https://doi.org/10.47460/minerva.v5i15.177

Effects of climate anomalies on the soil-

atmosphere interaction model and its

convergence with conventional climate

models

Received (29/06/2024), Accepted (27/07/2024)

Mara Girón

https://orcid.org/0000-0001-9215-1807

maragiron.777@gmail.com

Universidad Nacional Politécnica

Antonio José de Sucre (UNEXPO)

Puerto Ordaz-Venezuela

Abst ract. - The application of the Determination of the Effect of Climate Anomalies on Soil-Atmosphere

Interaction (DECASAI) model is described, which allows estimating the water evaporation over bodies of

water and soils, based on a thermodynamic and kinetic approach. The model studies seasonal climate

anomalies with emphasis on prolonged droughts (ENSO), to predict the vulnerability of selected water

bodies, in their hydraulic and pluvial aspects. The model is integrated into the Biotic Pump Theories,

evapotranspiration, and other conventional models such as Orchidee using the new absent information

provided by the model in their calculations. The analysis estimated the critical radius of the condensed water

droplets, for application in the conventional models. The proposed model is sufficiently robust and

complementary for use in certain localities located in the Hadley cells, depending on their continentality.

Keyw ords: DECASAI, climate anomalies, soil-atmosphere interaction, conventional models.

Resumen: Se describe la aplicación del modelo DEACISA (Determining the Effects of Climate Anomalies on

Soil-Atmosphere Interactions-DECASAI), que permite estimar la evaporación de agua de cuerpos de agua y

suelos con base en métodos termodinámicos y cinéticos. El modelo estudia anomalías climáticas

estacionales, con énfasis en sequías prolongadas (ENSO/ENOS), para predecir la vulnerabilidad de cuerpos

de agua seleccionados, en sus aspectos hidráulicos y pluviales. El modelo se integra con las Teorías de la

Bomba Biótica, la evotranspiración y otros modelos convencionales como el de Orchidee a través de la

nueva información faltante que proporciona el modelo en sus cálculos. El análisis estimó el radio crítico de

las gotas de agua condensada, para su aplicación en modelos convencionales. El modelo propuesto es

suficientemente robusto y complementario para su uso en determinadas localidades ubicadas en las celdas

de Hadley, dependiendo de su continentalidad.

Palabras clave: DECASAI, anomalías climáticas, interacción suelo-atmósfera, modelos convencionales.

Efectos de las anomalías climáticas en el modelo de interacción suelo-

atmósfera y su convergencia con los modelos climáticos convencionales

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

Oscar Dam

https://orcid.org/0000-0002-0594-6757

oscarcurmetales@gmail.com

Universidad Nacional Politécnica

Antonio José de Sucre (UNEXPO)

Puerto Ordaz-Venezuela

ISSN-E: 2697-3650

Minerva Journal

Vol.5, Issue N°15, (pp. 83-94)

I. INTRODUCTION

Climate models are important tools for predicting future climate change. It is essential that these models

accurately capture the changes already observed to increase confidence in future projections. Regardless of

the space-temporal scale, dynamic models of conventional climate systems generally share the same basic

structure, considering the same variables, and are governed by the same physical principles of conservation

of mass, energy, and momentum, just like any natural system. These models can be used for climate and

weather prediction and range from planetary to microscale.

Atmospheric behaviors are assumed to behave like ideal fluids in these models. Climate systems with a

smaller dimension of local space are modeled with their local characteristics. The model “Determination of

the Effect of Climate Anomalies on Soil-Atmosphere Interaction” (DECASAI/ DEACISA in Spanish) [1],

determines the effect of climate anomalies on soil-atmosphere interaction for different tropical belt

topographies according to the Hadley cell. It focuses on the entropic characterization of the associated

thermodynamics, effects of water evaporation from the considered water bodies, moisture evaporation from

the associated soils, and existing coupling force. It also considers the kinetics with the characteristics of the

vulnerable soils of affectation such as porosity, permeability, and density. It also takes into account the

humidity necessary to maintain biodiversity, affected areas that host water bodies of reservoirs and water

basins, and biodiverse areas considered microclimates. The model determines the formation of water

droplets, the behavior of the relative humidity for precipitation, and the amount of entropy exchanged

between the air masses.

The estimate of total evaporation is separated into the evaporation of biomass (evapotranspiration) and

that of the water mirrors of reservoirs and water basins, including the Amazon rainforest. The model was

compared with other conventional models such as the Biotic Pump and Orchidee [2], [3], to establish

convergences in the spatial variations of the coupling force and the observed forces, taking into account the

differences in parameterization, climatology, and hydrological regimes.

In this article, we discuss the importance of the evaporation rate for the DECASAI Model, the theory of the

Biotic Pump, and the Orchidee approach. It explains the methodology used to calculate relative humidity and

condensation, the adiabatic gradient of the atmosphere, and the radius of a water drop in a vapor cloud.

These calculations are essential for applying DECASAI to the evaporation of biomass for the Biotic Pump and

Orchidee. Finally, we present the DECASAI results for the selected biomass and draw our conclusions.

II. DEVELOPMENT

The DECASAI model [1] is a climate model designed to study the impact of non-seasonal climate anomalies

on soil-atmosphere interaction, water bodies, and surrounding biomass. It primarily focuses on the hydraulic

and pluvial dependence of bodies of water on the water currents that feed them.

The DECASAI model [1] complements conventional climate models such as Orchidee and Biotic Bomb [3],

[2], by taking into account the topography and sentimentality of regions within the tropical belt. It specifically

accounts for the role of inland water bodies in the evaporation process and considers their hydraulic and

pluvial behavior, as well as other convective and thermodynamic ranges. The model studies the

interrelationship between these factors, with a focus on how hydrological regimes [4], impact climate

prediction. The transversal approach for real-time assessment of the vulnerability of water bodies to climatic

anomalies is also considered. The results are presented in numerical and perceptual formats, similar to

those of more complex models.

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

Minerva Journal

Vol.5, Issue N°15, (pp. 83-94)

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

Minerva Journal

Vol.5, Issue N°15, (pp. 83-94)

A. Importance of evaporation rate for the DECASAI Model

It's essential to keep in mind that the amount of water evaporated by one hectare of tropical forest can vary

significantly in different weather conditions, such as temperature changes, relative humidity, wind speed, and

solar radiation. Moreover, the amount of water evaporated also depends on the forest's density and the total

amount of rainfall in the region. To determine the precise quantity of water evaporated by one hectare of

tropical forest in different meteorological stations, it is necessary to collect meteorological data such as

temperature, relative humidity, wind speed, and solar radiation. These data can be obtained from monthly

agro-climatic databases [5].

In addition, the theories of the biotic pump [2], and the ORCHIDEE [3], were useful in associating the

approach of the DECASAI Model [1], by calculating convection and evaporation considering: the prevailing

winds and the geopotential height to obtain the adiabatic gradient of the air (υ) below 11km, based on this,

the radius of a condensed drop can be obtained from convective water vapor, driving the energy of the liquid

phase in compensation and decreasing entropy. The model can be coupled to conventional models, in

particular the Biotic Pump Theory and ORCHIDEE, which needs the generated information on water vapor

convection in the tree crowns and evapotranspiration to measure foliar behavior, respectively; taking as an

example the evaporation of the Amazon rainforest.

B. The Biotic Pump Theory (PBT)

As per the theory, the biotic pump plays a crucial role in driving the circulation of air and water in the

atmosphere and on the Earth's surface, which is essential to maintain the climate and ecological balance [2],

[6], [7]. This mechanism releases moisture from vegetation, which turns into clouds and precipitation,

contributing to maintaining soil and vegetation moisture. Besides, vegetation also acts as a natural filter,

removing carbon dioxide and other pollutants from the air.

Also, by regulating local and regional temperatures, the biotic pump contributes to a cooling effect on the

environment through plant transpiration and soil evaporation. Vegetation also has the advantage of reducing

wind speed and protecting against soil erosion. This causes the relatively high-pressure air below to draw in

more humid air from the sea or the forest surface [2], [8], [9]. Although temperature is not the primary

determinant of air and water circulation in the atmosphere and on the Earth's surface, the biotic pump

theory acknowledges that temperature plays a crucial role in the ability of air to contain water vapor [3].

C. The Orchidee Approach

To relate the proposed model to Orchidee (Organizing Carbon and Hydrology in Dynamic Ecosystems) [4],

the calculation of reference evapotranspiration (ET0) using the FAO Penman-Monteith equation, which is one

of the most accurate methods for calculating evapotranspiration [10], is considered. That equation uses the

aforementioned meteorological data to calculate the average evaporation rate.

To estimate the actual evapotranspiration, the calculated ET0 is used, which depends on the density of the

biomass, the amount of rainfall the area receives, and other factors specific to the area. It is important to

consider the limitations when relating DECASAI [1] with Orchidee [3], in its soil-atmosphere interaction, it is

necessary to consider limitations and the fact that the average evaporation rate obtained may vary

depending on the specific conditions of the associated biomass.

The estimated average Total Field Evapotranspiration (TFE) value measures the total amount of water

transferred from the land to the atmosphere, including soil evaporation and plant transpiration. For example,

recent research using the ORCHIDEE-CAN-NHA model has simulated water and carbon fluxes in tropical

forests to predict tree mortality in response to drought. The model was tested in the Caxiuanã rainfall

exclusion experiment in eastern Amazonia, obtaining an average value of 0.18 m³/m³ of water in the soil,

measured at a depth of 5 cm, for soil moisture evaporation calculations [11]. The model evaluation was

based on a comparison of DECASAI data, which were included in the original TFE curves shown in Figure 1,

with fairly good agreement.

Fig. 1. Modeled (ORCHIDEE-CAN-NHA, black line) versus observed (black dots) volumetric soil

moisture content (SMC) 915 at different depths. Due to the limited time duration of observation data,

we only show the modeled SMC from 2001 to 2004. (a) The partitioning of evapotranspiration (ET)

was compared between CTL and TFE (b) The red line running horizontally represents the estimated

average TFE value. Source: [11], edited by AUTHORS.

III. METHODOLOGY

The study presents the relevant parameters that affect the seasonal climate prediction of a certain region

or microclimate, specifically in the evaporation process, and how it is related to the behavior of the type of

soil and water bodies. For the application of the model, significant climatological data were selected from

NASA's MERRA-2 Modern-Era Retrospective Analysis [12], combining it with the modern global meteorological

model in 50 km grids. (FAOH, Global Land Cover SHARE database) [13], [14] Based on a historical hourly

climatological statistical analysis and model reconstructions from 1980-2016 (Meeus J., Astronomical

Algorithms) [15],[2].

The selection of the Gurí Reservoir, for the application of the proposed model, included, on the one hand, its

conditions of internal continentality, Topography (The elevation data “SRTM”) [16], and the characteristics that

influence the values of relative humidity and evaporation conditions of the water mirror and proximity to the

Amazon Rainforest. On the other hand, it is hydrological and pluvial dependence. To analyze the convergence

of the results.

The DECASAI model [1] is based on the premises outlined in the introduction and focuses on the

thermodynamics variables and local parameters described in Table 2 in previous paper describing the

DECASAI model [1]. To analyze model convergence, climatic and meteorological data from the Gurí-

Venezuela Reservoir [1] were used as a reference point for its tropical location and proximity to the Amazon

rainforest. This allowed for comparisons with other locations within the tropics.

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

Minerva Journal

Vol.5, Issue N°15, (pp. 83-94)

This study utilizes the DECASAI model [1] to analyze evaporation, convection, and entropy in a specific

region. The model incorporates geographic and meteorological data such as:

Geographic: Water body size, biomass size, elevation (ASL), annual average soil temperature, solar

radiation, and wind speed.

Meteorological: Airflow speed (varying based on climatic conditions such as Northern Trades 20-22km/hr,

ENSO>28km/hr, tropical depressions>117, and storms) and DELTA T (°C) air-water vapor evaporation (2.5

ºC/g H20 evap.kg air).

The model includes two domains (continental and regional) and considers standardized soil porosity values

for a specific soil surface layer (-5cm to 10cm). Boundary conditions are applied assuming flow over a flat

plate.

The work focuses on complementary analysis of the models, with a specific focus on evaporation,

convection, and entropy. All calculations were performed using the optimization tool (DECASAI [1]) in MS

Excel®, assuming a standard deviation of 0.2% error for all correlation coefficients obtained. The coherence

of the comparison of the results confirms the physics of DECASAI [1], which has profound implications for

current mathematical climate models. This not only helps in predicting the consequences of widespread

evaporation but also helps in better understanding atmospheric processes that lead to the formation of air

masses.

The equations involved in the DECASAI model are the following:

D. Relative Humidity and Condensation

In this section of the analysis for the DECASAI model [1], it is considered that the relative humidity is

represented as the energy of the liquid phase in compensation, and condensation is assumed as the

presence of decreasing entropy, to calculate the partial pressure variation of the water vapor. Therefore,

when considering thermodynamics, the relative humidity Ǿ is defined as the ratio between the partial

pressure of water vapor Pv= 101.324 kPa and the saturating vapor pressure Pºsat.

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

Taking as premises that: If <1, the vapor state is maintained to wait for condensation, If >1, overcoming the

activation energy. The free energy for the evaporation of n moles of water is expressed as:

Assume that: steam behaves like an ideal gas, -dA = 8Π.r.dr, (7), A= 8.0713, B=1730.83, c= 233.42. Taking

the saturation of Equation Antoine [17]

Using Kelvin's equation to calculate the radius of the drops, the radius of the drops is calculated by the

expression:

Minerva Journal

Vol.5, Issue N°15, (pp. 83-94)

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

Minerva Journal

Vol.5, Issue N°15, (pp. 83-94)

E. Adiabatic Gradient of the atmosphere

It is assumed that within the control volume, there are adiabatic processes, to calculate the Adiabatic

Gradient of Air (ϒ), rescuing the thermodynamic evolution, Below 11km, Using Mayer's Relation and

Clapeyron's Equation

Variation of pressure as a function of height

Fig. 2. Variation of saturated pressure (mmHg) as a function of temperature (T°C). Source: Authors

The laws of Newtonian physics indicate a strong correlation (R²> 0.9) between temperature and saturated

pressure as illustrated in Figure 2, which is used to calculate the rate of evaporation. The curve obtained is

represented mathematically:

The relationship between pressure and height is illustrated in Figure 3a, which shows an inverse

proportionality, as reflected by the formula. Like Fig. 3b, the relationship is also inversely proportional to the

variation in air temperature as a function of height (km); the empirical equation that describes it is displayed

in Figures 3a and 3b. The following empirical equation can represent the inversely proportional relationship

between the temperature and the altitude.

Fig. 3. Effect of the altitude on the Pressure (a) and temperature (b) values.

Source: Authors.

F. Radius of a water drop in a vapor cloud

For rain to form, the droplets must contain air that is more than 100% saturated. Droplets with r<rc

evaporate, while those with r>rc grow through condensation on the surface. A drop of water of radius r in

equilibrium with its vapor in a cloud, at a given temperature T, with an internal pressure Pº1 and the vapor

around it Pv, is verified by the Laplace and Kelvin equations.

The Relationship between Water Droplet Size and Water Vapor Pressure, was determined by using the

Laplace and Kelvin equations, the researchers determined that droplets with a radius greater than a critical

value (rc) will grow through condensation, while those smaller than rc will evaporate. The study aimed to

illustrate this relationship at a temperature of 20°C and estimate the radius of the water droplets [18]. The

results, depicted in Figure 4, show a clear correlation between the size of the water droplets and the

surrounding water vapor pressure.

Fig. 4. Variation of droplet size (nm) in vapor clouds with vapor pressure Po.

Source: Authors.

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

G. Application of DECASAI to biomass evaporation

The equations involved in the DECASAI model for biomass evaporation are interrelated as follows:

Evaporation of water bodies of water

Calculating water evaporation in bodies of water is obtained with increasing entropy, as uncompensated

energy. In case of flat plate forced convection in laminar flow, at a distance x downstream of the plate edge,

in a simple way Re <5 ×, Pr>0,6, We have Re<2300 laminar flows and Re>2300 for turbulent flows, ρ= fluid

density, L= length (cm), Sa= air volume (m/sec), v= air speed (m/sec), ρ= density of atmospheric air at water

level 15°C=1.225 kg/m³ Prandtl number Pr air = 0.71000, α = thermal diffusivity heat transfer coefficient, Ʋ =

moment of diffusivity, Ʊ = viscosity of air (cc/sec).

Minerva Journal

Vol.5, Issue N°15, (pp. 83-94)

ISSN-E: 2697-3650

Revista Minerva

Vol.5, Tomo N°14, (pp. 85-95)

Andrade D. et al. Implementación de la estrategia V de Gowin en la enseñanza experimental de la física para estudiantes de bachillerato

G. Application of DECASAI to biomass evaporation

The equations involved in the DECASAI model for biomass evaporation are interrelated as follows:

·Evaporation Of Water Bodies Of Water

The calculation of water evaporation in bodies of water is obtained with increasing entropy, as

uncompensated energy. In case of flat plate forced convection in laminar flow, at a distance x downstream of

the plate edge, in a simple way Re <5 ×, Pr>0,6, We have Re<2300 laminar flows and Re>2300 for turbulent

flows, ρ= fluid density, L= length (cm), Sa= air volume (m/sec), v= air speed (m/sec), ρ= density of atmospheric

air at water level 15°C=1.225 kg/m³ Prandtl number Pr air = 0.71000, α = thermal diffusivity heat transfer

coefficient, Ʋ = moment of diffusivity, Ʊ = viscosity of air (cc/sec). Convection arises naturally in the

atmosphere. This process is governed by the Ideal Gas Law, which describes the relationship between the

pressure, volume, temperature, and quantity (in moles) of an ideal gas such that the amount of evaporated

water (EC water) given in gr/h.m , would be:

E(C water) expressed in m³ , t = anomaly time (hr), Vca = volume of body of water

Soil Water Evaporation

Soil water evaporation is a crucial process in the hydrological cycle due to its role in regulating atmospheric

temperature and water resource availability. The evaporation of water from soil follows similar patterns to

evaporation from water bodies. Momentum conservation equations are applied to the entire porous

medium to understand the environmental behavior [1, 19].

Considering soil conditions, where σ represents stress terms, ρ represents porous medium density, and g

represents gravitational acceleration, the following assumptions are made: ρ = 1225 kg/m³ (density of

atmospheric air at 15°C), Pr_air = 0.71000 (air pressure), V0 = 3.95 cm³ (volume occupied by air at 273.15 K),

Water vapor pressure (Pv) = 4.44 g/cc, The convection coefficient or surface transmission coefficient (h)

quantifies the influence of fluid, surface, and flow properties during convective heat transfer. It is modeled

using Newton's Law of Cooling:

Convection arises naturally in the atmosphere. This process is governed by the Ideal Gas Law, which

describes the relationship between the pressure, volume, temperature, and quantity (in moles) of an ideal

gas such that the amount of evaporated water (EC water) given in gr/h.m² , would be:

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

E(C water) expressed in m³ , t = anomaly time (hr), Vca = volume of body of water

In this way obtain

where Q is convective heat transfer (W), h is the film coefficient (W/K), A is the body's surface area in contact

with the fluid, Ts is the body's surface temperature (K), and T∞ is the fluid temperature at a distance.

Additional parameters include: Vapor heat transfer coefficient (hv) = 6000-15000 W/°C, Steam heat transfer

coefficient (h_steam) = 0.02422 Cal/(h°F), Total volume (Vt), Volume occupied by pores (Vp), Volume occupied

by solids (Vs), Volume of water (Vw), Volume of air (Va), Mass of solids (Ms), Mass of water (Mw). Assumed

values include: Air pressure (Pa) = 254 g/cc, water and air temperature (Ta, Tg), soil density (ρs) = 2.2 g/cc, soil

porosity = 5 (sandy loam soil), Floor humidity (%). The weight of soil solids without pores per unit volume

considered as a mineral soils average 2.65 g/cc. The ideal gas law governs the relationship between pressure,

volume, temperature, and quantity of an ideal gas, leading to the following equation for water evaporated

above the soil (EC water-soil) in g/hm²:

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Vol.5, Issue N°15, (pp. 83-94)

Where hp= transfer coefficient, water vapor pressure above the ground Pvs=6.28; Vapor pressure

Pv(gr/cc)=4.42; Air Temp ºC. The soil humidity (gr/cc) is taken into account, comparing it with Soil humidity %

(data from the region under study)

H. Evaporation of biomass for Biotic Pump and ORCHIDEE

Massive flows of water in the form of vapor, known as "flying rivers," originate from the tropical Atlantic

Ocean and are fed by moisture evaporation from the Amazon. These atmospheric rivers travel swiftly across

the atmosphere and cause rain more than 3,000 kilometers away. They are essential for agricultural

production [20, 21]. To apply this concept for DECASAI [1], the evaporation rate in the Amazon jungle is

estimated at approximately 4 millimeters per day per square meter. This corresponds to four liters of water

accumulated above the ground. This data can be used to calculate tree transpiration rates by measuring the

area of the tree's crown [21].

A leafy tree, with a crown 20 meters in diameter, transpires more than 1,000 liters in a single day. As an

example, the Amazon has 5.5 million square kilometers occupied by native forests, with approximately 400

billion trees of the most varied sizes. Obtaining 20,000 million tons (or 20 billion liters) of water are

transpired every day by the trees of the Amazon basin. The Amazon (tropical rainforest), with approximately

400 billion trees (of varied sizes) would be represented

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

E(C water) expressed in m³ , t = anomaly time (hr), Vca = volume of body of water

In this way obtain

I. Evaporation Rate of the model

Applying the DECASAI and equations in the methodology section yields climatic parameters and the

evapotranspiration equation.

Considering the effect of the anomaly on the body of water would remain m³:

It is assumed that DECASAI

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Vol.5, Issue N°15, (pp. 83-94)

A. Case of application Evaporation Rate of the model

Applying the DECASAI [1] and equations in the methodology section yields climatic parameters and the

evapotranspiration equation (23)–(26). Biomass soil evaporation is equivalent to plant evaporation. It

accounted for 5.2% of the trees. The amount of biomass evaporation varies depending on the selected

biomass, such as in the case of Gurí Reservoir in Venezuela. Using the meteorological variables described in

Table 2 in previous paper on the DECASAI model [1], along with the equations involved and shows the results

obtained in table 3 from applying in Gurí Dam-Venezuela, which includes the estimates from DECASAI model

[1], [15], and the variation of biomass evaporation.

The calculations of the DECASAI model allowed us to estimate the critical radius of the condensed water

droplets, in the order of 4.58 nm. This value is assumed constant for its application in the Orchidee and

Biotic Pum models. For the analysis of the TFE values, these are obtained from Figure 1 assuming an average

value of 0.18 m³/m³ of water in the soil. Table 1 summarizes the results of our analysis on soil water

evaporation.

RESULTS

The comparative values in Table 1 provide a preliminary indication, though not exhaustive, that the

evaporation rates of DECASAI and Orchidee are of the same order of magnitude. In the comparison

parameters, for the three cases calculated by the DECASAI model where the final soil moisture result

converges at 2.19 gr/hm³., the soil water removal (g/h.m²) ranges above 30%. The DECASAI model, as

described in [1], demonstrates its convergence and robustness by considering the topography and

continentality of the different area bodies.

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

Table 1. Comparison of evaporation index of the studied models. Source: Authors.

CONCLUSIONS

The results of the exercise indicate the complementarity of the DECASAI model with the Biotic Pump and

the Orchidee, being considered sufficiently robust, under its thermodynamic, moment, and physical

approach for certain localities located in the Hadley cells, according to their continentality, to study the

seasonal or non-seasonal climate anomalies, with special emphasis on periods of prolonged drought (such

as ENSO) at a global level or microclimates (microscale) and that can predict the vulnerability of selected

water bodies, in their hydraulic and pluvial aspects.

The developed model provides promising avenues for future research in the assimilation of experimental

data to parameterize convection, evaporation, and condensation due to the effects of water evaporation

from the considered water bodies, and the associated soil moisture evaporation, induced by the prolonged

drought.

Furthermore, the findings suggest the relevance of the integrated approach provided by the DECASAI

model, which combines thermodynamic, momentary, and physical elements, to address the challenges

associated with climate variability in specific regions. This holistic approach allows for a more complete

understanding of atmospheric processes and the interaction with local water bodies, which in turn improves

the predictive ability of the model in terms of extreme weather events and their impact on water supply and

availability. Of ter resources.

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Vol.5, Issue N°15, (pp. 83-94)

RECOGNITION

On the other hand, the successful implementation of the model in the studied regions highlights the

importance of considering both local and global factors in predicting water vulnerability. This highlights the

need for international collaboration and the adoption of transdisciplinary approaches to address challenges

related to climate change and sustainable water management, to develop effective adaptive strategies and

foster community resilience to extreme climate events.

Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

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Recognition is given to Universidad Nacional Experimental Politécnica UNEXPO, Vicerrectorado Puerto

Ordaz, for it support in the training of engineers aiming to generate knowledge of science and for science.

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Girón M. and Dam O. Effects of climate anomalies on the soil-atmosphere interaction model and its convergence with conventional climate models

ISSN-E: 2697-3650

Mara Girón, Industrial Engineer, MSc Industrial Engineer, Industrial Risk Prevention

Specialist, Student of the Doctorate of Engineering Sciences at UNEXPO vice-rector

Puerto Ordaz. Venezuelan.

Oscar Dam, UCV Metallurgical Engineer, PhD Engineering. University of London

England. Author of ten (10) patents and co-author of three (5), all with industrial

application and novel technologies. Professor at UNEXPO, UCV, IVIC. Venezuelan.

LOS AUTORES

Minerva Journal

Vol.5, Issue N°15, (pp. 83-94)