First Measurements of Gas Flux with a Low-Cost Smartphone Sensor-Based UV Camera on the Volcanoes of Northern Chile

: UV cameras have been used for over a decade in order to remotely sense SO 2 emission rates from active volcanoes, and to thereby enhance our understanding of processes related to active and passive degassing. Whilst SO 2 column density retrievals can be more accurate / sophisticated using alternative techniques (e.g., Di ﬀ erential Optical Absorption Spectrometer (DOAS), Correlation Spectrometer (COSPEC)), due to their higher spectral resolutions, UV cameras provide the advantage of high time-resolution emission rates, a much greater spatial resolution, and the ability to simultaneously retrieve plume speeds. Nevertheless, the relatively high costs have limited their uptake to a limited number of research groups and volcanic observatories across the planet. One recent intervention in this regard has been the introduction of the PiCam UV camera, which has considerably lowered instrumental cost. Here we present the ﬁrst data obtained with the PiCam system from seven persistently degassing volcanoes in northern Chile, demonstrating robust ﬁeld operation in challenging conditions and over an extended period of time, hence adding credence to the potential of these units for more widespread dissemination to the international volcanic gas measurement community. Small and weak plumes, as well as strongly degassing plumes were measured at distances ranging 0.6–10.8 km from the sources, resulting in a wide range of SO 2 emission rates, varying from 3.8 ± 1.8 to 361 ± 31.6 td − 1 . Our acquired data are discussed with reference to previously reported emission rates from other ground-based remotely sensed techniques at the same volcanoes, in particular considering: plume geometry, seasonal e ﬀ ects, and the applied plume speed measurement methodology. The main internal / external factors that inﬂuence positive / negative PiCam measurements include camera shake, light dilution, and the performance of the OpenCV and control points post processing methods. A simple reprocessing method is presented in order to correct the camera shake. Finally, volcanoes were separated into two distinct groups: low and moderate SO 2 emission rates systems. These groups correlate positively with their volcanological characteristics, especially with the ﬂuid compositions from fumaroles.

The UV camera technique is based on the principle of ultraviolet light absorption by SO 2 [21], and has been used for volcanological purposes since 2005 [22,23]. The UV camera has a high temporal resolution and allows simultaneous determination of the plume speed, solving two significant error sources in other previous SO 2 flux methodologies [4] associated with the frequency of the data acquisition and the necessity of estimating plume speed by indirect methods (e.g., atmospheric models). In particular, the UV camera is capable of capturing high time-resolution flux data, which when combined with other techniques can be used to: understand flow dynamics in volcanic conduits (e.g., [24,25]); determine mass flow rates models (e.g., [26]); evaluate eruptive periods of a single volcano (e.g., [27]); determine the gas fluxes arising along volcanic zones/arcs (e.g., [10]); correlate degassing and seismological data (e.g., [28,29]; among other applications. Despite the above, and even considering that the UV camera is a relatively simple method for measuring SO 2 emission rates, uptake from the international user community has been somewhat limited up until now, related to the relatively high cost of the equipment. However, the introduction of the low-cost smartphone sensor-based PiCam UV camera [30,31] can be considered as the starting point of a new stage in the applications of UV cameras in volcanology, based on the characteristics of these units, namely: their small size and light weight, which enables easy transportation; user friendly acquisition and post processing software; but, most importantly, their low cost, facilitating the potential for uptake by almost all volcanic gas research groups and volcanic observatories, worldwide. In spite of several prior measurements of gas emissions from the volcanoes of northern Chile, involving: direct sampling techniques (e.g., [32][33][34][35]), studies of aerosols in plumes (e.g., [36]), COSPEC [37], and based on DOAS instrumentation (e.g., [38]), only a few studies to date have been performed using UV cameras, and those cover only six of the thirteen volcanoes with permanent degassing activity. Those volcanoes, running from north to south are: Guallatiri [1]; Irruputuncu [39]; Ollagüe [39]; Putana [40,41]; Lascar [39]; and Lastarria [42] (Figure 1). The objectives of this paper are: (1) to present the first gas flux results obtained using the PiCam UV camera on 7 persistently passive degassing volcanoes in northern Chile; (2) to discuss the main factors that can influence positively and/or negatively the data quality of these UV camera field measurements; and (3) to compare our results with gas flux data from other prior ground-based remote sensing studies. Amongst this, we present the first SO 2 flux measurements from Olca volcano.

Central Volcanic Zone
The Central Volcanic Zone (CVZ) of the Andes is located between ca. 14° to 27°S, covering southern Peru, western Bolivia, northwestern Argentina and northern Chile (Figure 1). The volcanism in this area is a consequence of subduction of the oceanic Nazca Plate below the continental South American Plate, which is characterized by a convergence rate that ranges between 7.8 and 8.4 cmyr −1 [43,44] and an angle of subduction >25° at depths from 100 to 130 km [45]. CVZ is limited by two segments absent of volcanism, to the north by the Peruvian flat-slab (ca. 5°-14°S) and to the south by the Pampean flat-slab (ca. 27°-33°S), both associated with a decrease in the slab subduction angle [46]. CVZ contains more than 40 volcanic centers that have registered eruptive activity in the last ca. 10 ka (e.g., [47][48][49]. In the case of northern Chile, the active volcanism is present between 17.72°S (Tacora volcano) and 27.12° (Ojos del Salado volcano), and hosts more than half of Holocene actives centers of the CVZ [47][48][49]. The hyper-arid climate since the Pleistocene has allowed good

Central Volcanic Zone
The Central Volcanic Zone (CVZ) of the Andes is located between ca. 14 • to 27 • S, covering southern Peru, western Bolivia, northwestern Argentina and northern Chile (Figure 1). The volcanism in this area is a consequence of subduction of the oceanic Nazca Plate below the continental South American Plate, which is characterized by a convergence rate that ranges between 7.8 and 8.4 cmyr −1 [43,44] and an angle of subduction >25 • at depths from 100 to 130 km [45]. CVZ is limited by two segments absent of volcanism, to the north by the Peruvian flat-slab (ca. 5 • -14 • S) and to the south by the Pampean flat-slab (ca. 27 • -33 • S), both associated with a decrease in the slab subduction angle [46]. CVZ contains more than 40 volcanic centers that have registered eruptive activity in the last ca. 10 ka (e.g., [47][48][49]. In the case of northern Chile, the active volcanism is present between 17.72 • S (Tacora volcano) and 27.12 • (Ojos del Salado volcano), and hosts more than half of Holocene actives centers of the CVZ [47][48][49]. The hyper-arid climate since the Pleistocene has allowed good conservation of volcanic centers [47], characterizing this zone by well-preserved stratocones, cinder cones, and ignimbrite deposits [44]. The basement in the Chilean portion of the CVZ is constituted by Paleoproterozoic to Late Paleozoic igneous and metamorphic rocks [46,50,51] in a continental crust that reaches >70 km thickness [52,53], affecting the chemistry of volcanic products, through assimilation of this crustal material [54][55][56][57][58][59].

Study Cases
Nine of the thirteen persistently degassing volcanoes in northern Chile exhibit permanent gas plumes (Figure 1), which vary considerably in size and gas concentration. The main characteristics of the seven volcanic systems measured in this work are summarized as follows: Guallatiri (18 • 25 S; 69 • 05 W; 6071 m a.s.l. (meters above sea level)) is a Pleistocene-Holocene volcano, and its geological evolution can be divided into seven stages, which include the emission of thick lava flows, lava domes, pyroclastic flows and fallout deposits, with rock compositions ranging from andesites to dacites [71]). Despite having no records of confirmed eruptive activity, Guallatiri hosts hundreds of fumarolic emissions in two areas, the summit and the southern flank fumarolic fields, which produce two permanent gas plumes: the flank fumarolic field plume is the largest and related to a major fracture network, whilst the smaller summit plume is related to a lava dome from the last stage of evolution [71]. Measured outlet gas-temperatures vary from 82 to 265 • C. Several thermal and cold springs of sulfate to bicarbonate composition appear in the northern, western, and southwestern flanks, where temperatures reach up to 50.1 • C [72].
Isluga (19 • 09 S; 68 • 50 W; 5320 m a.s.l.) is a stratovolcano that was built in four stages during the Pleistocene-Holocene, being constituted by lava and pyroclastic flows (with trachy-andesite, trachy-dacite and dacite magmas), and lahar deposits [73,74]. Minor eruptions have occurred during the second half of the 19th and 20th centuries. The last confirmed eruption was in 1913 [60]. Céspedes et al. [63] reported a plume rising 400 m above the crater, a strong sulfur smell in zones close to the volcano, "underground" noises and low intensity seismicity during 2003. Isluga has persistent fumarolic activity, which is limited to its active crater (of~400 m diameter), and two major fumaroles located in the southern flank,~100 m below the crater rim. This activity produces a relatively dense single plume, rising to an altitude ranging between 400 and 900 m over the crater.
Irruputuncu (20 • 43 S; 68 • 34 W; 5163 m a.s.l.) is a compound volcano with two nested craters, one of them active. Two volcanic edifices form Irruputuncu, the second located in the amphitheater left by the collapse of the southwestern flank of the first edifice. This volcano's volcanic eruptive products include lava flows and domes, pyroclastic flows, block-and-ash flows, and debris avalanche deposits, with andesitic, dacitic, trachy-andesitic, and trachy-dacitic compositions [75]. There is only one report of recent eruptive activity; this pertains to a small phreatic eruption in 1995 [62]. Irruputuncu hosts fumarolic fields in its active crater, and in the outer southern border of this crater [76]. Fumarolic emissions have variable outlet temperatures, ranging between 83 • C and 240 • C, with high concentrations of CO 2 and SO 2 suggesting a magmatically-dominated system [33]. The vigorous fumarolic activity causes a single plume that reaches up to~200 m over the summit [76]. Additionally, several thermal springs are located in its west flank, with temperatures that reach up to 33 • C.
Olca presents persistent fumarolic activity, which is related to formation of a lava dome, which arose in the last eruptive episode [76]. Fumarole outlet temperatures vary between 84 • C and 91 • C, and the gas composition is dominated by hydrothermal components [33]. The fumaroles produce a very discrete single gas plume, with an average altitude of~50 m over the dome. There are no records of historical eruptive activity.
Ollagüe (21 • 18 S-68 • 11 W; 5868 m a.s.l.) is a composite stratovolcano situated 12 km southeast of Ollagüe village (~300 inhabitants). Ollagüe volcano summit hosts, in its outer southwestern side, permanent fumarolic emissions, which are related to a lava dome/flow and produce a single gas plume that rises up to 300-600 m over the summit. Ollagüe volcano has a multistage eruptive history, including rhyodacitic domes, silicic andesitic-to-dacitic lava flows and domes, pyroclastic flow and surge and block-and-ash flow deposits [44]. There are no records of historical eruptive activity.
San Pedro (21 • 53 S; 68 • 24 W; 6145 m a.s.l.) is a compound stratovolcano located 85 km northeast from Calama city and is part of the NW-SE trending volcanic chain San Pedro-Linzor (SPL; [79]) and of a short E-W chain formed by San Pablo and San Pedro volcanoes and La Poruña scoria cone [80]. San Pedro volcano is formed by two cones, with an estimated combined volume of 140 km 3 . San Pedro was built in four stages, and is constituted of lava flows and domes, several scoria and pumice pyroclastic deposits (pyroclastic flow and fallout deposits) and debris avalanche deposits [81,82], with basaltic andesite, andesite, and dacite compositions. Persistent fumarolic activity is present in the upper part of the younger cone nested in the border of a lava flow, producing a discrete single gas plume reaching up to~200 m over the crater. The historical activity includes more than ten events from the 1870s [83,84] and Martin [85] details an eruption which occurred in 1901, causing considerable damages to local infrastructure.
Putana (22 • 34 S-67 • 52 W; 5890 m a.s.l.) is located on the border between Chile and Bolivia, and is a stratovolcano with a relatively well-preserved summit crater, several satellite vents and a number of post-glacial eruptive features [47,48]. The edifice consists of several sequences of basaltic andesites, andesitic and dacitic lava flows-and-domes and pyroclastic deposits [47,48,86]. Putana volcano presents four active fumarolic fields in the summit crater area, related to a small crater and lava flows. Fumarole outlet temperatures vary from 82 to 88 • C and chemical compositions reflect two sources of fluids (magmatic and hydrothermal; [33]). The fumarolic activity produces a 100-500 m height plume [33], although it is very common to observe distinct plumes related to each individual fumarolic field. There are no records of historical eruptive activity.

PiCam UV Camera
The PiCam is a low-cost SO 2 UV camera, based on two modified Raspberry Pi v1 camera modules. Each camera sensor (Omnivision OV5647) was modified using the technique described in Wilkes et al. [30], by chemical removal of the sensor's Bayer filter. This vastly increases the detector's responsivity to UV radiation and removes the mosaic pattern response imposed by the Bayer filter. The optical system was built (following Wilkes et al. [30,31]) around these detectors using 3D printed lens holders and an off-the-shelf plano-convex lenses (9 mm focal length, 6 mm diameter; Edmund Optics Inc.). These modules were co-aligned, with an overall system field-of-view of 23.1 • × 17.3 • (width × height). A 10 nm full width and half maximum bandpass filter (Edmund Optics Inc.) was mounted to the fore of each lens, with peak transmissions wavelengths of 310 nm (Filter A) and 330 nm (Filter B) respectively, corresponding to spectral regions where SO 2 does, and does not absorb UV light (e.g., [22]).
The cameras were connected to Raspberry Pi 3 Model B computers for interfacing, all housed within a PeliCase instrument case along with a battery and GPS (Global Positioning System) for timestamping the acquisitions. A Windows laptop was used to communicate with the Raspberry Pi wirelessly, controlling data capture via custom Python 3 code. Image processing was achieved by contrasting the 310 nm and 330 nm channels to isolate the SO 2 absorption, then calibrating these images via gas cell calibration (e.g., [22,87]). The applied cells contained column densities of 100, 467, and 1989 (all ±10%) ppm·m, and in all cases the calculated apparent absorbances and column densities displayed a good linear fit ( Figure 2); furthermore, all measured field column densities presented herein were below 1989 ppm·m; therefore, falling within the range in which the calibrations were valid.
Remote Sens. 2020, 12, x FOR PEER REVIEW 6 of 24 contained column densities of 100, 467, and 1989 (all ±10%) ppm•m, and in all cases the calculated apparent absorbances and column densities displayed a good linear fit ( Figure 2); furthermore, all measured field column densities presented herein were below 1989 ppm•m; therefore, falling within the range in which the calibrations were valid.

Fieldwork
Here we present data from four field campaigns, which were carried out during November 2017, December 2017, February-March 2018, and April 2018. The details of the measurements from each site are summarized below (see also In Guallatiri, volcano measurements were performed during the 10, 12, and 13 December 2017, and 5 April 2018 from 4 points located between 4.8 and 10.8 km from the summit plume, at altitudes varying from 4305 to 4933 m a.s.l. A total of 7 measurement sequences were captured between 11:00 and 14:42 hrs local time (UTC-3), with time spans ranging 31-55 min. Shutter speed for filters A and B varied from 80 to 700 ms, and 11 to 100 ms, respectively, and the image capture frequency of the cameras was set to 0.2-0.25 Hz, providing images every 4 and 5 seconds.

Fieldwork
Here we present data from four field campaigns, which were carried out during November 2017, December 2017, February-March 2018, and April 2018. The details of the measurements from each site are summarized below (see also Table 1; Supplementary Material Figure S1): In Guallatiri, volcano measurements were performed during the 10, 12, and 13 December 2017, and 5 April 2018 from 4 points located between 4.8 and 10.8 km from the summit plume, at altitudes varying from 4305 to 4933 m a.s.l. A total of 7 measurement sequences were captured between 11:00 and 14:42 hrs local time (UTC-3), with time spans ranging 31-55 min. Shutter speed for filters A and B varied from 80 to 700 ms, and 11 to 100 ms, respectively, and the image capture frequency of the cameras was set to 0.2-0.25 Hz, providing images every 4 and 5 seconds.
Measurements in San Pedro, Olca, and Isluga volcanoes were performed during 28 February, 1 March, and 4 April 2018, respectively. The observations were carried out in locations 6, 0.6, and 6.2 km (at 4103; 5300; 4350 m a.s.l., respectively) from the plume source. For Isluga volcano, five measurement sequences were performed, whereas for Olca and San Pedro volcanoes, three and two image sequences, respectively, were acquired, with acquisitions between 11:05 and 14:23 hrs local time, lasting from 5 to 56 min. In this case, shutter speeds for filter A were between 55 and 350 ms, and for filter B, between 10 and 70 ms, with an image capture frequency of 0.2 Hz.
Two days of measurements were carried out in Putana (29 November, 2017 and 9 March, 2018), Ollagüe (1 and 2 March, 2018) and Irruputuncu (2 and 3 April, 2018) volcanoes. Two sites each were used for Ollagüe and Putana volcanoes, in the first case 5.9 and 6.3 km, respectively from the summit fumarolic field, and in the latter case 5.3 and 9.5 km from the plume source, with site altitudes that varied between 3965 and 4935 m a.s.l. In the case of Irruputuncu, all measurements were carried out from the same point, located 3.3 km from the active crater, at 4182 m a.s.l. Six measurement sequences were acquired at Irruputuncu and Putana, whereas five were captured at Ollagüe, between 9:48 and 18:47 hrs local time, spanning between 8 and 44 min in duration. In these cases shutter speeds for filter A were set between 65 and 600 ms, and for filter B, between 5 and 100 ms, and the image capture frequency ranged from 0.2 and 0.25 Hz.

Post Processing
Image processing was performed post-acquisition, using a custom written Python 3 code; for a comprehensive description of the range of processing techniques for determining SO 2 fluxes from UV cameras please see Gliß et al. [88]. Here, processing followed the protocols outlined by Kantzas et al. [87]. Image registration, in order to ensure co-alignment the images from each of the camera channels, was performed via two methods: (i) automated registration using the findTransformECC function of the OpenCV library (OCV). This finds the optimum image transformation with respect to the enhanced correlation coefficient (ECC) criterion with a Euclidean model; the off-band camera images can then be warped by this tranformation using the warpPerspective() function; (ii) manual control point selection (CP) registration allows manual mapping of points in one scene to those in another, and an optimal affine transformation is then generated to best fit these points. This uses the scikit-image python module, through a SimilarityTransform() object.
The OCV is a fast method that allows a first estimate of the plume speed and SO 2 rates retrieved from a single volcano. The performance of the two methods is assessed later.
Other processing steps included: all the captured images were dark image corrected; image vignetting was corrected using a clear-sky mask image acquired in the field; furthermore, the clear-sky background intensity was determined by averaging the pixel intensities in a region of the clear sky close to the plume; finally, plume speeds were calculated using the cross-correlation technique (e.g., [22]).
The PiCams' sensitivity to SO 2 has been shown to vary by up to 15% between the center of the image and the extreme edge of the field of view [31], due to changing filter transmission characteristics with changing illumination angle. Therefore, in order to avoid major differences in the measurements across the field-of-view of the PiCam, we placed the plume in the middle of the image and extracted column densities across a cross-section through the plume, which was generally quite central to the image (as showed in the Supplementary Material Figure S2). Therefore, we can anticipate it would not change more than 5% for the cross sections used to extract plume column densities.

Estimation of the PiCam UV Camera Uncertainties
Several uncertainties can affect the quality of the data, and their review is necessary in order to estimate the total uncertainty of the measurements. We determined possible sources of errors, which include the plume speed, which depends on plume distance and time uncertainty, gas cell column densities, calibration drift, light dilution, SO 2 detection, plume direction, and multiple scattering. We estimated the errors using our data, information available in the literature (especially information available from the studied zones) and field protocols, the last applied to minimize possible sources of errors, as mentioned previously.
The plume speed uncertainty depends directly on the time uncertainty associated with the difference in time of the plume movement between the two integrated columns amounts (ICA) during cross-correlation, and from the plume distance uncertainty (which translates to an uncertainty associated with the distance between the two ICA); for the latter we considered distance errors of 50, 100 and 200 m. The plume speed uncertainty is controlled mostly by the time uncertainty, which varies in our measurements from 8.3 and 25%, whereas in the case of the plume distance error, independently variation between 50 and 200 m, this is <3.8%, with the exception of Guallatiri, Irruputuncu and Olca, where maximum errors were 4.2, 6.1, and 17%, respectively ( Table 2). In consequence, we obtained a plume speed error range from 5.9 to 18% ( Table 2). Table 2. A list of sources of errors (uncertainties) and its respective values. The total root mean square (RMS) error is also reported. The higher error in the positive error reported in the total RMS correspond to the underestimation related to the light dilution. (-) negligible error, (*) maximum error considering the maximum light dilution for volcanoes measured in distances >8 km.

Total RMS Error
Another source of error can be related to the differences between the calibrations throughout the day, due to changes in the sun position and in consequence, changes in the illumination of the background. The calibration process depends directly on the gas cells concentration, which have an error of 10% (manufacturer quoted), and as mentioned previously, of the sun position and its incidence in the camera. We calculated the calibration drift error comparing two consecutive calibrations in all sites measured and considering all the calibrations done in a single day. This error varies widely between 0.4 and 15%, whereas in the case of Ollagüe volcano it reached up to 19%, which is explained by one calibration being performed in a different site from where measurements were performed, in fact, more than 50 km of distance, consequently, with very different illumination conditions. Light dilution, caused by scattering of photons into the FOV (Field of View) of the camera between the plume and the instrument, can have a considerable effect on measured emission rates, with Campion et al. [89] demonstrating that it can cause underestimation of up to 80%. This effect is dependent on atmospheric conditions, such as pressure, humidity and aerosol concentration, SO 2 concentration and distance of the measuring point from the plume. In the case of northern Chile volcanoes, where summit craters are located at altitudes over 5000 m a.s.l., the zone is characterized by a thin atmosphere and a very dry environment, where the dilution effect is more reduced. Lopez et al. [42] reported SO 2 emission rates from Lastarria volcano (northern Chile), where measurements were made at an altitude~4500 m a.s.l. and 7 km distance from the plume, estimating a light dilution in a range of 50-60%. Similarly, Stebel et al. [41] determined uncertainty of 25-30% for UV camera measurements carried out in Putana volcano (measuring point at~4900 m a.s.l. and 6 km from the plume), where light dilution is included. Llanko et al. [90], using two UV cameras simultaneously, found that at Sabancaya volcano (southern Peru) measurements performed 4.25 km from the active vent incorporated an underestimation of 50% due to light dilution. In order to have a general approach to light dilution effect in our measurements, we performed measurements in Guallatiri volcano at several distances from the gas plume sources (between 4.8 and 9.5 km from the gas plume source; Table 1). Despite all measurements being performed at different periods of time, they were carried out under broadly similar atmospheric conditions. Additionally, degassing has been constant in the last century and absent of eruptive activity in that period, and we compare exclusively measurements with similar plume speeds (a maximum difference of ±0.5 ms −1 ). In this case, measurements carried out 5.2 km from the summit plume, and plume speed 9 ms −1 , gave SO 2 rate average for a whole sequence of 49.4 ± 18.8 td −1 , whereas at 8.4 km distance, plume speeds of 8.5 and 9.3 ms −1 , SO 2 rates averaged 19.1 ± 4.5 and 28 ± 9.3 td −1 , respectively (Table 1). Assuming these differences in SO 2 emission rates are due exclusively to the light dilution effect, this effect could be causing an underestimation in our measurements of~42% less than the original SO 2 rate for measurements carried out at long distances (>8 km) from the gas plume sources (Figure 3). In consequence, for measurements made <3 km from the plume we anticipate that light dilution will be negligible (Figure 3), whilst our measurements at >3000 m distance may be underestimating at least by 20% up to 6 km distance. Due to snow being present on a number of the volcano flanks during measurements, using Campion [90], using two UV cameras simultaneously, found that at Sabancaya volcano (southern Peru) measurements performed 4.25 km from the active vent incorporated an underestimation of 50% due to light dilution. In order to have a general approach to light dilution effect in our measurements, we performed measurements in Guallatiri volcano at several distances from the gas plume sources (between 4.8 and 9.5 km from the gas plume source; Table 1). Despite all measurements being performed at different periods of time, they were carried out under broadly similar atmospheric conditions. Additionally, degassing has been constant in the last century and absent of eruptive activity in that period, and we compare exclusively measurements with similar plume speeds (a maximum difference of ±0.5 ms −1 ). In this case, measurements carried out 5.2 km from the summit plume, and plume speed 9 ms -1 , gave SO2 rate average for a whole sequence of 49.4 ± 18.8 td −1 , whereas at 8.4 km distance, plume speeds of 8.5 and 9.3 ms −1 , SO2 rates averaged 19.1 ± 4.5 and 28 ± 9.3 td −1 , respectively (Table 1). Assuming these differences in SO2 emission rates are due exclusively to the light dilution effect, this effect could be causing an underestimation in our measurements of ~42% less than the original SO2 rate for measurements carried out at long distances (>8 km) from the gas plume sources (Figure 3). In consequence, for measurements made <3 km from the plume we anticipate that light dilution will be negligible ( Figure 3), whilst our measurements at >3000 m distance may be underestimating at least by 20% up to 6 km distance. Due to snow being present on a number of the volcano flanks during measurements, using Campion et al.'s [89] light dilution correction was not possible. (a) Absorbance image from Olca volcano with negligible effect from light dilution (note that volcanic edifice appears completely black), which was taken from 0.6 km from the gas source; (b) absorbance image from Guallatiri volcano affected by light dilution (note that volcanic edifice in the background appears light gray, whereas in the foreground the outcrops appear completely black), which was taken from 10.8 km from the gas source.
The uncertainty relating to SO2 detection depends on the sensor noise and the sensitivity of the system to SO2 [18]. Wilkes et al. [31] found this uncertainty to be 3-4% for the PiCam during tests on Etna when measuring a strong plume. However, this used a detection limit estimated based on a significantly undersaturated sensor. Whilst plumes measured in this work were smaller, high image intensities were ensured by modifying shutter speeds appropriately, to minimize sensor noise. We therefore estimate that the uncertainty associated with this should not exceed 15%.
Klein et al [91] discuss the effects of the angle between the viewing direction and the plume motion, where measurements perpendicular to the plume up to 40° should not to produce major differences in the SO2 emission rates, but producing errors up to 50% at more acute angles. Figure 3. (a) Absorbance image from Olca volcano with negligible effect from light dilution (note that volcanic edifice appears completely black), which was taken from 0.6 km from the gas source; (b) absorbance image from Guallatiri volcano affected by light dilution (note that volcanic edifice in the background appears light gray, whereas in the foreground the outcrops appear completely black), which was taken from 10.8 km from the gas source.
The uncertainty relating to SO 2 detection depends on the sensor noise and the sensitivity of the system to SO 2 [18]. Wilkes et al. [31] found this uncertainty to be 3-4% for the PiCam during tests on Etna when measuring a strong plume. However, this used a detection limit estimated based on a significantly undersaturated sensor. Whilst plumes measured in this work were smaller, high image intensities were ensured by modifying shutter speeds appropriately, to minimize sensor noise. We therefore estimate that the uncertainty associated with this should not exceed 15%.
Klein et al. [91] discuss the effects of the angle between the viewing direction and the plume motion, where measurements perpendicular to the plume up to 40 • should not to produce major differences in the SO 2 emission rates, but producing errors up to 50% at more acute angles. Additionally, the variation of the angle can be produced by changes in the wind direction and consequently in the plume during the measurements. The majority of our measurements were carried out viewing perpendicular to the plume motion, except for Ollagüe, San Pedro and 1 sequence from Putana volcano, in all cases with angles less than 40 • . Our measurement sequences lasted for a maximum of 56 minutes, reducing the chances to variations in the propagation angle of the plume within an image sequence. Since no changes in the plume propagation were observed in any sequence measured, we assumed a maximum of 5% error due to this process ( Table 2). Multiple scattering is produced by presence of abundant condensed aerosol in the plume, which could produce errors in the SO 2 flux retrieved by changing photon paths through the plume. All of our measured plumes were very transparent, suggesting a very low content of condensed aerosol in the plume; consequently, we assume that the error related to multiple scattering is negligible.
The total root mean square (RMS) error estimated for all volcanoes measured varies in a range of 8.7 and 14% ( Table 2). In the cases where errors can be obtained with minimum and maximum values, we presented both values, consequently, minimum and maximum errors were also calculated ( Table 2). In the cases of Guallatiri and Putana volcanoes, where some measurements were done in a distance over 8 km from the plume, errors including high underestimations due light dilution were also calculated, producing higher total RMS error, up to 19 and 21%, respectively ( Table 2).

Results
Results from each volcano are presented in Table 1 and are summarized as follows (processed images from each volcano are also presented in Supplementary Material Figure S2): From Guallatiri volcano 7739 images were acquired, and 5922 images were processed. Images that are not processed, due to shaking of the PiCam during the field measuring producing errors in the plume speed calculation and/or SO 2 emission rates, will be discussed in the following sections. The determined plume speed ranged 1.0 to 10.3 ms −1 . Of the three image sequences from the December 2017 fieldwork, two provided reliable flux data (considering not reliable data when cross correlation technique did not work to obtain the plume speed or post processing methods can not retrieve emission rates), where the averages ± one standard deviation (1σ) of the SO 2 emission rate were 49.4 ± 18.8 and 50.5 ± 12.3 td −1 for the 10 and 12 December, 2017, respectively, whereas from the four sequences acquired during 5 April, 2018, the emission rates were 5.5 ± 2.8, 12.2 ± 3.1, 19.1 ± 4.5, and 28 ± 9.3 td −1 , respectively. The maximum rate was captured during 12 December, 2017: 101 td −1 . The overall average SO 2 outputs from the December 2017 and April 2018 measurements were 49.8 ± 17.1 and 19 ± 17.7 td −1 , respectively, and that across both periods was 29.1 ± 22.6 td −1 . The emission rates pertain to degassing from the gas plume from the summit fumarolic field, due to post processing for southern flank fumarolic field producing no reliable data.
A total of 3565 images were obtained during the one day of measurements from Isluga volcano, with 5 sequences acquired and all the images were processed, such that reliable fluxed were determined from all sequences, barring sequence 3. The determined plume speeds varied between 7.0 and 13.1 ms −1 and the SO 2 emission rates for sequences 1, 2, 4, and 5 were 329 ± 90.8, 199 ± 47.5, 361 ± 31.6 and 129 ± 28.3 td −1 , respectively, with an overall average of 254 ± 49.6 td −1 . The maximum SO 2 emission rate was measured in sequence 1:569 td −1 .
At Olca and San Pedro volcanoes, 3 and 2 sequences were acquired, with 1604 and 2656 images, respectively. All the Olca images were processed, whereas only 1096 images from San Pedro were processed. It was not possible to acquire reliable gas fluxes from sequence 1 from Olca volcano. A wide range of plume speeds were measured, varying from 0.9 to 9.1 ms −1 . In spite of it being possible to determine plume speed in sequences 1 and 3 for Olca volcano, the resulting SO 2 emission rates were close to zero, being here considered as a not reliable data, whereas for sequence 2 the average measured rate was 18.4 ± 13.4 td −1 , with a maximum of 58.4 td −1 . Plume speeds measured for San Pedro volcano varied from 6.8 to 12.9 ms −1 . The average SO 2 emissions rates ranged between 7.4 ± 1.6 and 16.2 ± 6.5 td −1 , with a maximum rate of 43.2 td −1 and an overall average SO 2 output of 13.2 ± 4.2 td −1 .
Flux data were obtainable from 4 of the 5 acquired sequences from Ollagüe volcano, whereby 3266 of the 3440 captured images were processed. The plume speed values ranged between 7.4 and 9.4 ms −1 , on 1 March 2018, and between 3.3 and 3.7 ms −1 on the 2 March, 2018. Measurements on the first day were carried out during the afternoon, when the wind speed normally increases, whereas the second day's measurements were performed during the morning. Average SO 2 emission rates during 1 March varied from 7.9 ± 2.1 to 19.2 ± 4.1 td −1 , and those during 2 March between 4.8 ± 2 and 21.5 ± 4.0 td −1 . The overall SO 2 output for the first and second days were 14.3 ± 3.1 and 10.7 ± 3.5 td −1 , respectively, and that averaged over the whole period was 12.5 ± 3.3 td −1 ; the maximum rate of 38 td −1 was measured on 2 March.
From Putana volcano 2654 images were obtained and processed. Plume speeds ranged from 4.5 to 8.0 ms −1 . SO 2 emission rates obtained during 29 November, 2017 averaged 31.9 ± 9.8 td −1 , with a maximum of 66.8 td −1 , whereas measurements during 9 March, 2018 had sequence averages ranging 2.8 ± 1.6 to 11.9 ± 3.1 td −1 , with the maximum rate of 24.2 td −1 obtained in the sequence 3. The overall average SO 2 output for 9 March was 5.8 ± 1.7 td −1 and for both days was 8.2 ± 2.4 td −1 . Despite there being several small plumes emitted from Putana volcano's summit, only the southernmost plume was processed, as it was not possible to obtain reliable data from the central and northernmost plumes.

External/Internal Effects during Measuring and Post Processing Methods Comparison
Several effects and capabilities were observed during the data acquisition and post processing, which depends on the external/internal factors and PiCam processing code properties. Camera shake is one of the most important external factors that can affect the PiCam UV camera measurements, influencing during the data acquisition and post processing. Lateral movement of the camera in the field due to wind gusts, generates displacement and blurring of the acquired images. The movement can be verified by checking the sequence producing stop motion videos, where movement of the sequence can be detected (Supplementary Material Figure S3). We observed that if a complete sequence is partially affected by the camera shake is processed, SO 2 emission rates can be under or overestimated, or the plume speed cannot be determined, and consequently, SO 2 emissions rates cannot be retrieved. In this case, we applied an extraction of the displaced/unfocussed images, in order to avoid errors related to the movement of the integrated column amounts (ICA's). Alternatively, future work on more secure tripod mounting, or the use of video stabilization, could provide solutions, which prevent the loss of data. Here we show two cases where improvements can be made using corrected wind-affected measuring sequences: (1) Sequence 3 from Guallatiri volcano carried out during 5 April 2018 between 13:21 and 14:06 hrs local time (Table 1) produced 1068 images, which only 320 images were not affected by the camera shake. The processing of the whole sequence was not able to obtain plume speed, and consequently, the retrieval of the SO 2 rates. After removing the camera shake-affected images (748 images), a plume speed of 8.5 ms −1 and an average SO 2 emission rate of 19.1 ± 14.5 td −1 were obtained for the summit plume, with measured minimum and maximum rates of 10.4 and 32 td −1 , respectively.
(2) Sequence 1 from Isluga volcano was acquired 4 April 2018, for 44 minutes starting at 11:05 hrs local time; 1062 images were obtained ( Table 1). The whole sequence was processed obtaining a plume speed of 8.6 ms −1 , whereas the average SO 2 emission rate was 177 ± 60.7 td −1 , with a maximum rate of 387 td −1 (Figure 4a). We detected 322 images not camera shake-affected, which were reprocessed (Figure 4b). The new data obtained was a plume speed of 10.9 ms −1 , an average SO 2 emission rate of 329 ± 90.1 td −1 and a maximum rate of 569 td −1 . The comparison between the original and the reprocessed sequences ( Figure 5) shows that the extraction of the camera shake-affected images does not produce changes in the general pattern of emission rates, which means that the small-scale shifts in ICA placement are not causing dramatic changes to the observed trends, but an increase in the SO 2 emission rates is produced once camera shake is removed, due to the associated increase in plume speed estimation.
Remote Sens. 2020, 12, x FOR PEER REVIEW 13 of 24 emission rate of 329 ± 90.1 td −1 and a maximum rate of 569 td −1 . The comparison between the original and the reprocessed sequences ( Figure 5) shows that the extraction of the camera shake-affected images does not produce changes in the general pattern of emission rates, which means that the small-scale shifts in ICA placement are not causing dramatic changes to the observed trends, but an increase in the SO2 emission rates is produced once camera shake is removed, due to the associated increase in plume speed estimation.   Figure 5) shows that the extraction of the camera shake-affected images does not produce changes in the general pattern of emission rates, which means that the small-scale shifts in ICA placement are not causing dramatic changes to the observed trends, but an increase in the SO2 emission rates is produced once camera shake is removed, due to the associated increase in plume speed estimation.  The extraction of the displaced/blurred images allows us to obtain information of plume speed and SO 2 emission rates from sequences where we are not able to calculate both parameters due to camera shake. In the cases where plume speed and SO 2 rates are retrieved, the camera shake-affected images extraction process allows us to detect an increasing of plume speed up to 21%, whereas in the case of the SO 2 emission rates these values increase up to 46% over the raw not corrected rates.
Light dilution is another external factor that can influence the final SO 2 emission rates at a single volcano, as discussed in Section 3.4. Campion et al. [89] demonstrated that changes in the atmospheric conditions can produce variations in the light dilution effect, despite light dilution having a high dependence on the distance of the measuring point from the plume. As was discussed in the Section 3.4, in the Altiplano of northern Chile the studied volcanoes are located at high altitudes, with a very dry environment, very low relative humidity, and a thin atmosphere, which considerably reduces the dilution effect. We have estimated that for measurements carried out at distance <3 km the light dilution is negligible, as observed in the case of Olca volcano (Figure 3a), whereas for measurements <6 km light dilution seems to be somewhat important, producing underestimation lower than 20% ( Table 2). Despite the limited effect of the light dilution on our measurements, this must be considered, especially in those measurements carried out at long distance, where the light dilution effects are more evident (Figure 3b; Table 2).
In order to compare OCV and CP image registration, we processed several sequences using both methods. Differences in plume speed mostly varied by 2% to 10.8%, although in exceptional cases they reached between 35.3% and 43.8%. In the case of SO 2 emission rates, a wider range of differences is found, from 0.6% to 28.2%, with a maximum difference of 50.3%. The low differences demonstrate that both methods are able to retrieve good quality data and broadly provide similar registration results. However, in the case of high differences, at times image alignment does not correctly register images with the OCV method, producing an overestimation of plume speed and SO 2 emission rates, as well as causing incorrect column amount retrievals due to incorrect off-band optical depth correction. The OCV method can produce errors in the alignment of the images, creating a false double plume, which is observed as a shadow of the original recorded plume and/or presence of artifacts, such as high SO 2 column density amounts in the volcanic edifice flanks or its borders (Figure 6a), similar to those observed previously with camera shake. This error is related to the occasional inability of the OCV method to automatically align the borders of the volcanic edifice; consequently, positive and negative differences could be produced by this error. Particularly, our data generates an overestimation of the SO 2 emission rates. The overestimation observed in our data can be avoided using the Control Points (CP) method, which allows manual alignment of the images from the two lenses, by use of control points in both images. These images produce a very well defined border of the volcanic edifice and, consequently, a very well defined gas plume (Figure 6b). Our data demonstrate that when image alignment cannot be reached using OCV post processing method, the use of CP method can produce a difference by at least 35% for SO 2 emission rates (Figure 7). (1) Measurements of several plumes in a single volcano: in the case of Guallatiri volcano, which produces two plumes (from the southern flank and summit region respectively), Gliß et al [1] reported SO2 average outputs for the whole system of 112 ± 43.2 td −1 , and a maximum rate of 251 td −1 . In our case, we reported data exclusively for the summit region plume, with image sequence averages varying from 5.5 ± 2.8 to 50.5 ± 12.3 td −1 , and a maximum peak of 101 td −1 . However, these data are rather similar to those reported for just the summit plume by Gliß et al [1], which ranged from 8.6 to 129 td −1 (Table 3), but in our case the span of fluxes is somewhat narrower. Indeed, differences in quoted emission rates can be attributed to the number of plumes considered at targets with multiple sources.   showing the comparison between OCV and CP methods. Note that the OCV method produce an overestimation of the SO2 emission rates due to the bad alignment of the images from the camera A and B, whereas a better SO2 emission rate is obtained using CP method.
(2) Measuring points position, light dilution effect and plume geometry: the comparison between our data and those from other authors can also be related to camera orientation and distance from the gas source. Indeed, this can influence the light dilution effect, which increases with this distance (e.g., [89,92]). Comparing data from Putana volcano reported by Tamburello et al [40] and our measurements, differences could also be attributed to light dilution, as Tamburello et al [40] measured 4.7 km from the summit fumaroles, whereas we worked up to 9.5 km from the source. Furthermore, it is ideal for UV camera measurements to be carried out viewing perpendicularly to the plume transport direction, due to the possibility that non-orthogonal measurements can produce notable differences in the SO2 rates (e.g., [91]). Comparing data from Tamburello et al [40] and Stebel et al [41], and our measurements from Putana volcano during November 2017, the reported average SO2 emission rates were 55.3 ± 17.3 td −1 , 40 ± 11 td −1 , and 31.9 ± 9.8 td −1 , respectively; in all cases measurements were carried out at a very similar distance to the same southernmost gas plume (between 4.7 and 6.2 km). Our data could therefore be underestimated since the plume motion was not perfectly perpendicular to our viewing orientation (~10 degrees), in contrast to Tamburello et al. [40] and Stebel et al. [41], who viewed almost perpendicularly to the plume transport vector. Additionally, our measurements were carried out during a cloudy day, which may have increased the humidity and, consequently, the light dilution effect. Considering that these differences are not very large, it is also possible to be attributed to natural volcanic variability.
(3) Seasonal effects: one of the most important factors that must be taken into account during discrete field campaigns are seasonal effects. Indeed, in our study area in northern Chile summer corresponds to the rainy and relatively hot season, influenced by Amazonian rains arriving from the east, and consequently producing relatively low-speed westward winds. On the contrary, autumn, winter, and spring correspond to dry and cold seasons, with faster eastward winds, with the fastest winds recorded during the end of autumn-early winter. A permanent NOVAC station (DOAS system) located on Isluga volcano and operative since December 2014, shows strong variations in the SO2 emission rates, where differences can reach up to 656 td −1 in a single year and 685 td −1 for the whole period (Figure 8; Table 3); these variations are seen to oscillate on seasonal timescales. Explanations of these variations could be attributed to: (i) seasonal variations influencing the degassing pattern of the studied volcanoes; (ii) inaccurate measurements from DOAS, possibly due to wind speed estimations or the location of the plume relative to the measuring instrument changing with the wind direction/speed; (iii) inaccurate measurements from both DOAS and UV cameras with some seasonal dependency. Since measurements between the UV camera and DOAS instruments are  (2 April 2018) showing the comparison between OCV and CP methods. Note that the OCV method produce an overestimation of the SO 2 emission rates due to the bad alignment of the images from the camera A and B, whereas a better SO 2 emission rate is obtained using CP method.

Comparison with Previous Measurements from Other Ground-Based Remote Techniques
Several authors have reported SO 2 emission rates from these studied volcanoes, mostly during discrete field campaigns with the DOAS techniques, but also with some prior use of UV cameras (Table 3). In contrast, Isluga volcano has been continuously monitored since December 2014 by OVDAS-SERNAGEOMIN using a permanent scanning DOAS station within the Network for Observation of Volcanic and Atmospheric Change (NOVAC) network (Table 3). In the case of Olca volcano, this is the first time that SO 2 rates have been reported using a ground-based remote sensing technique. In most cases, our SO 2 emission rates are lower than those reported by other authors, although in few cases our data are higher. A number of issues that could potentially impact upon acquired volcanic gas fluxes are listed below.
(1) Measurements of several plumes in a single volcano: in the case of Guallatiri volcano, which produces two plumes (from the southern flank and summit region respectively), Gliß et al. [1] reported SO 2 average outputs for the whole system of 112 ± 43.2 td −1 , and a maximum rate of 251 td −1 . In our case, we reported data exclusively for the summit region plume, with image sequence averages varying from 5.5 ± 2.8 to 50.5 ± 12.3 td −1 , and a maximum peak of 101 td −1 . However, these data are rather similar to those reported for just the summit plume by Gliß et al. [1], which ranged from 8.6 to 129 td −1 ( Table 3), but in our case the span of fluxes is somewhat narrower. Indeed, differences in quoted emission rates can be attributed to the number of plumes considered at targets with multiple sources.
(2) Measuring points position, light dilution effect and plume geometry: the comparison between our data and those from other authors can also be related to camera orientation and distance from the gas source. Indeed, this can influence the light dilution effect, which increases with this distance (e.g., [89,92]). Comparing data from Putana volcano reported by Tamburello et al. [40] and our measurements, differences could also be attributed to light dilution, as Tamburello et al. [40] measured 4.7 km from the summit fumaroles, whereas we worked up to 9.5 km from the source. Furthermore, it is ideal for UV camera measurements to be carried out viewing perpendicularly to the plume transport direction, due to the possibility that non-orthogonal measurements can produce notable differences in the SO 2 rates (e.g., [91]). Comparing data from Tamburello et al. [40] and Stebel et al. [41], and our measurements from Putana volcano during November 2017, the reported average SO 2 emission rates were 55.3 ± 17.3 td −1 , 40 ± 11 td −1 , and 31.9 ± 9.8 td −1 , respectively; in all cases measurements were carried out at a very similar distance to the same southernmost gas plume (between 4.7 and 6.2 km). Our data could therefore be underestimated since the plume motion was not perfectly perpendicular to our viewing orientation (~10 degrees), in contrast to Tamburello et al. [40] and Stebel et al. [41], who viewed almost perpendicularly to the plume transport vector. Additionally, our measurements were carried out during a cloudy day, which may have increased the humidity and, consequently, the light dilution effect. Considering that these differences are not very large, it is also possible to be attributed to natural volcanic variability.  [40], 5 [41]. (1) Peak in a single measurement sequence and/or daily peak, (2) calculated from monthly average reports, (3) overall after 3 days measurements, (4) optical flow post processing, (5) cross correlation post processing, n.r. not reported, * reported as a range. (3) Seasonal effects: one of the most important factors that must be taken into account during discrete field campaigns are seasonal effects. Indeed, in our study area in northern Chile summer corresponds to the rainy and relatively hot season, influenced by Amazonian rains arriving from the east, and consequently producing relatively low-speed westward winds. On the contrary, autumn, winter, and spring correspond to dry and cold seasons, with faster eastward winds, with the fastest winds recorded during the end of autumn-early winter. A permanent NOVAC station (DOAS system) located on Isluga volcano and operative since December 2014, shows strong variations in the SO 2 emission rates, where differences can reach up to 656 td −1 in a single year and 685 td −1 for the whole period ( Figure 8; Table 3); these variations are seen to oscillate on seasonal timescales. Explanations of these variations could be attributed to: (i) seasonal variations influencing the degassing pattern of the studied volcanoes; (ii) inaccurate measurements from DOAS, possibly due to wind speed estimations or the location of the plume relative to the measuring instrument changing with the wind direction/speed; (iii) inaccurate measurements from both DOAS and UV cameras with some seasonal dependency. Since measurements between the UV camera and DOAS instruments are very similar when comparing data from the same season, we cautiously suggest that either point i or iii is valid here (Figure 8; Table 1; Table 3); however, long-term UV camera data is required to robustly test these hypotheses. Future investigations will be carried out in order to determine the extent of these seasonal effects in the volcanic degassing pattern in northern Chile volcanoes.
Remote Sens. 2020, 12, x FOR PEER REVIEW 17 of 24 test these hypotheses. Future investigations will be carried out in order to determine the extent of these seasonal effects in the volcanic degassing pattern in northern Chile volcanoes.   (4) Plume speed estimation and intrinsic errors of ground-based remote techniques: one of the most important sources of differences and errors in the calculation of SO 2 output corresponds to plume speed estimation. The UV camera has solved this problem by recording simultaneous images where plume movements can be tracked through time and consequently the plume speed can be accurately estimated. On the contrary, DOAS techniques need an external instrument and/or method to determine the plume speed. Atmospheric models, use of in-situ anemometers and even balloon sondes at airports are typically used to determine the plume speed (e.g., [5,40,94]), where more accurate information can be obtained if plume altitude is determined in the field during the measurements (considering layered atmospheric models depending of the altitude), which adds more uncertainties to the plume speed data. Additionally, the low density of meteorological stations in or close to the Altiplano has a consequence in global atmospheric models, which have poor resolution and hence lower accuracy in that area. Field wind speed determined on the ground, where measuring instruments are deployed, produce high uncertainties, since they are a coarse approximation to the atmospheric conditions where plume is transported away from the gas source, especially at high altitude volcanoes with high altitude differences between the volcano summit and its base and, consequently, strong differences exist in the wind speed at several altitudes. Ideally, a meteorological station deployed in the crater rim allows accurate estimations of plume speed and can be compared with UV camera estimations; nevertheless, there are no meteorological stations in any of the craters of the measured volcanoes in northern Chile. Data from DOAS on Isluga, Ollagüe, San Pedro, and Putana volcanoes differ widely with our data (Table 3), and are characterized by its very high standard deviations, which could be partially attributed to the high variations in the plume speed estimations related with the method used to determine it, which are indirect and consequently inaccurate. In the case of Ollagüe, San Pedro, and Putana volcanoes, characterized by small and low intensity plumes, and a mix of several small plumes in the case of Putana volcano, SO 2 emission rates are particularly high. Here another factor can be added, corresponding to the differences in the "nature" of each technique, where several differences exist between the instruments characteristics. The UV camera is able to "see" the gas plume during the data acquisition, being capable of determining the plume speed simultaneously, and as we demonstrated previously, highly capable of detecting small plumes, even at long distances, as shown in the cases of Guallatiri and Putana, where plumes were measured at distances of 10.8 and 9.5 km, respectively (Table 1). On the contrary, the scanning pattern of DOAS technique is highly dependent on the plume geometry (as pointed in previously in Section 2), including its width, length, and propagation direction, and the size of the plume becomes highly important in long distance measurements. The addition of all these factors, including inaccurate plume speed determinations, can produce both under and overestimations of SO 2 emission rates, which could also add as a factor in the differences between our and previously reported data from northern Chile volcanoes.

Volcanological Implications of the SO 2 Emission
Rates SO 2 emission rates from the seven studied volcanoes can be preliminary divided into two groups: low and moderate emission rates volcanoes. Most of the studied volcanoes can be classified as displaying low emission rates, corresponding to the cases of Guallatiri, Olca, Ollagüe, San Pedro and Putana, with average rates being predominantly <20 td −1 . Those volcanoes emit fluids dominated by typical hydrothermal components, such as H 2 S and CH 4 , and relative low contents of SO 2 [33,95]. They are characterized by small gas plumes and the fumarolic emissions are related to lava domes or flows, where the gas is emitted from low temperature fumaroles (<84 • C). Only Guallatiri volcano has some high temperatures fumaroles (>200 • C), however, the fluid composition is dominated by hydrothermal components. Additionally, all these volcanoes have no records of historical eruptions, with the only exception of San Pedro volcano. The low SO 2 emission rates could be related to a long-lived passive degassing without eruptive activity over a very long period of time. On the contrary, moderate emission rate (>20 td −1 ) volcanoes corresponds to Irruputuncu and Isluga volcano, with more abundance of magmatic components, like SO 2 , high temperature fumaroles (>120 • C) and a larger gas plume [33]. Both volcanoes have records of eruptive activity in the last century, especially in the case of Isluga volcano, where its last crisis was recorded on 2003. In both cases, relatively moderate-to-high emission rates could be related to a higher level of activity, which could be correlated with more frequent eruptive activity in the records. Further studies must be carried out in order to confirm this classification, based on the combination of ground-based gas measurements and direct sampling of fumaroles. Additionally, the performance of frequent and prolonged surveys of ground-based techniques will help to improve the knowledge of the degassing pattern behavior of the studied volcanoes.

Conclusions
The PiCam UV camera has been successfully deployed on seven persistently degassing volcanoes from northern Chile, demonstrating the capacity to measure small and weak plumes (e.g., Olca and Putana volcanoes), as well as strongly degassing sources (e.g., Isluga volcano), resulting in resolution of SO 2 output rates ranging 3.8 ± 1.8-361 ± 31.6 td −1 , with measurements performed at a variety of distances from the gas sources (0.6-10.8 km). Given the low cost of the PiCam modules, with respect to traditionally applied scientific grade UV cameras, and the fact that these have delivered fail free service in these challenging field environments, over a protracted period of time, this affirms the suitability of these units for widespread dissemination to the end user community, worldwide. In addition, this article discusses additional factors relevant to all UV camera volcanic flux measurements: camera shake, light dilution, and protocols adopted in post processing, in particular considering image registration used to calculate plume speeds and retrieve SO 2 rates. Differences in SO 2 emission rates by camera shake can be solved by removing the affected images and reprocessing the data, whereas although light dilution is observed in most of the measurements, its effects seems to be very limited, due to the thin, dry atmosphere at our high altitude study locations. For image registration, when the automated OCV algorithm is unable to correctly align the images from both cameras, the manual CP method can produce changes in the SO 2 rates of up to 35%. When a comparison is done between our data and reported remote ground-based techniques (such as DOAS, UV camera, and NOVAC permanent stations) in the volcanoes presented here (except Olca), differences (in most cases our emission rates are lower) can be attributed to (i) measuring of single plumes in multi-plume volcanoes, (ii) instrument-plume distance and consequently the light dilution effect, (iii) the geometry of the plume measured, (iv) seasonal effects, and (v) the methods used to calculate the plume speed. In most of the cases, we suggest that the larger SO 2 emission rates from reported data are related to methods used to calculate the plume speed and strong seasonal effects. Finally, we define two distinct groups of volcanoes according to the SO 2 emission rates: low and moderate, which correlate positively with volcanological characteristics. Volcanoes defined as having low SO 2 emission rates (<20 t d −1 ) are systems dominated by hydrothermal fluids; magmatic dominated fluids systems produce moderate SO 2 rate plumes (>20 t d −1 ).