9) in the lower PR and a range of 0.01–0.21 (average = 0.08 ± 0.07 μg/g SPM, n = 7) in the estuary (Figures 3A,B; Table 1). Overall, larger variations in P-bGDGTs are associated with the sonication method than with the Bligh and Dyer for the water column samples (Figures 3A,B).
Figure 2. Core (C)- and polar(P)-lipids (L) of bGDGTs in the water column (A) and sediments (B) from the lower Pearl River to the estuary. Zero distance is arbitrarily set at PR-9 in Figure 1 and increasing distance is toward the estuary. The error bars in (A) represent SD of the average values between the surface water- and the bottom water samples in the estuary.
Figure 3. Comparison of concentrations of C- and P-bGDGTs extracted using the sonication (Soni) and Bligh and Dyer (BD) methods for water column (A,B) and sediment (C,D) samples from the lower Pearl River and estuary. CL, core lipids; PL, polar lipids.
Concentrations of P-bGDGTs in sediments had large variations in the lower PR (Figure 2B). In the lower PR, the sonication method yielded P-bGDGTs concentrations in a range of 2.2–52.7 ng/g sediment (0.2–2.6 μg/g TOC) with an average value of 17.1 ± 14.9 ng/g sediment (1.1 ± 0.7 μg/g TOC, n = 9; Figure 3C; Table 2); the Bligh and Dyer method yielded P-bGDGTs in a range of 6.4–46.7 ng/g sediment (0.2–4.4 μg/g TOC) with an average value of 33.6 ± 7.9 ng/g sediment (2.6 ± 1.2 μg/g TOC; Figure 3C; Table 2). In the estuary, the two methods yielded similar concentrations of P-bGDGTs at each station (Table 2), which had an average value of 15.4 ± 8.9 ng/g sediment (1.8 ± 0.7 μg/g TOC; n = 3) from the sonication method and 18.5 ± 8.7 ng/g sediment (2.2 ± 0.3 μg/g TOC) from the Bligh and Dyer method (Figure 3D).
Table 2. Basic information on water depth, the grain size distribution, total organic carbon (TOC) and carbon isotope compositions, and lipids of surface sediments from river bed and the estuary of the Pearl River.
The difference in P-bGDGTs concentration between the two methods was further evaluated using the student t-test, which gave P-values >0.05 for all water column samples from the lower PR and the estuary. In the sediments, however, the P-value was <0.05 in the lower PR and >0.05 in the estuary. This indicates that these two methods statistically yielded similar concentrations of P-bGDGTs in the water column; whereas in sediments the Bligh and Dyer method yielded significantly higher P-bGDGTs in the lower PR than the sonication method (Table 2).
When normalized to total bGDGTs (P-bGDGTs + C-bGDGTs), the P-bGDGTs in the water column averaged 50.4 ± 18.8% in the lower PR and 69.5 ± 16.1% in the estuary, by the sonication method (Table 1). On the other hand, the relative abundance of P-bGDGTs from the Bligh and Dyer method was much lower, averaging 21.6% for both the lower PR and the estuary (Table 1), which were both statistically (P < 0.05) lower than the sonication method. This lower ratio was apparently caused by the greater concentrations of C-bGDGTs produced by the Bligh and Dyer method than the sonication method (Figures 3A,B). In the sediments, the sonication method yielded 6.9 ± 3.8% of P-bGDGTs in total lipids in the lower PR, which was significantly (P < 0.05) lower than the Bligh and Dyer method (14.2 ± 8.6%; Table 2), mostly due to the higher concentrations of the P-bGDGTs by the latter method (avg. 33.6 ng/g vs. 17.1 ng/g; Table 2).
The soil samples were analyzed using the sonication method only, which yielded P-bGDGTs having a range of 0.5–146.2 ng/g in soil (0.1–12.8 μg/g TOC; Table 3). The relative abundance of P-bGDGTs in total lipids had a range of 1.4–31.0%, with an average value of 7.8 ± 7.1% (n = 20), which is close to the average value of P-bGDGTs in the sediments of the lower PR (Table 2).
Table 3. Basic information on pH, grain size distribution, total organic carbon (TOC) and carbon isotope compositions, and lipids of surface soils in the lower Pearl River drainage basin.
One caveat associated with the sonication method is that the PLs may be matrix-bonded rather than originating from intact microbial cells (Huguet et al., 2010a). This might be the case for the water column filters, which tended to yield higher concentrations of P-bGDGTs by the sonication method than by the Bligh and Dyer method (Table 1), even though the student t-test did not show a significant difference between the two methods for each sample. On the other hand, concentrations of P-bGDGTs from the lower PR sediments were significantly lower when determined by the sonication method than by the Bligh and Dyer, which is inconsistent with the excess extraction of PLs that are matrix-bonded when sonication is used (Huguet et al., 2010a). This suggests that the yield of matrix-bonded PLs may be affected by the structure and composition of the solids with which the lipids are bonded. The difference may also be caused by specific procedures used in each lab or by other unknown variables. The factors causing the differences in the yield of P-bGDGTs in different methods are not well understood.
Only a few studies have reported the abundances of P-bGDGTs in soil and peat bog environments and used them as biomarkers of living organisms (Liu et al., 2010; Peterse et al., 2010; Weijers et al., 2011). In this study, the P-bGDGTs in soil and sediments are in the same range as reported by Peterse et al. (2010) and Weijers et al. (2011). Early studies have showed that C-bGDGTs are widespread in soil and peat bogs (e.g., Weijers et al., 2006a, 2007a) and bGDGTs observed in marine systems are mostly derived from the terrestrial environments (Hopmans et al., 2004; Weijers et al., 2006a,b). However, it has been shown that the in situ production of bGDGTs appeared to contribute to some of the observed bGDGTs in a fjord environment where soil organic matter was low (Peterse et al., 2009). Most recently, in situ production of bGDGTs in the oxic East China Sea shelf was also reported (Zhu et al., 2011b). Both studies made the conclusions using measurements of core lipids. The ubiquitous presence of P-bGDGTs from filter and sediment samples in the Pearl River and estuary further supports those observations and indicates that living organisms producing P-bGDGTs may be present in these environments. However, the source of bGDGTs in the oxic water column is unknown. One possibility may be the production by aerobic or facultative aerobic organisms in the oxic water; the other possibility may be production by anaerobic organisms that reside in suspended particles containing micro-anoxic environments.
Correlations between Abundances of BGDGTs and PH or TOC in Sediments
bGDGTs were normalized to the clay fraction when compared with TOC because the abundance of bGDGTs tended to be higher with increasing clay content (data not shown). In the sediments, the abundances of C-bGDGTs from either the sonication or Bligh and Dyer increased significantly with TOC for concentration up to 2.5% (Figure 4). The P-bGDGTs from both methods remained low (<5%) with increasing TOC; one exception was the sample having the highest TOC, which had much higher P-bGDGT abundance from the sonication extraction than from the Bligh and Dyer method (Table 2). In the soil samples, no significant correlations existed between C-bGDGTs and TOC or between P-bGDGTs and TOC from both methods (data not shown). The results suggest that the abundance of C-bGDGTs was affected by the availability of TOC in the sediments but not in soils within the study area; and that the abundance of P-bGDGTs was insensitive to changes in TOC.
Figure 4. Scatter diagrams of TOC in sediments vs. clay-normalized bGDGTs in ng/g × 102 (A), and pH vs. clay-normalized bGDGTs in ng/g × 102 (B) and TOC-normalized bGDGTs in ng/g × 102 (C) for both sonication (Soni) and Bligh and Dyer (BD) methods. CL, core lipids; PL, polar lipids.
The correlation between clay-normalized bGDGTs and pH had a maximum around pH 7.4 (Figure 4B). When normalized to the content of TOC, a more significant negative correlation was observed for bGDGTs obtained from the sonication method than the Bligh and Dyer method (Figure 4C). Similarly, in soil samples, no correlation existed between pH and abundance of either C- or P-bGDGTs normalized to TOC, or when normalized to soil clay fractions (data not shown).
The pH–bGDGT correlation for the sediment samples in this study is consistent with observations from Weijers et al. (2007a) in a global survey of soil bGDGTs. A long-term soil manipulation also shows that soil pH is the only varying control on the abundance and distribution of branched GDGTs (Peterse et al., 2010). The lack of correlations between bGDGTs and pH in the PR soil, however, suggests that other variables (other than TOC) may play a role in controlling the abundance of bGDGTs in this region.
Changes in BGDGTs-Derived Proxies from the Lower Pearl River to Estuary
BIT, MBT, and CBT in the water column
The BIT values in the water column decreased in a non-linear pattern for both the C- and P-bGDGTs in the lower PR (Figures 5A,A′). In the estuary, BIT values (for either C- or P-bGDGTs) decreased sharply from above 0.81 at station 11 to less than 0.1 at station 14 in either method (Figures 5A,A′). The MBT values for C-bGDGTs were relatively constant and around 0.6 from the lower PR and estuary for the two methods (Figure 5B). The MBT values for P-bGDGTs obtained from the Bligh and Dyer method was also relatively constant and around 0.6; whereas, the values obtained from the sonication method showed much larger variations (Figure 5B′). The CBT values showed larger variations for both C- and P-bGDGTs in the lower PR than in the estuary, with the former varying between 0.6 and 1.2 and the latter between 0.4 and 1.4 in either method (Figures 5C,C′).
Figure 5. Changes in BIT, MBT, and CBT in the water column from lower Pearl River to the estuary for C-bGDGTs (A–C) and P-bGDGTs (A′–C′) for the sonication and Bligh and Dyer (BD) methods. Zero distance is arbitrarily set at PR-9 in Figure 1 and increasing distance is toward the estuary. The error bars in each panel represent SD of the average values between the surface water- and the bottom water samples in the estuary.
BIT, MBT, and CBT in the sediments
Variations in BIT, MBT, and CBT showed very little difference between the two methods for the C-bGDGTs (Figures 6A–C). For the P-bGDGTs, however, the proxies based on the sonication method varied more than those based on the Bligh and Dyer method (Figures 6A′–C′). These results along with those from the water column suggest that proxies derived from C-bGDGTs are not affected by different extraction methods; whereas, proxies derived from P-bGDGTs appeared to be more stable based on the Bligh and Dyer method than the sonication method.
Figure 6. Changes in BIT, MBT, and CBT in the sediments from lower Pearl River to the estuary for C-bGDGTs (A–C) and P-bGDGTs (A′–C′) for the sonication and Bligh and Dyer (BD) methods. Zero distance is arbitrarily set at PR-9 in Figure 1 and increasing distance is toward the estuary.
Implications for CBT- and MBT-Derived pH and Temperatures
The CBT proxy is known to correlate with the pH of the environment from which the bGDGTs are derived (e.g., Weijers et al., 2007a; Peterse et al., 2010). In this study, a student t-test was performed to compare calculated pH values from C-bGDGTs and P-bGDGTs (extracted using either sonication or Bligh and Dyer method) and compare them with the measured pH values (Figure 7). In the sonication method, the CBT-derived pH values of soil samples showed large variations and were statistically indifferent between the C- and P-bGDGTs, with their average pH values similar to the measured average soil pH value (6.56 ± 1.39, n = 20; Figure 7). These results suggest that CBT-derived pH values statistically reflect the in situ soil pH.
Figure 7. Comparison of CBT-derived pH to measured pH values of soil and sediments for the sonication (Soni) and Bligh and Dyer (BD) methods. CL, core lipids; PL, polar lipids.
The CBT-derived pH values of the sediments in both the sonication and Bligh and Dyer methods varied between the average measured pH values of the sediments (7.48 ± 0.34) and soil (6.56 ± 1.39; Figure 7). For the sonication method, the student t-test showed that the calculated pH values from either C-bGDGTs or P-bGDGTs (Table A1 in Appendix) were significantly different from the measured individual sediment pH values (Table 2). However, no significant differences existed between sediment C- or P-bGDGT-derived pH values and measured soil pH values (Table 3), possibly due to the large variation of the measured soil pH (Figure 7). Nevertheless, these results may suggest that the sonication-derived CBT proxy reflects soil pH and not the in situ sediment pH.
For the Bligh and Dyer method, the student t-test showed that the pH values from the C-bGDGTs and P-bGDGTs were significantly different (Table A2 in Appendix), with the latter close to the average measured sediment pH value (Figure 7) and significantly different from the average measured soil pH (P < 0.05). On the other hand, no significant difference existed in the average pH value between sediment C-bGDGTs and soil.
These results indicate that using the sonication method both C- and P-bGDGTs from the sediments likely reflect soil pH, whereas using the Bligh and Dyer method the C-bGDGTs likely reflect terrestrial soil pH but the P-bGDGTs may reflect in situ sediment pH.
The MBT–CBT proxy has been increasingly used to reconstruct past annual MAT in continental margins or shelves (Weijers et al., 2007b,c; Schouten et al., 2008; Donders et al., 2009; Bendle et al., 2010; Fawcett et al., 2011; Peterse et al., 2011). While the annual MAT in the lower PR basin is about 22°C (Zhang et al., 2008), in July when our cruise was carried out, a mean monthly temperature of 30°C was recorded near the city of Guangzhou (Liu et al., 2007). The measured water temperature averaged 30.4 ± 0.4°C in the lower PR and 28.8 ± 2.2°C in the estuary with the bottom water about 2.0–4.0°C lower than the surface water (Table 1). Statistically, the water temperature was not significantly different between the lower PR and the estuary and the average was 29.8 ± 1.6°C between the two environments.
Temperatures calculated according to Weijers et al. (2007a) resulted in higher values for C-bGDGTs than P-bGDGTs for all samples (Tables A1– A3 in Appendix). In soil samples, the calculated temperatures had a range of 18.7–28.1°C (average 24.3 ± 3.1°C, n = 20) for C-bGDGTs and a range of −2.9 to 29.2°C (average 13.8 ± 1.1°C) for P-bGDGTs (Figure 8). For the sediment samples, the calculated temperatures had similar ranges for C-bGDGTs using either the sonication (Table A1 in Appendix) or Bligh and Dyer (Table A2 in Appendix) method, with the former having an average temperature of 21.1 ± 1.0°C and the latter 20.7 ± 1.1°C (Figure 8). The P-bGDGTs again resulted in lower values for either the sonication or Bligh and Dyer method, with the former showing considerably greater variability than the latter (Figure 8).
Figure 8. Comparisons of MBT–CBT-derived temperatures from the sonication (Soni) and Bligh and Dyer (BD) methods to measured annual mean air temperature and monthly mean air temperatures of the lower Pearl River drainage basin, and water column temperature in the lower Pearl River and estuary. CL, core lipids; PL, polar lipids.
The calculated temperatures from the C-bGDGTs were all closer to the mean annual air temperature (22°C) of the region than to the monthly MAT in July when the samples were taken (Figure 8). The bGDGTs from sediments did not seem to register any temperature signatures from the water column (average 29.8 ± 1.6°C; Figure 8), which suggests that water column production of bGDGTs in the lower PR and estuary did not have a significant impact on the sediment C-bGDGTs. These results also indicate that temperatures calculated from the C-bGDGTs were not affected by different extraction methods, whereas those from the P-bGDGTs could be severely affected. The relatively higher temperatures from the C-bGDGTs calculated for the soil may indicate a seasonal bias favoring the period of the summer when soil samples were collected. However, Weijers et al. (2011) showed no seasonal variation in MBT/CBT-derived temperatures in mid-latitude soils. On the other hand, even if a slight seasonal preference of bGDGT production does exists in soil, it may be difficult to separate from natural variability caused by soil heterogeneity (Weijers et al., 2011). The temporal variation in MBT/CBT temperatures in the lower PR requires further evaluation by sampling in different seasons before a conclusion can be drawn.
Increasing evidence indicates that bGDGTs can be produced in situ in aquatic environments other than the soil, which has traditionally been considered to be the major source of these compounds. In this study, two extraction methods (sonication and Bligh and Dyer) yield substantial amounts of P-bGDGTs in the water column and sediments, suggesting in situ production of bGDGTs in the lower Pearl River and estuary. The BIT values decrease systematically from the lower Pearl River to the estuary and the pattern is not influenced by the method of extraction. The bGDGTs-derived temperature and pH proxies also are not affected by extraction method when calculations are performed using the C-bGDGTs. In such cases, the pHCBT values in sediments are not statistically different from those of the surrounding soil, indicating that the C-bGDGTs are predominantly derived from the terrestrial environment. Similarly, temperatures calculated by the MBT–CBT combination show no difference between the two methods using the C-bGDGTs; the results of which are close to the mean annual air temperature of the lower PR basin. These results suggest that the MBT–CBT proxies derived from C-bGDGTs may be valid for studying paleo-soil pH and continental air temperatures in the lower Pearl River drainage basin. On the other hand, temperatures calculated from the P-bGDGTs are significantly lower than those from the C-bGDGTs and may not be reliable indicators of annual MATs.
Conflict of Interest Statement
The authors declare that the research was conducted in the absence of any commercial or financial relationships that could be construed as a potential conflict of interest.
We thank Dai L., Li Y., Zhong D., Hong Y., Wong C., and Shao L. for helping with the sampling and analysis of some of the samples collected for this study. Captain Deng was greatly appreciated for helping with the field experiments during the cruise. We would like to thank the two Francien Peterse and Ping’An Peng reviewers and Courtney Warren for constructive comments on an early version of this paper. This research was supported by the South China Sea-Deep program of the National Science Foundation of China (91028005) and the State Key Laboratory of Marine Geology of Tongji University.
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Keywords: Pearl River, estuary, bGDGTs, paleoclimate proxies
Citation: Zhang CL, Wang J, Wei Y, Zhu C, Huang L and Dong H (2012) Production of branched tetraether lipids in the lower Pearl River and estuary: effects of extraction methods and impact on bGDGT proxies. Front. Microbio. 2:274. doi: 10.3389/fmicb.2011.00274
Received: 08 August 2011;
Accepted: 22 December 2011;
Published online: 09 January 2012.
Edited by:Josh David Neufeld, University of Waterloo, Canada
Reviewed by:Francien Peterse, ETH Zurich, Switzerland
Ping’An Peng, Guangzhou Institute of Geochemistry, China
Copyright: © 2012 Zhang, Wang, Wei, Zhu, Huang and Dong. This is an open-access article distributed under the terms of the Creative Commons Attribution Non Commercial License, which permits non-commercial use, distribution, and reproduction in other forums, provided the original authors and source are credited.
*Correspondence: Chuanlun L. Zhang, State Key Laboratory of Marine Geology, Tongji University, Shanghai 200092, China. e-mail: email@example.com