Correction: Carbon dioxide dynamics in a lake and a reservoir on a tropical island (Bali, Indonesia)

[This corrects the article DOI: 10.1371/journal.pone.0198678.].


Introduction
Lakes and reservoirs cover 2.2% of the global surface area [1]. Although relatively small in aerial extent, lakes play a significant and increasingly important role in the global carbon cycle [2,3]. Estimates of the global net CO 2 flux for lakes and reservoirs is~0.3 Pg C yr -1 (range 0.06 to 0.84 Pg C yr -1 ) but there are uncertainties in the number and area of small lakes [1]. With climate change, it is likely that there will be a global changes in lake abundance. It is predicted that there will be losses of natural lakes in regions where the climate is becoming drier [4] and increases in reservoir construction [5] in regions with rapidly expanding populations such as Southeast Asia [4] a1111111111 a1111111111 a1111111111 a1111111111 a1111111111 Lakes and reservoirs modify freshwater flows of inland waters and alter CO 2 fluxes by retaining~50% of the global carbon transported to the oceans [4]. Estimates of global reservoir numbers have varied significantly from 25, 410 to 515,149 [6,7], the latter study including smaller reservoirs. In spite of this variability, reservoirs are important compared to natural lakes (n = 304 million) with an estimated 277 million small lakes (0.001-0.01 km 2 ) [7]. Millions of smaller reservoirs (<0.5 km 2 ; [8]) are not accounted for in global carbon budgets, and reservoir construction is increasing [8] resulting in more terrestrial carbon entering and becoming trapped in lakes and reservoirs, and changes in landscape CO 2 emissions [9]. These shifts in CO 2 emissions are further compounded by predicted increases in extreme weather events such as flood and droughts [10] as well as watershed degradation and weathering [11,12].
Global assessments of CO 2 fluxes from lakes and reservoirs are not evenly distributed with temperate and boreal zones such as Europe and Northern America largely over-represented [13]. Tropical systems [14] and the southern hemisphere [15] are under-represented. Tropical systems comprise~40% of the global surface area of reservoirs. However,~70% of CO 2 fluxes from reservoirs are thought to originate in tropical regions [6]. As a result, tropical reservoirs are recognised as disproportionally large sources of CO 2 to the atmosphere [6,16]. Compared to temperate lakes, higher water temperatures in tropical regions result in higher organic matter decomposition rates, resulting in higher CO 2 production and emissions than their temperate counterparts [4,6]. CO 2 dynamics in both lakes and reservoirs are often driven by a combination of internal processes such as photosynthesis and respiration, as well as allochthonous inputs [17]. Allochthonous sources of CO 2 include weathering, soil organic matter and terrestrial root respiration [18,19] and precipitation of carbonate or silicate minerals [20]. Surface water runoff [21,22] and groundwater discharge [19,[23][24][25] can directly deliver terrestrial organic matter to aquatic systems, which is subsequently stored in lake sediments, exported downstream, remineralised or released to the atmosphere [4]. Since groundwater is often highly supersaturated in CO 2 when compared to surface waters and the atmosphere [26], several recent studies identified groundwater seepage as a major conduit of CO 2 to lakes [27][28][29].
Here, we contribute to filling knowledge gaps of inland water CO 2 dynamics in tropical regions, where there are fewer data on CO 2 outgassing rates and factors controlling this efflux than the more comprehensively studied temperate regions. We measured pCO 2 and estimate fluxes at the water-air interface along with potential drivers in a natural lake and a reservoir in Bali, Indonesia, one of the world's fastest growing tourist economies. Although Indonesia has been identified as having a high potential for groundwater recharge [30], comprehensive studies including groundwater-derived CO 2 seepage in Indonesian lakes have not been conducted to date. We hypothesize that groundwater seepage may release CO 2 to surface waters and that CO 2 concentrations will be higher in the wet season due to a relative increase in groundwater flow. Seasonal surveys of radon (a natural groundwater discharge tracer) and CO 2 are used to test this hypothesis.
quaternary Palasari Formation which includes Palasari conglomerate, sandstone, calcareous sandstone and limestone reef. The topography is low-lying hills with regional soils dominated by Brown Latisol (http://ppsp.nawasis.info/) which are highly permeable with vegetation cover. Without vegetation cover the soil is vulnerable to erosion and rapidly becomes impermeable. The Palasari Reservoir has a large watershed area-lake area ratio (~420:1) with surrounding land use dominated by small scale agriculture. Upstream of the reservoir is protected forest with a short (<5 km) topographic transition from hilly to mountainous terrain. The reservoir is a 27 year old, rock fill type dam with a central clay land fill core of 40 m. It functions as flood control and supplies irrigation water for~13 km 2 of rice fields downstream. Although there may be receiving inflow from the Sangiang Gode and Palareja Rivers, during the sampling period there was no notable surface water inflow into and out of the system (Table 1).

Approach and methods
We performed 4 seasonal surveys in Lake Batur and Palasari Reservoir using automated instrumentation (Fig 2). Instrumentation was installed on a small research vessel driven at 4-6 km/h to produce high spatial resolution sampling. The vessel was stopped or slowed down at sites of high interest such as areas where the landscape was modified, near stream inlets, around visible changes in nearshore vegetation, and large transitions in water depth. Location was logged continuously by a Garmin GPS72 or Maverick Pro 2.61 Android GPS.
Water column pCO 2 and 222 Rn concentrations were measured from a depth of~1 meter using a portable Li-820 CO 2 detector (calibrated with 0, 400 and 10 000 ppm standards) and a radon-in-air monitor calibrated prior to deployment by the manufacturer (RAD7, Durridge; Fig 2). The detectors were connected with a closed-air-loop and an equilibrator spray chamber [26,32] with the air stream dried with a desiccant column of Drierite. Water was continually pumped from a submersible bilge pump at about 3 L/min -1 into a shower head gas equilibration device (GED). A closed-air-loop was created between the GED and gas detectors which measure the gas concentrations in the air stream. Air was pumped into the RAD7 radon detector at 1 L min -1 by the RAD7 internal pump. The dissolved gas concentrations were determined by the gas solubility and temperature [33,34]. Measurements of temperature, conductivity and dissolved oxygen were undertaken using a Hydrolab DS-5 multiparameter water quality sonde, calibrated prior to each deployment at 1 min intervals to measure pH (± 0.02 units), salinity (± 0.02 ppt), dissolved oxygen (± 0.2 mg L-1), and water temperature (± 0.10˚C). pH was calibrated with 4, 7 and 10 buffer solutions (NBS scale) while conductivity was calibrated with deionised water and a 1413 μS cm -1 standard. Chlorophyll a was measured at 1 minute intervals with a WETlabs Eco triplet fluorometer equipped with a copper brush wiper to prevent biofouling of sensors and calibrated by the manufacturer using quinine dehydrate. Meteorogical data was sourced from Denpasar Ngurah Rai Weather Station 972300 (S08.749; E115.167).
The CO 2 flux across the water-air interface was calculated according to Wanninkhof (1992) [35]: where k is the CO 2 gas transfer velocity, K H is the solubility of CO 2 [33] and ΔpCO 2 is the difference between the partial pressure of pCO 2 in water and air. To calculate k, we used the average of six parameterizations to provide a reasonable range in evasion rate estimates ( Table 2). Positive values represent a water-to-air CO 2 flux and negative values represent an air-to-water flux. Water-to-air CO 2 fluxes were calculated by using five minute sampling times for pCO 2 and average annual windspeeds to reduce wind bias for the natural lake and reservoir, respectively. Integrated aereal CO 2 fluxes were calculated using the Spline-with-Barriers method [36] to prevent bias related to different research vessel speeds and time spent stationary. Permits and permissions for Palasari Reservoir and Lake Batur were provided by the Indonesian Foreign Research Permit Secretariat, Ministry of Research, Technology and Higher Education of the Republic of Indonesia (RISTEKDIKTI), the Directorate General of Water Resources, the Indonesian Ministry of Public Works (DGWRD) and the Governor of Bali, I Made Mangku Pastika. Field studies did not involve endangered or protected species.

Results
Both study sites experienced an extended drought period during the 2015 dry season (Fig 3) with no rainfall recorded 3 months prior to initial sampling in November 2015. In contrast the 2016 dry season (May-September) recorded significantly more rainfall than historical averages. This created a sampling period with initial dry conditions transitioning to wetter conditions in both systems.
The natural lake recorded lower average temperatures (25.8˚C) than the reservoir (31.9˚C) ( Table 3) while both ranges were similar, suggesting both have surface water temperature driven by differences in elevation (Table 1). Average annual conductivity in the natural lake was~7-fold higher (1991.4 μS/cm) than in the reservoir (290.6 μS/cm) increasing towards dry creek bed tributaries in the reservoir only (Figs 4 and 5) while dissolved oxygen was generally supersaturated in both systems. 222 Rn was 0.4 dpm/L -1 in the natural lake (Fig 4) and significantly higher in the reservoir during the drought period when it ranged from 0.6 dpm/L -1 to 18.1 dpm/L -1 (mean = 4.8 dpm/L -1 ). 222 Rn decreased seasonally with increasing rainfall in the dry, wet transition and wet periods (Figs 5 and 6; Table 3). CO 2 was undersaturated in the natural lake with the exception of a wet period (June, 2016) where~20% of locations were supersaturated, reaching 451 μatm (Fig 4). The reservoir remained supersaturated in CO 2 throughout the year (Fig 5). The highest reservoir CO 2 ranges of 432 to 7647 μatm occurred in the drought period and were~24-fold higher than that of the natural lake range (159-456 μatm) ( Table 3). CO 2 followed the same spatial trend as 222 Rn concentrations increasing towards the reservoir dry creek bed tributaries although no flowing streams were visible (Fig 5A). Table 2. Six wind-speed based parameterization formulas with respective authors, where k is the transfer velocity (cm h −1 ), u is the wind speed (ms −1 ) at a height of 10 m and Sc is the Schmidt number of CO 2 at in situ temperature and salinity.

Contrasting CO 2 dynamics in the natural lake and reservoir
We have assessed seasonal CO 2 dynamics on a natural and artificial lake in a tropical volcanic island, building on earlier work that focused mostly on boreal and temperate regions [37]. Volcanic caldera lakes such as Lake Batur typically have high groundwater recharge rates due to fracture-induced permeability [38], and small overall surface-groundwater interactions [39]. In contrast, artificial shallow lakes such as Palasari Reservoir typically have more pronounced terrestrial sources that may stimulate productivity [40]. This is highlighted in the reservoir's elevated ranges of surface water pCO 2 with spatially variable measurements of surface water conductivity, dissolved oxygen and chlorophyll a (Figs 5 and 8; Table 3). This reflects seasonal rainfall influences with larger catchment sizes and watershed-to-reservoir ratios, when compared to the smaller catchments found in caldera lakes [41]. This is strongly shown in the differences in CO 2 concentrations within the natural lake and reservoir during the sampling period (Figs 4 and 5; Table 3). Although higher pCO 2 values were measured in the shallow (< 2m) near-shore zones in the reservoir, this did not result in large emissions when taking into account area weighted pCO 2 measurements (Fig 7).
For large and small systems such as Lake Batur and Palasari Reservoir, respectively, differences in CO 2 may be influenced by depth (due to the volume-to-sediment surface ratios), catchment area and lake area ratios (2:1 and 420:1 respectively; Table 1). These ratios exert strong influences over delivery of terrestrial organic matter and water chemistry [42]. For example, a study of 82 boreal lakes (areas = 0.04-1540 km2; max depth = 1-93 m) in Finland found that lake area and depth are important predictors of CO 2 evasion with higher emissions found in small, shallow lakes [43] In addition, nutrient delivery results from variations of surface water inflow dependent on regional rainfall regimes and geographic location. These traits Table 3 are reflected in the lower average pCO 2 concentrations in the large, deep natural lake when compared to the small, shallow reservoir. Correlations between CO 2 and conductivity, dissolved oxygen and chlorophyll a were similar in the deeper reservoir and in the natural lake (Figs 8 and 9). The strongest reservoir pCO 2 correlations with conductivity, DO and chlorophyll a were in the drought period (r 2 = 0.77; p<0.0001), wet period (r 2 = 0.64; p<0.0001) and wet transition period (r 2 = 0.34; p<0.001) respectively. However, the reservoir near-shore zone had more linear correlations typical of other lotic systems [44] but represented a minimal spatial area (see Fig 5A and Fig 8). In the natural lake, chlorophyll a accounted for 34% and 32% of the CO 2 variability in the dry and wet period, respectively (Fig 9H and 9P). However, this relationship reversed from the drought to wet period. This reflected similarities with the reservoir which also showed a positive correlation between CO 2 and chlorophyll a (r 2 = 0.34) in the wet transition period (Fig 8L).

Lake Batur
Several previous studies have used 222 Rn as a tracer in inland waters [28,44,45]. By simultaneously measuring the groundwater tracer 222 Rn and pCO 2 , we found similarities to previous estuarine studies where radon followed CO 2 distributions [46,47] (Figs 5 and 8). Groundwater inputs were apparently negligible in the natural lake (average 222 Rn 0.06 dpm/L -1 ; Table 3) and was not considered as a significant driver of CO 2 dynamics. In the reservoir, 222 Rn decreased from the drought to wet periods. (Figs 5 and 8). Decreased wet period groundwater flow may Carbon dioxide in tropical inland waters be due to high surfacewater inputs with pCO 2 dynamics linked to this surfacewater loading [48]. Overall, our observations imply a stronger groundwater influence in the reservoir than in the natural lake.

Rainfall as a driver of CO 2 in tropical and temperate systems
Short, intense rainfall events, which are common in Bali's wet season, have recently been acknowledged as important pathways of terrestrial carbon loading to in inland waters [44,48]. Artificial reservoirs and natural lakes receive CO 2 produced and derived from their catchment areas as a result of rainfall events when large amounts of carbon are rapidly transported to these waterbodies [49]. Many studies have reported correlations between atmospheric CO 2 fluxes and rainfall events [29,50] with significant amounts of terrestrial CO 2 delivery to lake waters during these events [1].
In spite of the small sample size, we found a correlation between CO 2 and antecedent rainfall in the reservoir and lake (Fig 10). Rainfall events have previously been reported to deliver large amounts of particulate and dissolved organic carbon into aquatic systems [51,52]. Higher seepage of CO 2 enriched groundwaters in the wet transition and wet sampling periods implies that wetter conditions lead to higher groundwater input due to a larger hydraulic head. In small lakes in northern Europe, CO 2 increased in the soil and lake following a significant rainfall event (61 mm). Terrestrial flushing was reflected in the high surface water CO 2 concentrations, with pCO 2 increasing from 1800 to 4370 μatm soon after the rain event [27].
In the reservoir, the effects of rainfall are emphasised by the decoupling of pCO 2 and 222 Rn which was elevated near a stream in the northern area (Fig 5). Tropical reservoir studies have reported rainfall events which load high amounts of terrestrial CO 2 into receiving waters [27,29,49] by increased river discharge [53] and carbon rich terrestrial inputs as a result of soil erosion [51]. Tropical regions in particular are prone to high CO 2 terrestrial loading as a result of episodic heavy rainfall events, pronounced wet seasons and high surface water temperatures. The low lying topography and plantations in the northern area of the reservoir may support more groundwater interactions (Fig 5A and Table 1). This is reflected in Fig 5 and  A recent study showed that water-to-air CO 2 fluxes in Brazilian lakes were significantly enhanced in heavy rainfall events, recording 28.5 ± 6.0 mmol CO 2 m −2 d −1 in dry periods and 245.3.1 ± 51.5 mmol CO 2 m −2 d −1 shortly after the heavy rainfall event. The increased inputs of CO 2 following periods of high rainfall were believed to be derived from increased inputs of CO 2 from groundwater to the lakes, resulting in an~10-fold increase in lake pCO 2 [29]. Similarly, the natural lake from Bali sequestered atmospheric CO 2 throughout each sampling campaign but pCO 2 increased and approached atmospheric equilibrium in the wet period as a result of heavy rainfall events (Figs 10 and 11). The depth of the natural lake (mean = 50.8; max = 88 m; Table 1) may dilute elevations in pCO 2 as a result of terrestrial carbon inputs or groundwater inputs. Most previous lake investigations are from shallower systems [4,37]. There is a paucity of data on CO 2 dynamics from such water bodies as the dominant caldera lakes in tropical volcanic regions such as Indonesia. Therefore, our observations may help to fill a gap in global CO 2 observations in lakes.

Implications
Due to uneven spatial and temporal distribution of rainfall and river flow, reservoir construction is becoming increasingly important in regions of fast population growth such as Southeast Asia. We speculate that the accelerated construction of reservoirs [54,55] and population growth [55] will increase the contribution of Southeast Asia inland waters to the global carbon budget. In Bali, the current reservoir capacity has a ratio of storage per capita of only 63.5 m 3 which is inadequate to cope with the increasing water demand (Direktorat Jenderal Sumber Daya Air: http://sda.pu.go.id/). Bali's local population of 4,200,000 in 2012 had a water demand of 229,950,000 m 3 yr -1. This does not take into account irrigation water for rice, agriculture, industry and tourism growing 20% between 2015 and 2016. Assuming future reservoir construction will supply water demand, reservoirs may become a more significant regional CO 2 source that will need to be managed effectively. In 2015, Indonesia had 6 reservoirs under Table 4. Instantaneous windspeed and CO 2 fluxes of the 4 different transfer velocity parameterizations (see Table 2) for the natural lake (Lake Batur) and the reservoir (Palasari Reservoir) throughout the sampling period. Area weighted CO 2 fluxes for Lake Batur (left) and Palasari Reservoir (right) and interpolated GPS point data using the Arcmap GIS spline with barriers interpolation method. Carbon dioxide in tropical inland waters https://doi.org/10.1371/journal.pone.0198678.g008 construction, 6 in negotiation stages and 7 in design stages, not taking into account current small reservoir construction (www.narbo.jp/). Lakes and reservoirs in tropical regions, as a result of stable temperature and light, have been recently reported to have lower seasonal variations of biological activity when compared to boreal and temperate counterparts [56]. For example low variations of seasonal CO 2 concentrations in a tropical lake (Lake Kivu, East Africa) were linked to tropical climate and partly associated with minimal water temperature variations [56]. Predicted increases in both tropical monsoonal temperatures and reservoir construction may increase the inland water contribution to the global carbon budget.

Lake Batur
Tropical lakes and reservoirs are under-represented and comprise only 1.5% of the global dataset (n = 7939) of CO 2 emissions (Raymond et al., 2013). While tropical lakes may be responsible for 34% of the global atmospheric CO 2 fluxes from inland waters, they cover only 2.4% of the global lake area [1]. Lake ranges and averages of pCO 2 were found to be amongst the highest in tropical regions. Rainfall and temperature appeared to be a strong controls over pCO 2 in our study. The predicted temperature increase would increase bacterial metabolism resulting in more organic carbon respiration. Due to poor representation in global datasets, constraining CO 2 fluxes in tropical lakes and reservoirs is particularly important [4].  Carbon dioxide in tropical inland waters

Conclusions
Our observations in Bali revealed that antecedent rainfall seems to be a major control on seasonal CO 2 distributions in both the lake and reservoir. The spatial distribution of pCO 2 was driven primarily by autochthonous processes (water column metabolism) in the deep lake, and allochthonous processes (groundwater seepage) in the shallow reservoir. Overall, the natural lake was an atmospheric CO 2 sink, while the reservoir was releasing CO 2 to the atmosphere. We speculate that the predicted increase in reservoir area in tropical regions may increase CO 2 fluxes to the atmosphere and partially offset the sink provided by deep, volcanic, natural lakes. Site specific carbon investigations are needed to monitor inland waters on a regional scale. Due to the rapid expansion of reservoir construction, particularly in tropical regions, it may be necessary to develop long term monitoring programs that capture reservoir evolution and infilling process as well as large scale comparative studies already available for better studied northern hemisphere lakes.