On the distinct interannual variability of tropical cyclone activity over the eastern North Pacific

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The curve points are the spherical coordinates relative to a rotated pole N’(270.0°, 0.°) at (a) N’(180.0°, 45.°) at (b) with respect to the original system." ] ] ] "autores" => array:1 [ 0 => array:2 [ "autoresLista" => "Ismael Pérez-García" "autores" => array:1 [ 0 => array:2 [ "nombre" => "Ismael" "apellidos" => "Pérez-García" ] ] ] ] ] "idiomaDefecto" => "en" "EPUB" => "https://multimedia.elsevier.es/PublicationsMultimediaV1/item/epub/S0187623617300036?idApp=UINPBA00004N" "url" => "/01876236/0000002800000003/v2_201709141210/S0187623617300036/v2_201709141210/en/main.assets" ] "itemAnterior" => array:19 [ "pii" => "S0187623617300012" "issn" => "01876236" "doi" => "10.20937/ATM.2015.28.03.01" "estado" => "S300" "fechaPublicacion" => "2015-07-01" "aid" => "73849" "copyright" => "Universidad Nacional Autónoma de México" "documento" => "article" "crossmark" => 0 "licencia" => "http://creativecommons.org/licenses/by-nc-nd/4.0/" "subdocumento" => "fla" "cita" => "Atmósfera. 2015;28:149-60" "abierto" => array:3 [ "ES" => true "ES2" => true "LATM" => true ] "gratuito" => true "lecturas" => array:2 [ "total" => 337 "formatos" => array:3 [ "EPUB" => 31 "HTML" => 245 "PDF" => 61 ] ] "en" => array:11 [ "idiomaDefecto" => true "titulo" => "Recent warming in the Balearic Sea and Spanish Mediterranean coast. Towards an earlier and longer summer" "tienePdf" => "en" "tieneTextoCompleto" => "en" "tieneResumen" => array:2 [ 0 => "es" 1 => "en" ] "paginas" => array:1 [ 0 => array:2 [ "paginaInicial" => "149" "paginaFinal" => "160" ] ] "contieneResumen" => array:2 [ "es" => true "en" => true ] "contieneTextoCompleto" => array:1 [ "en" => true ] "contienePdf" => array:1 [ "en" => true ] "resumenGrafico" => array:2 [ "original" => 0 "multimedia" => array:7 [ "identificador" => "fig0030" "etiqueta" => "Fig. 6" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr6.jpeg" "Alto" => 680 "Ancho" => 1944 "Tamanyo" => 129549 ] ] "descripcion" => array:1 [ "en" => "(a) Changes in the seasonal cycle for SSTs in the Balearic Sea calculated for two time periods. (b) Absolute difference of monthly temperatures between the two periods." ] ] ] "autores" => array:1 [ 0 => array:2 [ "autoresLista" => "María José López García" "autores" => array:1 [ 0 => array:2 [ "nombre" => "María José" "apellidos" => "López García" ] ] ] ] ] "idiomaDefecto" => "en" "EPUB" => "https://multimedia.elsevier.es/PublicationsMultimediaV1/item/epub/S0187623617300012?idApp=UINPBA00004N" "url" => "/01876236/0000002800000003/v2_201709141210/S0187623617300012/v2_201709141210/en/main.assets" ] "en" => array:18 [ "idiomaDefecto" => true "titulo" => "On the distinct interannual variability of tropical cyclone activity over the eastern North Pacific" "tieneTextoCompleto" => true "paginas" => array:1 [ 0 => array:2 [ "paginaInicial" => "161" "paginaFinal" => "178" ] ] "autores" => array:2 [ 0 => array:4 [ "autoresLista" => "Haikun Zhao" "autores" => array:1 [ 0 => array:4 [ "nombre" => "Haikun" "apellidos" => "Zhao" "email" => array:1 [ 0 => "zhk2004y@nuist.edu.cn" ] "referencia" => array:1 [ 0 => array:2 [ "etiqueta" => "*" "identificador" => "cor0005" ] ] ] ] "afiliaciones" => array:1 [ 0 => array:2 [ "entidad" => "Pacific Typhoon Research Center, Key Laboratory of Meteorological Disaster of Ministry of Education, Nanjing University of Information Science and Technology, Nanjing, 210044, China" "identificador" => "aff0005" ] ] "correspondencia" => array:1 [ 0 => array:3 [ "identificador" => "cor0005" "etiqueta" => "*" "correspondencia" => "Corresponding author." ] ] ] 1 => array:3 [ "autoresLista" => "Graciela B. Raga" "autores" => array:1 [ 0 => array:2 [ "nombre" => "Graciela B." "apellidos" => "Raga" ] ] "afiliaciones" => array:1 [ 0 => array:2 [ "entidad" => "Centro de Ciencias de la Atmósfera, Universidad Nacional Autónoma de México, Circuito de la Investigación Científica s/n, Ciudad Universitaria, 04510 México, D.F." "identificador" => "aff0010" ] ] ] ] "resumenGrafico" => array:2 [ "original" => 0 "multimedia" => array:7 [ "identificador" => "fig0005" "etiqueta" => "Fig. 1" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr1.jpeg" "Alto" => 1219 "Ancho" => 942 "Tamanyo" => 151623 ] ] "descripcion" => array:1 [ "en" => "Observed number of tropical cyclones (TCs) reaching at least tropical storm strength in the NHC best track dataset over the Eastern North Pacific (ENP) during the period 1965-2013 for (a) the peak season (June through October) and (b) the whole year (January-December)" ] ] ] "textoCompleto" => "1IntroductionThe eastern North Pacific (ENP) basin (0-30° N, 140-80° W) exhibits a high level of tropical cyclone (TC) activity, being the second most active region in the globe after the western North Pacific (WNP) basin and the most active in terms of tropical cyclones developed per unit area. About 15 TCs develop in the ENP basin per year on average, accounting for about 19% of global TCs. Since most TCs tend to move westward and/or northwestward, TCs in the ENP make landfall less frequently when compared to other basins; hence, TC activity in the ENP basin has possibly received relatively less attention. However, ENP TC activity is an important factor in the summer precipitation regime across Central America and southwestern North America (<a class="elsevierStyleCrossRef" href="#bib0090">Englehart and Douglas, 2001</a>, <a class="elsevierStyleCrossRef" href="#bib0095">2002</a>; <a class="elsevierStyleCrossRef" href="#bib0040">Corbosiero et al., 2009</a>; <a class="elsevierStyleCrossRef" href="#bib0290">Wood and Ritchie, 2013</a>). These regions are projected to experience prolonged drought-like condition in the future climate, so a better understanding of TC activity in the ENP basin has not only scientific relevancy but also a profound socioeconomic impact.There is currently no generally accepted theory on TC genesis; however, many studies throughout the decades have proposed that a number of physical conditions are needed for, and affect, tropical cyclogenesis. Environmental factors that affect TC genesis include: the Coriolis parameter, sea surface temperature (SST), low-level vorticity, mid-tropospheric humidity and vertical wind shear (<a class="elsevierStyleCrossRef" href="#bib0110">Gray, 1968</a>; <a class="elsevierStyleCrossRef" href="#bib0210">Mcbride and Zehr, 1981</a>; <a class="elsevierStyleCrossRef" href="#bib0165">Klotzbach and Gray, 2008</a>). The formation of TCs largely occurs over warm waters with SSTs greater than 26.5 °C, away from the equator and in environments with strong cyclonic low-level relative vorticity, moderate/high mid-tropospheric humidity and weak vertical wind shear. A genesis potential index (GPI) was developed based upon those large-scale parameters (<a class="elsevierStyleCrossRef" href="#bib0115">Gray, 1979</a>; <a class="elsevierStyleCrossRef" href="#bib0270">Watterson et al., 1995</a>; <a class="elsevierStyleCrossRef" href="#bib0065">Emanuel and Nolan, 2004</a>) to understand the variability of TC genesis and to aid in the prediction of TC activity.The interannual variability of TC activity in various ocean basins is strongly influenced by ENSO, as summarized in reviews by <a class="elsevierStyleCrossRef" href="#bib0185">Landsea (2000)</a> and <a class="elsevierStyleCrossRef" href="#bib0030">Chu (2004)</a>, but its impact varies from basin to basin. In the North Atlantic basin, the number of TCs is usually below normal during El Niño years (<a class="elsevierStyleCrossRef" href="#bib0120">Gray, 1984</a>; <a class="elsevierStyleCrossRef" href="#bib0170">Knaff, 1998</a>) and above normal during La Niña years. In addition to TC frequency, ENSO also impacts TC intensity (<a class="elsevierStyleCrossRef" href="#bib0185">Landsea, 2000</a>), genesis location (<a class="elsevierStyleCrossRef" href="#bib0055">Elsner and Kara, 1998</a>) and landfall probabilities in the US and Caribbean (<a class="elsevierStyleCrossRef" href="#bib0005">Bove et al., 1998</a>; Pielke and Landsea, 1999). In the western North Pacific basin, ENSO has no significant impact on TC frequency but has a significant impact on TC intensity, location and track (<a class="elsevierStyleCrossRef" href="#bib0215">Nicholls, 1979</a>, <a class="elsevierStyleCrossRef" href="#bib0220">1992</a>; <a class="elsevierStyleCrossRef" href="#bib0050">Dong, 1998</a>; <a class="elsevierStyleCrossRef" href="#bib0265">Wang and Chan, 2002</a>; <a class="elsevierStyleCrossRef" href="#bib0315">Zhao et al., 2010</a>; <a class="elsevierStyleCrossRef" href="#bib0325">Zhao and Raga, 2014</a>).<a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood (1997)</a> found no effect of ENSO on the TC frequency in the ENP basin, although the number of intense TCs tends to increase during El Niño years (<a class="elsevierStyleCrossRef" href="#bib0125">Gray and Sheaffer, 1991</a>; <a class="elsevierStyleCrossRef" href="#bib0035">Collins and Mason, 2000</a>; <a class="elsevierStyleCrossRef" href="#bib0245">Romero-Vadillo et al., 2007</a>), similarly to the effect observed in the WNP basin. Using GPI anomaly composites associated with ENSO, <a class="elsevierStyleCrossRef" href="#bib0015">Camargo et al. (2007)</a> concluded that over the eastern North Pacific, vertical wind shear is the main contributor towards the ENSO effect on cyclogenesis with potential intensity also playing a role, and vorticity and relative humidity acting in the opposite sense to the total observed anomaly.An inverse relationship has been noted between TC activity in the North Atlantic and ENP basin as a function of the ENSO phase (<a class="elsevierStyleCrossRef" href="#bib0120">Gray, 1984</a>; <a class="elsevierStyleCrossRef" href="#bib0180">Lander and Guard, 1998</a>; <a class="elsevierStyleCrossRef" href="#bib0190">Larson et al., 2005</a>). These studies indicate that the anti-correlation can be partly explained by the different effects of ENSO on the tropospheric zonal wind shear in the North Atlantic and ENP basins. Moreover, the ENSO-related signal in ENP TC activity seems to be statistically weaker than that in the North Atlantic (<a class="elsevierStyleCrossRef" href="#bib0120">Gray, 1984</a>; <a class="elsevierStyleCrossRef" href="#bib0200">Magaña et al., 2003</a>; <a class="elsevierStyleCrossRef" href="#bib0100">Frank and Yong, 2007</a>), and the robustness of the relationship between ENSO and TC activity in the ENP basin has been questioned (<a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood, 1997</a>; <a class="elsevierStyleCrossRef" href="#bib0240">Ralph and Gough, 2009</a>).While the relation between cyclogenesis and SST globally was postulated several decades ago<a name="p3"></a> (<a class="elsevierStyleCrossRef" href="#bib0110">Gray, 1968</a>), studies indicate that the difference of tropopause temperature and SST act as an upper bound on the maximum potential intensity of a TC but other environmental factors ultimately determine its actual intensity. More recent studies have highlighted the role of oceanic features with elevated heat content and suggested that this variable is more important than the actual SST once it is above the 26.5 °C threshold. Examples of this impact have been published of cases in the Gulf of Mexico and in the WNP, such as hurricanes Katrina and Rita (<a class="elsevierStyleCrossRef" href="#bib0135">Jaimes and Shay, 2009</a>) and super-typhoon Maemi (<a class="elsevierStyleCrossRef" href="#bib0195">Lin et al., 2005</a>), respectively. In the ENP, <a class="elsevierStyleCrossRef" href="#bib0225">Oropeza and Raga (2015)</a> showed that there is a link between oceanic features with high heat content and rapid intensification.In this study, we focus on the period 1965-2013, from the start of the satellite era. The ENP shows a pronounced interannual and decadal variability in the number of TCs during the period 1965-2013 (<a class="elsevierStyleCrossRef" href="#fig0005">Fig. 1</a>). Note that the minimum TC frequency is observed in 2010, while 1992 presents the maximum frequency during the period considered. <a class="elsevierStyleCrossRef" href="#bib0295">Wu and Chu (2007)</a> compared the changes in large-scale factors between two extreme years 1992 and 1977, representing extreme high and low tropical cyclone activity during the period 1966-2003. Although <a class="elsevierStyleCrossRef" href="#bib0295">Wu and Chu (2007)</a> suggested the environmental factors undergo pronounced changes over the major development region (MDR) for the two extreme years, the interannual variability of TC activity over the ENP basin remains not well understood, particularly the role of factors in contributing towards the interannual variability of TC intensity.<elsevierMultimedia ident="fig0005"></elsevierMultimedia>The main objectives of this study are: (1) to discuss the composite differences in several environmental parameters during periods of high and low TC activity over the ENP basin and to explore the possible physical factors for the differences in activity; and (2) to investigate the relative role of SST, wind shear and TC tracks on the changes in TC intensity over the ENP basin. The rest of this paper is arranged as follows. Section 2 introduces the data employed in this study. Section 3 gives statistical analyses of TC activity over the ENP basin between periods of high and low TC activity and contrasts the associated environmental conditions. Section 4 further investigates the key environmental factors affecting TC intensity over the ENP basin using a numerical intensity model. A discussion of the results and conclusions are presented in Section 5.2Data and methods2.1TC dataThe TC data utilized in this study correspond to the best track dataset from Northeast and North Central Pacific Hurricane (HURDAT2) available through the National Hurricane Center, which includes position and intensity at six-hour intervals. Only TCs with maximum sustained winds greater than 17.2 ms–1 are considered in this study. The annual distribution of TC frequency in the basin is shown in <a class="elsevierStyleCrossRef" href="#fig0010">Figure 2</a>; note that the majority of TCs occur from June to October (hereafter referred to as peak TC season). This study will focus on the peak season TC activity over the ENP basin; this is mainly based on the following three reasons: i) the TC frequency over the peak season accounts for about 93% of total season TCs; ii) there is a significant correlation of TC frequency<a name="p4"></a> over the peak season and total season (correlation coefficient=0.97); and iii) the environmental circulations during the peak TC season are relatively steady.<elsevierMultimedia ident="fig0010"></elsevierMultimedia>In addition to the TC frequency, two other intensity parameters are used to measure changes in the TC activity: the Power Dissipation Index (PDI) (<a class="elsevierStyleCrossRef" href="#bib0070">Emanuel, 2005</a>) and the number of major hurricanes during the peak season. The PDI represents the destructive capability of TC activity and major hurricanes are those with Categories 3, 4 and 5 in the Saffir-Simpson scale (category 3-5 TCs). These parameters have been used in previous studies (<a class="elsevierStyleCrossRef" href="#bib0070">Emanuel, 2005</a>; <a class="elsevierStyleCrossRef" href="#bib0275">Webster et al., 2005</a>; <a class="elsevierStyleCrossRef" href="#bib0305">Wu et al., 2008</a>) to evaluate TC impacts; moreover, the number of major hurricanes may be sensitive to climate change, as suggested by many previous studies (<a class="elsevierStyleCrossRef" href="#bib0020">Chan, 2005</a>; <a class="elsevierStyleCrossRef" href="#bib0080">Emanuel, 2008</a>; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao et al., 2011</a>; <a class="elsevierStyleCrossRef" href="#bib0310">Wu and Zhao, 2012</a>; <a class="elsevierStyleCrossRef" href="#bib0330">Zhao et al., 2014</a>).2.2Selection of periods of high and low TC activityThe annual TC frequency during the peak season (JJASO) in the ENP basin shows substantial interannual and decadal variability (<a class="elsevierStyleCrossRef" href="#fig0005">Fig. 1a</a>), with a climatological mean value of 14.08 and a standard deviation of 3.78. The TC frequency during the peak season has a correlation with the annual TC frequency of 0.97, significant at the 95% confidence level (<a class="elsevierStyleCrossRef" href="#fig0005">Fig. 1b</a>). In this study we define a period of high activity as one during which the total number of TCs observed during the peak season (JJASO) is greater than the mean for the period considered in this study (1965-2013) plus one standard deviation. Conversely, a period of low activity has fewer than the mean minus one standard deviation. During the 49 years considered in this study, there are 7 years with high activity: 1968, 1982, 1983, 1985, 1987, 1990 and 1992, and 10 years with low activity: 1965, 1969, 1977,1979, 1995, 1996, 1999, 2007, 2010, and 2011.In order to investigate the relationship between ENSO and TC activity over the ENP basin, we define ENSO events as five consecutive overlapping three- month periods at or above the +0.5 °C anomaly for warm (El Niño) events and at or below the -0.5 °C anomaly for cold (La Niña) events; other events are defined as neutral years. The threshold is further broken down into weak (with a 0.5 to 0.9 °C SST anomaly), moderate (1.0 to 1.4 °C) and strong (≥1.5 °C) events.During the seven years with high TC activity we find two strong El Niño years (1982 and 1987), one moderate El Niño year (1968), three neutral years (1985, 1990 and 1992) and a weak La Niña year (1983). During the 10 years with low TC activity we find two strong La Niña years (1999 and 2010), one moderate La Niña year (2007), two weak La Niña years (1995 and 2011), two neutral years (1979 and 1996), one strong El Niño year (1965) and two weak El Niño years (1969 and 1977). There appears to be no significant relationship between ENSO and TC activity over the ENP basin, coinciding with results from some previous studies (<a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood, 1997</a>; <a class="elsevierStyleCrossRef" href="#bib0240">Ralph and Gough, 2009</a>). The influence of El Niño Southern Oscillation on ENP TC activity has been carefully and comprehensively discussed by <a class="elsevierStyleCrossRef" href="#bib0140">Jien et al. (2015)</a>. In this study, we mainly focus on the distinct interannual variability leading to anomalously high and low TC activity over the ENP basin, but the relationship between ENSO and TC activity over the ENP basin will not discussed. We also explore the large multi-decadal variability of TC activity observed over the ENP basin (<a class="elsevierStyleCrossRef" href="#fig0005">Fig. 1</a>) that results in clustering of years with high and low activities. In particular, note that 6 of the 7 years with high activity occur in the period 1980-1994, while 4 years with low activity occur between 1965 and 1980 and the other 6 years of low activity are observed between 1995 and 2013.<a name="p5"></a>2.3Large-scale field dataThe monthly environmental variables (i.e., wind, relative humidity and vertical velocity) are derived from NCEP/NCAR, centered on a 2.5 x 2.5 grid (<a class="elsevierStyleCrossRef" href="#bib0150">Kalnay et al., 1996</a>). In order to examine the influence ofthe vertical shear ofthe horizontal wind on TC variability, the vertical shear is computed as the wind difference of the magnitude of the shear vector between 200 hPa and 850 hPa (Vshear=U200−U8502+V200−V8502). The monthly Extended Reconstructed SST version 2 dataset developed on a 2°x 2°grid by <a class="elsevierStyleCrossRef" href="#bib0255">Smith and Reynolds (2004)</a>, is used in the present study.2.4Intensity model<a class="elsevierStyleCrossRef" href="#bib0075">Emanuel et al. (2006)</a> successfully reproduced the observed TC climatology from 1980 to 2006 with formation, motion and intensity models. Subsequently, <a class="elsevierStyleCrossRef" href="#bib0085">Emanuel et al. (2008)</a> used this approach to quantify the possible influence of global warming on TC activity, indicating that global TC frequency can be reduced by global warming, but intensity may increase in some places. In this approach, the TC intensity is predicted using a deterministic, coupled air-sea model, the Coupled Hurricane Intensity Prediction System (CHIPS). <a class="elsevierStyleCrossRef" href="#bib0320">Zhao et al. (2011</a>, 2014b) used this intensity model to investigate interannual and decadal variability of TC activity over the WNP basin. The same intensity model is used in this study, now applied to the ENP basin. The TC intensity model is an axisymmetric numerical atmospheric model, coupled with a simple one dimensional ocean model. In this model, we only consider that changes in three environmental parameters (SST, environmental vertical wind shear and TC tracks) can affect the intensity of tropical cyclones. The simulated TCs are allowed to move along the observed TC tracks during the period 1965-2013, experiencing the observed vertical wind shear and SST along the TC tracks, in order to simulate the evolution of their intensity. The intensity model is initialized with a warm-core cyclonic vortex. The maximum wind speed of the initial vortex is set to be 21m/s after a series of numerical experiments as the model vortex weakens at the beginning of the simulations; this value is also used by other studies (<a class="elsevierStyleCrossRef" href="#bib0310">Wu and Zhao, 2012</a>; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao et al., 2011</a>, <a class="elsevierStyleCrossRef" href="#bib0330">2014</a>). The other parameters of the initial vortex needed for the model were taken to be as in <a class="elsevierStyleCrossRef" href="#bib0085">Emanuel et al. (2008)</a> and the same initial model setup is used for all the simulations in this study.The model skill is determined through correlations of the predicted and observed time series. The statistical significance of the correlations and the differences of the means are tested with Student's t-test method (<a class="elsevierStyleCrossRef" href="#bib0285">Wilks, 1995</a>).3Role of environmental factors on TC frequencyAn annual average of 20.8 TCs is observed during the 7 years of high activity, which is significantly higher than those generated on average during the 10 years of low activity (9 TCs) at a 95% confidence level. Statistically significant differences can also be observed when separating TCs into their intensity categories, as seen in <a class="elsevierStyleCrossRef" href="#fig0015">Figure 3a</a>. The years with low<a name="p6"></a> overall TC activity also show lower frequency in each of the categories. Further investigation shows that the fraction of major hurricanes (category 3-5 TCs) is significantly higher in years with high activity compared to that in years with low activity, while the proportion of category 1-2 TCs is significantly lower in years with high activity compared to that in years with low activity (<a class="elsevierStyleCrossRef" href="#fig0015">Fig. 3b</a>) at a 95% confidence level. These significant differences may be attributed to the differences observed in the location of TC genesis and occurrence in years with high and low activity (<a class="elsevierStyleCrossRef" href="#fig0020">Fig. 4</a>). There is a significant region of enhanced TC formation centered around 12° N and 105° W during years of high activity compared to years of low activity (<a class="elsevierStyleCrossRef" href="#fig0020">Fig. 4a</a>). The average TC formation location shows a significant easterly shift in the years with high activity compared to years of low activity. Correspondingly, more TCs have west- and northwestward tracks during the active versus inactive periods. This difference in frequency of occurrence (<a class="elsevierStyleCrossRef" href="#fig0020">Fig. 4b</a>) is due to differences in TC formation location and also on TC lifetime. The average lifetime is 4.9 days during active years, which is significantly more than 4.2 days during inactive years at a 95% confidence level. The difference of trajectories can be clearly seen in <a class="elsevierStyleCrossRef" href="#fig0025">Figure 5</a> that shows all the TC tracks observed during the active and inactive periods.<elsevierMultimedia ident="fig0015"></elsevierMultimedia><elsevierMultimedia ident="fig0020"></elsevierMultimedia><elsevierMultimedia ident="fig0025"></elsevierMultimedia>The thermal and dynamical components of the GPI (<a class="elsevierStyleCrossRef" href="#bib0110">Gray, 1968</a>; <a class="elsevierStyleCrossRef" href="#bib0065">Emanuel and Nolan, 2004</a>) are examined to determine the role that each may play towards cyclogenesis during years of high and low activity in the ENP basin. The low-level cyclonic vorticity is very important for the development of convection, its organization and its intensification to TC, reducing the local Rossby radius of deformation and focusing the convective heating locally (<a class="elsevierStyleCrossRef" href="#bib0025">Chen et al., 2006</a>). <a class="elsevierStyleCrossRef" href="#fig0030">Figure 6</a> shows the composite streamfunction at 850 hPa, and it indicates a significant anticyclonic circulation anomaly over the main development region (MDR) for TC genesis during the active compared to inactive years.<a name="p7"></a> This anticyclonic vorticity anomaly observed during the high activity years would tend to reduce tropical cyclogenesis in this region.<elsevierMultimedia ident="fig0030"></elsevierMultimedia>The presence of high mid-level humidity in the environment allows a parcel of air inside clouds to remain saturated as it entrains the surrounding air during its ascent and it is conductive for maintaining convective activity of the TC development (<a class="elsevierStyleCrossRef" href="#bib0155">Kaplan et al., 2010</a>). The results of the composite show a significant decrease in relative humidity at 600 hPa in the MDR during the active years (<a class="elsevierStyleCrossRef" href="#fig0035">Fig. 7</a>). Lower values<a name="p8"></a> of relative humidity would tend to inhibit TC genesis in this region during the active years. Therefore, the low-level vorticity and mid-troposphere relative humidity both appear to be more favorable for tropical cyclogenesis in the region during the inactive years compared to that during the active years.<elsevierMultimedia ident="fig0035"></elsevierMultimedia>A warm ocean surface allows for enough latent heat flux from ocean to maintain secondary circulation when energy is released near the TC core in the eyewall (<a class="elsevierStyleCrossRef" href="#bib0110">Gray, 1968</a>). A significantly warm SST anomaly is observed over the MDR area in the ENP basin during active years compared with inactive years, as shown in <a class="elsevierStyleCrossRef" href="#fig0040">Figure 8</a>. Note that the SST pattern during the active years somewhat resembles the pattern associated with the positive phase of the Pacific Decadal Oscillation (PDO), which suggests that the TC activity may be modulated by the PDO; however, the HURDAT time series is currently not long enough to evaluate this potential influence.<elsevierMultimedia ident="fig0040"></elsevierMultimedia>The presence of significant vertical wind shear inhibits TC development by advecting away the heating and moisture from the center of the convection (<a class="elsevierStyleCrossRef" href="#bib0045">DeMaria, 1996</a>). A significant decrease of vertical wind shear is observed over the ENP basin during the years of high activity compared to inactive years, as can be seen in <a class="elsevierStyleCrossRef" href="#fig0045">Figure 9</a>. During high TC activity years the shear between 850 and 200 hPa is up to 4 ms–1 lower than during inactive years in the MDR of this basin; this decrease in shear leads to more vertical coherence of developing cyclones and is conducive of further intensification during active years.<elsevierMultimedia ident="fig0045"></elsevierMultimedia>In order to further investigate the relative roles of these environmental factors, we calculate the correlation coefficient between TC frequency and<a name="p9"></a> the analyzed large-scale factors over the MDR. The results indicate that the low-level vorticity and relative humidity are anti-correlated with MDR TC frequency, with correlation coefficients –0.11 and –0.21, respectively. These coefficients are in agreement with anticyclonic anomalies (<a class="elsevierStyleCrossRef" href="#fig0030">Fig. 6</a>) and decrease in relative humidity (<a class="elsevierStyleCrossRef" href="#fig0035">Fig. 7</a>) during the active years. Note, however, that neither correlation is significant at the 95% confidence level. A positive but not significant correlation (0.15) is found for SST and MRD TC frequency. This result suggests that while the SST anomalies appear large in the basin (<a class="elsevierStyleCrossRef" href="#fig0040">Fig. 8</a>), the local SST may not play a dominant role in TC frequency. Moreover, the correlation between MDR TC frequency over the ENP basin and Niño-3.4 SST suggests no significant correlation between them, in agreement with previous studies (<a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood, 1997</a>; <a class="elsevierStyleCrossRef" href="#bib0245">Romero-Vadillo et al., 2007</a>; <a class="elsevierStyleCrossRef" href="#bib0240">Ralph and Gough, 2009</a>). The largest correlation is obtained between MDR TC frequency and vertical wind shear (–0.31, which is significant at the 95% confidence level), consistent with the results of Camargo et al. (2007), and indicative of the dominant role that the vertical wind shear plays in modulating TC genesis over the ENP basin.We calculate the four factors of the GPI separately: vorticity at 850hPa, relative humidity at 600hPa, potential intensity and vertical wind shear to gain more insight into the role of each of them. The details of the calculation of the GPI can be found in <a class="elsevierStyleCrossRef" href="#bib0065">Emanuel and Nolan (2004)</a>. Following <a class="elsevierStyleCrossRef" href="#bib0015">Camargo et al. (2007)</a> and <a class="elsevierStyleCrossRef" href="#bib0325">Zhao and Raga (2014)</a>, we evaluate the relative contribution of each of the four factors to the overall GPI anomaly between years with high and low activity. Specifically, we compute the GPI using the long-term climatology (1965-2013) of three of the factors and used the actual data for the fourth factor; this calculation is then repeated for each of the other three factors. For each factor, the individual GPI anomalies between years with high and low activity are then calculated. Although the net anomaly cannot be simply described as the sum of the four fields combined due to the nonlinearity of the GPI, to a certain extent, the index can provide weights that appropriately quantify the influence of the different factors for the difference of TC genesis between years with high and low activity.<a class="elsevierStyleCrossRef" href="#fig0050">Figure 10</a> shows the average GPI during years with high and low TC activity and the difference of active minus inactive years. There is a large positive GPI anomaly evident over the ENP basin, with a maximum over 8-12° N, 105-80° W. There is an eastward shift of the GPI anomalies to the observed TC genesis anomaly. <a class="elsevierStyleCrossRef" href="#fig0055">Figures 11a, b, c</a> and d display the GPI anomalies between years<a name="p10"></a> with high and low activity calculated when the relative humidity, vorticity, potential intensity and vertical wind shear are respectively varied while keeping the other three variables fixed at their climatologically values. Comparing the panels in <a class="elsevierStyleCrossRef" href="#fig0055">Figure 11</a> with the GPI anomalies between years with high and low activity when all four factors are varying (<a class="elsevierStyleCrossRef" href="#fig0050">Fig. 10c</a>), it is possible to determine the relative contribution of each factor to the overall GPI anomaly pattern. Note the overall negative GPI anomalies over the ENP basin in <a class="elsevierStyleCrossRef" href="#fig0055">Fig. 11a, b</a>; these negative anomalies indicate that changes in relative humidity and vorticity do not contribute towards TC genesis during the active years compared to that during inactive years. In contrast, there are positive GPI anomalies in the MDR of the ENP basin in <a class="elsevierStyleCrossRef" href="#fig0055">Figures 11c, d</a>, indicating that the SST and vertical wind shear make a positive contribution towards TC genesis during the active years compared to that during the inactive years. Moreover, note that the magnitude of the GPI anomaly when vertical wind shear varies (<a class="elsevierStyleCrossRef" href="#fig0055">Fig. 11d</a>) is higher than the magnitude of the GPI anomaly when potential intensity varies (<a class="elsevierStyleCrossRef" href="#fig0055">Fig. 11c</a>). This clearly suggests that the vertical wind shear is the dominant contributor towards favoring TC genesis during active years and suppressing it during the inactive years. These GPI results are consistent with the differences in composite large-scale patterns between active and inactive years and correlation analyses reported above.<elsevierMultimedia ident="fig0050"></elsevierMultimedia><elsevierMultimedia ident="fig0055"></elsevierMultimedia>4Role of environmental factors on TC intensityThe intensity of TCs in the ENP basin shows significant interannual variability, as can be seen in <a class="elsevierStyleCrossRef" href="#fig0060">Figure 12a</a> (black line), which displays the number of major hurricanes in the basin (category 3-5 TCs). During the active years, an average of 5.71 category 3-5 TCs are observed during the peak TC season over the ENP basin, while only 1.9 on average is present in the inactive years. A large and significant (3.8, at 95% confidence level) difference in the frequency of major hurricanes is observed between active and inactive years.<elsevierMultimedia ident="fig0060"></elsevierMultimedia>In order to evaluate the contributions of vertical wind shear, SST and track changes to TC intensity change, we follow the methodology used by <a class="elsevierStyleCrossRef" href="#bib0320">Zhao et al. (2011</a>, <a class="elsevierStyleCrossRef" href="#bib0330">2014</a>) and apply the same intensity model to the ENP basin to evaluate TC intensity along the observed TC tracks. We perform a control experiment (CTRL)<a name="p11"></a><a name="p12"></a> and three other sensitivity simulations: T65, V65 and VT65, as noted in <a class="elsevierStyleCrossRef" href="#tbl0005">Table I</a>. The experiment labeled T65 is similar to CTRL, but keeps SST along the TC track fixed and corresponds to the values observed in 1965. In experiment V65, the vertical wind shear is fixed (corresponding to the observations of 1965) and in experiment VT65 both the SST and vertical wind shear are fixed corresponding to the values observed in 1965. Note that the tracks of individual TCs remain unchanged in the sensitivity experiments; the tracks correspond to the observed trajectories from the HURDAT2 dataset.<elsevierMultimedia ident="tbl0005"></elsevierMultimedia>In the CTRL experiment, all the TCs move along their observed tracks and experience the observed monthly vertical wind shear and SST along their lifetimes, in the period (1965-2013). The results from the CTRL experiment indicate that the simulated frequency of major hurricanes (TCs with Categories 3 through 5) and PDI are in good agreement with the observations (<a class="elsevierStyleCrossRef" href="#fig0060">Fig. 12</a>). The correlation coefficients are 0.64 and 0.87, respectively during the period 1965-2013, both statistically significant at a 95% confidence level. Due to a successful simulation in annual PDI and category 3-5 TC frequency, it raise our confidence for further exploring the relative role of SST, wind shear and TC tracks to changes in PDI and category 3-5 TC frequency in terms of correlation and magnitude.The values of the correlation coefficients presented in <a class="elsevierStyleCrossRef" href="#tbl0010">Table II</a> indicate that the simulated annual frequency of major hurricanes, as well as the PDI, in the three sensitivity experiments is well correlated with results from the CTRL experiment (all correlation coefficients are above 0.8 and statistically significant). Recall that although all three sensitivity experiments are highly idealized because they consider fixed conditions at 1965 values for the SST and/or the vertical wind shear, the TC tracks remain unchanged in the three sensitive experiments and CTRL experiment. The high correlations between the CTRL and the three sensitive experiments suggest that the primary controlling factor for the interannual variability may actually be the trajectories of the TCs.<elsevierMultimedia ident="tbl0010"></elsevierMultimedia><a class="elsevierStyleCrossRef" href="#tbl0015">Table III</a> presents the correlations of the difference in PDI and frequency of category 3-5 TCs for each of the sensitivity experiments and the CTRL experiment. The influence of the SST on the interannual variability can be determined by comparing the results for the CTRL and (CTRL – T65) experiments. The effect of SST is small for the set of experiments, since the correlations are 0.06 and 0.22 and non-significant. Similarly, the effect of the vertical wind shear on TC intensity, evaluated by comparing the results from the CTRL and (CTRL – V65) experiments, indicates a stronger dependence than with SST, with larger and significant correlation coefficients. Note that the combined effect of SST and vertical wind shear changes to the interannual variability, by comparing CTRL and (CTRL – VT65), is larger than the sum of their individual contributions. The correlation coefficients for the frequency of category 3-5 TCs and PDI are –0.30, and –0.49, respectively, both significant at a 95% confidence level.<elsevierMultimedia ident="tbl0015"></elsevierMultimedia>A similar analysis was performed to compare the results of the simulations against observations for<a name="p13"></a> the periods of high and low activity identified. The results are presented in <a class="elsevierStyleCrossRef" href="#tbl0020">Table IV</a> and show again that the dominant role in the interannual variability of the frequency of major hurricanes and PDI (not shown) in associated with reduced wind shear in the basin and that the local SST anomalies play a secondary role compared to the wind shear negative anomalies. These results are in agreement with previous studies (<a class="elsevierStyleCrossRef" href="#bib0060">Emanuel, 1987</a>, <a class="elsevierStyleCrossRef" href="#bib0080">2008</a>; <a class="elsevierStyleCrossRef" href="#bib0105">Goldenberg et al., 2001</a>; <a class="elsevierStyleCrossRef" href="#bib0275">Webster et al., 2005</a>; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao et al., 2011</a>), that indicate that decreased vertical wind shear is related to increased TC intensity, and that higher SST correspond to higher TC intensity.<elsevierMultimedia ident="tbl0020"></elsevierMultimedia>As mentioned briefly above, the interannual variability of TC trajectories may also be playing a significant role in the variability of TC intensity. We explore further this possibility by comparing results from the CTRL and VT65 experiments. Note that the frequency of major hurricanes is well correlated between these two experiments (0.84, significant at the 95% confidence level, see <a class="elsevierStyleCrossRef" href="#tbl0010">Table II</a>). This indicates that the changes in the TC tracks can account for most of the observed interannual variability, partly due to the combined effect of changes in SST and vertical wind shear. These results confirm that the change in TC duration is the main factor for the observed change in TC intensity (<a class="elsevierStyleCrossRef" href="#bib0010">Camargo and Sobel, 2005</a>; <a class="elsevierStyleCrossRef" href="#bib0300">Wu and Wang, 2008</a>; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao et al., 2011</a>). Changes in TC lifetime are closely associated with changes in TC tracks. TC lifetime is also closely associated with TC genesis location. During the years with high activity, the region of enhanced TC formation shifts eastward and leads to longer TC tracks and thus, longer lifetimes. This in turn will result in TCs having more time for intensification and an increased likelihood of developing into intense TCs compared to that during the years with low activity. The eastward shift of the region of enhanced TC formation is also closely associated with warmer SST and lower vertical wind shear during years with high activity than during years with low activity.5Discussion and conclusionsThe ENP basin exhibits very large interannual variability in the frequency of TCs. The analysis of the 49-year period between 1965 and 2013 indicates that during the high activity period, more than twice as many TCs develop on average in the basin compared to the low activity period. This study investigates the large-scale conditions affecting TC genesis and the key factors affecting TC intensity, to try to evaluate their roles on the interannual variability analyzing periods of high and low activity during the period 1965-2013. As was shown in <a class="elsevierStyleCrossRef" href="#fig0020">Figure 4</a>, the years of high activity show a statistically significant easterly shift of the genesis location of tropical cyclones. <a class="elsevierStyleCrossRef" href="#bib0130">Gutzler et al. (2013)</a> found that TCs in the ENP basin occurred near the coast of Mexico more often during La Niña years in the early season for the period 1951-2006. But recall that the years of high activity in our study also include neutral years of the ENSO, suggesting that there are other factors that may modulate genesis location.The results of the analysis of composites of large-scale environmental conditions for active versus inactive years (presented in <a class="elsevierStyleCrossRefs" href="#fig0030">Figs. 6 through 9</a>) are very interesting. The low-level vorticity shows an anticyclonic anomaly and the mid-tropospheric relative<a name="p14"></a> humidity shows a dry anomaly during the active years. Both these anomalies would tend to reduce tropical cyclogenesis in the basin, not contributing towards active years. The most important environmental aspect that favors an increase in the frequency of tropical cyclones is the reduced vertical shear of the horizontal wind over the whole ENP basin. These results are further supported and confirmed by the GPI analyses.These results are consistent with those presented by <a class="elsevierStyleCrossRef" href="#bib0015">Camargo et al. (2007)</a> in their analysis of the composites of El Niño and La Niña years. In their study, vertical wind shear was also the main contributor to ENSO genesis potential anomalies in the ENP, and low-level vorticity and mid-tropospheric relative humidity contributing in the opposite sense. However, the active and inactive periods studied here do not correspond exclusively to either La Niña or El Niño years. The ENSO signal on TC activity seems to be statistically weaker in the ENP basin than that in the North Atlantic, as has been noted by previous studies (<a class="elsevierStyleCrossRef" href="#bib0120">Gray, 1984</a>; <a class="elsevierStyleCrossRef" href="#bib0200">Magaña et al., 2003</a>; <a class="elsevierStyleCrossRef" href="#bib0100">Frank and Yong, 2007</a>; <a class="elsevierStyleCrossRef" href="#bib0245">Romero-Vadillo et al., 2007</a>; <a class="elsevierStyleCrossRef" href="#bib0205">Martínez-Sánchez and Cavazos, 2014</a>, among others). Furthermore, <a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood (1997)</a> and <a class="elsevierStyleCrossRef" href="#bib0240">Ralph and Gough (2009)</a> have questioned the robustness of the relationship between ENSO and TC activity in the ENP basin. However, the recent study by <a class="elsevierStyleCrossRef" href="#bib0140">Jien et al. (2015)</a> found a statistical dependency of TC activity on the ENSO phases, but significant only on the western portion of the development region, between 112 and 140° W. Specifically, their results indicate that El Niño years are characterized by more frequent and more intense events compared to La Niña conditions for this western sub-region of the basin. These new results are not in agreement with results by <a class="elsevierStyleCrossRef" href="#bib0015">Camargo et al. (2007)</a>. And our results of active years indicate that the maximum anomaly in the reduction of wind shear covers a large section of the western sub-region defined in <a class="elsevierStyleCrossRef" href="#bib0140">Jien et al. (2015)</a>. This suggests to us that the ENSO modulation may not be a good predictor for years of high activity in the ENP basin as claimed by <a class="elsevierStyleCrossRef" href="#bib0140">Jien et al. (2015)</a>.Also interesting to discuss are the results related to the SST anomalies, which appear to contribute positively towards tropical cyclogenesis during the active years, yet the correlations with TC frequency are not significant. <a class="elsevierStyleCrossRef" href="#fig0040">Figure 8</a> shows a spatial distribution of the SST anomalies between active and inactive years that somewhat resembles the pattern associated with the positive phase of the Pacific Decadal Oscillation (PDO), which suggests that the TC activity may be modulated by the PDO. <a class="elsevierStyleCrossRef" href="#bib0235">Raga et al. (2013)</a> determined that the time series of 161 years of landfalling TCs (reconstructed from historical records and combined with modern best track data) exhibits a moderate correlation with the PDO. A previous study by <a class="elsevierStyleCrossRef" href="#bib0095">Englehart and Douglas (2002)</a> showed that precipitation in NW Mexico is correlated also with PDO. It is noteworthy that landfalls are only marginally larger (but not significant) during active years (2.00±1.15) than inactive years (1.70±1.16), while the ratio of landfalls to the total count of TCs is almost a factor of 2 different (0.10 versus 0.19), respectively. Inactive years do not necessarily imply fewer landfalls and, thus, less-affected regions of western Mexico.The eastern North Pacific basin exhibits very large interannual variability in the frequency of major hurricanes, as seen in <a class="elsevierStyleCrossRef" href="#fig0060">Figure 12a</a>, and active years also show a significant increase in major hurricanes (<a class="elsevierStyleCrossRef" href="#fig0015">Fig. 3a</a>). The forecast of TC intensity has remained problematic not only in the ENP basin, but also globally. Our results show a lack of significance in the correlation between SST anomalies and TC frequency and also TC intensity. Even though during El Niño years and during the most active years the SST positive anomalies in the basin are quite large, and would in principle contribute to increased convection, the correlations are mostly not significant. The answer may be related to the ocean heat content and not SST, as suggested by <a class="elsevierStyleCrossRef" href="#bib0250">Shay and Brewster (2010)</a>. The recent paper by <a class="elsevierStyleCrossRef" href="#bib0145">Jin et al. (2014)</a> argues that the intensification of TCs in the ENP basin is related to subsurface ocean heat the season after the maximum of El Niño, through a delayed ocean transport mechanism. Another aspect to be considered when studying TC intensification is the presence of transient anticyclonic eddies in the ENP basin that locally can enhance the ocean heat content available for fueling tropical cyclones. <a class="elsevierStyleCrossRef" href="#bib0225">Oropeza and Raga (2015)</a> have shown the importance of the presence of such eddies in the rapid and explosive intensification of hurricanes in the ENP basin.In this study, we used a hurricane intensity model (<a class="elsevierStyleCrossRef" href="#bib0075">Emanuel et al., 2006</a>) to evaluate the individual contributions of changes in the SST, vertical wind shear and TC tracks to changes in TC intensity on<a name="p15"></a> the interannual time scale and considering also the active and inactive periods. Two parameters are used to quantify TC intensity in the basin: the frequency of major hurricanes and the PDI. The results suggest that the primary controlling factor for the interannual variability may actually be the trajectories of the TCs, as was also indicated in the WNP basin in studies by <a class="elsevierStyleCrossRef" href="#bib0265">Wang and Chan (2002)</a> and <a class="elsevierStyleCrossRef" href="#bib0010">Camargo and Sobel (2005)</a>. TC intensity exhibits a stronger dependence on the effect of the vertical wind shear than on the local SST. Note that the combined effects of vertical wind shear and SST appear to be more important than their respective roles and that the frequency of major hurricanes is a more sensitive variable to climate change than the PDI.Studies by <a class="elsevierStyleCrossRef" href="#bib0300">Wu and Wang (2008)</a>, <a class="elsevierStyleCrossRef" href="#bib0320">Zhao et al. (2011)</a>, <a class="elsevierStyleCrossRef" href="#bib0310">Wu and Zhao (2012)</a> and <a class="elsevierStyleCrossRef" href="#bib0330">Zhao et al. (2014)</a> have investigated TC activity in the WNP basin, and suggested that shifts in the TC tracks may have allowed more TCs to have longer lifetimes, favoring more intense TCs. Our results from the ENP basin clearly indicate that TC formation is enhanced around 12° N, 105° W in a region of statistically significant reduced vertical wind shear, and that TCs favor a northwestward track during the active years (<a class="elsevierStyleCrossRef" href="#fig0020">Fig. 4</a>). These tracks during the active years expose TCs to the warmer SST anomalies in the region that resemble the PDO pattern (<a class="elsevierStyleCrossRef" href="#fig0040">Fig. 8</a>), resulting in longer lifetimes and more intense TCs. The study by Martinez-Sanchez and Cavazos (2014) shows a correlation between PDO hurricanes with category 4 and 5 in the ENP basin.Finally, it seems pertinent to briefly discuss our results of TC frequency and intensity during active years in the context of climate change scenarios. Several studies in the last decades (<a class="elsevierStyleCrossRef" href="#bib0060">Emanuel, 1987</a>, <a class="elsevierStyleCrossRef" href="#bib0070">2005</a>, <a class="elsevierStyleCrossRef" href="#bib0080">2008</a>; <a class="elsevierStyleCrossRef" href="#bib0275">Webster et al., 2005</a>; <a class="elsevierStyleCrossRef" href="#bib0305">Wu et al., 2008</a>) have discussed the influence of SST and vertical wind shear on changes in TC intensity either globally or focusing primarily on the North Atlantic basin (<a class="elsevierStyleCrossRef" href="#bib0105">Goldenberg et al., 2001</a>). Results of a global coupled climate model (<a class="elsevierStyleCrossRef" href="#bib0260">Vecchi and Soden, 2007</a>) for the twenty first century suggest that the maximum potential intensity in the ENP basin will increase from the coast of Mexico westward to 120° W and between 10 and 20° N, well within the region of enhanced TC genesis and enhanced tracks during the high activity years. While our results indicate that the potential intensity does not appear to be a dominant contributor to cyclogenesis in the active years, it is possible that large-scale conditions may lead to more intense TCs during active years in the basin. Nevertheless, further studies analyzing the results of coupled models are needed to evaluate the role of the most favorable factor (reduced vertical wind shear) in the basin." "textoCompletoSecciones" => array:1 [ "secciones" => array:10 [ 0 => array:3 [ "identificador" => "xres901030" "titulo" => "Resumen" "secciones" => array:1 [ 0 => array:1 [ "identificador" => "abst0005" ] ] ] 1 => array:3 [ "identificador" => "xres901029" "titulo" => "Abstract" "secciones" => array:1 [ 0 => array:1 [ "identificador" => "abst0010" ] ] ] 2 => array:2 [ "identificador" => "xpalclavsec882095" "titulo" => "Keywords" ] 3 => array:2 [ "identificador" => "sec0005" "titulo" => "Introduction" ] 4 => array:3 [ "identificador" => "sec0010" "titulo" => "Data and methods" "secciones" => array:4 [ 0 => array:2 [ "identificador" => "sec0015" "titulo" => "TC data" ] 1 => array:2 [ "identificador" => "sec0020" "titulo" => "Selection of periods of high and low TC activity" ] 2 => array:2 [ "identificador" => "sec0025" "titulo" => "Large-scale field data" ] 3 => array:2 [ "identificador" => "sec0030" "titulo" => "Intensity model" ] ] ] 5 => array:2 [ "identificador" => "sec0035" "titulo" => "Role of environmental factors on TC frequency" ] 6 => array:2 [ "identificador" => "sec0040" "titulo" => "Role of environmental factors on TC intensity" ] 7 => array:2 [ "identificador" => "sec0045" "titulo" => "Discussion and conclusions" ] 8 => array:2 [ "identificador" => "xack299706" "titulo" => "Acknowledgements" ] 9 => array:1 [ "titulo" => "References" ] ] ] "pdfFichero" => "main.pdf" "tienePdf" => true "fechaRecibido" => "2015-01-01" "fechaAceptado" => "2015-05-19" "PalabrasClave" => array:1 [ "en" => array:1 [ 0 => array:4 [ "clase" => "keyword" "titulo" => "Keywords" "identificador" => "xpalclavsec882095" "palabras" => array:4 [ 0 => "Interannual variability" 1 => "large-scale factors" 2 => "intensity model" 3 => "eastern Pacific basin" ] ] ] ] "tieneResumen" => true "resumen" => array:2 [ "es" => array:2 [ "titulo" => "Resumen" "resumen" => "La cuenca del Pacifico tropical nororiental presenta una gran variabilidad interanual en cuanto a la frecuencia de ocurrencia de ciclones, con años muy activos (con más de 20 ciclones durante la temporada) y años muy poco activos (con sólo ocho ciclones). En este estudio se investigan los factores de gran escala que pueden influenciar la variabilidad interanual analizando los compuestos de siete años muy activos y 10 años muy poco activos durante los 49 años del periodo 1965-2013. Los resultados del análisis de compuestos indican que la vorticidad a niveles bajos y la humedad relativa en la troposfera media son poco favorables para la ciclogénesis tropical durante los años activos. La temperatura superficial del mar (TSM) parece desempeñar un pequeño rol modulando la frecuencia, y la disminución observada en la cizalladura del viento entre 850 y 200 hPa domina la ciclogénesis durante los años activos, confirmando resultados previos de Camargo et al. (2007). Se investigan además los factores ambientales de gran escala que afectan la intensidad de los ciclones tropicales en la cuenca con un modelo numérico de intensidad (Emanuel et al., 2006, 2008), el cual predice la intensidad con base en la cizalladura del viento, la TSM y las trayectorias observadas. Los resultados indican que la variabilidad interanual en la frecuencia de huracanes mayores (categorías 3 a 5) se simula mejor cuando ambos parámetros se combinan. También es posible que los cambios en las trayectorias puedan ser determinantes para la intensidad alcanzada. En particular, durante los años activos, la zona de ciclogénesis se desplaza hacia el este y hay más ciclones con trayectoria norte-noroeste, lo cual determina que tengan una vida más larga y sean de mayor intensidad que los que se desarrollan en años con poca actividad en la cuenca." ] "en" => array:2 [ "titulo" => "Abstract" "resumen" => "The tropical eastern North Pacific (ENP) basin exhibits very large interannual variability in the frequency of occurrence of tropical cyclones, presenting very active (more than 20 tropical cyclones per season) and very inactive years (only eigth tropical cyclones). The large-scale factors that may influence the distinct interannual variability are investigated in this study, by analyzing the composites of seven years of high activity and 10 years of low activity from 1965 to 2013. The results of composite analyses indicate that the low-level vorticity and mid-tropospheric relative humidity are mostly unfavorable for tropical cyclogenesis during active years. The sea surface temperature (SST) may play a small role modulating the occurrence of tropical cyclones, but the reduced vertical shear of the horizontal wind between 850 and 200 hPa is the main contributor to clyclogenesis during the active years, confirming earlier results by Camargo et al. (2007). We use an intensity model (Emanuel et al., 2006, 2008) to further investigate the key environmental factors affecting TC intensity, exploring the relative roles of changes in SST, vertical wind shear and TC tracks. The results indicate that the interannual variability in the frequency of major hurricanes (categories 3 through 5) is best simulated when the effects of both SST and vertical wind shear are combined. Furthermore, changes in TC tracks may play an important role in the intensity achieved. In particular, during the years with high activity, the location for cyclogenesis shifts eastward and more TCs have west-northwestward tracks, leading to longer lifetime and higher intensity, compared to years with low TC activity in the basin." ] ] "multimedia" => array:16 [ 0 => array:7 [ "identificador" => "fig0005" "etiqueta" => "Fig. 1" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr1.jpeg" "Alto" => 1219 "Ancho" => 942 "Tamanyo" => 151623 ] ] "descripcion" => array:1 [ "en" => "Observed number of tropical cyclones (TCs) reaching at least tropical storm strength in the NHC best track dataset over the Eastern North Pacific (ENP) during the period 1965-2013 for (a) the peak season (June through October) and (b) the whole year (January-December)" ] ] 1 => array:7 [ "identificador" => "fig0010" "etiqueta" => "Fig. 2" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr2.jpeg" "Alto" => 728 "Ancho" => 942 "Tamanyo" => 60591 ] ] "descripcion" => array:1 [ "en" => "Climatological monthly mean of the number of observed tropical cyclones (TCs) reaching tropical storm intensity in the NHC best track dataset over the eastern North Pacific (ENP) basin during the period 1965-2013 and the corresponding standard deviation for each month with red closed dots." ] ] 2 => array:7 [ "identificador" => "fig0015" "etiqueta" => "Fig. 3" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr3.jpeg" "Alto" => 1468 "Ancho" => 943 "Tamanyo" => 99761 ] ] "descripcion" => array:1 [ "en" => "(a) Average observed number; and (b) proportion of tropical cyclones (TCs) separated as a function of their intensity in the NHC best track dataset over the eastern North Pacific (ENP) during the peak season for periods of high (red) and low (black) activity. The grey bar corresponds to one standard deviation for the study period 1965-2013." ] ] 3 => array:7 [ "identificador" => "fig0020" "etiqueta" => "Fig. 4" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr4.jpeg" "Alto" => 1226 "Ancho" => 942 "Tamanyo" => 145600 ] ] "descripcion" => array:1 [ "en" => "Composite difference (active minus inactive years) through the peak TC season of: (a) TC genesis frequency; and (b) occurrence frequency. The shading indicates statistical significant differences at the 95% confidence level." ] ] 4 => array:7 [ "identificador" => "fig0025" "etiqueta" => "Fig. 5" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr5.jpeg" "Alto" => 1198 "Ancho" => 940 "Tamanyo" => 225184 ] ] "descripcion" => array:1 [ "en" => "Trajectories of the tropical cyclones observed during the peak season of (a) active, and (b) inactive years in the period 1965-2013." ] ] 5 => array:7 [ "identificador" => "fig0030" "etiqueta" => "Fig. 6" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr6.jpeg" "Alto" => 1968 "Ancho" => 940 "Tamanyo" => 612509 ] ] "descripcion" => array:1 [ "en" => "Composite 850 hPa stream function through the peak TC season for (a) active years, (b) inactive years, and (c) the difference (active minus inactive years). The shading indicates statistical significant differences at the 95% confidence level." ] ] 6 => array:7 [ "identificador" => "fig0035" "etiqueta" => "Fig. 7" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr7.jpeg" "Alto" => 2002 "Ancho" => 943 "Tamanyo" => 260881 ] ] "descripcion" => array:1 [ "en" => "Composite 600 hPa relative humidity through the peak TC season for (a) active years, (b) inactive years, and (c) the difference (active minus inactive years). The shading indicates statistical significant differences at the 95% confidence level." ] ] 7 => array:7 [ "identificador" => "fig0040" "etiqueta" => "Fig. 8" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr8.jpeg" "Alto" => 1398 "Ancho" => 1129 "Tamanyo" => 335794 ] ] "descripcion" => array:1 [ "en" => "Composite SST anomalies from the climatological mean SST over the period of 1965-2013 through the peak TC season for (a) active years, (b) inactive years, and (c) the difference (active minus inactive years)." ] ] 8 => array:7 [ "identificador" => "fig0045" "etiqueta" => "Fig. 9" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr9.jpeg" "Alto" => 1995 "Ancho" => 943 "Tamanyo" => 277752 ] ] "descripcion" => array:1 [ "en" => "Composite vertical wind shear through the peak TC season for (a) active years, (b) inactive years, and (c) the difference (active minus inactive years). The shading indicates statistical significant differences at the 95% level." ] ] 9 => array:7 [ "identificador" => "fig0050" "etiqueta" => "Fig. 10" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr10.jpeg" "Alto" => 1090 "Ancho" => 968 "Tamanyo" => 141601 ] ] "descripcion" => array:1 [ "en" => "GPI during (a) active years, (b) inactive years, and (c) their difference." ] ] 10 => array:7 [ "identificador" => "fig0055" "etiqueta" => "Fig. 11" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr11.jpeg" "Alto" => 1464 "Ancho" => 992 "Tamanyo" => 160117 ] ] "descripcion" => array:1 [ "en" => "Difference of the GPI between active and inactive years over the ENP basin in JJASO, while varying: (a) relative humidity, (b) vorticity, (c) potential intensity, and (d) vertical wind shear. The rest of the terms are kept as their climatological values (using the period 1965-2013)." ] ] 11 => array:7 [ "identificador" => "fig0060" "etiqueta" => "Fig. 12" "tipo" => "MULTIMEDIAFIGURA" "mostrarFloat" => true "mostrarDisplay" => false "figura" => array:1 [ 0 => array:4 [ "imagen" => "gr12.jpeg" "Alto" => 566 "Ancho" => 1841 "Tamanyo" => 124560 ] ] "descripcion" => array:1 [ "en" => "Time series of the annual frequency of (a) observed major hurricanes (categories 3 through 5)<a name="p2"></a> (black line) and simulated (red line) from the CTRL experiment; and (b) observed (black line) and simulated (red line) power dissipation index (PDI)." ] ] 12 => array:7 [ "identificador" => "tbl0005" "etiqueta" => "Table I" "tipo" => "MULTIMEDIATABLA" "mostrarFloat" => true "mostrarDisplay" => false "tabla" => array:1 [ "tablatextoimagen" => array:1 [ 0 => array:2 [ "tabla" => array:1 [ 0 => """ <table border="0" frame="\n \t\t\t\t\tvoid\n \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Experiment \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Description \t\t\t\t\t\t\n \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">CTRL \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">Both SST and vertical wind shear correspond to the observed values for each TC, from 1965 to 2013. \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">T65 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">SST is fixed at the observed value in 1965 and vertical wind shear varies for each TC, from 1965 to 2013. \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">V65 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">Shear is fixed at the observed value in 1965 and SST varies for each TC, from 1965 to 2013. \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">VT65 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="left" valign="top">Both SST and vertical wind shear are fixed at the observed values in 1965. \t\t\t\t\t\t\n \t\t\t\t</td></tr></tbody></table> """ ] "imagenFichero" => array:1 [ 0 => "xTab1513547.png" ] ] ] ] "descripcion" => array:1 [ "en" => "Summary of experiments conducted with the tropical cyclone intensity model." ] ] 13 => array:7 [ "identificador" => "tbl0010" "etiqueta" => "Table II" "tipo" => "MULTIMEDIATABLA" "mostrarFloat" => true "mostrarDisplay" => false "tabla" => array:2 [ "tablatextoimagen" => array:1 [ 0 => array:2 [ "tabla" => array:1 [ 0 => """ <table border="0" frame="\n \t\t\t\t\tvoid\n \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head " align="left" valign="bottom" scope="col" style="border-bottom: 2px solid black">Experiment \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="bottom" scope="col" style="border-bottom: 2px solid black">CTRL-PDI \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="left" valign="bottom" scope="col" style="border-bottom: 2px solid black">CTRL- Frequency of major hurricanes \t\t\t\t\t\t\n \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td" title="table-entry " align="left" valign="bottom">T65 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">0.96<a class="elsevierStyleCrossRef" href="#tblfn0005">**</a> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">0.81<a class="elsevierStyleCrossRef" href="#tblfn0005">**</a> \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="bottom">V65 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">0.98<a class="elsevierStyleCrossRef" href="#tblfn0005">**</a> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">0.92<a class="elsevierStyleCrossRef" href="#tblfn0005">**</a> \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">VT65 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">0.94<a class="elsevierStyleCrossRef" href="#tblfn0005">**</a> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">0.84<a class="elsevierStyleCrossRef" href="#tblfn0005">**</a> \t\t\t\t\t\t\n \t\t\t\t</td></tr></tbody></table> """ ] "imagenFichero" => array:1 [ 0 => "xTab1513549.png" ] ] ] "notaPie" => array:1 [ 0 => array:3 [ "identificador" => "tblfn0005" "etiqueta" => "**" "nota" => "Signiicance at the 95% level." ] ] ] "descripcion" => array:1 [ "en" => "Correlation coefficients between the values of PDI and frequency of major hurricanes (category 3-5) in the CTRL and sensitivity experiments (T65, V65 and VT65)." ] ] 14 => array:7 [ "identificador" => "tbl0015" "etiqueta" => "Table III" "tipo" => "MULTIMEDIATABLA" "mostrarFloat" => true "mostrarDisplay" => false "tabla" => array:2 [ "tablatextoimagen" => array:1 [ 0 => array:2 [ "tabla" => array:1 [ 0 => """ <table border="0" frame="\n \t\t\t\t\tvoid\n \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head " align="" valign="top" scope="col" style="border-bottom: 2px solid black"> \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">PDI \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">Frequency of major hurricanes \t\t\t\t\t\t\n \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">SST effect \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">0.22 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">0.06 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">Wind shear effect \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">–0.45<a class="elsevierStyleCrossRef" href="#tblfn0010">**</a> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">–0.27<a class="elsevierStyleCrossRef" href="#tblfn0015">*</a> \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">Combined SST \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="" valign="top"> \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">and wind shear effects \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">–0.49<a class="elsevierStyleCrossRef" href="#tblfn0010">**</a> \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="bottom">–0.30<a class="elsevierStyleCrossRef" href="#tblfn0010">**</a> \t\t\t\t\t\t\n \t\t\t\t</td></tr></tbody></table> """ ] "imagenFichero" => array:1 [ 0 => "xTab1513548.png" ] ] ] "notaPie" => array:2 [ 0 => array:3 [ "identificador" => "tblfn0010" "etiqueta" => "**" "nota" => "Significance at the 95% level" ] 1 => array:3 [ "identificador" => "tblfn0015" "etiqueta" => "*" "nota" => "significance at the 90% level." ] ] ] "descripcion" => array:1 [ "en" => "Effects of SST, wind shear, and combined SST and wind shear, represented by the correlation between the CTRL experiment and the difference (CTRL - experiment). See text for more details." ] ] 15 => array:7 [ "identificador" => "tbl0020" "etiqueta" => "Table IV" "tipo" => "MULTIMEDIATABLA" "mostrarFloat" => true "mostrarDisplay" => false "tabla" => array:2 [ "tablatextoimagen" => array:1 [ 0 => array:2 [ "tabla" => array:1 [ 0 => """ <table border="0" frame="\n \t\t\t\t\tvoid\n \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head " align="" valign="top" scope="col" style="border-bottom: 2px solid black"> \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">Active period \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">Inactive period \t\t\t\t\t\t\n \t\t\t\t</th><th class="td" title="table-head " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">Difference \t\t\t\t\t\t\n \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">HURDAT2 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">5.71 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">1.90 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">3.81<a class="elsevierStyleCrossRef" href="#tblfn0020">**</a> \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">CTRL \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">4.60 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">1.60 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">3.00<a class="elsevierStyleCrossRef" href="#tblfn0020">**</a> \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">T65 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">4.00 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">1.70 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">2.30<a class="elsevierStyleCrossRef" href="#tblfn0025">*</a> \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">V65 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">3.50 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">1.70 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">1.80 \t\t\t\t\t\t\n \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry " align="left" valign="top">VT65 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">4.20 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">1.50 \t\t\t\t\t\t\n \t\t\t\t</td><td class="td" title="table-entry " align="char" valign="top">2.70<a class="elsevierStyleCrossRef" href="#tblfn0025">*</a> \t\t\t\t\t\t\n \t\t\t\t</td></tr></tbody></table> """ ] "imagenFichero" => array:1 [ 0 => "xTab1513546.png" ] ] ] "notaPie" => array:2 [ 0 => array:3 [ "identificador" => "tblfn0020" "etiqueta" => "**" "nota" => "Significance at the 95% level" ] 1 => array:3 [ "identificador" => "tblfn0025" "etiqueta" => "*" "nota" => "significance at the 90% level." ] ] ] "descripcion" => array:1 [ "en" => "Simulated and observed frequency of major hurricanes for active and inactive periods and their difference." ] ] ] "bibliografia" => array:2 [ "titulo" => "References" "seccion" => array:1 [ 0 => array:2 [ "identificador" => "bibs0005" "bibliografiaReferencia" => array:66 [ 0 => array:3 [ "identificador" => "bib0005" "etiqueta" => "Bove et al., 1998" "referencia" => array:1 [ 0 => array:2 [ "contribucion" => array:1 [ 0 => array:2 [ "titulo" => "Effect of El Niño on U" "autores" => array:1 [ 0 => array:2 [ "etal" => false "autores" => array:5 [ 0 => "M.C. 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"vista" => "all" ] ] ] "idiomaDefecto" => "en" "url" => "/01876236/0000002800000003/v2_201709141210/S0187623617300024/v2_201709141210/en/main.assets" "Apartado" => null "PDF" => "https://static.elsevier.es/multimedia/01876236/0000002800000003/v2_201709141210/S0187623617300024/v2_201709141210/en/main.pdf?idApp=UINPBA00004N&text.app=https://www.elsevier.es/" "EPUB" => "https://multimedia.elsevier.es/PublicationsMultimediaV1/item/epub/S0187623617300024?idApp=UINPBA00004N"]

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Haikun Zhao

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zhk2004y@nuist.edu.cn

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Pacific Typhoon Research Center, Key Laboratory of Meteorological Disaster of Ministry of Education, Nanjing University of Information Science and Technology, Nanjing, 210044, China

Graciela B. Raga

Centro de Ciencias de la Atmósfera, Universidad Nacional Autónoma de México, Circuito de la Investigación Científica s/n, Ciudad Universitaria, 04510 México, D.F.

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    "textoCompleto" => "<span class="elsevierStyleSections"><span id="sec0005" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleLabel">1</span><span class="elsevierStyleSectionTitle" id="sect0020">Introduction</span><p id="par0005" class="elsevierStylePara elsevierViewall">The eastern North Pacific &#40;ENP&#41; basin &#40;0-30&#176; N&#44; 140-80&#176; W&#41; exhibits a high level of tropical cyclone &#40;TC&#41; activity&#44; being the second most active region in the globe after the western North Pacific &#40;WNP&#41; basin and the most active in terms of tropical cyclones developed per unit area&#46; About 15 TCs develop in the ENP basin per year on average&#44; accounting for about 19&#37; of global TCs&#46; Since most TCs tend to move westward and&#47;or northwestward&#44; TCs in the ENP make landfall less frequently when compared to other basins&#59; hence&#44; TC activity in the ENP basin has possibly received relatively less attention&#46; However&#44; ENP TC activity is an important factor in the summer precipitation regime across Central America and southwestern North America &#40;<a class="elsevierStyleCrossRef" href="#bib0090">Englehart and Douglas&#44; 2001</a>&#44; <a class="elsevierStyleCrossRef" href="#bib0095">2002</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0040">Corbosiero <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2009</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0290">Wood and Ritchie&#44; 2013</a>&#41;&#46; These regions are projected to experience prolonged drought-like condition in the future climate&#44; so a better understanding of TC activity in the ENP basin has not only scientific relevancy but also a profound socioeconomic impact&#46;</p><p id="par0010" class="elsevierStylePara elsevierViewall">There is currently no generally accepted theory on TC genesis&#59; however&#44; many studies throughout the decades have proposed that a number of physical conditions are needed for&#44; and affect&#44; tropical cyclogenesis&#46; Environmental factors that affect TC genesis include&#58; the Coriolis parameter&#44; sea surface temperature &#40;SST&#41;&#44; low-level vorticity&#44; mid-tropospheric humidity and vertical wind shear &#40;<a class="elsevierStyleCrossRef" href="#bib0110">Gray&#44; 1968</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0210">Mcbride and Zehr&#44; 1981</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0165">Klotzbach and Gray&#44; 2008</a>&#41;&#46; The formation of TCs largely occurs over warm waters with SSTs greater than 26&#46;5 &#176;C&#44; away from the equator and in environments with strong cyclonic low-level relative vorticity&#44; moderate&#47;high mid-tropospheric humidity and weak vertical wind shear&#46; A genesis potential index &#40;GPI&#41; was developed based upon those large-scale parameters &#40;<a class="elsevierStyleCrossRef" href="#bib0115">Gray&#44; 1979</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0270">Watterson <span class="elsevierStyleItalic">et al&#46;</span>&#44; 1995</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0065">Emanuel and Nolan&#44; 2004</a>&#41; to understand the variability of TC genesis and to aid in the prediction of TC activity&#46;</p><p id="par0015" class="elsevierStylePara elsevierViewall">The interannual variability of TC activity in various ocean basins is strongly influenced by ENSO&#44; as summarized in reviews by <a class="elsevierStyleCrossRef" href="#bib0185">Landsea &#40;2000&#41;</a> and <a class="elsevierStyleCrossRef" href="#bib0030">Chu &#40;2004&#41;</a>&#44; but its impact varies from basin to basin&#46; In the North Atlantic basin&#44; the number of TCs is usually below normal during El Ni&#241;o years &#40;<a class="elsevierStyleCrossRef" href="#bib0120">Gray&#44; 1984</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0170">Knaff&#44; 1998</a>&#41; and above normal during La Ni&#241;a years&#46; In addition to TC frequency&#44; ENSO also impacts TC intensity &#40;<a class="elsevierStyleCrossRef" href="#bib0185">Landsea&#44; 2000</a>&#41;&#44; genesis location &#40;<a class="elsevierStyleCrossRef" href="#bib0055">Elsner and Kara&#44; 1998</a>&#41; and landfall probabilities in the US and Caribbean &#40;<a class="elsevierStyleCrossRef" href="#bib0005">Bove <span class="elsevierStyleItalic">et al&#46;</span>&#44; 1998</a>&#59; Pielke and Landsea&#44; 1999&#41;&#46; In the western North Pacific basin&#44; ENSO has no significant impact on TC frequency but has a significant impact on TC intensity&#44; location and track &#40;<a class="elsevierStyleCrossRef" href="#bib0215">Nicholls&#44; 1979</a>&#44; <a class="elsevierStyleCrossRef" href="#bib0220">1992</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0050">Dong&#44; 1998</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0265">Wang and Chan&#44; 2002</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0315">Zhao <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2010</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0325">Zhao and Raga&#44; 2014</a>&#41;&#46;</p><p id="par0020" class="elsevierStylePara elsevierViewall"><a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood &#40;1997&#41;</a> found no effect of ENSO on the TC frequency in the ENP basin&#44; although the number of intense TCs tends to increase during El Ni&#241;o years &#40;<a class="elsevierStyleCrossRef" href="#bib0125">Gray and Sheaffer&#44; 1991</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0035">Collins and Mason&#44; 2000</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0245">Romero-Vadillo <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2007</a>&#41;&#44; similarly to the effect observed in the WNP basin&#46; Using GPI anomaly composites associated with ENSO&#44; <a class="elsevierStyleCrossRef" href="#bib0015">Camargo <span class="elsevierStyleItalic">et al&#46;</span> &#40;2007&#41;</a> concluded that over the eastern North Pacific&#44; vertical wind shear is the main contributor towards the ENSO effect on cyclogenesis with potential intensity also playing a role&#44; and vorticity and relative humidity acting in the opposite sense to the total observed anomaly&#46;</p><p id="par0025" class="elsevierStylePara elsevierViewall">An inverse relationship has been noted between TC activity in the North Atlantic and ENP basin as a function of the ENSO phase &#40;<a class="elsevierStyleCrossRef" href="#bib0120">Gray&#44; 1984</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0180">Lander and Guard&#44; 1998</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0190">Larson <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2005</a>&#41;&#46; These studies indicate that the anti-correlation can be partly explained by the different effects of ENSO on the tropospheric zonal wind shear in the North Atlantic and ENP basins&#46; Moreover&#44; the ENSO-related signal in ENP TC activity seems to be statistically weaker than that in the North Atlantic &#40;<a class="elsevierStyleCrossRef" href="#bib0120">Gray&#44; 1984</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0200">Maga&#241;a <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2003</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0100">Frank and Yong&#44; 2007</a>&#41;&#44; and the robustness of the relationship between ENSO and TC activity in the ENP basin has been questioned &#40;<a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood&#44; 1997</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0240">Ralph and Gough&#44; 2009</a>&#41;&#46;</p><p id="par0030" class="elsevierStylePara elsevierViewall">While the relation between cyclogenesis and SST globally was postulated several decades ago<a name="p3"></a> &#40;<a class="elsevierStyleCrossRef" href="#bib0110">Gray&#44; 1968</a>&#41;&#44; studies indicate that the difference of tropopause temperature and SST act as an upper bound on the maximum potential intensity of a TC but other environmental factors ultimately determine its actual intensity&#46; More recent studies have highlighted the role of oceanic features with elevated heat content and suggested that this variable is more important than the actual SST once it is above the 26&#46;5 &#176;C threshold&#46; Examples of this impact have been published of cases in the Gulf of Mexico and in the WNP&#44; such as hurricanes Katrina and Rita &#40;<a class="elsevierStyleCrossRef" href="#bib0135">Jaimes and Shay&#44; 2009</a>&#41; and super-typhoon Maemi &#40;<a class="elsevierStyleCrossRef" href="#bib0195">Lin <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2005</a>&#41;&#44; respectively&#46; In the ENP&#44; <a class="elsevierStyleCrossRef" href="#bib0225">Oropeza and Raga &#40;2015&#41;</a> showed that there is a link between oceanic features with high heat content and rapid intensification&#46;</p><p id="par0035" class="elsevierStylePara elsevierViewall">In this study&#44; we focus on the period 1965-2013&#44; from the start of the satellite era&#46; The ENP shows a pronounced interannual and decadal variability in the number of TCs during the period 1965-2013 &#40;<a class="elsevierStyleCrossRef" href="#fig0005">Fig&#46; 1</a>&#41;&#46; Note that the minimum TC frequency is observed in 2010&#44; while 1992 presents the maximum frequency during the period considered&#46; <a class="elsevierStyleCrossRef" href="#bib0295">Wu and Chu &#40;2007&#41;</a> compared the changes in large-scale factors between two extreme years 1992 and 1977&#44; representing extreme high and low tropical cyclone activity during the period 1966-2003&#46; Although <a class="elsevierStyleCrossRef" href="#bib0295">Wu and Chu &#40;2007&#41;</a> suggested the environmental factors undergo pronounced changes over the major development region &#40;MDR&#41; for the two extreme years&#44; the interannual variability of TC activity over the ENP basin remains not well understood&#44; particularly the role of factors in contributing towards the interannual variability of TC intensity&#46;</p><elsevierMultimedia ident="fig0005"></elsevierMultimedia><p id="par0040" class="elsevierStylePara elsevierViewall">The main objectives of this study are&#58; &#40;1&#41; to discuss the composite differences in several environmental parameters during periods of high and low TC activity over the ENP basin and to explore the possible physical factors for the differences in activity&#59; and &#40;2&#41; to investigate the relative role of SST&#44; wind shear and TC tracks on the changes in TC intensity over the ENP basin&#46; The rest of this paper is arranged as follows&#46; Section 2 introduces the data employed in this study&#46; Section 3 gives statistical analyses of TC activity over the ENP basin between periods of high and low TC activity and contrasts the associated environmental conditions&#46; Section 4 further investigates the key environmental factors affecting TC intensity over the ENP basin using a numerical intensity model&#46; A discussion of the results and conclusions are presented in Section 5&#46;</p></span><span id="sec0010" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleLabel">2</span><span class="elsevierStyleSectionTitle" id="sect0025">Data and methods</span><span id="sec0015" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleLabel">2&#46;1</span><span class="elsevierStyleSectionTitle" id="sect0030">TC data</span><p id="par0045" class="elsevierStylePara elsevierViewall">The TC data utilized in this study correspond to the best track dataset from Northeast and North Central Pacific Hurricane &#40;HURDAT2&#41; available through the National Hurricane Center&#44; which includes position and intensity at six-hour intervals&#46; Only TCs with maximum sustained winds greater than 17&#46;2 ms<span class="elsevierStyleSup">&#8211;1</span> are considered in this study&#46; The annual distribution of TC frequency in the basin is shown in <a class="elsevierStyleCrossRef" href="#fig0010">Figure 2</a>&#59; note that the majority of TCs occur from June to October &#40;hereafter referred to as peak TC season&#41;&#46; This study will focus on the peak season TC activity over the ENP basin&#59; this is mainly based on the following three reasons&#58; i&#41; the TC frequency over the peak season accounts for about 93&#37; of total season TCs&#59; ii&#41; there is a significant correlation of TC frequency<a name="p4"></a> over the peak season and total season &#40;correlation coefficient&#61;0&#46;97&#41;&#59; and iii&#41; the environmental circulations during the peak TC season are relatively steady&#46;</p><elsevierMultimedia ident="fig0010"></elsevierMultimedia><p id="par0050" class="elsevierStylePara elsevierViewall">In addition to the TC frequency&#44; two other intensity parameters are used to measure changes in the TC activity&#58; the Power Dissipation Index &#40;PDI&#41; &#40;<a class="elsevierStyleCrossRef" href="#bib0070">Emanuel&#44; 2005</a>&#41; and the number of major hurricanes during the peak season&#46; The PDI represents the destructive capability of TC activity and major hurricanes are those with Categories 3&#44; 4 and 5 in the Saffir-Simpson scale &#40;category 3-5 TCs&#41;&#46; These parameters have been used in previous studies &#40;<a class="elsevierStyleCrossRef" href="#bib0070">Emanuel&#44; 2005</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0275">Webster <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2005</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0305">Wu <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2008</a>&#41; to evaluate TC impacts&#59; moreover&#44; the number of major hurricanes may be sensitive to climate change&#44; as suggested by many previous studies &#40;<a class="elsevierStyleCrossRef" href="#bib0020">Chan&#44; 2005</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0080">Emanuel&#44; 2008</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2011</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0310">Wu and Zhao&#44; 2012</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0330">Zhao <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2014</a>&#41;&#46;</p></span><span id="sec0020" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleLabel">2&#46;2</span><span class="elsevierStyleSectionTitle" id="sect0035">Selection of periods of high and low TC activity</span><p id="par0055" class="elsevierStylePara elsevierViewall">The annual TC frequency during the peak season &#40;JJASO&#41; in the ENP basin shows substantial interannual and decadal variability &#40;<a class="elsevierStyleCrossRef" href="#fig0005">Fig&#46; 1a</a>&#41;&#44; with a climatological mean value of 14&#46;08 and a standard deviation of 3&#46;78&#46; The TC frequency during the peak season has a correlation with the annual TC frequency of 0&#46;97&#44; significant at the 95&#37; confidence level &#40;<a class="elsevierStyleCrossRef" href="#fig0005">Fig&#46; 1b</a>&#41;&#46; In this study we define a period of high activity as one during which the total number of TCs observed during the peak season &#40;JJASO&#41; is greater than the mean for the period considered in this study &#40;1965-2013&#41; plus one standard deviation&#46; Conversely&#44; a period of low activity has fewer than the mean minus one standard deviation&#46; During the 49 years considered in this study&#44; there are 7 years with high activity&#58; 1968&#44; 1982&#44; 1983&#44; 1985&#44; 1987&#44; 1990 and 1992&#44; and 10 years with low activity&#58; 1965&#44; 1969&#44; 1977&#44;1979&#44; 1995&#44; 1996&#44; 1999&#44; 2007&#44; 2010&#44; and 2011&#46;</p><p id="par0060" class="elsevierStylePara elsevierViewall">In order to investigate the relationship between ENSO and TC activity over the ENP basin&#44; we define ENSO events as five consecutive overlapping three- month periods at or above the &#43;0&#46;5 &#176;C anomaly for warm &#40;El Ni&#241;o&#41; events and at or below the -0&#46;5 &#176;C anomaly for cold &#40;La Ni&#241;a&#41; events&#59; other events are defined as neutral years&#46; The threshold is further broken down into weak &#40;with a 0&#46;5 to 0&#46;9 &#176;C SST anomaly&#41;&#44; moderate &#40;1&#46;0 to 1&#46;4 &#176;C&#41; and strong &#40;&#8805;1&#46;5 &#176;C&#41; events&#46;</p><p id="par0065" class="elsevierStylePara elsevierViewall">During the seven years with high TC activity we find two strong El Ni&#241;o years &#40;1982 and 1987&#41;&#44; one moderate El Ni&#241;o year &#40;1968&#41;&#44; three neutral years &#40;1985&#44; 1990 and 1992&#41; and a weak La Ni&#241;a year &#40;1983&#41;&#46; During the 10 years with low TC activity we find two strong La Ni&#241;a years &#40;1999 and 2010&#41;&#44; one moderate La Ni&#241;a year &#40;2007&#41;&#44; two weak La Ni&#241;a years &#40;1995 and 2011&#41;&#44; two neutral years &#40;1979 and 1996&#41;&#44; one strong El Ni&#241;o year &#40;1965&#41; and two weak El Ni&#241;o years &#40;1969 and 1977&#41;&#46; There appears to be no significant relationship between ENSO and TC activity over the ENP basin&#44; coinciding with results from some previous studies &#40;<a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood&#44; 1997</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0240">Ralph and Gough&#44; 2009</a>&#41;&#46; The influence of El Ni&#241;o Southern Oscillation on ENP TC activity has been carefully and comprehensively discussed by <a class="elsevierStyleCrossRef" href="#bib0140">Jien <span class="elsevierStyleItalic">et al&#46;</span> &#40;2015&#41;</a>&#46; In this study&#44; we mainly focus on the distinct interannual variability leading to anomalously high and low TC activity over the ENP basin&#44; but the relationship between ENSO and TC activity over the ENP basin will not discussed&#46; We also explore the large multi-decadal variability of TC activity observed over the ENP basin &#40;<a class="elsevierStyleCrossRef" href="#fig0005">Fig&#46; 1</a>&#41; that results in clustering of years with high and low activities&#46; In particular&#44; note that 6 of the 7 years with high activity occur in the period 1980-1994&#44; while 4 years with low activity occur between 1965 and 1980 and the other 6 years of low activity are observed between 1995 and 2013&#46;<a name="p5"></a></p></span><span id="sec0025" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleLabel">2&#46;3</span><span class="elsevierStyleSectionTitle" id="sect0040">Large-scale field data</span><p id="par0070" class="elsevierStylePara elsevierViewall">The monthly environmental variables &#40;i&#46;e&#46;&#44; wind&#44; relative humidity and vertical velocity&#41; are derived from NCEP&#47;NCAR&#44; centered on a 2&#46;5 x 2&#46;5 grid &#40;<a class="elsevierStyleCrossRef" href="#bib0150">Kalnay <span class="elsevierStyleItalic">et al&#46;</span>&#44; 1996</a>&#41;&#46; In order to examine the influence ofthe vertical shear ofthe horizontal wind on TC variability&#44; the vertical shear is computed as the wind difference of the magnitude of the shear vector between 200 hPa and 850 hPa &#40;Vshear&#61;U200&#8722;U8502&#43;V200&#8722;V8502&#41;&#46; The monthly Extended Reconstructed SST version 2 dataset developed on a 2&#176;x 2&#176;grid by <a class="elsevierStyleCrossRef" href="#bib0255">Smith and Reynolds &#40;2004&#41;</a>&#44; is used in the present study&#46;</p></span><span id="sec0030" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleLabel">2&#46;4</span><span class="elsevierStyleSectionTitle" id="sect0045">Intensity model</span><p id="par0075" class="elsevierStylePara elsevierViewall"><a class="elsevierStyleCrossRef" href="#bib0075">Emanuel <span class="elsevierStyleItalic">et al&#46;</span> &#40;2006&#41;</a> successfully reproduced the observed TC climatology from 1980 to 2006 with formation&#44; motion and intensity models&#46; Subsequently&#44; <a class="elsevierStyleCrossRef" href="#bib0085">Emanuel <span class="elsevierStyleItalic">et al&#46;</span> &#40;2008&#41;</a> used this approach to quantify the possible influence of global warming on TC activity&#44; indicating that global TC frequency can be reduced by global warming&#44; but intensity may increase in some places&#46; In this approach&#44; the TC intensity is predicted using a deterministic&#44; coupled air-sea model&#44; the Coupled Hurricane Intensity Prediction System &#40;CHIPS&#41;&#46; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao <span class="elsevierStyleItalic">et al&#46;</span> &#40;2011</a>&#44; 2014b&#41; used this intensity model to investigate interannual and decadal variability of TC activity over the WNP basin&#46; The same intensity model is used in this study&#44; now applied to the ENP basin&#46; The TC intensity model is an axisymmetric numerical atmospheric model&#44; coupled with a simple one dimensional ocean model&#46; In this model&#44; we only consider that changes in three environmental parameters &#40;SST&#44; environmental vertical wind shear and TC tracks&#41; can affect the intensity of tropical cyclones&#46; The simulated TCs are allowed to move along the observed TC tracks during the period 1965-2013&#44; experiencing the observed vertical wind shear and SST along the TC tracks&#44; in order to simulate the evolution of their intensity&#46; The intensity model is initialized with a warm-core cyclonic vortex&#46; The maximum wind speed of the initial vortex is set to be 21m&#47;s after a series of numerical experiments as the model vortex weakens at the beginning of the simulations&#59; this value is also used by other studies &#40;<a class="elsevierStyleCrossRef" href="#bib0310">Wu and Zhao&#44; 2012</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2011</a>&#44; <a class="elsevierStyleCrossRef" href="#bib0330">2014</a>&#41;&#46; The other parameters of the initial vortex needed for the model were taken to be as in <a class="elsevierStyleCrossRef" href="#bib0085">Emanuel <span class="elsevierStyleItalic">et al&#46;</span> &#40;2008&#41;</a> and the same initial model setup is used for all the simulations in this study&#46;</p><p id="par0080" class="elsevierStylePara elsevierViewall">The model skill is determined through correlations of the predicted and observed time series&#46; The statistical significance of the correlations and the differences of the means are tested with Student&#39;s t-test method &#40;<a class="elsevierStyleCrossRef" href="#bib0285">Wilks&#44; 1995</a>&#41;&#46;</p></span></span><span id="sec0035" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleLabel">3</span><span class="elsevierStyleSectionTitle" id="sect0050">Role of environmental factors on TC frequency</span><p id="par0085" class="elsevierStylePara elsevierViewall">An annual average of 20&#46;8 TCs is observed during the 7 years of high activity&#44; which is significantly higher than those generated on average during the 10 years of low activity &#40;9 TCs&#41; at a 95&#37; confidence level&#46; Statistically significant differences can also be observed when separating TCs into their intensity categories&#44; as seen in <a class="elsevierStyleCrossRef" href="#fig0015">Figure 3a</a>&#46; The years with low<a name="p6"></a> overall TC activity also show lower frequency in each of the categories&#46; Further investigation shows that the fraction of major hurricanes &#40;category 3-5 TCs&#41; is significantly higher in years with high activity compared to that in years with low activity&#44; while the proportion of category 1-2 TCs is significantly lower in years with high activity compared to that in years with low activity &#40;<a class="elsevierStyleCrossRef" href="#fig0015">Fig&#46; 3b</a>&#41; at a 95&#37; confidence level&#46; These significant differences may be attributed to the differences observed in the location of TC genesis and occurrence in years with high and low activity &#40;<a class="elsevierStyleCrossRef" href="#fig0020">Fig&#46; 4</a>&#41;&#46; There is a significant region of enhanced TC formation centered around 12&#176; N and 105&#176; W during years of high activity compared to years of low activity &#40;<a class="elsevierStyleCrossRef" href="#fig0020">Fig&#46; 4a</a>&#41;&#46; The average TC formation location shows a significant easterly shift in the years with high activity compared to years of low activity&#46; Correspondingly&#44; more TCs have west- and northwestward tracks during the active versus inactive periods&#46; This difference in frequency of occurrence &#40;<a class="elsevierStyleCrossRef" href="#fig0020">Fig&#46; 4b</a>&#41; is due to differences in TC formation location and also on TC lifetime&#46; The average lifetime is 4&#46;9 days during active years&#44; which is significantly more than 4&#46;2 days during inactive years at a 95&#37; confidence level&#46; The difference of trajectories can be clearly seen in <a class="elsevierStyleCrossRef" href="#fig0025">Figure 5</a> that shows all the TC tracks observed during the active and inactive periods&#46;</p><elsevierMultimedia ident="fig0015"></elsevierMultimedia><elsevierMultimedia ident="fig0020"></elsevierMultimedia><elsevierMultimedia ident="fig0025"></elsevierMultimedia><p id="par0090" class="elsevierStylePara elsevierViewall">The thermal and dynamical components of the GPI &#40;<a class="elsevierStyleCrossRef" href="#bib0110">Gray&#44; 1968</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0065">Emanuel and Nolan&#44; 2004</a>&#41; are examined to determine the role that each may play towards cyclogenesis during years of high and low activity in the ENP basin&#46; The low-level cyclonic vorticity is very important for the development of convection&#44; its organization and its intensification to TC&#44; reducing the local Rossby radius of deformation and focusing the convective heating locally &#40;<a class="elsevierStyleCrossRef" href="#bib0025">Chen <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2006</a>&#41;&#46; <a class="elsevierStyleCrossRef" href="#fig0030">Figure 6</a> shows the composite streamfunction at 850 hPa&#44; and it indicates a significant anticyclonic circulation anomaly over the main development region &#40;MDR&#41; for TC genesis during the active compared to inactive years&#46;<a name="p7"></a> This anticyclonic vorticity anomaly observed during the high activity years would tend to reduce tropical cyclogenesis in this region&#46;</p><elsevierMultimedia ident="fig0030"></elsevierMultimedia><p id="par0095" class="elsevierStylePara elsevierViewall">The presence of high mid-level humidity in the environment allows a parcel of air inside clouds to remain saturated as it entrains the surrounding air during its ascent and it is conductive for maintaining convective activity of the TC development &#40;<a class="elsevierStyleCrossRef" href="#bib0155">Kaplan <span class="elsevierStyleItalic">et al</span>&#46;&#44; 2010</a>&#41;&#46; The results of the composite show a significant decrease in relative humidity at 600 hPa in the MDR during the active years &#40;<a class="elsevierStyleCrossRef" href="#fig0035">Fig&#46; 7</a>&#41;&#46; Lower values<a name="p8"></a> of relative humidity would tend to inhibit TC genesis in this region during the active years&#46; Therefore&#44; the low-level vorticity and mid-troposphere relative humidity both appear to be <span class="elsevierStyleItalic">more favorable</span> for tropical cyclogenesis in the region during the inactive years compared to that during the active years&#46;</p><elsevierMultimedia ident="fig0035"></elsevierMultimedia><p id="par0100" class="elsevierStylePara elsevierViewall">A warm ocean surface allows for enough latent heat flux from ocean to maintain secondary circulation when energy is released near the TC core in the eyewall &#40;<a class="elsevierStyleCrossRef" href="#bib0110">Gray&#44; 1968</a>&#41;&#46; A significantly warm SST anomaly is observed over the MDR area in the ENP basin during active years compared with inactive years&#44; as shown in <a class="elsevierStyleCrossRef" href="#fig0040">Figure 8</a>&#46; Note that the SST pattern during the active years somewhat resembles the pattern associated with the positive phase of the Pacific Decadal Oscillation &#40;PDO&#41;&#44; which suggests that the TC activity may be modulated by the PDO&#59; however&#44; the HURDAT time series is currently not long enough to evaluate this potential influence&#46;</p><elsevierMultimedia ident="fig0040"></elsevierMultimedia><p id="par0105" class="elsevierStylePara elsevierViewall">The presence of significant vertical wind shear inhibits TC development by advecting away the heating and moisture from the center of the convection &#40;<a class="elsevierStyleCrossRef" href="#bib0045">DeMaria&#44; 1996</a>&#41;&#46; A significant decrease of vertical wind shear is observed over the ENP basin during the years of high activity compared to inactive years&#44; as can be seen in <a class="elsevierStyleCrossRef" href="#fig0045">Figure 9</a>&#46; During high TC activity years the shear between 850 and 200 hPa is up to 4 ms<span class="elsevierStyleSup">&#8211;1</span> lower than during inactive years in the MDR of this basin&#59; this decrease in shear leads to more vertical coherence of developing cyclones and is conducive of further intensification during active years&#46;</p><elsevierMultimedia ident="fig0045"></elsevierMultimedia><p id="par0110" class="elsevierStylePara elsevierViewall">In order to further investigate the relative roles of these environmental factors&#44; we calculate the correlation coefficient between TC frequency and<a name="p9"></a> the analyzed large-scale factors over the MDR&#46; The results indicate that the low-level vorticity and relative humidity are anti-correlated with MDR TC frequency&#44; with correlation coefficients &#8211;0&#46;11 and &#8211;0&#46;21&#44; respectively&#46; These coefficients are in agreement with anticyclonic anomalies &#40;<a class="elsevierStyleCrossRef" href="#fig0030">Fig&#46; 6</a>&#41; and decrease in relative humidity &#40;<a class="elsevierStyleCrossRef" href="#fig0035">Fig&#46; 7</a>&#41; during the active years&#46; Note&#44; however&#44; that neither correlation is significant at the 95&#37; confidence level&#46; A positive but not significant correlation &#40;0&#46;15&#41; is found for SST and MRD TC frequency&#46; This result suggests that while the SST anomalies appear large in the basin &#40;<a class="elsevierStyleCrossRef" href="#fig0040">Fig&#46; 8</a>&#41;&#44; the local SST may not play a dominant role in TC frequency&#46; Moreover&#44; the correlation between MDR TC frequency over the ENP basin and Ni&#241;o-3&#46;4 SST suggests no significant correlation between them&#44; in agreement with previous studies &#40;<a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood&#44; 1997</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0245">Romero-Vadillo <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2007</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0240">Ralph and Gough&#44; 2009</a>&#41;&#46; The largest correlation is obtained between MDR TC frequency and vertical wind shear &#40;&#8211;0&#46;31&#44; which is significant at the 95&#37; confidence level&#41;&#44; consistent with the results of Camargo <span class="elsevierStyleItalic">et al&#46;</span> &#40;2007&#41;&#44; and indicative of the dominant role that the vertical wind shear plays in modulating TC genesis over the ENP basin&#46;</p><p id="par0115" class="elsevierStylePara elsevierViewall">We calculate the four factors of the GPI separately&#58; vorticity at 850hPa&#44; relative humidity at 600hPa&#44; potential intensity and vertical wind shear to gain more insight into the role of each of them&#46; The details of the calculation of the GPI can be found in <a class="elsevierStyleCrossRef" href="#bib0065">Emanuel and Nolan &#40;2004&#41;</a>&#46; Following <a class="elsevierStyleCrossRef" href="#bib0015">Camargo <span class="elsevierStyleItalic">et al&#46;</span> &#40;2007&#41;</a> and <a class="elsevierStyleCrossRef" href="#bib0325">Zhao and Raga &#40;2014&#41;</a>&#44; we evaluate the relative contribution of each of the four factors to the overall GPI anomaly between years with high and low activity&#46; Specifically&#44; we compute the GPI using the long-term climatology &#40;1965-2013&#41; of three of the factors and used the actual data for the fourth factor&#59; this calculation is then repeated for each of the other three factors&#46; For each factor&#44; the individual GPI anomalies between years with high and low activity are then calculated&#46; Although the net anomaly cannot be simply described as the sum of the four fields combined due to the nonlinearity of the GPI&#44; to a certain extent&#44; the index can provide weights that appropriately quantify the influence of the different factors for the difference of TC genesis between years with high and low activity&#46;</p><p id="par0120" class="elsevierStylePara elsevierViewall"><a class="elsevierStyleCrossRef" href="#fig0050">Figure 10</a> shows the average GPI during years with high and low TC activity and the difference of active minus inactive years&#46; There is a large positive GPI anomaly evident over the ENP basin&#44; with a maximum over 8-12&#176; N&#44; 105-80&#176; W&#46; There is an eastward shift of the GPI anomalies to the observed TC genesis anomaly&#46; <a class="elsevierStyleCrossRef" href="#fig0055">Figures 11a&#44; b&#44; c</a> and d display the GPI anomalies between years<a name="p10"></a> with high and low activity calculated when the relative humidity&#44; vorticity&#44; potential intensity and vertical wind shear are respectively varied while keeping the other three variables fixed at their climatologically values&#46; Comparing the panels in <a class="elsevierStyleCrossRef" href="#fig0055">Figure 11</a> with the GPI anomalies between years with high and low activity when all four factors are varying &#40;<a class="elsevierStyleCrossRef" href="#fig0050">Fig&#46; 10c</a>&#41;&#44; it is possible to determine the relative contribution of each factor to the overall GPI anomaly pattern&#46; Note the overall negative GPI anomalies over the ENP basin in <a class="elsevierStyleCrossRef" href="#fig0055">Fig&#46; 11a&#44; b</a>&#59; these negative anomalies indicate that changes in relative humidity and vorticity do not contribute towards TC genesis during the active years compared to that during inactive years&#46; In contrast&#44; there are positive GPI anomalies in the MDR of the ENP basin in <a class="elsevierStyleCrossRef" href="#fig0055">Figures 11c&#44; d</a>&#44; indicating that the SST and vertical wind shear make a positive contribution towards TC genesis during the active years compared to that during the inactive years&#46; Moreover&#44; note that the magnitude of the GPI anomaly when vertical wind shear varies &#40;<a class="elsevierStyleCrossRef" href="#fig0055">Fig&#46; 11d</a>&#41; is higher than the magnitude of the GPI anomaly when potential intensity varies &#40;<a class="elsevierStyleCrossRef" href="#fig0055">Fig&#46; 11c</a>&#41;&#46; This clearly suggests that the vertical wind shear is the dominant contributor towards favoring TC genesis during active years and suppressing it during the inactive years&#46; These GPI results are consistent with the differences in composite large-scale patterns between active and inactive years and correlation analyses reported above&#46;</p><elsevierMultimedia ident="fig0050"></elsevierMultimedia><elsevierMultimedia ident="fig0055"></elsevierMultimedia></span><span id="sec0040" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleLabel">4</span><span class="elsevierStyleSectionTitle" id="sect0055">Role of environmental factors on TC intensity</span><p id="par0125" class="elsevierStylePara elsevierViewall">The intensity of TCs in the ENP basin shows significant interannual variability&#44; as can be seen in <a class="elsevierStyleCrossRef" href="#fig0060">Figure 12a</a> &#40;black line&#41;&#44; which displays the number of major hurricanes in the basin &#40;category 3-5 TCs&#41;&#46; During the active years&#44; an average of 5&#46;71 category 3-5 TCs are observed during the peak TC season over the ENP basin&#44; while only 1&#46;9 on average is present in the inactive years&#46; A large and significant &#40;3&#46;8&#44; at 95&#37; confidence level&#41; difference in the frequency of major hurricanes is observed between active and inactive years&#46;</p><elsevierMultimedia ident="fig0060"></elsevierMultimedia><p id="par0130" class="elsevierStylePara elsevierViewall">In order to evaluate the contributions of vertical wind shear&#44; SST and track changes to TC intensity change&#44; we follow the methodology used by <a class="elsevierStyleCrossRef" href="#bib0320">Zhao <span class="elsevierStyleItalic">et al&#46;</span> &#40;2011</a>&#44; <a class="elsevierStyleCrossRef" href="#bib0330">2014</a>&#41; and apply the same intensity model to the ENP basin to evaluate TC intensity along the observed TC tracks&#46; We perform a control experiment &#40;CTRL&#41;<a name="p11"></a><a name="p12"></a> and three other sensitivity simulations&#58; T65&#44; V65 and VT65&#44; as noted in <a class="elsevierStyleCrossRef" href="#tbl0005">Table I</a>&#46; The experiment labeled T65 is similar to CTRL&#44; but keeps SST along the TC track fixed and corresponds to the values observed in 1965&#46; In experiment V65&#44; the vertical wind shear is fixed &#40;corresponding to the observations of 1965&#41; and in experiment VT65 both the SST and vertical wind shear are fixed corresponding to the values observed in 1965&#46; Note that the tracks of individual TCs remain unchanged in the sensitivity experiments&#59; the tracks correspond to the observed trajectories from the HURDAT2 dataset&#46;</p><elsevierMultimedia ident="tbl0005"></elsevierMultimedia><p id="par0135" class="elsevierStylePara elsevierViewall">In the CTRL experiment&#44; all the TCs move along their observed tracks and experience the observed monthly vertical wind shear and SST along their lifetimes&#44; in the period &#40;1965-2013&#41;&#46; The results from the CTRL experiment indicate that the simulated frequency of major hurricanes &#40;TCs with Categories 3 through 5&#41; and PDI are in good agreement with the observations &#40;<a class="elsevierStyleCrossRef" href="#fig0060">Fig&#46; 12</a>&#41;&#46; The correlation coefficients are 0&#46;64 and 0&#46;87&#44; respectively during the period 1965-2013&#44; both statistically significant at a 95&#37; confidence level&#46; Due to a successful simulation in annual PDI and category 3-5 TC frequency&#44; it raise our confidence for further exploring the relative role of SST&#44; wind shear and TC tracks to changes in PDI and category 3-5 TC frequency in terms of correlation and magnitude&#46;</p><p id="par0140" class="elsevierStylePara elsevierViewall">The values of the correlation coefficients presented in <a class="elsevierStyleCrossRef" href="#tbl0010">Table II</a> indicate that the simulated annual frequency of major hurricanes&#44; as well as the PDI&#44; in the three sensitivity experiments is well correlated with results from the CTRL experiment &#40;all correlation coefficients are above 0&#46;8 and statistically significant&#41;&#46; Recall that although all three sensitivity experiments are highly idealized because they consider fixed conditions at 1965 values for the SST and&#47;or the vertical wind shear&#44; the TC tracks remain unchanged in the three sensitive experiments and CTRL experiment&#46; The high correlations between the CTRL and the three sensitive experiments suggest that the primary controlling factor for the interannual variability may actually be the trajectories of the TCs&#46;</p><elsevierMultimedia ident="tbl0010"></elsevierMultimedia><p id="par0145" class="elsevierStylePara elsevierViewall"><a class="elsevierStyleCrossRef" href="#tbl0015">Table III</a> presents the correlations of the difference in PDI and frequency of category 3-5 TCs for each of the sensitivity experiments and the CTRL experiment&#46; The influence of the SST on the interannual variability can be determined by comparing the results for the CTRL and &#40;CTRL &#8211; T65&#41; experiments&#46; The effect of SST is small for the set of experiments&#44; since the correlations are 0&#46;06 and 0&#46;22 and non-significant&#46; Similarly&#44; the effect of the vertical wind shear on TC intensity&#44; evaluated by comparing the results from the CTRL and &#40;CTRL &#8211; V65&#41; experiments&#44; indicates a stronger dependence than with SST&#44; with larger and significant correlation coefficients&#46; Note that the combined effect of SST and vertical wind shear changes to the interannual variability&#44; by comparing CTRL and &#40;CTRL &#8211; VT65&#41;&#44; is larger than the sum of their individual contributions&#46; The correlation coefficients for the frequency of category 3-5 TCs and PDI are &#8211;0&#46;30&#44; and &#8211;0&#46;49&#44; respectively&#44; both significant at a 95&#37; confidence level&#46;</p><elsevierMultimedia ident="tbl0015"></elsevierMultimedia><p id="par0150" class="elsevierStylePara elsevierViewall">A similar analysis was performed to compare the results of the simulations against observations for<a name="p13"></a> the periods of high and low activity identified&#46; The results are presented in <a class="elsevierStyleCrossRef" href="#tbl0020">Table IV</a> and show again that the dominant role in the interannual variability of the frequency of major hurricanes and PDI &#40;not shown&#41; in associated with reduced wind shear in the basin and that the local SST anomalies play a secondary role compared to the wind shear negative anomalies&#46; These results are in agreement with previous studies &#40;<a class="elsevierStyleCrossRef" href="#bib0060">Emanuel&#44; 1987</a>&#44; <a class="elsevierStyleCrossRef" href="#bib0080">2008</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0105">Goldenberg <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2001</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0275">Webster <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2005</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2011</a>&#41;&#44; that indicate that decreased vertical wind shear is related to increased TC intensity&#44; and that higher SST correspond to higher TC intensity&#46;</p><elsevierMultimedia ident="tbl0020"></elsevierMultimedia><p id="par0155" class="elsevierStylePara elsevierViewall">As mentioned briefly above&#44; the interannual variability of TC trajectories may also be playing a significant role in the variability of TC intensity&#46; We explore further this possibility by comparing results from the CTRL and VT65 experiments&#46; Note that the frequency of major hurricanes is well correlated between these two experiments &#40;0&#46;84&#44; significant at the 95&#37; confidence level&#44; see <a class="elsevierStyleCrossRef" href="#tbl0010">Table II</a>&#41;&#46; This indicates that the changes in the TC tracks can account for most of the observed interannual variability&#44; partly due to the combined effect of changes in SST and vertical wind shear&#46; These results confirm that the change in TC duration is the main factor for the observed change in TC intensity &#40;<a class="elsevierStyleCrossRef" href="#bib0010">Camargo and Sobel&#44; 2005</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0300">Wu and Wang&#44; 2008</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2011</a>&#41;&#46; Changes in TC lifetime are closely associated with changes in TC tracks&#46; TC lifetime is also closely associated with TC genesis location&#46; During the years with high activity&#44; the region of enhanced TC formation shifts eastward and leads to longer TC tracks and thus&#44; longer lifetimes&#46; This in turn will result in TCs having more time for intensification and an increased likelihood of developing into intense TCs compared to that during the years with low activity&#46; The eastward shift of the region of enhanced TC formation is also closely associated with warmer SST and lower vertical wind shear during years with high activity than during years with low activity&#46;</p></span><span id="sec0045" class="elsevierStyleSection elsevierViewall"><span class="elsevierStyleLabel">5</span><span class="elsevierStyleSectionTitle" id="sect0060">Discussion and conclusions</span><p id="par0160" class="elsevierStylePara elsevierViewall">The ENP basin exhibits very large interannual variability in the frequency of TCs&#46; The analysis of the 49-year period between 1965 and 2013 indicates that during the high activity period&#44; more than twice as many TCs develop on average in the basin compared to the low activity period&#46; This study investigates the large-scale conditions affecting TC genesis and the key factors affecting TC intensity&#44; to try to evaluate their roles on the interannual variability analyzing periods of high and low activity during the period 1965-2013&#46; As was shown in <a class="elsevierStyleCrossRef" href="#fig0020">Figure 4</a>&#44; the years of high activity show a statistically significant easterly shift of the genesis location of tropical cyclones&#46; <a class="elsevierStyleCrossRef" href="#bib0130">Gutzler <span class="elsevierStyleItalic">et al&#46;</span> &#40;2013&#41;</a> found that TCs in the ENP basin occurred near the coast of Mexico more often during La Ni&#241;a years in the early season for the period 1951-2006&#46; But recall that the years of high activity in our study also include neutral years of the ENSO&#44; suggesting that there are other factors that may modulate genesis location&#46;</p><p id="par0165" class="elsevierStylePara elsevierViewall">The results of the analysis of composites of large-scale environmental conditions for active versus inactive years &#40;presented in <a class="elsevierStyleCrossRefs" href="#fig0030">Figs&#46; 6 through 9</a>&#41; are very interesting&#46; The low-level vorticity shows an anticyclonic anomaly and the mid-tropospheric relative<a name="p14"></a> humidity shows a dry anomaly during the active years&#46; Both these anomalies would tend to reduce tropical cyclogenesis in the basin&#44; not contributing towards active years&#46; The most important environmental aspect that favors an increase in the frequency of tropical cyclones is the reduced vertical shear of the horizontal wind over the whole ENP basin&#46; These results are further supported and confirmed by the GPI analyses&#46;</p><p id="par0170" class="elsevierStylePara elsevierViewall">These results are consistent with those presented by <a class="elsevierStyleCrossRef" href="#bib0015">Camargo <span class="elsevierStyleItalic">et al&#46;</span> &#40;2007&#41;</a> in their analysis of the composites of El Ni&#241;o and La Ni&#241;a years&#46; In their study&#44; vertical wind shear was also the main contributor to ENSO genesis potential anomalies in the ENP&#44; and low-level vorticity and mid-tropospheric relative humidity contributing in the opposite sense&#46; However&#44; the active and inactive periods studied here do not correspond exclusively to either La Ni&#241;a or El Ni&#241;o years&#46; The ENSO signal on TC activity seems to be statistically weaker in the ENP basin than that in the North Atlantic&#44; as has been noted by previous studies &#40;<a class="elsevierStyleCrossRef" href="#bib0120">Gray&#44; 1984</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0200">Maga&#241;a <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2003</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0100">Frank and Yong&#44; 2007</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0245">Romero-Vadillo <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2007</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0205">Mart&#237;nez-S&#225;nchez and Cavazos&#44; 2014</a>&#44; among others&#41;&#46; Furthermore&#44; <a class="elsevierStyleCrossRef" href="#bib0280">Whitney and Hobgood &#40;1997&#41;</a> and <a class="elsevierStyleCrossRef" href="#bib0240">Ralph and Gough &#40;2009&#41;</a> have questioned the robustness of the relationship between ENSO and TC activity in the ENP basin&#46; However&#44; the recent study by <a class="elsevierStyleCrossRef" href="#bib0140">Jien <span class="elsevierStyleItalic">et al&#46;</span> &#40;2015&#41;</a> found a statistical dependency of TC activity on the ENSO phases&#44; but significant only on the western portion of the development region&#44; between 112 and 140&#176; W&#46; Specifically&#44; their results indicate that El Ni&#241;o years are characterized by more frequent and more intense events compared to La Ni&#241;a conditions for this western sub-region of the basin&#46; These new results are not in agreement with results by <a class="elsevierStyleCrossRef" href="#bib0015">Camargo <span class="elsevierStyleItalic">et al&#46;</span> &#40;2007&#41;</a>&#46; And our results of active years indicate that the maximum anomaly in the reduction of wind shear covers a large section of the western sub-region defined in <a class="elsevierStyleCrossRef" href="#bib0140">Jien <span class="elsevierStyleItalic">et al&#46;</span> &#40;2015&#41;</a>&#46; This suggests to us that the ENSO modulation may not be a good predictor for years of high activity in the ENP basin as claimed by <a class="elsevierStyleCrossRef" href="#bib0140">Jien <span class="elsevierStyleItalic">et al&#46;</span> &#40;2015&#41;</a>&#46;</p><p id="par0175" class="elsevierStylePara elsevierViewall">Also interesting to discuss are the results related to the SST anomalies&#44; which appear to contribute positively towards tropical cyclogenesis during the active years&#44; yet the correlations with TC frequency are not significant&#46; <a class="elsevierStyleCrossRef" href="#fig0040">Figure 8</a> shows a spatial distribution of the SST anomalies between active and inactive years that somewhat resembles the pattern associated with the positive phase of the Pacific Decadal Oscillation &#40;PDO&#41;&#44; which suggests that the TC activity may be modulated by the PDO&#46; <a class="elsevierStyleCrossRef" href="#bib0235">Raga <span class="elsevierStyleItalic">et al&#46;</span> &#40;2013&#41;</a> determined that the time series of 161 years of landfalling TCs &#40;reconstructed from historical records and combined with modern best track data&#41; exhibits a moderate correlation with the PDO&#46; A previous study by <a class="elsevierStyleCrossRef" href="#bib0095">Englehart and Douglas &#40;2002&#41;</a> showed that precipitation in NW Mexico is correlated also with PDO&#46; It is noteworthy that landfalls are only marginally larger &#40;but not significant&#41; during active years &#40;2&#46;00<span class="elsevierStyleHsp" style=""></span>&#177;<span class="elsevierStyleHsp" style=""></span>1&#46;15&#41; than inactive years &#40;1&#46;70<span class="elsevierStyleHsp" style=""></span>&#177;<span class="elsevierStyleHsp" style=""></span>1&#46;16&#41;&#44; while the ratio of landfalls to the total count of TCs is almost a factor of 2 different &#40;0&#46;10 versus 0&#46;19&#41;&#44; respectively&#46; Inactive years do not necessarily imply fewer landfalls and&#44; thus&#44; less-affected regions of western Mexico&#46;</p><p id="par0180" class="elsevierStylePara elsevierViewall">The eastern North Pacific basin exhibits very large interannual variability in the frequency of major hurricanes&#44; as seen in <a class="elsevierStyleCrossRef" href="#fig0060">Figure 12a</a>&#44; and active years also show a significant increase in major hurricanes &#40;<a class="elsevierStyleCrossRef" href="#fig0015">Fig&#46; 3a</a>&#41;&#46; The forecast of TC intensity has remained problematic not only in the ENP basin&#44; but also globally&#46; Our results show a lack of significance in the correlation between SST anomalies and TC frequency and also TC intensity&#46; Even though during El Ni&#241;o years and during the most active years the SST positive anomalies in the basin are quite large&#44; and would in principle contribute to increased convection&#44; the correlations are mostly not significant&#46; The answer may be related to the ocean heat content and not SST&#44; as suggested by <a class="elsevierStyleCrossRef" href="#bib0250">Shay and Brewster &#40;2010&#41;</a>&#46; The recent paper by <a class="elsevierStyleCrossRef" href="#bib0145">Jin <span class="elsevierStyleItalic">et al&#46;</span> &#40;2014&#41;</a> argues that the intensification of TCs in the ENP basin is related to subsurface ocean heat the season after the maximum of El Ni&#241;o&#44; through a delayed ocean transport mechanism&#46; Another aspect to be considered when studying TC intensification is the presence of transient anticyclonic eddies in the ENP basin that locally can enhance the ocean heat content available for fueling tropical cyclones&#46; <a class="elsevierStyleCrossRef" href="#bib0225">Oropeza and Raga &#40;2015&#41;</a> have shown the importance of the presence of such eddies in the rapid and explosive intensification of hurricanes in the ENP basin&#46;</p><p id="par0185" class="elsevierStylePara elsevierViewall">In this study&#44; we used a hurricane intensity model &#40;<a class="elsevierStyleCrossRef" href="#bib0075">Emanuel <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2006</a>&#41; to evaluate the individual contributions of changes in the SST&#44; vertical wind shear and TC tracks to changes in TC intensity on<a name="p15"></a> the interannual time scale and considering also the active and inactive periods&#46; Two parameters are used to quantify TC intensity in the basin&#58; the frequency of major hurricanes and the PDI&#46; The results suggest that the primary controlling factor for the interannual variability may actually be the trajectories of the TCs&#44; as was also indicated in the WNP basin in studies by <a class="elsevierStyleCrossRef" href="#bib0265">Wang and Chan &#40;2002&#41;</a> and <a class="elsevierStyleCrossRef" href="#bib0010">Camargo and Sobel &#40;2005&#41;</a>&#46; TC intensity exhibits a stronger dependence on the effect of the vertical wind shear than on the local SST&#46; Note that the combined effects of vertical wind shear and SST appear to be more important than their respective roles and that the frequency of major hurricanes is a more sensitive variable to climate change than the PDI&#46;</p><p id="par0190" class="elsevierStylePara elsevierViewall">Studies by <a class="elsevierStyleCrossRef" href="#bib0300">Wu and Wang &#40;2008&#41;</a>&#44; <a class="elsevierStyleCrossRef" href="#bib0320">Zhao <span class="elsevierStyleItalic">et al&#46;</span> &#40;2011&#41;</a>&#44; <a class="elsevierStyleCrossRef" href="#bib0310">Wu and Zhao &#40;2012&#41;</a> and <a class="elsevierStyleCrossRef" href="#bib0330">Zhao <span class="elsevierStyleItalic">et al&#46;</span> &#40;2014&#41;</a> have investigated TC activity in the WNP basin&#44; and suggested that shifts in the TC tracks may have allowed more TCs to have longer lifetimes&#44; favoring more intense TCs&#46; Our results from the ENP basin clearly indicate that TC formation is enhanced around 12&#176; N&#44; 105&#176; W in a region of statistically significant reduced vertical wind shear&#44; and that TCs favor a northwestward track during the active years &#40;<a class="elsevierStyleCrossRef" href="#fig0020">Fig&#46; 4</a>&#41;&#46; These tracks during the active years expose TCs to the warmer SST anomalies in the region that resemble the PDO pattern &#40;<a class="elsevierStyleCrossRef" href="#fig0040">Fig&#46; 8</a>&#41;&#44; resulting in longer lifetimes and more intense TCs&#46; The study by Martinez-Sanchez and Cavazos &#40;2014&#41; shows a correlation between PDO hurricanes with category 4 and 5 in the ENP basin&#46;</p><p id="par0195" class="elsevierStylePara elsevierViewall">Finally&#44; it seems pertinent to briefly discuss our results of TC frequency and intensity during active years in the context of climate change scenarios&#46; Several studies in the last decades &#40;<a class="elsevierStyleCrossRef" href="#bib0060">Emanuel&#44; 1987</a>&#44; <a class="elsevierStyleCrossRef" href="#bib0070">2005</a>&#44; <a class="elsevierStyleCrossRef" href="#bib0080">2008</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0275">Webster <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2005</a>&#59; <a class="elsevierStyleCrossRef" href="#bib0305">Wu <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2008</a>&#41; have discussed the influence of SST and vertical wind shear on changes in TC intensity either globally or focusing primarily on the North Atlantic basin &#40;<a class="elsevierStyleCrossRef" href="#bib0105">Goldenberg <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2001</a>&#41;&#46; Results of a global coupled climate model &#40;<a class="elsevierStyleCrossRef" href="#bib0260">Vecchi and Soden&#44; 2007</a>&#41; for the twenty first century suggest that the maximum potential intensity in the ENP basin will increase from the coast of Mexico westward to 120&#176; W and between 10 and 20&#176; N&#44; well within the region of enhanced TC genesis and enhanced tracks during the high activity years&#46; While our results indicate that the potential intensity does not appear to be a dominant contributor to cyclogenesis in the active years&#44; it is possible that large-scale conditions may lead to more intense TCs during active years in the basin&#46; Nevertheless&#44; further studies analyzing the results of coupled models are needed to evaluate the role of the most favorable factor &#40;reduced vertical wind shear&#41; in the basin&#46;</p></span></span>"
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          "titulo" => "Role of environmental factors on TC intensity"
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        "resumen" => "<span id="abst0005" class="elsevierStyleSection elsevierViewall"><p id="spar0005" class="elsevierStyleSimplePara elsevierViewall">La cuenca del Pacifico tropical nororiental presenta una gran variabilidad interanual en cuanto a la frecuencia de ocurrencia de ciclones&#44; con a&#241;os muy activos &#40;con m&#225;s de 20 ciclones durante la temporada&#41; y a&#241;os muy poco activos &#40;con s&#243;lo ocho ciclones&#41;&#46; En este estudio se investigan los factores de gran escala que pueden influenciar la variabilidad interanual analizando los compuestos de siete a&#241;os muy activos y 10 a&#241;os muy poco activos durante los 49 a&#241;os del periodo 1965-2013&#46; Los resultados del an&#225;lisis de compuestos indican que la vorticidad a niveles bajos y la humedad relativa en la troposfera media son poco favorables para la ciclog&#233;nesis tropical durante los a&#241;os activos&#46; La temperatura superficial del mar &#40;TSM&#41; parece desempe&#241;ar un peque&#241;o rol modulando la frecuencia&#44; y la disminuci&#243;n observada en la cizalladura del viento entre 850 y 200 hPa domina la ciclog&#233;nesis durante los a&#241;os activos&#44; confirmando resultados previos de Camargo <span class="elsevierStyleItalic">et al&#46;</span> &#40;2007&#41;&#46; Se investigan adem&#225;s los factores ambientales de gran escala que afectan la intensidad de los ciclones tropicales en la cuenca con un modelo num&#233;rico de intensidad &#40;Emanuel <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2006&#44; 2008&#41;&#44; el cual predice la intensidad con base en la cizalladura del viento&#44; la TSM y las trayectorias observadas&#46; Los resultados indican que la variabilidad interanual en la frecuencia de huracanes mayores &#40;categor&#237;as 3 a 5&#41; se simula mejor cuando ambos par&#225;metros se combinan&#46; Tambi&#233;n es posible que los cambios en las trayectorias puedan ser determinantes para la intensidad alcanzada&#46; En particular&#44; durante los a&#241;os activos&#44; la zona de ciclog&#233;nesis se desplaza hacia el este y hay m&#225;s ciclones con trayectoria norte-noroeste&#44; lo cual determina que tengan una vida m&#225;s larga y sean de mayor intensidad que los que se desarrollan en a&#241;os con poca actividad en la cuenca&#46;</p></span>"
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        "resumen" => "<span id="abst0010" class="elsevierStyleSection elsevierViewall"><p id="spar0010" class="elsevierStyleSimplePara elsevierViewall">The tropical eastern North Pacific &#40;ENP&#41; basin exhibits very large interannual variability in the frequency of occurrence of tropical cyclones&#44; presenting very active &#40;more than 20 tropical cyclones per season&#41; and very inactive years &#40;only eigth tropical cyclones&#41;&#46; The large-scale factors that may influence the distinct interannual variability are investigated in this study&#44; by analyzing the composites of seven years of high activity and 10 years of low activity from 1965 to 2013&#46; The results of composite analyses indicate that the low-level vorticity and mid-tropospheric relative humidity are mostly unfavorable for tropical cyclogenesis during active years&#46; The sea surface temperature &#40;SST&#41; may play a small role modulating the occurrence of tropical cyclones&#44; but the reduced vertical shear of the horizontal wind between 850 and 200 hPa is the main contributor to clyclogenesis during the active years&#44; confirming earlier results by Camargo <span class="elsevierStyleItalic">et al&#46;</span> &#40;2007&#41;&#46; We use an intensity model &#40;Emanuel <span class="elsevierStyleItalic">et al&#46;</span>&#44; 2006&#44; 2008&#41; to further investigate the key environmental factors affecting TC intensity&#44; exploring the relative roles of changes in SST&#44; vertical wind shear and TC tracks&#46; The results indicate that the interannual variability in the frequency of major hurricanes &#40;categories 3 through 5&#41; is best simulated when the effects of both SST and vertical wind shear are combined&#46; Furthermore&#44; changes in TC tracks may play an important role in the intensity achieved&#46; In particular&#44; during the years with high activity&#44; the location for cyclogenesis shifts eastward and more TCs have west-northwestward tracks&#44; leading to longer lifetime and higher intensity&#44; compared to years with low TC activity in the basin&#46;</p></span>"
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          "en" => "<p id="spar0015" class="elsevierStyleSimplePara elsevierViewall">Observed number of tropical cyclones &#40;TCs&#41; reaching at least tropical storm strength in the NHC best track dataset over the Eastern North Pacific &#40;ENP&#41; during the period 1965-2013 for &#40;a&#41; the peak season &#40;June through October&#41; and &#40;b&#41; the whole year &#40;January-December&#41;</p>"
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          "en" => "<p id="spar0025" class="elsevierStyleSimplePara elsevierViewall">&#40;a&#41; Average observed number&#59; and &#40;b&#41; proportion of tropical cyclones &#40;TCs&#41; separated as a function of their intensity in the NHC best track dataset over the eastern North Pacific &#40;ENP&#41; during the peak season for periods of high &#40;red&#41; and low &#40;black&#41; activity&#46; The grey bar corresponds to one standard deviation for the study period 1965-2013&#46;</p>"
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          "en" => "<p id="spar0030" class="elsevierStyleSimplePara elsevierViewall">Composite difference &#40;active minus inactive years&#41; through the peak TC season of&#58; &#40;a&#41; TC genesis frequency&#59; and &#40;b&#41; occurrence frequency&#46; The shading indicates statistical significant differences at the 95&#37; confidence level&#46;</p>"
        ]
      ]
      4 => array:7 [
        "identificador" => "fig0025"
        "etiqueta" => "Fig&#46; 5"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr5.jpeg"
            "Alto" => 1198
            "Ancho" => 940
            "Tamanyo" => 225184
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0035" class="elsevierStyleSimplePara elsevierViewall">Trajectories of the tropical cyclones observed during the peak season of &#40;a&#41; active&#44; and &#40;b&#41; inactive years in the period 1965-2013&#46;</p>"
        ]
      ]
      5 => array:7 [
        "identificador" => "fig0030"
        "etiqueta" => "Fig&#46; 6"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr6.jpeg"
            "Alto" => 1968
            "Ancho" => 940
            "Tamanyo" => 612509
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0040" class="elsevierStyleSimplePara elsevierViewall">Composite 850 hPa stream function through the peak TC season for &#40;a&#41; active years&#44; &#40;b&#41; inactive years&#44; and &#40;c&#41; the difference &#40;active minus inactive years&#41;&#46; The shading indicates statistical significant differences at the 95&#37; confidence level&#46;</p>"
        ]
      ]
      6 => array:7 [
        "identificador" => "fig0035"
        "etiqueta" => "Fig&#46; 7"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr7.jpeg"
            "Alto" => 2002
            "Ancho" => 943
            "Tamanyo" => 260881
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0045" class="elsevierStyleSimplePara elsevierViewall">Composite 600 hPa relative humidity through the peak TC season for &#40;a&#41; active years&#44; &#40;b&#41; inactive years&#44; and &#40;c&#41; the difference &#40;active minus inactive years&#41;&#46; The shading indicates statistical significant differences at the 95&#37; confidence level&#46;</p>"
        ]
      ]
      7 => array:7 [
        "identificador" => "fig0040"
        "etiqueta" => "Fig&#46; 8"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr8.jpeg"
            "Alto" => 1398
            "Ancho" => 1129
            "Tamanyo" => 335794
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0050" class="elsevierStyleSimplePara elsevierViewall">Composite SST anomalies from the climatological mean SST over the period of 1965-2013 through the peak TC season for &#40;a&#41; active years&#44; &#40;b&#41; inactive years&#44; and &#40;c&#41; the difference &#40;active minus inactive years&#41;&#46;</p>"
        ]
      ]
      8 => array:7 [
        "identificador" => "fig0045"
        "etiqueta" => "Fig&#46; 9"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr9.jpeg"
            "Alto" => 1995
            "Ancho" => 943
            "Tamanyo" => 277752
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0055" class="elsevierStyleSimplePara elsevierViewall">Composite vertical wind shear through the peak TC season for &#40;a&#41; active years&#44; &#40;b&#41; inactive years&#44; and &#40;c&#41; the difference &#40;active minus inactive years&#41;&#46; The shading indicates statistical significant differences at the 95&#37; level&#46;</p>"
        ]
      ]
      9 => array:7 [
        "identificador" => "fig0050"
        "etiqueta" => "Fig&#46; 10"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr10.jpeg"
            "Alto" => 1090
            "Ancho" => 968
            "Tamanyo" => 141601
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0060" class="elsevierStyleSimplePara elsevierViewall">GPI during &#40;a&#41; active years&#44; &#40;b&#41; inactive years&#44; and &#40;c&#41; their difference&#46;</p>"
        ]
      ]
      10 => array:7 [
        "identificador" => "fig0055"
        "etiqueta" => "Fig&#46; 11"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr11.jpeg"
            "Alto" => 1464
            "Ancho" => 992
            "Tamanyo" => 160117
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0065" class="elsevierStyleSimplePara elsevierViewall">Difference of the GPI between active and inactive years over the ENP basin in JJASO&#44; while varying&#58; &#40;a&#41; relative humidity&#44; &#40;b&#41; vorticity&#44; &#40;c&#41; potential intensity&#44; and &#40;d&#41; vertical wind shear&#46; The rest of the terms are kept as their climatological values &#40;using the period 1965-2013&#41;&#46;</p>"
        ]
      ]
      11 => array:7 [
        "identificador" => "fig0060"
        "etiqueta" => "Fig&#46; 12"
        "tipo" => "MULTIMEDIAFIGURA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "figura" => array:1 [
          0 => array:4 [
            "imagen" => "gr12.jpeg"
            "Alto" => 566
            "Ancho" => 1841
            "Tamanyo" => 124560
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        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0070" class="elsevierStyleSimplePara elsevierViewall">Time series of the annual frequency of &#40;a&#41; observed major hurricanes &#40;categories 3 through 5&#41;<a name="p2"></a> &#40;black line&#41; and simulated &#40;red line&#41; from the CTRL experiment&#59; and &#40;b&#41; observed &#40;black line&#41; and simulated &#40;red line&#41; power dissipation index &#40;PDI&#41;&#46;</p>"
        ]
      ]
      12 => array:7 [
        "identificador" => "tbl0005"
        "etiqueta" => "Table I"
        "tipo" => "MULTIMEDIATABLA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "tabla" => array:1 [
          "tablatextoimagen" => array:1 [
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              "tabla" => array:1 [
                0 => """
                  <table border="0" frame="\n
                  \t\t\t\t\tvoid\n
                  \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Experiment&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="top" scope="col" style="border-bottom: 2px solid black">Description&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">CTRL&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">Both SST and vertical wind shear correspond to the observed values for each TC&#44; from 1965 to 2013&#46;&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">T65&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">SST is fixed at the observed value in 1965 and vertical wind shear varies for each TC&#44; from 1965 to 2013&#46;&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">V65&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">Shear is fixed at the observed value in 1965 and SST varies for each TC&#44; from 1965 to 2013&#46;&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">VT65&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="left" valign="top">Both SST and vertical wind shear are fixed at the observed values in 1965&#46;&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr></tbody></table>
                  """
              ]
              "imagenFichero" => array:1 [
                0 => "xTab1513547.png"
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          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0075" class="elsevierStyleSimplePara elsevierViewall">Summary of experiments conducted with the tropical cyclone intensity model&#46;</p>"
        ]
      ]
      13 => array:7 [
        "identificador" => "tbl0010"
        "etiqueta" => "Table II"
        "tipo" => "MULTIMEDIATABLA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "tabla" => array:2 [
          "tablatextoimagen" => array:1 [
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                0 => """
                  <table border="0" frame="\n
                  \t\t\t\t\tvoid\n
                  \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head  " align="left" valign="bottom" scope="col" style="border-bottom: 2px solid black">Experiment&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="bottom" scope="col" style="border-bottom: 2px solid black">CTRL-PDI&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="left" valign="bottom" scope="col" style="border-bottom: 2px solid black">CTRL- Frequency of major hurricanes&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="bottom">T65&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">0&#46;96<a class="elsevierStyleCrossRef" href="#tblfn0005"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">0&#46;81<a class="elsevierStyleCrossRef" href="#tblfn0005"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="bottom">V65&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">0&#46;98<a class="elsevierStyleCrossRef" href="#tblfn0005"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">0&#46;92<a class="elsevierStyleCrossRef" href="#tblfn0005"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">VT65&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">0&#46;94<a class="elsevierStyleCrossRef" href="#tblfn0005"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">0&#46;84<a class="elsevierStyleCrossRef" href="#tblfn0005"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr></tbody></table>
                  """
              ]
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                0 => "xTab1513549.png"
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              "etiqueta" => "&#42;&#42;"
              "nota" => "<p class="elsevierStyleNotepara" id="npar0005">Signiicance at the 95&#37; level&#46;</p>"
            ]
          ]
        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0080" class="elsevierStyleSimplePara elsevierViewall">Correlation coefficients between the values of PDI and frequency of major hurricanes &#40;category 3-5&#41; in the CTRL and sensitivity experiments &#40;T65&#44; V65 and VT65&#41;&#46;</p>"
        ]
      ]
      14 => array:7 [
        "identificador" => "tbl0015"
        "etiqueta" => "Table III"
        "tipo" => "MULTIMEDIATABLA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "tabla" => array:2 [
          "tablatextoimagen" => array:1 [
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              "tabla" => array:1 [
                0 => """
                  <table border="0" frame="\n
                  \t\t\t\t\tvoid\n
                  \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head  " align="" valign="top" scope="col" style="border-bottom: 2px solid black">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">PDI&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">Frequency of major hurricanes&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">SST effect&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">0&#46;22&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">0&#46;06&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">Wind shear effect&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">&#8211;0&#46;45<a class="elsevierStyleCrossRef" href="#tblfn0010"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">&#8211;0&#46;27<a class="elsevierStyleCrossRef" href="#tblfn0015"><span class="elsevierStyleSup">&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">Combined SST&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="" valign="top">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="" valign="top">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">and wind shear effects&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">&#8211;0&#46;49<a class="elsevierStyleCrossRef" href="#tblfn0010"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="bottom">&#8211;0&#46;30<a class="elsevierStyleCrossRef" href="#tblfn0010"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr></tbody></table>
                  """
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              "nota" => "<p class="elsevierStyleNotepara" id="npar0010">Significance at the 95&#37; level</p>"
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            1 => array:3 [
              "identificador" => "tblfn0015"
              "etiqueta" => "&#42;"
              "nota" => "<p class="elsevierStyleNotepara" id="npar0015">significance at the 90&#37; level&#46;</p>"
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        ]
        "descripcion" => array:1 [
          "en" => "<p id="spar0085" class="elsevierStyleSimplePara elsevierViewall">Effects of SST&#44; wind shear&#44; and combined SST and wind shear&#44; represented by the correlation between the CTRL experiment and the difference &#40;CTRL - experiment&#41;&#46; See text for more details&#46;</p>"
        ]
      ]
      15 => array:7 [
        "identificador" => "tbl0020"
        "etiqueta" => "Table IV"
        "tipo" => "MULTIMEDIATABLA"
        "mostrarFloat" => true
        "mostrarDisplay" => false
        "tabla" => array:2 [
          "tablatextoimagen" => array:1 [
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                0 => """
                  <table border="0" frame="\n
                  \t\t\t\t\tvoid\n
                  \t\t\t\t" class=""><thead title="thead"><tr title="table-row"><th class="td" title="table-head  " align="" valign="top" scope="col" style="border-bottom: 2px solid black">&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">Active period&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">Inactive period&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th><th class="td" title="table-head  " align="center" valign="top" scope="col" style="border-bottom: 2px solid black">Difference&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</th></tr></thead><tbody title="tbody"><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">HURDAT2&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">5&#46;71&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">1&#46;90&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">3&#46;81<a class="elsevierStyleCrossRef" href="#tblfn0020"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">CTRL&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">4&#46;60&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">1&#46;60&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">3&#46;00<a class="elsevierStyleCrossRef" href="#tblfn0020"><span class="elsevierStyleSup">&#42;&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">T65&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">4&#46;00&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">1&#46;70&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">2&#46;30<a class="elsevierStyleCrossRef" href="#tblfn0025"><span class="elsevierStyleSup">&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">V65&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">3&#46;50&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">1&#46;70&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">1&#46;80&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr><tr title="table-row"><td class="td" title="table-entry  " align="left" valign="top">VT65&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">4&#46;20&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">1&#46;50&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td><td class="td" title="table-entry  " align="char" valign="top">2&#46;70<a class="elsevierStyleCrossRef" href="#tblfn0025"><span class="elsevierStyleSup">&#42;</span></a>&nbsp;\t\t\t\t\t\t\n
                  \t\t\t\t</td></tr></tbody></table>
                  """
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        "titulo" => "Acknowledgements"
        "texto" => "<p id="par0205" class="elsevierStylePara elsevierViewall">This research was jointly supported by the <span class="elsevierStyleGrantSponsor" id="gs1">National Natural Science Foundation of China</span> &#40;Grants No&#46; <span class="elsevierStyleGrantNumber" refid="gs1">41305050</span>&#44; <span class="elsevierStyleGrantNumber" refid="gs1">41275093</span>&#44; <span class="elsevierStyleGrantNumber" refid="gs1">41475091</span> and <span class="elsevierStyleGrantNumber" refid="gs1">41375098</span>&#41; and the <span class="elsevierStyleGrantSponsor" id="gs2">Priority Academic Program Development of Jiangsu Higher Education Institutions &#40;PAPD&#41;</span>&#46; GBR acknowledges the support of the <span class="elsevierStyleGrantSponsor" id="gs3">Inter-American Institute for Global Change Research</span> &#40;IAI&#44; Grant <span class="elsevierStyleGrantNumber" refid="gs3">CRNA-2048</span>&#41;&#44; which is supported by the <span class="elsevierStyleGrantSponsor" id="gs4">U&#46;S&#46; National Science Foundation</span> &#40;Grant <span class="elsevierStyleGrantNumber" refid="gs4">GEO-0452325</span>&#41;&#46; We also acknowledge K&#46; Emanuel for the CHIPS model&#46;</p>"
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Article information

ISSN: 01876236
Original language: English

DOI:10.20937/ATM.2015.28.03.02

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2023 March	19	8	27
2023 February	11	7	18
2023 January	23	2	25
2022 December	15	5	20
2022 November	18	4	22
2022 October	12	18	30
2022 September	19	6	25
2022 August	24	6	30
2022 July	19	10	29
2022 June	19	6	25
2022 May	21	6	27
2022 April	8	6	14
2022 March	15	10	25
2022 February	23	4	27
2022 January	20	5	25
2021 December	9	9	18
2021 November	22	8	30
2021 October	38	14	52
2021 September	16	13	29
2021 August	27	10	37
2021 July	21	12	33
2021 June	16	4	20
2021 May	11	10	21
2021 April	38	3	41
2021 March	11	9	20
2021 February	13	3	16
2021 January	18	9	27
2020 December	17	5	22
2020 November	14	8	22
2020 October	21	6	27
2020 September	17	3	20
2020 August	23	1	24
2020 July	18	1	19
2020 June	22	2	24
2020 May	18	5	23
2020 April	27	1	28
2020 March	35	3	38
2020 February	18	5	23
2020 January	16	3	19
2019 December	10	4	14
2019 November	7	5	12
2019 October	8	4	12
2019 September	12	6	18
2019 August	8	5	13
2019 July	7	12	19
2019 June	16	11	27
2019 May	48	40	88
2019 April	37	9	46
2019 March	2	3	5
2019 February	5	1	6
2019 January	3	5	8
2018 December	1	0	1
2018 November	6	1	7
2018 October	14	3	17
2018 September	33	3	36
2018 August	8	1	9
2018 July	9	0	9
2018 June	13	1	14
2018 May	12	0	12
2018 April	24	2	26
2018 March	2	0	2
2018 February	3	0	3
2018 January	7	0	7
2017 December	6	0	6
2017 November	4	0	4
2017 October	0	1	1
2017 September	2	0	2
2017 August	5	2	7
2017 July	3	1	4
2017 June	2	1	3
2017 April	1	0	1
2017 March	2	1	3

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