Impact of the Southern Ecuadorian Andes on Oxygen and Hydrogen Isotopes in Precipitation

Determining how the elevation of the Northern Andes has evolved over time is of paramount importance for understanding the response of the Northern Andes to deformational and geodynamic processes and its role as an orographic barrier for atmospheric vapor transport over geologic time. However, a fundamental requirement when using stable isotope data for paleoaltimetry reconstructions is knowledge about the present-day changes of δ18O and δD with elevation (isotopic lapse rate). This study defines the present-day river isotopic lapse rate near the Equator (∼3°S) based on analysis of δ18O and δD of surface waters collected from streams across the Western Cordillera and the Inter-Andean depression in Southern Ecuador. The results for the two domains show a decrease of δ18O with elevation which fits a linear regression with a slope of −0.18‰/100 m (R2 = 0.73, n = 83). However, we establish a present-day lapse rate of −0.15‰/100 m for δ18O (R2 = 0.88, n = 19) and -1.4‰/100 m for δD (R2 = 0.93, n = 19) from water samples collected along the west facing slopes of the Western Ecuadorian Cordillera which is mainly subject to moisture transport from the Pacific. We argue that this empirical relationship, consistent with those obtained in different tropical areas of the world, can inform stable isotope paleoaltimetry reconstructions in tropical latitudes.


INTRODUCTION
The long-term climatic evolution and atmospheric circulation patterns of the Earth are influenced on the first order by the topography of large mountain chains (e.g., Molnar and England, 1990;Boos and Kuang, 2010;Barnes et al., 2012).
The Andes are a non-collisional subduction orogen and represent one of the main topographic features on Earth. However, uncertainties remain about how long this belt has been acting as a barrier to atmospheric circulation and moisture transport (e.g., Garzione et al., 2006;Garzione et al., 2008;Rech et al., 2006;Barnes and Ehlers, 2009;Ehlers and Poulson, 2009;Mulch 2016;Garzione et al., 2017;Sundell et al., 2019). Most studies aiming at understanding the links among geodynamic processes, Andean topography, and climate have focused on the Southern and Central Andes; the role and overall long-term landscape evolution of the Northern Andes remains enigmatic. This negligence is partly due to the scarce paleoaltimetry data obtained in the Northern Andes, and especially in the Ecuadorian Andes, a region of intense debate about the timing and rate of topographic development (e.g., Steinmann et al., 1999;Gregory-Wodzicky, 2000;Hungerbuhler et al., 2002;Witt et al., 2017;Jackson et al., 2019).
Most paleoaltimetry studies use the stable oxygen (δ 18 O) and hydrogen (δD) isotopic composition of meteoric water that scales with elevation in a predictable fashion to retrieve the elevation signal from near-surface paleoenvironmental archives (e.g., Garzione et al., 2000;Mulch et al., 2006;Sundell et al., 2019) or crustal-scale deformation zones (e.g., Mulch et al., 2004;Gébelin et al., 2012;Gébelin et al., 2013). This relationship results from distillation of heavy isotopes ( 18 O or D) through condensation and precipitation as air masses rising across a mountain range cool adiabatically during ascent. As a result, oxygen (δ 18 O) and hydrogen (δD) isotope ratios of rainfall scale systematically with elevation on the windward side of a mountain range. Compilations of isotope data sets from regions in the low to mid-latitudes provide an average of ∼2.8 ‰ in δ 18 O or ∼20 ‰ in δD per km (Poage and Chamberlain, 2001;Quade et al., 2011).
Here, we present the first comprehensive study of this empirical relationship near the Equator across the Western Andean Cordillera and the Inter-Andean depression in southern Ecuador by analysing surface waters from tributaries along five transects (Figure 1, Supplementary Table S1). In agreement with previous studies identifying the altitude effect on the isotopic composition of tropical precipitation (e.g., Garcia et al., 1998;Gonfiantini et al., 2001;Saylor et al., 2009), our results indicate that δ 18 O and δD values of tributary waters decrease systematically as a function of increasing elevation on the windward side of the Western Cordillera, yet with a lower lapse rate than commonly observed at mid-latitudes (e.g., Poage and Chamberlain, 2001). Projecting such isotope-elevation relationship to past environments is inherently difficult, yet an important parameter in paleoaltimetry reconstructions. Present-day lapse rates established in different climate zones, latitudes or hydrological settings allows us to explore how different environmental settings in the past may have affected isotope lapse rates.

CLIMATE OF THE ECUADORIAN ANDES
Topography exerts an important control on atmospheric moisture flux over the Northern Andes (Garcia et al., 1998;Windhorst et al., 2013). Due to the presence of two northsouth trending Eastern and Western Cordilleras separated by an Inter-Andean valley, their equatorial location, at the junction between the Pacific Ocean and the Amazon Basin, the Ecuadorian Andes are characterized by a complex climate ( Figure 1B). Currently, Ecuador is influenced by two main precipitation sources: 1) Air masses originating from the Pacific (Garcia et al., 1998), and 2) Atlantic air masses carried across the Amazon Basin (Windhorst et al., 2013). Also, precipitation regime and atmospheric circulation patterns in Ecuador are governed by three main factors: 1) Altitude of the Andes acting as a weather divide between Pacific air masses from the west and Atlantic air masses from the east (Garreaud et al., 2009), 2) Passage of the Intertropical Convergence Zone (ITCZ) (e.g., Rozanski and Araguas-Araguas, 1995), and 3) El Niño-Southern Oscillation (ENSO) (e.g., Rossel and Cardier, 2009). The Western Cordillera and coastal areas are affected by western trade winds advecting moisture from the Pacific Ocean (Emsk, 2007). This Pacific domain is marked by a unimodal precipitation regime with increased rainfall from December to April that accounts for more than 90% of annual precipitation and coincides with the southernmost extent of the ITCZ (Rozanski and Araguas-Araguas, 1995;Garcia et al., 1998;Campozano et al., 2016).
The South Ecuadorian Coast is affected by ENSO cyclicity that brings warm surface waters carried by trade winds from the West Pacific and causes heavy rainfall during the El Niño years (Philander, 1983;Rossel and Cardier, 2009). Convective storms from the Pacific cause a significant decrease in δ 18 O and δD values of precipitation in the coastal areas of Ecuador (Garcia et al., 1998). The impact of ENSO on precipitation Modern δ 18 O water and δD water values (blue dots) from our sampling sites along two main transects across the Western Southern Ecuadorian Cordillera (see location in A). Minimum and maximum topographic profiles (gray lines) were obtained at a swath distance of 5 km at each side of the main central section.
Frontiers in Earth Science | www.frontiersin.org May 2021 | Volume 9 | Article 664590 depends on the local topography; it is highest at low to moderate elevations on west facing slopes of the Cordillera (< 1500 m) and negligible at high elevations (Rossel et al., 1998;Rollenbeck and Bendix, 2011;Ochoa et al., 2016). Rainfall intensity also depends on the latitude and is higher in the north (> 700 and 3,500 mm in the coast and foothills, respectively) than in the south (< 80 and 800 mm in the coast and foothills, respectively) (Garcia et al., 1998). This latitudinal effect is reflected in the isotopic composition of precipitation of Pacific coastal stations, which display lower mean δ 18 O water values in the north (∼−5‰) than in the south (∼−2‰) (Garcia et al., 1998). The Eastern Cordillera is controlled by moisture-bearing winds from the Atlantic and the Amazon Basin and not by the Pacific westerlies (Emck, 2007;Windhorst et al., 2013). Atlantic air masses are carried by strong south-easterly winds, that once they have reached the eastern slopes of the Eastern Cordillera, are adiabatically lifted forming the Andean Occurring System (AOS, Campozano et al., 2016) that is progressively transported to the Inter-Andean depression (Celleri et al., 2007;Windhorst et al., 2013;Mora et al., 2014;Ochoa et al., 2016).
The climate of the Inter-Andean valley is influenced by moisture sources in the Western Pacific and continental and tropical Atlantic air masses (Vuille et al., 2000). Strong southeasterly trade winds carry moisture from the Amazon and enter the Inter-Andean valley leading to a mixing of moisture with Pacific trade winds . Air masses in the Inter-Andean depression can also originate in the Atlantic, and may get enriched in 18 O or D due to high evapotranspiration during passage over the Amazon Basin (e.g., Salati et al., 1979). The Cuenca Basin ( Figure 1A) is part of this domain and has an outlet towards the east, into the Amazon Basin (Ochoa et al., 2016). In contrast to the Pacific domain that shows a unimodal distribution of precipitation, the Inter-Andean depression is characterized by two contrasting rainfall regimes, a unimodal (UMR) and a bimodal (BMR) regime that respectively cover ∼15 and ∼85% of the Cuenca basin area (Celleri et al., 2007). Based on different distributions of mean annual rainfall, two UMR with a single rainfall peak in June and July (UM1: 2,900-3,400 mm a −1 and UM2: 1,100-1,600 mm a −1 ) are defined in the eastern part of the basin, and two BMR with rainfall peaks in April and October (BM1: 660-100 mm a −1 and BM2: 1,000-1,800 mm a −1 ) occur on the high eastern and western flanks of the basin (see Figure 5 in Celleri et al., 2007). The UMR is closely related to the AOS reaching the basin via the Paute Canyon ( Figure 1A), and the difference in precipitation amount is interpreted to reflect an abrupt change in elevation where moisture originating from the Amazon Basin produces high orographic rainfall volumes (UM1), followed by reduced orographic precipitation (UM2) (Celleri et al., 2007). The BMR is identified at the junction between the Inter-Andean depression, the Amazon and Pacific basin and is controlled by the seasonal north-south migration of the ITCZ that causes peak rainfall and low δ 18 O (and low δD) precipitation values in March-April and then October-November (Rozanski and Araguas-Araguas, 1995;Garcia et al., 1998;Celleri et al., 2007;Ochoa et al., 2016).

METHODS
To establish a river-based δDand δ 18 O-elevation relationship at the Equator, we sampled a total of 89 surface waters from perennial streams during the dry season (mid September) from an array of elevations across the Southern part of the Ecuadorian Western Cordillera and the adjacent Inter-Andean depression ( Figure 1 and Supplementary Table S1). River-based isotope-elevation relationships may be skewed to select elevation intervals due to uneven precipitation intensity within a given hypsometry (e.g., Bookhagen and Burbank, 2006) or biased by groundwater recharge from unknown catchment sizes. However, they have proven extremely informative as a) they reflect the competing effects of climatic and topographic controls on regional isotopic lapse rates (e.g., Rohrmann et al., 2014), and b) contribute largely to averaging precipitation events or seasonality of precipitation (e.g., Garzione et al., 2000;Schemmel et al., 2013). We hence feel confident that, with respect to paleaoaltimetry applications where time scales of isotopic proxy development play an important role, such riverbased lapse rates are robust since nature has already provided a lot of the spatial averaging.
We established two main transects (Puerto Inca and Pasaje) on the windward side from the Ecuadorian Pacific coast (near sea level) to the top of the mountain range (∼4,000 m). We analyzed δD and δ 18 O values from tributaries along three transects in the Inter-Andean valley. Two of them have been conducted in the Cuenca Basin along the Yanuncay and Burgay Rivers and one further south in the Nabón Basin to 1) test whether the δD and δ 18 O values of stream waters reflect the presence of an orographic rain shadow on the leeward side of the Western Cordillera, 2) analyze surface waters sourced at high elevations, and 3) evaluate the influence of the mixing between Pacific and Atlantic air masses as well as from the Amazon rainforest on δD and δ 18 O values in precipitation. The deuterium excess values defined as d δD −8xδ 18 O (Craig and Gordon, 1965) have been used to estimate the amount of evaporation in meteoric water that may have affected this depression area (e.g., Windhorst et al., 2013).
At each sampling site 30 ml of water was collected in polyethylene bottles with little to no air in the closed bottles. Samples were stored in the dark at room temperature until returned to the laboratory for analysis. Measurements of stable hydrogen (δD) and oxygen (δ 18 O) isotope ratios were carried out on 1 ml aliquots using an LGR LWIA-24d (CRD Laser Spectroscopy) liquid isotope water analyzer in the joint Goethe University-Senckenberg BiK-F Stable Isotope Facility, Frankfurt. δD and δ 18 O values were corrected against internal lab standards that are calibrated against VSMOW. The analytical precision is 1.0 and 0.3‰ (both 2σ) for δD and δ 18 O, respectively. Absolute stable isotope values range from −15 to −83‰ for δD and −3.2 to −12.0‰ for δ 18 O (Figure 2 and Supplementary Table S1).
Sampling perennial streams provides an amount-weighted long-term average of precipitation for each catchment, but can lead to an underestimation of the elevation at which the majority of the precipitation falls, especially in high-relief or large catchments areas (Currie, et al., 2005;Rowley and Garzione, 2007;Quade et al., 2011;Schemmel et al., 2013). We calculated mean catchment elevations for each sample using an elevationweighted flow accumulation model in ESRI ® ArcGISTM 10.0 based on version 11 of the National Aeronautics and Space Administration (NASA) ASTER Global Digital Elevation Model at a spatial resolution of 1 arc-second (∼30 m). δ 18 O and δD lapse rates use results from all water samples except 1) WS21 (lake de Busa; Pasaje transect), WS30 and WS31 (lake and related stream; Nabón Basin) that reflect evaporative lake conditions, 2) WS61 and WS62 (near Azogues; Cuenca Basin) affected by urban pollution and, 3) WS72 (Canar River; Puerto Inca transect) for which an accurate mean catchment elevation calculation is difficult due to large catchment size and insignificant relief.

RESULTS
Two main observations characterize our δD and δ 18 O data. 1) Air masses from the Pacific Ocean that directly rise across the Western Cordillera (Puerto Inca transect) experience Rayleigh distillation on the windward side; δD and δ 18 O values define a linear relationship between δ 18 O and altitude of -0.15‰/100 m ( Figure 3A) (δD −1.4‰/100 m; Figure 3B). 2) The δD and δ 18 O values of precipitation in the Inter-Andean valley cannot be directly correlated with elevation; they display additional variability that can be explained by a combination of factors such as mixing of air masses from the Pacific, the Atlantic and the Amazon Basin, evaporation, and seasonality.

Spatial Distribution of δD and δ 18 O Values
We observe a generally good correlation between δD and δ 18 O values of surface water and elevation at the map scale of southern Ecuador. On the windward flanks of the Western Cordillera, between Puerto Inca and El Cajas National Park, low elevation areas (0 < mean catchment elevations <2000 m) display relatively high δD and δ 18 O values ranging from −42 to −36‰ and −7.2 to −6.3‰, respectively, and contrast mountainous areas (2000 m < mean catchment elevations <4200 m) with δD −83 to −48‰ and δ 18 O −12.0 to −7.8‰ for δ 18 O (Figures 1,2 and Supplementary Table S1). We additionally collected water samples further south between ∼50 m and ∼2,800 m elevation along the Pasaje transect ( Figure 1A). All samples show strong correlation with elevation with δ 18 O values varying from −3.2 to −10.6‰ between the lowest (∼300 m) and highest (∼3000 m) mean catchment elevation while equivalent δD values range between −15 and −71‰ ( Figures 1C,2 and Supplementary Table S1). The difference in δD and δ 18 O values between lowland and mountainous areas on the windward flanks of the Western Cordillera is also observed in deuterium excess values with higher d-excess values (d 15.0 ± 3.5) below 2,000 m mean catchment elevations when compared to the highlands (d 11.0 ± 3.4) (Supplementary Figure 1S).
We further collected water samples between the Western and Eastern Cordilleras, in the Cuenca Basin and the Nabón area ( Figure 1A) including tributaries of the Yanuncay River with sampling elevations varying from 3,239 and 2,689 m (Supplementary Table S1). δ 18 O values display large variability between −11.2 and −9.6‰ and δD values are low  Table S1). We further focused on the north-north east part of the Cuenca region where we sampled tributaries of the Burgay River between Azogues and La Escalera ( Figure 1A). δ 18 O and δD values vary from −10.6 to −9.0‰ and −65 to −58‰, respectively ( Figure 2 and Supplementary Table S1).
Finally, we collected water samples from the Nabón area ( Figure 1A), located within close proximity of the Amazon rainforest. Sampling occurred between 2,340 and 2,754 m of elevation. δ 18 O and δD values vary between −9.28 and −7.52‰ and −59 to −44‰ respectively and are generally higher than those obtained from the two other areas investigated in the Inter-Andean valley (Figure 2 and Supplementary Table S1). Although mean catchment elevations are systematically above 2,000 m elevation, d-excess values are generally higher than those in high areas of the windward side of the Western Cordillera with d 14.0 ± 3.7 for Yanuncay, d 17.1 ± 3.2 for Burgay, and d 12.8 ± 7.4 for Nabón (Supplementary Table S1 and Supplementary Figure 1S).

Meteoric Water Lines
The δD and δ 18 O values of all our surface water samples collected in southern Ecuador define a Local Meteoric Water line (LMWL) with δD 7.57 δ 18 O + 10 (R 2 0.94) (Figure 4). When plotting only results from the windward side of the Western Cordillera (Puerto Inca and Pasaje transects) we obtain a meteoric water line with δD 7.83 δ 18 O + 10.68 (PPMWL, R 2 0.94) (Figure 4). The close resemblance of the LMWL and PPMWL with the GMWL (δD 8.17 δ 18 O + 10.35; Rozanski et al. (1993) highlights the robustness of our results.

Establishment of Isotopic Lapse Rates
We evaluated the magnitude of δD and δ 18 O gradients across the Western Cordillera based on the results obtained on the windward side of the range. Some studies have constrained the FIGURE 3 | (A) δ 18 O of river water vs. mean catchment elevation for all data (n 83, black diamonds) defining a slope of −1.8‰/ km (or −0.18‰/ 100 m, R 2 0.73). Highlighted using green diamonds are samples collected in the Cuenca basin along the Burgay River that define an isotope-elevation lapse rate of −2.8‰/ km (or −0.28‰/100 m). Inset: Plot of the δ 18 O of river water vs. mean catchment elevation (m) for the Puerto Inca (small black diamonds) and Pasaje (small white diamonds) transects (windward side of the Western Ecuadorian Cordillera). Note that both transects provide a same lapse rate of −1.5‰/ km (or −0.15‰/100 m). (B)δD of river water vs. mean catchment elevation for all data (n 83, black squares) providing a slope of −14.7‰/ km (or −1.47‰/100 m, R 2 0.79). Highlighted using green squares are samples collected in the Cuenca basin along the Burgay River that define an elevation lapse rate of −11‰/ km (or −1.1‰/100 m). Inset highlights data from the Puerto Inca and Pasaje transects plotted against mean catchment elevation. The decrease in δD values on the windward side of the Western Cordillera allows to define an isotopic lapse rate for both transects of −14.7‰/ km (or −1.47‰/100 m).  Rozanski et al. (1993) (Windhorst et al., 2013) or shallow groundwater springs (Maldonado et al., 1995) or by using International Atomic Energy Agency (IAEA) weather stations (Rozanski and Araguas-Araguas, 1995;Garcia et al., 1998). Here, we use a flow accumulation model in ArcGIS (see above). δ 18 O values of samples collected along the Puerto Inca transect and plotted against mean catchment elevation yield a slope of −0.15‰/100 m ( Figure 3A; R 2 0.88, n 19). The δD vs. elevation relationship displays a linear regression with a slope of −1.4‰/100 m for δD ( Figure 3B; R 2 0.93, n 19). This result is also supported by the linear regression calculated from the Pasaje transect that gives a slope of −0.15‰/100 m (R 2 0.65, n 30) for δ 18 O and −1.4‰/100 m for δD (R 2 0.78, n 30) ( Figures 3A,B).
In the Inter-Andean valley, the correlation between δ 18 O values and elevation is absent, especially along the Yanuncay River and Nabón area ( Figure 1A). An isotope-elevation relationship of −0.28‰/100 m for δ 18 O (R 2 0.52, Figure 3A) and −1.1‰/100 m for δD (R 2 0.33, Figure 3B) can be defined from samples collected to the north of Cuenca (Burgay River) but display low correlation coefficients.

Impact of Pacific Air Masses on Stable Isotopes in Precipitation
The spatial patterns of δD and δ 18 O values of stream waters collected in southern Ecuador across the Western Cordillera and the Inter-Andean depression reflect the topography of this region. First, samples collected from the windward flanks of the Western Cordillera between Puerto Inca and El Cajas National Park ( Figure 1A) show a net decrease in both δD and δ 18 O values (50‰ in δD and 6‰ in δ 18 O from near sea level to ∼ 4,000 m) across the mountain range ( Figure 1C). This decrease in both δ 18 O and δD values allows to define an isotopic lapse rate of -0.15‰/100 m for δ 18 O (R 2 0.88; Figure 3A) and -1.4‰/100 m for δD (R 2 0.93; Figure 3B). We interpret this lapse rate to reflect the altitude effect for δD and δ 18 O originating from Pacific air masses and orographic rainout on the western facing slopes of the Ecuadorian Andes.
Although calculated from samples sourced at lower elevation, the lapse rate from the Pasaje transect provides a δ 18 O and δD vs. altitude relationship of -0.15‰/100 m (δ 18 O; R 2 0.65; Figure 3A) and -1.4‰/100 m (δD; R 2 0.78; Figure 3B) and confirms the altitude effect on the isotope composition of tropical rains observed at higher elevation. These lapse rates are lower than those compiled or modeled for mid-latitude settings (-0.28 ‰/100 m in δ 18 O or -2.0 ‰/100 m in δD) (e.g., Poage and Chamberlain, 2001;Quade et al., 2011). However, they are in good agreement with isotope-elevation relationships defined from the isotopic composition of tropical rains in Cameroon (−0.156‰/100 m in δ 18 O; Gonfiantini et al., 2001), in the Colombian Eastern Cordillera (-0.18‰/100 m in δ 18 O and −1.46‰/100 m in δD; Saylor et al., 2009) and in Ecuador (−0.17‰/100 m in δ 18 O; Garcia et al., 1998) using water samples from springs and IAEA weather stations along two transects across the Western and Eastern Cordillera near 1 and 3°S latitude (Supplementary Table S1 and Supplementary Figure 2S). In the latter study, δ 18 O water and δD water values are influenced by the amount of precipitation which varies over the year and causes D and 18 O-depleted precipitation during the wet season. In addition to this amount effect, Garcia and coauthors highlight a latitudinal effect in their dataset which is also well illustrated in our data, as δ 18 O water values are ∼ −3‰ more negative to the north along the Puerto Inca transect (Figures 1C,2). The latitudinal difference for our low elevation sites that share the same Pacific moisture source can be explained by a lower precipitation amounts in the south (from Pasaje to La Tarabita) when compared to the north (Puerto Inca).

Comparison Between Results Obtained Along the Puerto Inca and Pasaje Transects
Samples collected along the Puerto Inca and Pasaje transects define a similar elevation lapse rate of −0.15‰/100 m for δ 18 O. However, we note a better correlation for Puerto Inca than for Pasaje that can be explained by two main factors shared by Puerto Inca samples: 1) the location on the windward side of the Western Cordillera and, 2) an unique moisture source (the Pacific Ocean). Although the main moisture source for samples collected along the Pasaje transect is provided by the Pacific trade winds, we cannot preclude the possibility of mixing with Atlantic air masses that experienced evapo-transpiration over the Amazon (Salati et al., 1979). This is consistent with the observation of moist air masses along the Pasaje transect through side valleys (e.g., to the south-east of La Tarabita, black arrow on Figure 1A). In addition, evaporation associated with the dry climate that characterizes part of this transect could explain some of the variability in the results with enrichment of 18 O and D (e.g., Schemmel et al., 2013) observable in some samples (e.g., WS13 and WS24, Supplementary Table S1).

The Inter-Andean Valley
In contrast to samples from the windward side of the Western Cordillera, δ 18 O and δD values from the Cuenca region, in the Inter-Andean valley and further south in the Nabón Basin, do not show a clear correlation with elevation.
Data acquired along the Puerto Inca transect on the leeward side of the Western Cordillera display relatively low δ 18 O and δD values that can be explained by Rayleigh distillation of the heavy isotopes on the windward side ( Figure 1C). However, together with data acquired from tributaries along the Yanuncay River (from sample 51 to 60 on Figure 1C and Supplementary Table S1), the δ 18 O and δD values on the leeward side cannot be correlated with elevation and show increased variability. However, leeward δ 18 O and δD vs. elevation gradients are inherently more complex once an orographic rain shadow develops (e.g., Quade et al., 2011). In addition to local evaporation that may shift near surface ground water δ 18 O and δD values to higher values (consistent with d 14.0 ± 3.7), 18 O or D-depleted precipitation from the windward side, moisture mixing, and continental water vapor recycling represent multiple and confounding factors that render the interpretation of leeward rainfall δ 18 O and δD signals difficult (e.g., Blisniuk and Stern, 2005;Schemmel et al., 2013). Also, stable isotopic variability in our dataset could reflect the passage of the ITCZ, which significantly affects this area as highlighted by the BMR (Celleri et al., 2007). However, the ENSO system seems to have a negligible effect on the basin's seasonal distribution of rainfall due to the high elevation of the Cuenca area (1840-4680 m; Celleri et al., 2007).
Second, the δ 18 O and δD values acquired north of Cuenca, between Azogues and La Escalera ( Figure 1A) show a weak correlation with altitude that allows to define a δ 18 O vs. elevation relationship of −0.28‰/100 m with R 2 0.52 (−1.1‰/100 m with R 2 0.33 for δD) (see green line and samples on Figure 3). While the correlation coefficient is moderate, the isotopeelevation relationship is close to −0.22‰/100 m for δ 18 O and −1.12‰/100 m for δD defined by Windhorst et al. (2013) who investigated the isotopic composition of precipitation in South Ecuadorian montane cloud forests from 1,800 to 2,800 m elevation using open rainfall sampling (on the east-facing slopes of the Andes in the San Francisco Valley). Windhorst et coauthors have highlighted an enrichment of heavy isotopes during southeasterly trade winds that carry re-evaporated and recycled precipitation from the Amazon Basin.
Results obtained from samples collected in the Nabón Basin display higher δ 18 O (>2‰), and δD (>13‰) values than those measured from samples in the Cuenca Basin. No elevation lapse rate can be defined from these values that vary from −9.3 to −7.5‰ for δ 18 O, and −59 and −44‰ for δD. This lack of correlation with elevation could be partly explained by the small range of mean catchment elevations, which does not exceed ∼600 m. In addition, and as highlighted in previous work conducted in South America (e.g., Nieto-Moreno et al., 2016), the variation of these tropical rainfall values could reflect a mixed signal resulting from different air mass trajectories.

CONCLUSION
We analysed the oxygen and hydrogen isotope ratios of surface waters from tributaries across the Ecuadorian Northern Andes to establish a δ 18 O and δD vs. elevation gradients near the Equator (∼3°S); essential for stable isotope paleoaltimetry reconstructions.
The west facing slopes of the Western Cordillera are subject to moisture incoming from the Pacific which gets orographically lifted and produces a lapse rate of −0.15‰/100 m for δ 18 O (R 2 0.88, n 19) and −1.4‰/100 m for δD (R 2 0.93, n 19) that takes into account precipitation from near sea level up to 4,000 m elevation (Puerto Inca transect). This isotope-elevation relationship is supported by results acquired further south along the Pasaje transect that provides a similar result [−0.15‰/100 m with R 2 0.65 (n 30) for δ 18 O and −1.4‰/ 100 m for δD with R 2 0.78 (n 30)], although covering a lower range of mean catchment elevation.
Evaluating the magnitude of δ 18 O and δD gradients across the Inter-Andean depression is more difficult as this domain receives air masses from the Pacific, Atlantic, and Amazon Basin. In addition, part of this region experiences the seasonal passage of the ITCZ that impacts the temperature and humidity of air masses. Therefore, the δ 18 O and δD values obtained from our water samples here reflect a mixed signal resulting from a combination of factors including air mass mixing, evaporation, humidity.
In agreement with previous studies conducted in Ecuador (e.g., Maldonado et al., 1995;Garcia et al., 1998;Jackson et al., 2019;Supplementary Table 1S and Supplementary Figure 2S) and other tropical regions (e.g., Gonfiantini et al., 2001;Saylor et al., 2009), our work demonstrates that an empirical relationship between elevation and the stable isotope composition of precipitation and surface waters can be established at (or near) the Equator. Therefore, the δ 18 O and δD elevation relationships of −0.15‰/100 m for δ 18 O and −1.4‰/100 m for δD may serve as a guide for stable isotope paleoaltimetry reconstructions at tropical latitudes.

DATA AVAILABILITY STATEMENT
The original contributions presented in the study are included in the article/Supplementary Material, further inquiries can be directed to the corresponding author.

AUTHOR CONTRIBUTIONS
AG wrote the manuscript, made the figures, and conducted the study (collection of water samples in the field, results analysis and interpretation). CW participated in writing the manuscript, made some figures and collected samples in the field. MR collected samples in the field, participated in the results analysis and interpretation. AM participated in writing and interpreting the data.

ACKNOWLEDGMENTS
We thank Ulrich Treffert (Senckenberg BiK-F) for continuous laboratory support. Comments and suggestions by L. J. Jackson, two anonymous reviewers and the editor, A. Licht, are gratefully acknowledged.