Marín Pompa-García

Facultad de Ciencias Forestales, Universidad Juárez del estado de Durango, Río Papaloapan y Blvd. Durango s/n, col. Valle del Sur, 34120 Durango, Durango, México. Corresponding author; e-mail: mpgarcia@ujed.mx, work.shapes@gmail.com

Xanat Antonio Némiga

Facultad de Geografía, Universidad Autónoma del Estado de México, Cerro Coatepec s/n, Ciudad Universitaria, 50110 Toluca, Estado de México, México

Received April 25, 2014; accepted October 21, 2014

RESUMEN

La Oscilación del Sur El Niño (ENSO, por sus siglas en inglés) es el principal fenómeno de circulación de gran escala que ocasiona variabilidad climática en el norte de México. El desafío actual consiste en entender sus consecuencias para los procesos climáticos y ecológicos de los ecosistemas. En este contexto, se comparó el grado de asociación de tres diferentes índices de ENSO con la precipitación local (P) en el norte de México, y se utilizaron series dendrocronológicas (cronologías de anillos de crecimiento [TRI, por su siglas en inglés]) de Pinus cooperi para valorar su impacto en el crecimiento forestal. Los resultados mostraron un asociación importante entre ENSO, la precipitación del invierno anterior y el TRI (r > 0.5, p = 0.05), lo cual indica que hay una relación directa entre las fases cálidas de ENSO y el crecimiento de los árboles. El índice multivariado de ENSO explicó ligeramente mejor que otros índices la conexión entre P y el crecimiento radial. Estos resultados pueden apoyar futuras investigaciones sobre los efectos de ENSO en el clima local y los ecosistemas forestales.

ABSTRACT

El Niño Southern Oscillation (ENSO) is the most important large-scale circulatory phenomenon that causes climatic variability in northern Mexico. The current challenge is to understand its consequences for both local climate and ecological processes of ecosystems. Within this context, we compared the degree of association of three different ENSO indices with local seasonal precipitation (P) in northern Mexico, and used dendrochronological series (tree-ring chronologies [TRI]) of Pinus cooperi to assess the impact of forest growth. The results showed a strong association between ENSO, previous winter precipitation and TRI (r > 0.5, p = 0.05), indicating a positive relationship between warm ENSO phases and subsequent tree growth. The multivariate ENSO index was slightly better at explaining the connection between P and radial growth than other indices. These results could be used to support further research on the effects of ENSO on local climate and forest ecosystems.

Keywords: winter precipitation, Pinus cooperi, tree rings, Niño 3.4, MEI, MEI.ext.

1. Introduction

The teleconnections of El Niño Southern Oscillation (ENSO) with global climate have been widely documented (e.g., Peralta, 2008; Birk et al, 2010). The different phases of ENSO are strongly associated with the occurrence of extreme climatic phenomena, including tropical cyclone incidence (e.g. Gutzler et al. 2013). This is a matter of major concern because such climatic variations add to the stresses imposed on ecosystems by anthropogenically induced global warming (e.g., Williams et al 2013). This becomes vitally important in geographic areas that are highly sensitive to ENSO, but where its effects allow the prediction of seasonal-scale climate behavior with some degree of confidence (Wolter et al., 1999; Gutzler et al., 2013).

The relationships of ENSO with the aforementioned phenomena have been assessed using conventional ENSO indices, such as the Southern Oscillation Index and the Niño 3.4 index. However, the use of these indices is complicated as a result of their variations and climate responses through annual cycles, which reduce their reliability (Wolter and Timlin, 1998). An alternative index is the multi-variate ENSO index (MEI), which is the first principal component of six observed fields (Wolter and Timlin, 1993). However, a major limitation of the MEI is the reduced time span of available records, i.e., from 1950 to the present. To overcome this, an extended MEI (MEI.ext) was proposed by Wolter and Timlin (2011), who generated index values from 1871 to 1950. They claim that the MEI is more reliable and robust relative to conventional indices; however, there has been no comparative evaluation of its potential in explaining local climate.

As ENSO remains the most relevant large-scale circulatory phenomenon that induces climatic variability, the important issue is to understand its effects on local climate and thus, on the ecological processes of ecosystems. Therefore, we performed a comparison of the degree of association of three different ENSO indices with local seasonal precipitation, and related them to the radial growth of Pinus cooperi. This coniferous tree, which has high ecological and economic value, is representative of northern Mexico and its growth has previously been shown to relate to large-scale circulatory patterns (Cruz et al., 2008; Pompa-García and Jurado-Ybarra, 2013).

2. Methods

2.1 Study area

The study area, bounded by the coordinates 24° 13'-23° 44' N, 105° 22'-105° 34' W, is located in the temperate ecosystem of the Sierra Madre Occidental in Mexico, where P. cooperi is abundant (Fig. 1). Pompa-García and Jurado-Ybarra (2013) reported a teleconnection response of precipitation in this area to ENSO. Tree-ring samples were collected from five sampling locations within the study area for growth evaluation. Using standard dendrochronological techniques, local tree-ring chronologies (TRI) were generated (Pompa-García et al., 2013a), which were taken as representatives of the common climate signal for the site.

2.2 Data and statistical analysis

To evaluate how ENSO affects local climate, we considered the instrumental records from two meteorological stations located nearest to the source of the dendrochronology data. These weather stations, called El Salto and Otinapa, belong to the Comisión Nacional del Agua (National Water Commission) (CNA, 2012). We organized and analyzed the historical records from 1950 to 2005 for the following climate variables: previous summer precipitation (PSP), previous winter precipitation, (PWP), and current summer precipitation (CSP). These variables were calculated by adding the precipitation in millimeters recorded over different time spans, for which the current year corresponds to the year of tree-ring formation: PSP, from June to September in the previous year; PWP, from the previous October to the current February; and CSP, from June to September in the current year (which is the growing season).

We related these variables to values of the following ENSO indices: MEI, MEI.ext, and Niño 3.4 for 1950-2005, considering lags from the previous-year January to the current-year December. The MEI is the first seasonally varying principal component of six atmosphere-ocean variable fields in the Tropical Pacific basin (Wolter and Timlin, 1993): sea level pressure, zonal and meridional components of surface wind, sea surface temperature, surface air temperature, and total cloud fraction. We retrieved its values from http://www.esrl.noaa.gov/psd/ENSO/MEI/table.html. As an alternative to Niño 3.4, the MEI.ext, which is based on sea level pressure and sea surface temperature, is potentially more reliable (Wolter and Timlin, 2011). Information regarding this index is available at http://www.esrl.noaa.gov/psd/ENSO/MEI.ext/table.ext.html. The Niño 3.4 index is a measure of sea surface temperature anomaly in the east-central equatorial Pacific, and it is available athttp://iridl.ldeo.columbia.edu/SOURCES/.Indices/.nino/.EXTENDED/.

3. Results

There is a strong association between the ENSO index, local seasonal precipitation, and the behavior of the tree-ring series (Fig. 2). This yielded Pearson correlation coefficients from -0.25 to 0.53 (with significances at a 0.05 level). Two of the three considered ENSO indices revealed strong coherence with CSP and tree growth; the exception was Niño 3.4, which exhibited no coherence at all.

The values of ENSO indices from the previous-year May to the current-year June showed the highest correlation with PWP. ENSO values from the previous May to the current April also had a consistent and positive relation with PSP in Niño 3.4. It was found that such a relation extends up to the current May, although in a weakened form. ENSO values from the previous May to the current January showed the highest correlation with CSP. However, the Niño 3.4 index showed a negative association in the current-year April and May. A similar pattern was found for TRI, which had the closest association with ENSO in the winter before the growing season.

The bootstrapped procedure conducted on TRI and monthly ENSO indices presented positive associations with radial growth over the study area.

Positive and significant correlations were consistently found for PWP, PSP and TRI from the previous May to the current May. Pearson's correlation coefficient (r) for CSP were smaller (< 0.29) and negatives (-0.24, to -0.25) in current April and May, respectively. The graphical results for each of the indices show that Niño 3.4 has the most variable pattern, because it even yielded negative relations between CSP and the previous winter values. In contrast, the MEI and MEI.ext exhibited the most consistent and homogenous behavior throughout the 24 studied months. The MEI showed particularly strong correlation with PWP and CSP, while its correlation with TRI was unclear. In general, there was a period of strong correlation from the previous May to the current April between seasonal precipitation and the radial growth of trees (Fig. 2).

Graphs showing the influence of the large-scale atmospheric circulation patterns of ENSO (measured with the three selected indices) on P and its effect on tree-radial growth TRI are displayed in Figure 3. PWP exhibits strong association with ENSO and has an effect on TRI. This relation is stronger in the wet years of El Niño and weaker in the dry years of La Niña (Fig. 4).

4. Discussion

Historically, ENSO has been linked with interannual variability of climate over decades and even centuries (Li et al., 2013). There is strong variability at the 3- to 7-year timescale as well as on inter-decadal times-cales between 12 and 15 years (Birk et al., 2010). However, our study is the first to use ENSO records over 55 years, and to examine its influence on local climate and the ecological processes of a temperate forest in northern Mexico.

Seager et al. (2009) and Méndez-González et al. (2007) have previously shown connections between ENSO and precipitation in northern Mexico. Here, we show that the strongest correlations with ENSO are exhibited by PWP and TRI. This shows a positive relation whereby warm ENSO phases cause increased winter precipitation and subsequent tree growth. According to our results, ENSO is likely to enhance growth of P. cooperi via positive effects related to soil moisture in the preceding winter (Figs. 3, 4). Several authors have argued that damp winters contribute to tree growth because the rain is usually of low intensity, which favors high infiltration and low evapotranspiration, resulting in a positive soil water balance(Constante-García et al., 2009; Pompa-García et al., 2013a, 2013b). These findings confirm the hypothesis of Chen et al. (2010), who proposed that damp winters contribute to tree growth. In contrast, Meko et al. (2013) reported that ENSO affects tree growth via strong monsoon-specific precipitation signals.

Our results show that the correlations between ENSO and the current-summer and previous-summer precipitation are weaker. In summer, ENSO conditions can increase precipitation, but to a lesser extent than in winter, because of the substantial difference between the winter and summer teleconnections to subtropical North America (Seager et al, 2009), which can be complicated by the frequent change of ENSO phase between winter and the following summer (Stahle et al, 2011). This reveals a clearly marked response between summer and winter, which is important to understand given the strong season-ality of precipitation and ecology within the region (Therrell et al, 2004; Griffin et al, 2011).

Compared with the MEI and MEI.ext, the relationships in Mexico to the Niño 3.4 index have been studied thoroughly. For example, it has been found that ENSO influences precipitation and runoff in northern Durango (Villanueva-Díaz et al, 2007), which agrees with the findings of Cerano-Paredes et al. (2011) for the upper basin of the Nazas River. One of the few studies to use the MEI and MEI. ext, performed by Herrera-Cervantes et al., (2010), reported that patterns associated with the MEI index vary spatially according to regional topography.

Here we show for Mexico that a strong teleconnection exists between ENSO and monthly precipitation on interannual timescales. Precipitation has the strongest positive teleconnection with ENSO in February, December, and November. In June, August, and September, it has a slightly negative teleconnection with ENSO; while in April, October, and July it shows no relation. Correlation between precipitation and ENSO, measured using the MEI, seems to be stronger in the northern parts of the country, especially near the Pacific Ocean, whereas the negative correlations are located in the south. During the warm phases of ENSO, this causes precipitation to increase in higher latitudes and to decrease in lower latitudes (Méndez-González et al., 2007). Furthermore, a preliminary prognosis of the MEI by these authors indicated the likelihood of ENSO to have a stronger effect around the world in years to come. For instance, Seager et al, (2012) reported that interannual variability of precipitation minus evaporation becomes stronger in the 21st century compared to the 20th.

The relation between ENSO and climatic change is not yet clear (Li et al., 2013). Thus, how best to generate scenarios of regional climate change remains a current research topic that will continue to be debated in the future (Conde et al, 2011). A number of authors have recommended evaluating the potential impacts of climate change using techniques such as the principle of maximum entropy (Gay and Estrada, 2010).

Moreover, our findings revealed different responses of P and TRI to ENSO depending on the ENSO index used; the MEI and MEI.ext indicated the strongest influence, particularly for PWP and TRI. While all other ENSO indices are fixed geographically, the MEI accounts for the spatial and temporal evolution of climate anomalies within the seasonal cycle (Wolter and Timlin, 2011). Despite this benefit, this means that some inconsistencies can occur because of poor data coverage away from major coastlines (Worley et al., 2005). Furthermore, the MEI and MEI.ext are based on multiple variables, rather than just one variable (SST), as in the case of the Niño 3.4 index. Although the MEI has a very limited temporal span, the MEI.ext has achieved reliable measurements for longer time spans (Wolter and Timlin, 2011). The tropical Pacific SST-Mexico precipitation relationship, associated with earlywood and latewood width (Griffin et al., 2011; Meko et al., 2013), could reveal valuable temporal information regarding seasonal precipitation and ENSO variation for the study area.

The results presented show clear evidence of the teleconnection of ENSO with local seasonal precipitation and tree growth in northern Mexico. Winter precipitation has a particularly strong correlation to ENSO. Radial growth shows considerable dependence on the climatic conditions of the winter months preceding the growing season and hence, on ENSO conditions. The MEI explains seasonal precipitation and radial growth slightly better than the other indices assessed in this study. As ENSO clearly affects local climate and ecological processes (e.g., radial growth) in northern Mexico, our results constitute a useful predictor of its potential future impact.

Acknowledgments

We want to thank the support given by CENID-RASPA Lab from INIFAP in Mexico, which supported the gathering and processing of dendrochronological data. The authors are grateful to the editorial team and anonymous reviewers for their helpful reviews. In particular, we recognize Richard Seager of Lamont Doherty Earth Observatory for his useful comments and suggestions that improved this manuscript.

References

Biondi F. and J. Waikul, 2004. DENDROCLIM2002: A C++ program for statistical calibration of climate signals in tree-ring chronologies. Comp. Geosci. 30, 303-311, doi:10.1016/j.cageo.2003.11.004.         [ Links ]

Birk K., A. R. Lupo, P. Guinan and C. E. Barbieri, 2010. The interannual variability of midwestern temperatures and precipitation as related to the ENSO and PD. Atmósfera 23, 95-128.         [ Links ]

Cerano-Paredes J., J. Villanueva-Díaz, R. D. Valdez-Cepeda, J. G. Arreola-Ávila and V. Constante-García, 2011. Effects of the El Niño Southern Oscillation on precipitation in the upper Nazas river watershed. Chapingo 17, 207-215.         [ Links ]

Chen P., C. Welsh and A. Hamann, 2010. Geographic variation in growth response of Douglas-fir to inter-annual climate variability and projected climate change. Glob. Change Bio. 16, 3374-3385, doi:10.1111/j.1365-2486.2010.02166.x.         [ Links ]

Cleaveland M. K., D. W. Stahle, M. D. Therrell, J. Villanueva-Díaz and B. T Burns, 2003. Tree-ring reconstructed winter precipitation and tropical tele-connections in Durango, Mexico. Climatic Change 59, 369-388.         [ Links ]

Conde C., F. Estrada, B. Martínez, O. Sánchez and C. Gay, 2011. Regional climate change scenarios for Mexico. Atmósfera 24, 125-140.         [ Links ]

Constante-García V., J. Villanueva-Díaz, J. Cerano-Paredes, E. H. Cornejo-Oviedo and S. Valencia-Manzo, 2009. Dendrocronología de Pinus cembroides Zucc. y reconstrucción de precipitación estacional para el Sureste de Coahuila. Ciencia Forestal en México 34, 17-38.         [ Links ]

CNA, 2012. Datos climáticos de estaciones meteorológicas de Durango: El Salto y Otinapa. Comisión Nacional del Agua, México. Disponible en: http://smn.cna.gob.mx/emas/ [last accessed on February 8, 2013]         [ Links ].

Cruz C. F., P. H. M. de los Santos and L. J. R. Valdez, 2008. Compatible taper-volume system for Pinus cooperi Blanco in Durango, México. Agrociencia 42, 473-485.         [ Links ]

Gay C. and F. Estrada, 2010. Objective probabilities about future climate are a matter of opinion. Climatic Change 99, 27-46.         [ Links ]

Holmes R. L, 1983. Computer-assisted quality control in tree-ring dating and measurement. Tree-Ring Bulletin 43, 69-78.         [ Links ]

Griffin D., D. M. Meko, R. Touchan, S. W. Leavitt and C. A. Woodhouse, 2011. Latewood chronology development for summer-moisture reconstruction in the U.S. Southwest. Tree-Ring Res. 67, 87-101, doi:10.3959/2011-4.1.         [ Links ]

Gutzler D. S., K. Wood, E. Ritchie, A. Douglas and M. D. Lewis, 2013. Interannual variability of tropical cyclone activity along the Pacific coast of North America. Atmósfera 26, 149-162.         [ Links ]

Herrera-Cervantes H., S. E. Lluch-Cota, D. B. Lluch-Cota, G. Gutiérrez de Velazco and D. Lluch-Belda, 2010. ENSO influence on satellite-derived chlorophyll trends in the Gulf of California. Atmósfera 23, 253-262.         [ Links ]

Li J., S.-P. Xie, E. R. Cook, M. S. Morales, D. A. Christie, N. C. Johnson, F. Chen, R. D'Arrigo, A. M. Fowler, X. Gou and K. Fang, 2013. El Niño modulations over the past seven centuries. Natural Climate Change 3, 822-826, doi:10.1038/NCLIMATE1936.         [ Links ]

Meko D. M., R. Touchan, J. Villanueva-Díaz, D. Griffin, C. A. Woodhouse, C. L. Castro, C. Carillo and S. W. Leavitt, 2013. Sierra San Pedro Mártir, Baja California, cool-season precipitation reconstructed from earlywood width of Abies concolor tree rings. J. Geophys. Res. Biogeosci. 118, 1660-1673, doi:10.1002/ 2013JG002408.         [ Links ]

Méndez-González J., J. J. Návar-Cháidez, H. González-Rodríguez and J. E. Treviño González, 2007. Teleconexiones del fenómeno ENSO a la precipitación mensual en México. Ciencia UANL 10, 290-298.         [ Links ]

Peralta Hernández A. R., L. R. Barba Martínez, V. O. Magaña Rueda, A. D. Matthias and J. J. Luna-Ruiz, 2008. Temporal and spatial behavior of temperature and precipitation during the canícula (midsummer drought) under El Niño conditions in central Mexico. Atmósfera 21, 265-280.         [ Links ]

Pompa-García M., J. Cerano-Paredes and Z. P. Fulé, 2013a. Variation in radial growth of Pinus cooperi in response to climatic signals across an elevational gradient. Dendrochronologia 31,198-204.         [ Links ]

Pompa-García M., F. J. Rodríguez-Flores, J. Cerano-Paredes, R. D. Valdez-Cepeda and F. A. Roig, 2013b. Effect of monthly precipitation on the radial growth of Pseudotsuga menziesii in northern Mexico. African Journal of Agricultural Research 8, 1636-1640, doi:10.5897/AJAR12.2074.         [ Links ]

Pompa-García M. and E. Jurado-Ybarra, 2013. Seasonal precipitation reconstruction and teleconnections with ENSO based on tree ring analysis of Pinus cooperi. Theor. Appl. Climatol. 117, 495-500, doi:10.1007/s00704-013-1018-6.         [ Links ]

Seager R., M. Ting, M. Davis, M. Cane, N. Naik, J. Nakamura, C. Li, E. Cook and D. Stahle, 2009. Mexican drought: an observational modeling and tree ring study of variability and climate change. Atmósfera 22, 1-31.         [ Links ]

Seager R., N. Naik and L. Vogel, 2012. Does global warming cause intensified interannual hydroclimate variability? J. Climate 25, 3355-3372.         [ Links ]

Stahle D. W., J. Villanueva-Díaz, D. J. Burnette, J. Cerano-Paredes, R. R. Heim, F. K. Fye, R. Acuña, M. D. Therrell, M. K. Cleaveland and D. K. Stahle, 2011. Major Mesoamerican droughts of the past millennium. Geophys. Res. Lett. 38, doi:10.1029/2010GL046472.         [ Links ]

Therrell M. D., D. W. Stahle and R. Acuña Soto, 2004. Aztec drought and the curse of one rabbit. Bull. Am. Meteorol. Soc. 85, 1263-1272, doi:10.1175/BAMS-85-9-1263.         [ Links ]

Villanueva-Díaz J., D. W. Stahle, B. Luckman, J. Cerano-Paredes, M. D. Therrell, M. K. Cleaveland and E. Cornejo-Oviedo, 2007. Winter-spring precipitation reconstructions from tree rings for northeast México. Climatic Change 83, 117-131, doi:10.1007/s10584-006-9144-0.         [ Links ]

Williams A. P., C. D. Allen, A. K. Macalady. D. Griffin, C. A. Woodhouse, D. M. Meko, T. W. Swetnam, S. A. Rauscher, R. Seager, H. D. Grissino-Mayer, J. S. Dean, E. R. Cook, C. Gangodagamage, M. Cai and N. G. McDowell, 2013. Temperature as a potent driver of regional forest drought stress and tree mortality. Nature Climate Change 3, 292-297, doi:10.1038/NCLIMATE1693.         [ Links ]

Wolter K. and M. S. Timlin, 1993. Monitoring ENSO in COADS with a seasonally adjusted principal component index. Proceedings of the 17th Climate Diagnostics Workshop, Norman, Oklahoma. NOAA/NMC/CAC-NSSL-Oklahoma Climate Survey-CIMMS-School of Meteorology of the University of Oklahoma, pp. 52-57.         [ Links ]

Wolter K. and M. S. Timlin, 1998. Measuring the strength of ENSO events - how does 1997/98 rank? Weather 53, 315-324.         [ Links ]

Wolter K., R. M. Dole and C. A. Smith, 1999. Short-term climate extremes over the continental U.S. and ENSO. Part I: Seasonal temperatures. J. Climate 12, 3225-3272.         [ Links ]

Wolter K. and M. S. Timlin, 2011. El Nino/Southern Oscillation behavior since 1871 as diagnosed in an extended multivariate ENSO index (MEI. ext). Int. J. Climatol. 31, 1074-1087.         [ Links ]

Worley S. J., S. D. Woodruff, R. W. Reynolds, S. J. Lubker and N. Lott, 2005. ICOADS Release 2.1 data and products. Int. J. Climatol. 25, 823-842, doi:10.1002/ joc.1166 (CLIMAR-II Special Issue).         [ Links ]

Yocom L. L., P. Z. Fule, P. M. Brown, J. Cerano, J. Villanueva-Diaz, D. A. Falk and O. E. Cornejo, 2010. El Nino-Southern Oscillation effect on a fire regime in northeastern Mexico has changed over time. Ecology 91, 1660-1671.         [ Links ]