Quantifying Transport of Particulate Inorganic
Carbon in the Madre de Dios River
Daniel Stirton
Department of Earth Sciences
University of Southern California
Abstract
Transport of particulate inorganic carbon in the Amazon River System is significant but not
widely studied. Here we analyze samples collected at two locations on the Madre de Dios River,
a tributary to the Amazon, and take measurements of total sediment load and PIC load over time.
By coupling with discharge measurements, we determine the fluxes of total sediment load and
POC and examine the importance of storm events. We also characterize the behavior of percent
particulate inorganic carbon of river sediments, a parameter that is not usually explored, but
which may be important for understanding chemical weathering processes and their role in the
carbon cycle.
1
1. Introduction
Transport of particulate carbon by mountain rivers is an important part the global carbon
cycle, but the mechanics of this transport have not been fully characterized. The majority of
studies on carbon transport in rivers focus on organic carbon, but much of the carbon transported
by rivers is inorganic (Earth Observatory, NASA), existing as carbonate minerals dissolved in
water or as carbonate mineral particles in river sediments. Whereas organic carbon is sourced
from plants, soils, and fossilized organisms, inorganic carbon is eroded from sedimentary rocks
and can act as a link between the “fast” biological carbon cycle and the “slow” geologic carbon cycle.
Mountain rivers efficiently transport carbon-laden sediments, eventually depositing them
in the ocean where carbon is fixed in limestone and other sedimentary rocks. These sedimentary
rocks act as an important carbon sink for thousands of millions of years before CO2 is returned to
the atmosphere in volcanic eruptions (Burdige, 2005). Because rivers carry particulate organic
and inorganic carbon from multiple different sources that play different roles in the global carbon
cycle, it is crucial to quantify the proportions of these different forms of carbon and understand
how they mix during transport.
When associated with clastic sediment particles coarser than 0.22 µm, this carbon is
referred to as particulate organic and inorganic carbon (POC and PIC, respectively). Particulate
inorganic carbon is often overlooked in scientific studies of river carbon transport. However, PIC
contributes to outgassing of CO2 from rivers when it undergoes a hydrolysis reaction, in which
solid calcium carbonate particles react with hydrogen ions to form calcium ion, water and CO2 in
the following two-step reaction (Thurman, 1985):
CaCO3 + 2H+ -> H2CO3 + Ca2+ -> H2O + CO2 + Ca2+
Unlike particulate organic carbon (POC), which can act as a sink of atmospheric CO2, PIC can
only act as a net source, because it is by definition being transported from a geologic carbon
sink.
The interface between the Andes mountain range and the Amazon River is especially
important in the study of the region’s carbonate geochemistry because of the high rates of
erosion and nutrient transport that occur on its steep gradients. This interface, called the Andes2
Amazon Transition, is both extremely biodiverse, with more than 226 species of mammals
(Upham et al., 2013), and extremely productive, with the region’s rivers acting as the largest
point sources of carbon to the world’s oceans (Medeiros et al., 2015). Overall, the study of this
region can provide valuable insights into the global biogeochemical cycles that sustain
ecosystems around the world.
In this study, I analyze carbon-containing suspended sediment from two locations along
the Madre de Dios River and construct time-series plots of PIC and total sediment concentrations
and fluxes to characterize the role of PIC in overall carbon transport by the Amazon River
System. I consider samples collected on timescales of hours as well as months and examine
changes in mass percent inorganic carbon of total river sediment load between the wet and dry
seasons. Using discharge measurements from Ballew (2011), I examine the relationship between
storm events and sediment transport to investigate the hypothesis that the vast majority of
sediment transport occurs during these events. These relationships allow me to draw conclusions
about the composition and behavior of inorganic carbon in the tributaries to the Amazon River,
an under-researched component of a critical avenue in the global carbon cycle.
2. Review of Literature
The transport of organic carbon in the Amazon river system gained attention in the mid1980’s when Hedges et al. (1986) tracked the relative content of different forms of carbon in
coarse (>63 µm) and fine (<63 µm) suspended particles over a 1,950-km reach of the lower
Amazon River. Their study focused on the mixing of modern POC from different types of
vascular plant tissue and tracked it by measuring % organic carbon, C/N, δ13C, and multiple
phenolic products derived from lignin, a class of organic polymers that forms plant cell walls. By
measuring these values for different Amazon plants and comparing them to values obtained from
suspended sediments, Hedges and his team found that the coarse organic material was composed
of 70-80% leaf tissue, 15-25% wood, and 0-10% C4 grasses by mass (Hedges et al., 1986). They
were not able to precisely define the origin of fine organic material due to low yields of ligninderived content, but did show that the finer material was older and more degraded. Overall, their
notable conclusions were that the composition of particulate organic material was nearly constant
3
over the studied length of the river and was best described as a mixture of vascular plant debris
and soil humic material.
More recently, riverine transport of organic carbon has been characterized at higher
elevation in order to better understand the source of carbon in suspended sediments derived from
Andean headwaters. Townsend-Small et al., (2008) sampled the sediment load of the
Chorobamba River, approximately 1800 m above sea level in the Peruvian Andes. This study
examined changes in carbon and nitrogen isotope ratios between the wet and dry seasons in
addition to comparing the relative amounts of coarse and fine POC that were transported.
Samples were collected weekly and at higher resolution during flood events and paired with
discharge measurements, and were decarbonated and analyzed with an isotope mass
spectrometer using methods that served as a model for our study. Isotopic analysis yielded δ13C
values that were much higher in the dry season than the wet season for both fine and coarse
sediments. By contrast, δ15N was constant over different seasons but varied with sediment grain
size. These differences suggested that wet season sediments originate in mineral soils, whereas
dry season sediments originate in surface soils. But Townsend-Small’s most significant observation was that 81% of the total transported sediment was observed during only five storm
events, suggesting that studies of suspended sediment transport must include high-resolution
sampling around these flood events (Townsend-Small et al., 2008). These results showed that
mountain tributaries feeding into the Amazon behave very differently from the low-elevation
tributaries.
Recent investigations of POC transport at the Andes-Amazon Transition have focused on the
effects of factors such as slope angle, particle size, river depth, and stage height on sediment
concentration and mixing of POC (Bouchez et al., 2014; Clark et al., 2014). Clark et al. (2014)
examined sources of POC and their mixing at high-elevation sampling sites on the Kosñipata
River in the Andes Mountains and collected samples during flood events, many of which were
also considered in this study. They used analysis of carbon and nitrogen isotopes of POC
sediments to determine the fractions of fossil and biospheric organic carbon. A linear
relationship between δ 13Corg and N/C showed a binary mixture between fossil and biospheric
carbon, so they were able to use a two-component mixing model and found that fossil POC
4
consistently contributed 80% of total POC, much higher than previous estimates, while input of
biospheric POC varied with time.
Bouchez et al., (2014) used similar methods to quantify fossil and biospheric POC mixing in
the Solimoes and Madeira Rivers, as well as the Amazon at Obidos, while also testing for age of
organic carbon and variations in POC composition across depth. They found much smaller
proportions of fossil POC in these rivers, ranging from 5-10% of total POC flux in all rivers
samples. However, none of these studies also considered the transport of particulate inorganic
carbon. But this year, Torres et al. (2016) examined the CO2 budget of the Madre de Dios River
by comparing rates of alkalinity-producing carbonate (and silicate) mineral dissolution versus
rates of acid-producing sulfide mineral oxidation. Torres found that lower in the Amazon,
samples showed high proportions of carbonate weathering, implying that CO2 is consumed at
these sites. At a higher-elevation site near the front of the Andes, higher proportions of sulfuric
acid weathering indicated that weathering occurring there does not result in changes in net CO2
fluxes. This paper showed the geochemical changes along elevation gradients and the importance
of inorganic carbon weathering.
3. Methods
3.1. Sample Collection
Suspended sediment samples were collected by Kathryn Clark at the same two stations
that were examined in Torres et al. (2016), one at the front of the Peruvian Andes and one in the
Foreland floodplain region (see Torres et al., 2015 for description of study sites). Mountain-Front
samples were collected at the Manu Learning Center (MLC), with a mean catchment elevation of
2,012 m and catchment area of 6,025 km2. Foreland floodplain samples were collected at the
CICRA research station, with a mean catchment elevation of 822 m and catchment area of
27,830 km2. By sampling from a higher-elevation site underlain by plutonic, sedimentary, and
metasedimentary rocks as well as a lower site underlain by marine sediments, we are able to
explore the behavior of suspended carbonate sediments across the Andes-Amazon Transition.
Samples were collected at approximately two-week time intervals from January 2010
through December 2011, spanning the wet seasons (January through early April) and dry seasons
(mid-April through December) of 2010 and 2011. Additionally, samples were collected at three5
hour time intervals over two weeks in the 2010 wet season during a period of frequent flood
events. Collection of samples during flood events ensured that a significant amount of sediment
transfer was occurring, and allowed us to observe changes in sediment composition over short
timescales. To obtain samples, a pole was used to reach the surface of the stream at its center,
and a measured volume of river water was filtered through 0.7-µm glass fiber filters, which were
then dried at ~40°C to obtain the suspended river sediment. Because the rough riverbed causes
turbulent flow and mixing at the MLC site, samples taken at the surface should reflect the
composition at depth at that site (Clark et al., 2013), but may reflect some bias at the foreland
site, where sediment may be more fractionated with depth.
Samples were chosen for gravimetric and hydrodynamic analysis to facilitate
investigation of sediment composition and transport over timescales of hours, days, and months.
Thus approximately half of the samples chosen for analysis were collected over a two-week
period in early February 2010 while half were collected at approximately one-month intervals
from March 2010 through November 2011. Location, stage height, date and time of collection,
and volume of water filtered were measured for each sample.
3.2. Decarbonation
In the lab, samples were washed off of their respective filters with DI water, dried
overnight at 50°C, and weighed. Inorganic carbon was then removed from the samples via
liquid-phase decarbonation, during which samples were immersed in a 5 M HCl leach for four
hours at 75°C. The samples were then rinsed with DI water three times, dried, and weighed again
in order to determine the difference between the decarbonated and non-decarbonated weight of
each sample. Decarbonated samples, composed of petrogenic and biospheric organic carbon and
silicate clasts, were homogenized with a mortar and pestle for future isotope analysis.
3.3. Gravimetric analysis
The pre-decarbonation sample masses were used to determine suspended sediment
concentrations (SSC, mg L-1) by dividing the sample mass by the volume of river water filtered
to obtain each sample. Suspended sediment concentration is used to characterize the Madre de
Dios River’s capacity for sediment transport. We multiplied SSC at each point in time by discharge (m3 sec-1, calculated by Ballew 2011) to obtain total sediment flux (g s-1), and
6
converted to kg s-1 . When observed in a time series, sediment flux can be integrated to find total
mass of material transported and to test the proposed hypothesis that the majority of sediment
transport by mountain rivers occurs during few scattered flood events.
Because liquid-phase decarbonation is meant to remove only inorganic carbon from a
sample, we were able to find the mass of inorganic carbon in each sample by subtracting the
post-decarbonation mass from the pre-decarbonation mass. Mass of inorganic carbon was
divided by volume filtered to obtain PIC concentration, which was observed at each station over
time. We also multiplied PIC concentration by discharge to obtain PIC flux (kg s-1).
Lastly, we divided the pre-decarbonation sample masses by the decarbonated masses to
find the percent particulate inorganic carbon in each sample. Quantifying the amount of PIC in
sediments can complement biospheric and petrogenic organic carbon ratios in characterizing the
composition of river particulate carbon.
4. Results
4.1. Suspended Sediment Concentration
Total suspended sediment concentration (SSC) showed high variability across timescales
of both days and months. At MLC during the period of high-resolution sampling from January
31st, 2010 to February 3rd, 2010, suspended sediment concentration ranged from 178 mg/L to
2,218 mg/L. The mean of the data was 735 mg/L (n = 20) with a standard error of 134 mg/L
(figure 1a). At CICRA, the period of high-resolution sampling from February 3rd, 2010 to
February 11th, 2010 yielded suspended sediment concentrations ranging from 134 mg/L to 1,740
a.)
mg/L. The mean of these data was 649 mg/L (n = 39) with standard error of 64 mg/L (figure 1b).
b.)
7
Figure 1: Suspended sediment concentration and river discharge a.) at MLC from
01/31/10 to 02/03/10, and b.) at CICRA from 02/03/10 to 02/12/10
The overall increase in SSC values at MLC marks the rising limb of a storm event in
which runoff from the area’s steep terrain results in an increase in river discharge and SSC. The decrease in the concentration values at CICRA corresponds to the falling limb of that storm
during which discharge and SSC return to normal. During storm events, SSC also shows wider
variation over time.
At MLC during the period of low-resolution sampling from January 31st, 2010 to May
6th, 2011, suspended sediment concentration ranged from 3 mg/L to 1,089 mg/L. The mean of
the data was 372 mg/L (n = 21) with a standard error of 81 mg/L (figure 2a). At CICRA, the
period of low-resolution sampling from January 29th, 2010 to December 27th, 2010 yielded
suspended sediment concentrations ranging from 51 mg/L to 1077 mg/L. The mean of these data
was 482 mg/L (n = 18) with a standard error of 81 mg/L (figure 2b).
a.)
b.)
8
Figure 2: Suspended sediment concentration a.) at MLC from
01/31/10 to 05/10/11, and b.) at CICRA from 01/29/10 to 12/31/10
The low SSC values occurring from April 2010 to December 2010 correspond to the area’s dry season, during which low runoff results in low discharge and SSC. Data from CICRA for this period
was not available, but would most likely show a similar trend.
5.2. Particulate Inorganic Carbon Concentration
PIC concentration over time behaved very similarly to total SSC. At MLC during the
period of high-resolution sampling from January 31st, 2010 to February 3rd, 2010, PIC
concentration ranged from 23 mg/L to 142 mg/L. The mean of the data was 68 mg/L (n = 20)
with a standard error of 9 mg/L (figure 3a). At CICRA, the period of high-resolution sampling
from February 3rd, 2010 to February 11th, 2010 yielded suspended sediment concentrations
ranging from 2 mg/L to 114.4 mg/L. The mean of these data was 55 mg/L (n = 37) with a
standard error of 5 mg/L (figure 3b).
a.)
b.)
Figure 3: Particulate inorganic carbon concentration and river discharge a.) at
MLC from 01/31/10 to 02/03/10, and b.) at CICRA from 02/03/10 to 02/12/10
At MLC during the period of low-resolution sampling from January 31st, 2010 to May
6th, 2011, PIC concentration ranged from 0.64 mg/L to 99 mg/L. The mean of the data was 34
mg/L (n = 21) with a standard error of 7 mg/L (figure 4a). At CICRA, the period of lowresolution sampling from January 29th, 2010 to December 27th, 2010 yielded suspended sediment
concentrations ranging from 5 mg/L to 88 mg/L. The mean of these data was 35 mg/L (n = 18)
with a standard error of 6 mg/L (figure 4b).
9
a.)
b.)
Figure 4: Particulate inorganic carbon concentration a.) at MLC from
01/31/10 to 05/10/11, and b.) at CICRA from 01/29/10 to 12/31/10
5.3. Mass Percent inorganic Carbon
The mass percent inorganic carbon of suspended sediments was generally higher at MLC
than at CICRA. At MLC during the period of high-resolution sampling from January 31st, 2010
to February 3rd, 2010, percent PIC of sediments ranged from 5.8% to 18.6%. The mean was
11.0% (n = 20) with a standard error of 0.6%. (figure 5a). At CICRA, percent PIC calculated for
samples taken during the high-resolution sampling period from February 3rd, 2010 to February
11th, 2010 ranged from 0.74% to 13.3%. The mean of these values was 8.0% (n = 37) with a
standard error of 0.4% (figure 5b).
10
a.)
b.)
Figure 5: Percent particulate organic carbon and river discharge a.) at MLC
from 01/31/10 to 02/03/10, and b.) at CICRA from 02/03/10 to 02/12/10
Unlike suspended sediment and PIC concentration, percent PIC shows opposite variation
with respect to discharge at MLC versus CICRA, increasing during the storm event at CICRA
and decreasing during the storm event at MLC. This discrepancy is explored further in the
discussion.
At MLC during the period of low-resolution sampling from January 31st, 2010 to May
6th, 2011, percent PIC ranged from 2.7% to 19.0%. The mean of the data was 10.4% (n=21) with
a standard error of 0.79% (figure 6a). The percent PIC of samples collected at CICRA during the
low-resolution sampling period from January 29th, 2010 to December 27th, 2010 were again
generally lower than the values at MLC, ranging from 2.1% to 9.9%. The mean value was 7.5%
(n = 18) with a standard error of 0.6% (figure 6b).
11
a.)
b.)
Figure 6: Percent particulate inorganic carbon a.) at MLC from 01/31/10 to
05/10/11, and b.) at CICRA from 01/29/10 to 12/31/10
Percent PIC in sediments collected at MLC shows an overall increase from April 2010
through September 2010, corresponding to the end of the wet season and the majority of the dry
season. This is in agreement with the observed decrease during flood events, suggesting that
discharge and percent PIC are inversely proportional. However, it is not clear why percent PIC
decreases during the last three months of the dry season.
5.4. Sediment Flux
Total sediment flux showed very different behaviors and ranges of values across the two
sampled locations and timescales. Computed for samples collected at MLC at high temporal
resolution, sediment flux ranged from 85 kg/sec to 1,278 kg/sec. The mean flux was 384 kg/sec
12
(n = 20) with a standard error of 81 kg/sec (figure 7a). Sediment flux computed for samples
collected at CICRA at high resolution ranged from 238 kg/sec to 4108 kg/sec. The mean of these
a.)
values was 1,382 kg/sec (n = 37) with a standard error of 159 kg/sec (figure 7b).
b.)
Figure 7: Total sediment flux a.) at MLC from 01/31/10 to
02/03/10, and b.) at CICRA from 02/03/10 to 02/12/10
Discharge values were not included on plots of sediment flux because flux is directly
proportional to discharge and sediment concentration. As the product of two values that sharply
increase during storm events, sediment flux will generally increase exponentially in storm
events.
During the period of low-resolution sampling, sediment flux for samples collected at
MLC ranged from 0.7 kg/sec to 673 kg/sec. The mean flux was 177 kg/sec (n=21) with a
standard error of 48 kg/sec (figure 8a). At CICRA, sediment flux ranged from 69 kg/sec to 2,567
kg/sec. The mean value was 854 kg/sec (n = 18) with a standard error of 173 kg/sec (figure 8b).
13
a.)
b.)
Figure 8: Total sediment flux a.) at MLC from 01/31/10 to 05/10/11, and b.) at
CICRA from 01/29/10 to 12/31/10
5.5. PIC Flux
Particulate inorganic carbon flux exhibited relatively consistent means and ranges within
sampling sites, and differed by a factor of approximately 3.5 between sites. Computed for
samples collected at MLC at high temporal resolution, sediment flux ranged from 10 kg/sec to 77
kg/sec. The mean flux was 35 kg/sec (n = 20) with a standard error of 5 kg/sec (figure 9a).
Sediment flux computed for samples collected at CICRA at high resolution ranged from 4 kg/sec
to 280 kg/sec. The mean of these values was 118 kg/sec (n = 37) with a standard error of 13
kg/sec (figure 9b).
14
a.)
b.)
Figure 9: Particulate inorganic carbon flux a.) at MLC from 01/31/10 to 02/03/10,
and b.) at CICRA from 02/03/10 to 02/12/10
During the period of low-resolution sampling, PIC flux for samples collected at MLC
ranged from 0.1 kg/sec to 59 kg/sec. The mean flux was 16 kg/sec (n=21) with a standard error
of 4 kg/sec (figure 10a). At CICRA, sediment flux ranged from 6 kg/sec to 209 kg/sec. The mean
value was 65 kg/sec (n = 18) with a standard error of 15 kg/sec (figure 10b).
a.)
15
b.)
Figure 10: Particulate inorganic carbon flux a.) at MLC from 01/31/10 to 05/10/11,
and b.) at CICRA from 01/29/10 to 12/31/10
6. Discussion
6.1. Trends in Sediment and PIC Concentration
Many of the time-series results were in agreement with previous research on sediment
transport in the Andes-Amazon region. Increases in river discharge were correlated with
increases in suspended sediment and PIC concentrations during short flooding events, which has
been demonstrated by Townsend-Small et al (2008) and Clark et al (2013). Average SSC at
MLC increased from 305 mg L-1 (n = 7, standard error 34 mg L-1) before the storm event to 1260
mg L-1 (n =9, standard error = 176) immediately after the peak, and average SSC at CICRA was
recorded during the falling limb of the storm as it decreased from 852 mg L-1 (n = 23, standard
error = 77 mg L-1) directly after the peak to 356 mg L-1 (n = 16, standard error = 53 mg L-1 )
three days later.
At both sites, discharge was approximately 1.5 times greater during storm events, but at
MLC, average SSC increased by a factor of 4.1 during the storm event, whereas at CICRA it
decreased by a factor of only 2.4 after the storm event. Though it is probable that dilution in SSC
after a storm event is more gradual than the SSC increase from sudden inputs, SSC measured
five days after the storm event had still only decreased by a factor of 2.5. A more probable
explanation is that the MLC catchment’s steeper slope angle (22° versus 9° at CICRA) and
16
sparser vegetation at high elevation make it extremely conducive to runoff, which is likely to
carry fossil organic carbon, inorganic carbon, and other clastic particles weathered from exposed
rock. Thus a storm event of similar magnitude would result in greater sediment input at MLC
than at CICRA. Additionally, average discharge is lower at MLC than at CICRA by a factor of
4.4 during the wet season, so the same mass of sediment input will have a much greater effect on
concentration.
6.2. Factors Affecting Percent PIC
Variations in mass percent inorganic carbon of suspended sediments at MLC and CICRA
showed the unusual behavior of PIC and the importance of storm events for its transport.
Because percent PIC is inversely proportional to total sediment load, it is often negatively
correlated with changes in discharge and total PIC concentration. Figure 11 shows changes in
percent PIC, PIC concentration, suspended sediment concentration, and discharge measured at
MLC. During the rising limb of the profiled storm event, percent PIC increases while PIC and
suspended sediment concentrations decrease due to dilution. Whereas PIC and suspended
sediments increase rapidly during the falling limb of the storm, percent PIC falls to 7.8%, well
below its average value.
17
Figure 11: Variations in percent PIC opposite of variation in PIC concentration
and suspended sediment concentration surrounding a storm event at MLC
As percent PIC of sediments decreases at MLC, it exhibits opposite behavior at CICRA,
increasing from 5.7% to 11.8% with the peak and falling limb of the storm event. Percent PIC
increases even as total suspended sediment concentration increases, meaning that large amounts
of PIC are being incorporated into the sediment load. Because the lowland floodplain at CICRA
lacks exposed sedimentary rocks, the additional PIC must have originated at higher elevation
near MLC. Thus PIC displays opposite behavior at CICRA and MLC because it is transported
downstream more quickly than it is weathered during storm events, resulting in a net decrease at
MLC and a net increase at CICRA.
Percent PIC also shows variation opposite of suspended sediment and PIC concentration
in samples collected during the dry season, from mid-April through December. Low-resolution
measurements from January 2010 through March 2011 at MLC show that percent PIC reaches
peak values in July and September, comprising 18% of total suspended sediment when measured
in July and 19% when measured in September. Monthly variations in PIC and total suspended
sediment at CICRA could not be analyzed due to a lack of data for March through August.
Although concentration of PIC is low during the dry season (MLC average = 14 mg/L), total
organic carbon concentration is also low enough that the proportion of PIC reaches its highest
values in the year. Sediment concentrations in these months are low but not negligible, and
particulate inorganic carbon can have significant contributions to carbon outgassing (England et
al., 2011).
7. Conclusion
The results of our high-resolution time-series measurements confirms the importance of
storm events for sediment and carbon transfer in the Amazon River system. We also explored
percent PIC as a useful characteristic of sediment load that provides a new perspective on its
behavior. Although we calculated PIC flux over the course of the year, we were unable to
reliably use this value to obtain total yearly PIC transport in kilograms because the yearly data
was not high-resolution enough.
For future studies, we would obtain more robust yearly data from both study sites, in
addition to supplementing PIC and total sediment masses with isotope data to find proportions of
18
fossil and biospheric POC in order to fully characterize the particulate carbon composition. Over
a time series, this could yield even more important insights about the river’s behavior.
Our aim is for this paper to motivate future studies of the region and its rivers to include
behavior and effects of PIC transport, as we have shown that the percent of PIC transported
during flood events throughout the year is significant and should not be discounted. Thus we can
move one step closer to fully understanding this important system in the global carbon cycle.
Acknowledgements
I would first like to thank Dr. Josh West for advising me on the direction, science, and
logistics this project, and for helping revise and edit drafts. I would also like to thank Dr.
Kathryn Clark for collecting the sediment samples in the field, and Joyce Yager and Ellie Hara
for assisting with the decarbonation process.
19
Data Tables
MLC, High Resolution
Date
Time
SSC
(mg/L)
1/31/2010
1/31/2010
1/31/2010
1/31/2010
2/1/2010
2/1/2010
2/1/2010
2/1/2010
2/1/2010
2/2/2010
2/3/2010
2/4/2010
2/5/2010
2/6/2010
2/7/2010
2/8/2010
2/9/2010
2/3/2010
2/3/2010
2/3/2010
9:00 AM
12:00 PM
6:00 PM
9:00 PM
3:00 AM
6:00 AM
12:00 PM
3:00 PM
9:00 AM
12:00 AM
3:00 AM
6:00 AM
9:00 AM
12:00 PM
3:00 PM
6:00 PM
9:00 PM
12:00 AM
3:00 AM
6:00 AM
530.4
323.4
206.9
257.9
311.9
250.4
498.8
282.2
221.4
288.3
178
2217.7
1588.5
918.8
1538.1
1177.7
634.7
553.4
1152.9
1561.7
PIC
concentration
(mg/L)
56.13
40.43
38.55
34.52
37.93
36.94
58.85
28.19
24.28
33.21
23.48
128.08
121.35
91.67
142.11
108.76
58.49
64.98
108.75
121.77
% PIC
10.58
12.5
18.63
13.38
12.16
14.75
11.8
9.99
10.97
11.52
13.19
5.78
7.64
9.98
9.24
9.23
9.22
11.74
9.43
7.8
Discharge Sediment
(m^3/sec) flux
(kg/s)
433.7
230
422.2
136.5
410.8
85
399.3
103
387.8
120.9
377.6
94.54
367.4
183.3
357.2
100.8
410.8
90.9
464.3
133.9
520.4
92.6
576.5
1,278.50
632.6
1,004.90
515.3
473.4
476.2
732.4
515.3
606.9
533.2
338.4
551
304.9
568.9
655.8
586.7
916.2
PIC flux
(kg/s)
24.34
17.07
15.83
13.78
14.71
13.95
21.62
10.07
9.97
15.42
12.22
73.84
76.77
47.24
67.67
56.04
31.18
35.81
61.86
71.44
MLC, Low Resolution
Date
SSC (mg/L)
1/31/2010
329.7
2/1/2010
312.9
2/2/2010
1067.7
2/3/2010
1089.3
2/10/2010
161.5
3/15/2010
441.4
3/29/2010
614.4
4/26/2010
24.8
5/17/2010
29.6
5/24/2010
7.6
7/26/2010
22.8
PIC
concentration
(mg/L)
% PIC
42.41
37.24
88.39
98.5
11.83
41.07
0.8
2.878
57.78
1
4.1
13.78
11.93
9.47
9.66
7.33
9.3
9.4
11.59
2.7
13.2
17.99
Discharge
Sediment
PIC flux
(m^3/sec)
flux (kg/s)
(kg/s)
409.9
135.1
17.38
378.4
118.4
14.09
630.7
673.4
55.75
594.7
647.8
58.57
405.5
65.5
4.8
315.4
139.2
12.95
333.4
204.8
0.27
283.8
7
0.82
234.3
6.9
13.54
234.3
1.8
0.23
252.3
5.8
1.04
20
7/30/2010
7/31/2010
9/13/2010
11/15/2010
12/13/2010
1/24/2011
2/7/2011
3/7/2011
4/4/2011
5/3/2011
50.9
22.2
3.4
371.4
336.2
947.8
542.8
310.4
995
129.4
CICRA, High Resolution
Date
Time
SSC
(mg/L)
2/3/2010
2/3/2010
2/4/2010
2/4/2010
2/4/2010
2/4/2010
2/4/2010
2/4/2010
2/4/2010
2/4/2010
2/5/2010
2/5/2010
2/5/2010
2/5/2010
2/5/2010
2/5/2010
2/5/2010
2/6/2010
2/6/2010
2/6/2010
2/6/2010
2/6/2010
2/6/2010
2/9/2010
2/9/2010
2/10/2010
2/10/2010
6:00 PM
9:00 PM
12:00 AM
3:00 AM
6:00 AM
9:00 AM
12:00 PM
3:00 PM
6:00 PM
9:00 PM
12:00 AM
3:00 AM
6:00 AM
12:00 PM
3:00 PM
6:00 PM
9:00 PM
12:00 AM
3:00 AM
6:00 AM
9:00 AM
12:00 PM
3:00 PM
3:00 PM
6:00 PM
12:00 AM
3:00 AM
998.4
541.2
1448.4
1740
1096.8
518.8
1394
1131.6
544.4
740
935.6
928.4
388
972.8
1076.4
622.8
540.8
770.4
375.2
507.6
459.6
660.4
1206.8
348.4
174.8
270
295.2
4.51
2.26
0.64
39.6
25.6
62.2
52.4
38
87.4
12.2
PIC
concentration
(mg/L)
57.2
38
101.2
113.6
88.4
54.8
114.4
88.4
57.6
83.2
94.4
81.6
51.6
94
88.8
60.4
50
70
44.4
50.4
41.2
50.8
87.6
7.2
n.d
2
7.2
8.87
252.3
10.15
252.3
19.05
207.2
10.66
243.3
7.61
288.3
6.56
522.6
9.65
540.6
12.24
1,171.30
8.78 n.d.
9.43 n.d.
-
% PIC
5.73
7.02
6.99
6.53
8.06
10.56
8.21
7.81
10.58
11.24
10.09
8.79
13.3
9.66
8.25
9.7
9.25
9.09
11.83
9.93
8.96
7.69
7.26
2.07
0.74
2.44
12.8
5.6
0.7
90.4
96.9
495.3
293.4
363.6
Discharge Sediment
(m^3/sec) flux
(kg/s)
2277.8
2274.2
2305.6
1247.8
2333.4
3379.6
2361.1
4108.4
2388.9
2620.2
2416.7
1253.8
2444.5
3407.6
2410.2
2727.3
2375.8
1293.4
2341.5
1732.7
2307.2
2158.6
2272.9
2110.2
2238.6
868.6
2204.3
2144.3
2169.9
2335.7
2135.6
1330.1
2101.3
1136.4
2067
1592.4
2032.7
762.7
1998.4
1014.4
1964
902.7
1929.7
1274.4
1895.4
2287.4
1861.1
648.4
1826.4
319.3
1791.7
483.7
1781.7
526
1.14
0.57
0.13
9.63
7.38
32.5
28.33
44.51
-
PIC flux
(kg/s)
130.29
87.61
236.14
268.23
211.18
132.44
279.65
213.06
136.85
194.82
217.8
185.47
115.51
207.2
192.69
128.99
105.07
144.69
90.25
100.72
80.92
98.03
166.04
13.4
3.58
12.83
21
2/10/2010
2/10/2010
2/10/2010
2/10/2010
2/10/2010
2/11/2010
2/11/2010
2/11/2010
2/11/2010
2/11/2010
2/11/2010
2/11/2010
6:00 AM
9:00 AM
12:00 PM
3:00 PM
6:00 PM
12:00 AM
3:00 AM
6:00 AM
9:00 AM
12:00 PM
3:00 PM
6:00 PM
134.4
186.8
492.8
433.2
957.6
531.6
544.8
237.6
150.4
331.6
431.6
180.4
n.d
5.6
27.6
36.4
80
49.2
42.4
22.8
12.4
22.4
33.6
16.4
CICRA, Low Resolution
Date
SSC
PIC
(mg/L)
concentration
(mg/L)
1/29/2010
299.6
22
1/31/2010
282.7
22.53
2/1/2010
184.8
13.6
2/3/2010
769.8
47.6
2/4/2010
1076.8
87.7
2/5/2010
780.7
74.4
2/6/2010
663.3
57.4
2/9/2010
348.4
7.2
2/10/2010
395.7
22.23
2/11/2010
344
28.46
9/21/2010
136.1
11.23
9/27/2010
1038.9
34.38
10/19/2010 98.1
9.41
11/8/2010
50.9
4.71
11/22/2010 600.5
52.38
12/27/2010 635
59
3
5.6
8.4
8.35
9.26
7.78
9.6
8.24
6.76
7.78
9.09
1771.8
1761.9
1752
1742
1732.1
1722.2
1717.6
1712.9
1708.3
1703.7
1699
1694.4
238.1
329.1
863.4
754.7
1658.7
915.5
935.7
407
256.9
564.9
733.3
305.7
9.87
48.35
63.41
138.57
84.73
72.82
39.05
21.18
38.16
57.09
27.79
% PIC
Discharge
(m^3/sec)
Sediment
flux (kg/s)
PIC flux
(kg/s)
7.62
7.99
7.36
6.38
8.75
9.86
9.13
2.07
3.74
8.36
8.18
3.31
9.59
9.27
8.72
9.29
2000
1,944.40
1,916.70
2291.7
2384
2204.3
1981.2
1843.7
1761.9
1708.3
606
606
848.4
1,363.50
1,560.50
1,666.50
599.2
549.6
354.2
1764.1
2567
1720.8
1314.2
642.4
697.2
587.7
82.48
629.6
83.2
69.4
937
1058.2
44
43.81
26.07
109.08
209.08
164
113.72
13.27
39.16
48.61
6.81
20.84
7.99
6.43
81.74
98.32
22
References
Ballew, Natalie. "Quantifying Discharge in the Kosñipata-Madre De Dios River System, Peru."
(2011): n. pag. Web.
Bouchez, Julien, Valier Galy, Robert G. Hilton, Jérôme Gaillardet, Patricia Moreira-Turcq,
Marcela Andrea Pérez, Christian France-Lanord, and Laurence Maurice. "Source,
Transport and Fluxes of Amazon River Particulate Organic Carbon: Insights from River
Sediment Depth-profiles." Geochimica Et Cosmochimica Acta 133 (2014): 280-98. Web.
Burdige, David J. “Burial of Terrestrial Organic Matter in Marine Sediments: A ReAssessment.”Global Biogeochemical Cycles 19.4 (2005): n/a–n/a. Web.
Riebeek, Holli. The carbon cycle: Feature articles. NASA Earth Observatory, 16 June 2011.
Web.
Clark, K. E., R. G. Hilton, A. J. West, Y. Malhi, D. R. Gröcke, C. L. Bryant, P. L. Ascough, A.
Robles Caceres, and M. New. "New Views on “old” Carbon in the Amazon River: Insight from the Source of Organic Carbon Eroded from the Peruvian
Andes." Geochemistry, Geophysics, Geosystems Geochem. Geophys. Geosyst. 14.5 (2013):
1644-659. Web.
Hedges, John I., Wayne A. Clark, Paul D. Quay, Jeffrey E. Richey, Allan H. Devol, and
Umberto De M. Santos. "Compositions and Fluxes of Particulate Organic Material in the
Amazon River." Limnol. Oceangr. Limnology and Oceanography31.4 (1986): 717-38.
Web.
Medeiros, Patricia M., Michael Seidel, Nicholas D. Ward, Edward J. Carpenter, Helga R.
Gomes, Jutta Niggemann, Alex V. Krusche, Jeffrey E. Richey, Patricia L. Yager, and
Thorsten Dittmar. "Fate of the Amazon River Dissolved Organic Matter in the Tropical
Atlantic Ocean." Global Biogeochem. Cycles Global Biogeochemical Cycles 29.5
(2015): 677-90. Web.
Thurman, E. M. Organic Geochemistry of Natural Waters. Dordrecht: M. Nijhoff, 1985. Print.
Torres, Mark A., A. Joshua West, Kathryn E. Clark, Guillame Paris, Julian Bouchez, Camilo
Ponton, and Sarah J. Feakins. "The Acid and Alkalinity Budgets of Weathering in the
Andes–Amazon 78 System: Insights into the Erosional Control of Global
23
Biogeochemical Cycles?" Earth and Planetary Science Letters (2016): n. pag. Web.
Townsend-Small, Amy, Michael E. Mcclain, Bonnie Hall, Jorge L. Noguera, Carlos A. Llerena,
and Jay A. Brandes. "Suspended Sediments and Organic Matter in Mountain Headwaters
of the Amazon River: Results from a 1-year Time Series Study in the Central Peruvian
Andes." Geochimica Et Cosmochimica Acta 72.3 (2008): 732-40. Web.
Upham, Nathan S., Reed Ojala-Barbour, Jorge Brito M, Paúl M. Velazco, and Bruce D.
Patterson. "Transitions between Andean and Amazonian Centers of Endemism in the
Radiation of Some Arboreal Rodents." BMC Evol Biol BMC Evolutionary Biology 13.1
(2013): 191. Web.
24