Collected and simulated data.
\r\n\t
",isbn:"978-1-78984-671-3",printIsbn:"978-1-78984-670-6",pdfIsbn:"978-1-78985-657-6",doi:null,price:0,priceEur:0,priceUsd:0,slug:null,numberOfPages:0,isOpenForSubmission:!0,hash:"d5feb836870aef4d30893f10898e7791",bookSignature:"Dr. Gokul Sridharan",publishedDate:null,coverURL:"https://cdn.intechopen.com/books/images_new/10791.jpg",keywords:"HPV, Inflammation and Immunity, Cancer Stem Cells, Genomics and Epigenomics, Transcriptomics, Proteomics, Targeted Therapy, Immunotherapy, Surgery, Next-Gen Sequencing, Bioinformatics, Pharmacogenomics",numberOfDownloads:null,numberOfWosCitations:0,numberOfCrossrefCitations:null,numberOfDimensionsCitations:null,numberOfTotalCitations:null,isAvailableForWebshopOrdering:!0,dateEndFirstStepPublish:"February 10th 2021",dateEndSecondStepPublish:"March 10th 2021",dateEndThirdStepPublish:"May 9th 2021",dateEndFourthStepPublish:"July 28th 2021",dateEndFifthStepPublish:"September 26th 2021",remainingDaysToSecondStep:"9 days",secondStepPassed:!1,currentStepOfPublishingProcess:2,editedByType:null,kuFlag:!1,biosketch:"A pioneering researcher and academician with an interest in oral pre-cancer and oral cancer with special emphasis on salivary diagnostics.",coeditorOneBiosketch:null,coeditorTwoBiosketch:null,coeditorThreeBiosketch:null,coeditorFourBiosketch:null,coeditorFiveBiosketch:null,editors:[{id:"82453",title:"Dr.",name:"Gokul",middleName:null,surname:"Sridharan",slug:"gokul-sridharan",fullName:"Gokul Sridharan",profilePictureURL:"https://mts.intechopen.com/storage/users/82453/images/system/82453.jpeg",biography:"Dr. Gokul Sridharan is currently an associate professor in the Department of Oral Pathology and Microbiology at Y.M.T. Dental College and Hospital, Navi Mumbai. He obtained his Ph.D. for the work titled “Salivary and serum metabolomics in oral leukoplakia and oral squamous cell carcinoma.” His fields of interest include oral pre-cancer, oral cancer, salivary diagnostics, oral and maxillofacial diseases, and advanced diagnostic aids with an emphasis on bioinformatics and metabolomics. He has several scientific publications to his credit and actively contributes as a peer reviewer to numerous journals. He is an active member of the editorial boards of several journals of repute. 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From chapter submission and review, to approval and revision, copyediting and design, until final publication, I work closely with authors and editors to ensure a simple and easy publishing process. I maintain constant and effective communication with authors, editors and reviewers, which allows for a level of personal support that enables contributors to fully commit and concentrate on the chapters they are writing, editing, or reviewing. I assist authors in the preparation of their full chapter submissions and track important deadlines and ensure they are met. I help to coordinate internal processes such as linguistic review, and monitor the technical aspects of the process. As an ASM I am also involved in the acquisition of editors. 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It creates strong winds and intense precipitation in the regions around the system. There are seven global basins that conceive TCs, viz. North Atlantic Ocean, eastern and western parts of North Pacific Ocean, south-western pacific, south-western and south-eastern Indian Ocean and North Indian Ocean (NIO) region. The cyclonic storms are often known as hurricanes and typhoons in the Atlantic and northwest Pacific, whereas TCs in other Ocean basins. The average frequency of occurrence, season and intensity of TCs vary from basin to basin. NIO basin shows bi-modal TC season with maximum frequency during post-monsoon period (October–December) and are comparatively stronger than pre-monsoon ones. Though the size of the TCs is relatively smaller and their intensity is comparatively less over NIO basin as compared to the other global basins, this region is quite important in view of the densely populated rim countries with poor socioeconomic conditions. Hence, loss of life and property is quite significant in this region. Based on the intensity, TCs formed over NIO basin can be classified into (i) depression if the associated 10-m maximum sustained wind (MSW) is in between 17 and 33 kt; (ii) cyclonic storm (CS) if MSW is in between 34 and 47 kt; (iii) severe cyclonic storm (SCS) if it has MSW of 48–63 kt; (iv) very severe cyclonic storm (VSCS) if the MSW is within the range 64–90 kt, and extremely severe cyclonic storm (ESCS) if the MSW is in range of 91–119 kt; and (v) super cyclonic storm (SuCS) if it has MSW of 120 kt or more (http://www.rsmcnewdelhi.imd.gov.in). This classification may differ from those over other global basins including that of the widely used Saffir-Simpson hurricane wind scale or SSHWS (http://www.nhc.noaa.gov/aboutsshws.php). Both types of classifications, that is, the earlier one from India Meteorological Department (IMD) and the SSHWS consider the tropical low-pressure system as a depression if MSW is <34 kt. The consideration of CS and SCS lies in the tropical storm category (MSW lies in the range 34–63 kt) of SSHWS. The VSCS category over NIO basin is similar to that of the category 1 hurricane (MSW lies in the range 64–82 kt) type. The category 3 (MSW lies in between 96 and 112 kt) and category 4 (MSW is within the range 113-136 kt) major hurricanes are comparable to ESCS over NIO basin. The IMD classification categorizes MSW above 120 kt as super cyclonic storm (SuCS), whereas SSHWS considers the desired wind speed above 137 kt for category 5 hurricane. However, the basic structure of NIO TCs is similar to hurricanes and typhoons.
\nHaving a prolonged coast line, about 96 districts (lying within 100 km from the coast) of India are vulnerable to the occurrence of TCs with varying intensity [2]. Out of these 96 districts, ∼59% are at least highly vulnerable. The number of CS and SCS with a core of MSW (between 34 and 63 kt) crossing different countries of the NIO region is found to be 504 during 1891–2015 (derived from the available IMD data at http://www.rmcchennaieatlas.tn.nic.in). Out of these, about 328 (>65%) crossed the Indian coasts, whereas 127 (>25%) have crossed the east coast of India between Gopalpur and Kolkata. In general, the proneness to TCs is quite high for the coastal districts of West Bengal, Odisha, Andhra Pradesh, and Tamil Nadu [2, 3]. In view of these, TCs over NIO basin can be considered as quite lethal and expensive natural disaster as they bring widespread destruction in these regions. The consequent loss of human life and properties impacts the economy of a country. Therefore, it is important to forecast the evolution of TCs by using numerical models as the frequency of such storms is increasing in several basins of the world in the present warming period [4]. Therefore, it is attempted to put forward the recent developments in understanding the related meteorological characteristics, their predictability, climatological aspects and the gaps identified in the area of TC research.
\nThis section describes the general understanding about life cycle of TCs. The description includes a brief overview about their genesis, structural evolution, propagation and dissipation.
\nThe TC research has evolved over several decades and researchers use observations as well as numerical models for this purpose. For example, some observational studies [5–7] discuss about TC formation and evolution. The pioneering works by Gray [8, 9] have shown that the formation of TC at any location depends on six factors: (i) appropriate Coriolis parameter ‘f’ that is practically effective 5° away from the equator in both the hemispheres, (ii) low-level positive relative vorticity (ζr), that is, existence of initial disturbance, (iii) low tropospheric vertical wind shear (Sz), (iv) ocean thermal energy (E) signified by sea surface temperature (SST), that is, SST should be ≥26.5°C within vertical extent of 60 m, (v) atmospheric instability measured in terms of difference in equivalent potential temperature (θe) between the surface and 500 mb or Δθe and (vi) mid-tropospheric relative humidity ‘RH’. Some of these aspects are discussed explicitly over the years using observations and numerical models [7, 10]. The first three parameters produce a dynamic potential (fζr/Sz), while the remaining three parameters yield a thermal potential (E Δθe RH). And, the product of dynamic and thermal potentials provides the seasonal genesis frequency.
\nCyclogenesis do not occur spontaneously even if all the environmental conditions are met. Further, only about 10% of all cyclonic disturbances intensify into TCs. These low-pressure systems gradually form from a pre-existing (or initial) disturbance that consists of wind vortex and organized clouds. Thus, the necessary conditions for tropical cyclogenesis must be supported by the deep convection in the presence of a low-level absolute vorticity maximum and the initial convection must survive for sufficient time. The survival ability of the initial convection depends on ‘ζr’, ‘f ’ atmospheric stability (defined by Brunt Vaisala frequency ‘N’) and depth of the system (H). This ability is defined by the Rossby radius of deformation ‘LR’ typically for a large tropical cyclonic system (www.meted.ucar.edu):\n
The average life expectancy of a TC is about 1 week, whereas it is found that few cyclones remain active for more than 4 weeks (exact time frame may change from basin to basin) as seen in case of a hurricane, provided the system must be able to stay over the warm tropical waters. In most of the TCs, the Coriolis and centripetal forces oppose the pressure gradient force [11]. In the lowest kilometres near the surface, the frictional force destroys the gradient balance and consequently, air spirals inward towards the storm centres. The primary circulation (horizontal axisymmetric) during tropical cyclogenesis gains latent heat through the process of evaporation and exchange of sensible heat with the underlying ocean as it spirals towards the storm centre [12]. Consequently, it gains large angular momentum and kinetic energy because of the acceleration towards the low-pressure centre. The evaporation of sea spray provides the necessary moisture supply. Because of the high velocity demanded by the quasi-conservation of angular momentum, the air may not penetrate beyond some small radius. To conserve the angular momentum, the air spirals upward in the eyewall forming intense ring of cumulus cloud and a calm eye at the centre and brings in the latent heat it acquired during the upward motion in the boundary layer to the free atmosphere. Due to the cooling of this rising air, latent heat releases into the atmosphere to add more energy to the storm. Across the top of the boundary layer, the turbulent eddies generated by the mechanical mixing due to the prevailing strong winds cause a significant downward flux of sensible heat from the free atmosphere through subsidence (Figure 1).
\nVertical cross section of a mature cyclonic storm and associated basic characteristics (adopted from http://www.hko.gov.hk/informtc/nature.htm).
As the convective updrafts in the eyewall ascends to the tropopause, the latent heat is converted to sensible heat through condensation in order to provide the much-needed buoyancy for lifting air from the surface to tropopause level. After reaching at the upper level, the air turns outwards and eventually spread out at high altitudes, where it forms anticyclonic circulation and eventually the cool air above the eye begins to sink into the central core (Figure 1). Thus, the storm can be termed as a quasi-steady thermodynamic heat engine that is primarily driven by latent heat release. This heat engine runs between a warm heat reservoir as sea that is at ∼300°K and a cold reservoir located at 15–18 km up in the troposphere having a temperature ∼200°K. A baroclinic structure is maintained by the latent heat release in the warm core, which is continuously converted to kinetic energy that is responsible to drive the TC.
\nApart from the basic factors discussed so far, there is a significant role of Madden-Julian oscillation (MJO) and El Niño in the frequency of occurrence of TCs (see [13]). In certain scenarios, equatorial Rossby waves (ER), mixed Rossby-gravity waves (MRG), Kelvin waves and easterly waves also influence the tropical cyclogenesis [14]. However, equatorial Kelvin waves do not appear to play a major role in tropical cyclogenesis. Several hurricanes in the North Atlantic form from African waves, MJO has a significant role in tropical cyclogenesis in North Pacific and the formation of cyclonic storms in the northwest Pacific is associated with MRG waves [13, 15]. These waves enhance the local conditions for the genesis of TCs by increasing upward motion, convection and the low-level vorticity by altering the local vertical shear pattern. The larger-scale waves, such as the MJO and ER, can also alter the mean zonal wind in large spatial and temporal scales in order to influence the mean flow.
\nThe active phase of MJO is generally found over Indian Ocean, the maritime continent, and western pacific [13], which seem to play a major role in regulating the frequency of occurrence (usually increases) and formation of TCs in these regions. MJO increases the westerly wind which blows from west to east and its active phase through the region increases convective activity. During El Niño events, the atmospheric response to SST anomalies (SSTA) in the equatorial Pacific perturbs the Walker circulation [16]. The most common form of genesis occurs when they interact with the Asian monsoon. However, such type of interaction is still not studied well though few studies emphasized the role of El Niño or El Niño Southern Oscillation (ENSO) in TC formation over the Bay of Bengal (BOB) region indicating a decrease in the number of TCs [17].
\nThe general structure of the TC can be understood through the visualization of vertical cross-section of a mature TC as depicted in Figure 1, which consists of eye, eyewall and rainbands. The centre of the structure signifies the low-pressure cyclone eye, where a strong downward flow occurs indifferent to the immediate neighbouring updrafts. However, subsidence is also visible alongside the updrafts in the neighbourhood eyewall region away from the eye. The appearance of eye, its growth, intensification of eyewall and disappearance of eye are described in this section.
\nThe life cycle of the TC is shown in Figure 2(a), where the inner and outer cores of a TC are considered besides its intensification in order to depict the strengthening and weakening. Figure 2(b) depicts the different stages of TC life period including genesis, development, mature stage and dissipation by considering the evolution of TC Phailin (2013) in BOB region as an example to the illustration shown in Figure 2(a).
\nIn the intensification period (or phase 1), the momentum from outer core towards the inner one helps in strengthening the 700 hPa wind field and subsequently it helps in the eye wall cloud formation [18]. Prior to the appearance of eye, the intensification process is quite slow (at a rate ∼8 hPa/day). The increase in maximum wind field is ∼5 ms−1day−1 and the outer core strengthens at a rate of ∼2 ms−1day−1. Gradually, when the eye appears, the central pressure is about 987 hPa and the rate of intensification increases by ∼250 times, at a rate of about 20 hPa/day. The rapidly deepening cyclone (at a rate ∼42 hPa/day) supports an earlier eye formation. During the filling phase, the central pressure starts rising by drawing momentum through the outer core and strengthening the outer core’s wing.
\n(a) Conceptual rendering from the main events in the life cycle of a tropical cyclone [18] and (b) different stages of tropical cyclone Phailin formed over Bay of Bengal [80].
The phase 2 is usually marked by the strengthening of outer core wind (similar to the stage (c) of TC Phailin shown in Figure 2(b)), whereas the inner core wind diminishes. During this phase, the eye expands and the filling of the inner core continues through the inflowing air towards the cyclone centre. During the filling phase, the inertial stability of the outer core is twice as large as that of the deepening stage making the outer core rigid for the inflowing air. Gradually the expansion of the eye ceases and the central core fills. It is important to note that the longer a cyclone spends in phase 2, stronger the outer radius will be and the radius of the damaging winds expand as long as the eye exists.
\nDuring phase 3, the outer wind starts weakening (e.g. stage (d) of TC Phailin shown in Figure 2(b)) with the disappearance of eye. Once the eye is vanished, the inflow of angular momentum ceases that was responsible for the strengthening of the outer core and from where the decay of outer radius low level wind field begins. These characteristics are valid for the cyclones which do not suffer landfall because the landfall would erode the wind field irrespective of the appearance of eye.
\nThough the basic principles of structural evolution may hold good for the TCs occurring in NIO basin (refer to Figure 2(b) for different stages of the TC Phailin), the formation of a distinguished eye structure may always not be feasible. A distinguished eye may be seen in case of a very severe cyclonic storm in this basin during phase 2. However, an explicit analysis in this direction is not available in literature for the NIO basin even though few studies like [19] computed the radius of maximum wind seen in case of TC intensification.
\nTCs generally originate in tropics and thereafter, travel westward [20, 21] or turn poleward and recurve towards eastward direction [21, 22] or suffers extratropical transition over land or water [23] before dissipation. If a time scale of 1–3 weeks is considered, then the evolution of Rossby wave train significantly influences the track of a TC. Across the subtropical regions, under the influence of synoptic scale ridging, the TCs tend to move more westerly, and under the influence of synoptic scale trough, TCs tend to recurve into the mid-latitude [24]. On a seasonal scale, it is seen that over the Indian Ocean, the advancement of monsoon has a considerable impact on TCs’ growth and their track [25].
\nIn principle, TCs move under the influence of its surrounding environment. When the easterlies are added with the wind at certain level from the storm, the resulting effect forces the system to move in a westward direction [26]. Since the winds are not constant with height, it complicates the movement. The ‘β effect’ or ‘β drift’ pushes the cyclone towards the northwest direction in the northern hemisphere. It superimposes a weak northwest ward (southwest ward) steering current upon the TC in the northern (southern) hemisphere.
\nApart from the factors mentioned earlier, the wind shear around anti-cyclonic flow at the top of the TCs also impacts their movement and can influence the track as much as the ‘β drift’. There is a more complex phenomenon which influences the motion of a cyclone, known as ‘Fujiwhara effect’ [27]. Fujiwhara interaction describes the mutual rotation of two vortices about a common centre [28]. This centre typically refers to the mass weighted centroid of the two vortices, if they are of equal strength. In the presence of the β effect, the two vortices rotate around each other relative to the centre of rotation. This centre of rotation is not fixed and, instead, moves northwest ward in response to the ‘β effect’. ‘Fujiwhara effect’ is noticed over other basins of the world including Atlantic, but is not applicable for TCs formed over NIO.
\nThe most common way of dissipation of a TC is its landfall. When the storm moves over land, it deprives itself from warm water and the available moisture over ocean. Consequently, it is deprived from the energy source and the warm core with thunderstorms near the centre turns into a remnant low-pressure area due to quick loss of energy. Weakening can also occur if it encounters a vertical wind shear that causes the heat engine and convection shift away from the centre. The rate of power dissipation of TCs can be computed [29] as
\nwhere ED is the rate of energy dissipation per unit time per unit horizontal surface area, v defines the wind speed, ρ is for air mass density, and ‘CD’ is the drag coefficient that depends upon the surface irregularities. Since the power dissipation in TCs is proportional to the cube of its wind velocity, the severity can be computed as the cumulative sum of the cube of the wind velocity over time according to the above equation.
\nThere are two sources which are capable of changing the TC intensity, one is internal variability and other one is environmental interaction. One important aspect of later source is the interaction between the ocean and the storm system. Usually TC is regarded as the most forceful case in air-sea interaction studies where energy from the warm ocean waters is delivered via surface heat flux [30]. The ocean response is quite sensitive to the surface drag coefficient. Emanuel [31] used a simple numerical model to establish the progress of hurricane intensity. Their findings advocate that in most cases, the intensity depends on three factors, viz. initial intensity of cyclone, thermodynamic state of atmosphere through which the cyclone propagates and finally the heat exchange with the upper layer of the ocean underlying the core of the cyclone. Rapid intensification of TC is noticed when it passes over the deep upper ocean mixed layer and that upper ocean thermal structure plays a significant role in the intensification process [32–34]. Sutyrin [35] performed simulations with a coupled model of the oceanic and atmospheric boundary layers and concluded that the interaction is strong enough to change the supply of heat and moisture fluxes from the ocean into the atmosphere significantly within few hours of the formation of the storm and consequently, influence the TC intensity.
\nThe intensity of TC increases with increase in SST and upper ocean heat content [36]. The positive feedback occurs when genesis and intensification happens. During this phase, the evaporation from the ocean surface stimulates surface wind that subsequently increases the moisture supply and consequently increasing the latent heat that is further utilized to drive the circulation. As a negative feedback, the decrease in SST results in the decrease in total heat flux (sum of latent heat and sensible heat), resulting in decrease in intensity of the storm. Besides these interactions, some of the mechanical energy supplied by the TC is dispersed laterally and vertically by the internal inertia-gravity waves with time [37].
\nOn the other hand, the intensification of TC depends not only on SST but also on subsurface ocean thermal structure also considered as an important predictor for the TC intensification (e.g. see [38–40]). In the changing climate scenario, SST plays a bigger role during pre-monsoon season as compared to the post-monsoon period for governing TC activity over NIO region [41]. In contrast, the same may not be valid for other basins including North Atlantic Ocean, where an increasing trend in correlation between SST and TC power dissipative index is observed [42]. The influence of the changing climate on the TC genesis and intensification in the NIO region may therefore not be limited to the analysis relating SST only.
\nA significant number of studies regarding TC propagation, track prediction, time and place of landfall and intensity of the storm are carried out for several ocean basins including NIO. Considerable improvements in predicting the TCs are also achieved till date. In view of these, this section highlights the recent developments regarding TC predictability over NIO region and the current scenario.
\nVarious regional models such as GFDL (USA), ALADIN (France), Quasi-Lagrangian Limited Area Model or QLM (India), MM5 (USA), etc. are used for TC research and operational forecasting purpose. Apart from these, the Eulerian-mass-based dynamical core of Weather Research and Forecasting (WRF) model, designed as the successor to MM5 is also used to predict TCs. The variants of WRF regional model are Advanced Research WRF or ARW and non-hydrostatic mesoscale model or WRF-NMM. Though these numerical models are quite capable for real-time predictions in regional scale, they need appropriate initial and boundary conditions from global models. For example, a recent study carried out by Kumar [43] discusses about the impact of European Centre for Medium-Range Weather Forecasts (ECMWF), National Centers for Environmental Prediction (NCEP) and National Centre for Medium Range Weather Forecasting (NCMRWF) global model analysis on the WRF model forecast for TC prediction over Indian region. This study indicates some of the inherent limitations of such global analyses data sets including the consideration of few fundamental aspects like that of the middle tropospheric humidity profiles those are important for TC genesis. Another limitation of such data sets is their horizontal resolution though recent advancements have made availability of some of the usable global analyses for the desired purpose with higher spatial resolutions up to 0.25°.
\nSince NWP models are equipped with real-time prediction capability, they are being used increasingly for the TC prediction over NIO region as well. Some of the numerical models and their skills are discussed here. For instance, QLM regional model was adopted by Prasad [44] for cyclone track prediction over NIO region and found the performance to be reasonable. The recurvature of the cyclones were also well predicted. However, the model performance for TC intensity prediction was not satisfactory. Another notable study by Mohanty et al. [45] used MM5 to simulate Orissa (Odisha) super cyclone (1999) for predicting track, intensity, mean sea level pressure and associated precipitation. Though such types of studies were able to improve the prediction of several relevant parameters including TC tracks, they were not so successful in predicting the intensity accurately like the studies performed using QLM. Similarly, some recent studies used three variants of the next-generation mesoscale WRF model (i.e. ARW, WRF-NMM, and Hurricane Weather Research and Forecasting Model or HWRF) for TC research and operational purpose as well [51, 53, 56, 57, 66]. It may be noted that ARW uses Arakawa C-grid staggering while WRF-NMM and HWRF use Arakawa E-grid. All of the WRF model variants use terrain following co-ordinate system and specific physical parameterizations. Since several modelling features in WRF are quite advanced (e.g. moving nest feature in HWRF) as compared to MM5, it is expected that at least one or more variants of it would show better performance for TC prediction over NIO region. Extensive research in this direction using ARW suggests some significant improvements in predicting the tropical cyclogenesis and cyclone tracks [10, 46–54]. However, it is noticed that improvement in prediction of TC intensity is found to be slower than that of track [51, 55].
\nA comparison study among MM5, WRF-ARW and WRF-NMM for very severe cyclone Mala (2006) developed over BOB found that ARW could simulate the TC intensity in terms of minimum central pressure and maximum sustainable wind with better accuracy [56]. However, MM5 simulated a more rapidly intensified storm and delayed landfall and WRF-NMM failed to simulate the intensity of the storm properly. On the other hand, WRF-NMM predicted TC track more accurately as compared to ARW and MM5. The TC Mala when simulated using HWRF with different initial conditions, the track error was found to be ∼200 km and the intensity prediction was reasonably good for some considered initial conditions though the amount and spatial distribution of rainfall was well simulated by the model [57]. In order to improve the predictability, appropriate nesting technique, horizontal and vertical resolutions as well as physical parameterizations are considered [59, 68] besides data assimilation [60]. In view of these aspects, the HWRF system is now implemented at IMD along with the already operational ARW model for forecasting of TCs over NIO basin. As part of the Forecast Demonstration Project (FDP) conducted by IMD, it is analysed that the performance of ARW without data assimilation is reasonable over BOB [61]. Its performance improves when available observations are assimilated. Similar is the case with WRF-NMM. On the other hand, HWRF is capable of simulating rapid intensification of TCs over NIO region due to its improved vortex relocation and initialization procedures [49].
\nThe high-resolution mesoscale modelling systems provide better guidance for TC forecast up to 72 h over NIO region [61]. They require high-resolution global analyses data sets for appropriate initial and boundary conditions in order to bring in large-scale boundary forcing [62]. In order to reduce model errors, the initial and boundary conditions can be improved by adopting appropriate data assimilation techniques by incorporating the conventional, radar and satellite observations before running the model [61]. Thus, these aspects need special attention as far as predictability of TCs over NIO region is concerned.
\nThe physical parameterizations which include cumulus convection, surface fluxes of heat, moisture, momentum and vertical mixing in the planetary boundary layer play an important role in determining structural development, intensification and movement of TCs [10, 46, 48, 50, 53, 58, 63–65]. A number of studies emphasized upon these aspects during the past three decades. For the simulation purpose, they use the previously mentioned models (see Section 5.1). Most of these studies conduct simulations over a particular ocean basin. For instance, Osuri et al. [50] conducted a systematic study on customization of ARW model considering several physical parameterization schemes for the simulation of five TCs over NIO region. The study found that the combination of Yonsei University (YSU) planetary boundary layer (PBL) parameterization with KF convection scheme provided a better prediction for structural characteristics, intensity, track and rainfall. Similar results were also achieved by several studies including that of [10, 46, 48]. Thus, most of the studies (including [65]) found the performance of KF scheme to be better for the prediction of TCs over NIO region. However, recent studies by Kanase and Salvekar [53] obtained that the Betts-Miller-Janjic (BMJ) convection scheme performs better as compared to other parameterizations in the group although the study also favoured using YSU PBL physics. On the other hand, it found that WRF single-moment (WSM)-6 microphysics better represents mid-tropospheric heating as compared to WSM-3 favouring better intensity simulation.
\nThough HWRF has not been extensively used for sensitivity studies with respect to physical parameterizations for simulation of TCs over NIO region, its primitive variant WRF-NMM was used in recent past by some of the researchers. For example, studies by Pattanayak et al. [66] found that the combination of Simplified Arakawa-Schubert (SAS) convection, YSU PBL, Ferrier microphysics and NMM land-surface parameterization schemes in WRF-NMM performs better in predicting track and intensity of TC Nargis (2008) over BOB. Therefore, an extensive evaluation of HWRF is needed in order to determine the combination of physical parameterizations that performs better for TC prediction over NIO region before it is adopted for the operational forecasting purpose.
\nThe grid resolution of a model also impacts the TC prediction [51, 58, 59, 67]. However, there are very few studies available relating to the impact of grid resolution on TC prediction over NIO region. One of the notable studies by Rao [68] evaluated the impact of horizontal resolution and the advantages of the nested domain approach in the prediction of Orissa (Odisha) super cyclone intensification and movement by using MM5 model. Results from this study indicate that the enhancement of resolution produces higher intensity but does not influence the track of the storm. The nested experiments produced cyclone track closely agreeing with the observations, while the single domain based simulations show the deviation of the track towards north. A more recent study by Osuri et al. [51] found that the use of high resolutions in operational ARW model improves the prediction of recurving TC tracks and their intensity. In a climatological framework, Community Atmospheric Model or CAM showed sensitiveness to the prediction of more number of intensified tropical cyclones over most of the global basins including NIO. Further, it also found that the duration of tropical storms would be much larger in high resolutions simulations. Thus, it is realized that the model horizontal grid resolution impacts significantly the TC track, intensity and duration besides other relevant meteorological parameters.
\nMost of the times, the use of data assimilation techniques in TC simulations helps in improving the model predictability. For this purpose, satellite-based observations, aircraft measurements and radar data are used besides the conventional data sets. The widely used data assimilation techniques are primarily based on either ensemble Kalman filter (EnKF) or variational techniques (3DVAR or 4DVAR). Most of the studies related to TC simulation were done using variational data assimilation techniques for improving the TC prediction over NIO region. For example, the studies such as [52, 69–71] used 3DVAR techniques for assimilating satellite, radar and conventional measurements for improving the initial and boundary conditions of MM5 and ARW mesoscale models in order to better predict TC structure, track, intensity and associated relevant meteorological variables including rainfall. In some situations, the improvement was not significantly noticed. For instance, the studies by Singh et al. [70] found that assimilation of SSM/I wind speed data resulted in simulating weak intensity and failed to make an impact on track prediction.
\nAlthough there are no significant studies related to the use of 4DVAR and EnKF techniques for simulating NIO TCs, there are literatures, which demonstrate the usage of four dimensional data assimilation (FDDA) nudging technique in order to improve the ARW model predictability. For example, [71–73] used FDDA nudging technique in order to improve ARW initial and boundary conditions for the simulation of several TCs over NIO region those occurred during 2007–2010. These studies primarily emphasized upon TC track and intensity forecasts. While some of them reported remarkable improvements in track prediction and landfall position with either 12- or 18-h of nudging yielding maximum impact [72, 74], some others noticed relatively less impact of FDDA observational nudging on intensity prediction [73].
\nSince hundreds of years, the Indian Ocean is a breeding basin for disastrous TCs associated with heavy rainfall, torrential wind and storm surges. The cyclones in 1970 and 1991 caused a loss of more than 400,000 lives. During the Odisha super cyclone (1999), more than 10,000 lives were lost and a destruction of 1.9 million houses occurred in 14 districts. Recently, Nargis (2008) caused ∼1 40,000 deaths in Myanmar. In 2015, cyclonic storm Komen caused a heavy loss throughout Bangladesh, Myanmar, northeast India and eastern parts of India although the loss of lives was very few as compared to previous cases because of the improvement in TC predictability. This was also realized in case of Phailin (2013) and Hudhud (2014).
\nTCs usually form over NIO basin in two seasons, that is, pre-monsoon (March-April-May) and post-monsoon (October–November–December) period. In total, about 1108 numbers of cyclonic systems are formed over NIO region (includes both BOB and Arabian Sea, AS) during 1891–2015. It includes depressions (or D), cyclonic storms (or CS) and severe cyclonic storms (or SCS). However, the cyclonic systems do not form each month of every year. If the average monthly distribution of these three types of cyclonic systems (Figure 3) is analysed, it is evident that maximum number of cyclones occur between the months of May to December. Maximum numbers of depressions are formed in August. Maximum numbers of CS are formed in the month of October, while November is the most favourable month for the formation of SCS. Though the number of total cyclonic systems in May is relatively less, ∼48.7% of cyclonic disturbances are transformed to very severe cyclonic storms. However, this transformation is found to be 43.9 and 41.7%, respectively, in the months of April and November. Annually the probability of intensification of depression to CS is ∼44.8%, depression to SCS is ∼21.3% and the probability of intensification of CS to SCS is ∼47.5%.
\nMonthly frequency of cyclonic disturbances in North Indian Ocean region during 1891–2015. Here depression signifies the low-pressure systems which do not transform to cyclonic storms; CS is for the cyclonic storms and SCS represents the severe cyclonic storms.
BOB contributes about 75% of TCs during cyclone seasons (pre- and post-monsoon periods) and the AS contributes ∼25% [75]. The possible reason could be that BOB is generally more stratified than AS because its upper-ocean part is relatively warmer resulting in higher SST. In addition, low flat coastal terrain and funnel shape, shallow water of BOB [76], monsoonal wind (trough), more middle tropospheric moisture availability and lower tropospheric westward travelling disturbances such as easterly waves (often serve as the ‘seedling’ circulations) play roles in generating more number of cyclonic systems over BOB. Most of the monsoon troughs generated because of re-intensification of westerly propagating disturbances or from in situ depressions help in the formation of cyclonic systems over this region as well. Boreal summer intraseasonal oscillation (BSISO) also modulates the topical cyclogenesis over BOB [77], and it may be noted that the genesis potential index is high during the active phase of the BSISO.
\nThe studies like that of [4] indicate that under the global warming scenario, the number and proportion of cyclones reaching SCS are increasing in almost all basins of the world especially indicating the impact of climate change. Figure 4 shows the decadal variation of cyclonic disturbances and CSs over NIO, that is, over BOB and AS. It is clear from the curve that there is a significant decreasing trend in the number of cyclonic disturbances and CS. When the number of SCS are analysed, it shows a slight increase or may be considered as a constant trend in decadal scale (Figure 4). During 1961–1970 and 1971–1980, there was most number of SCS. Besides El-Nino Southern Oscillation (ENSO), MJO (Madden-Julian Oscillation) and IOD (Indian Ocean Dipole) may also play appreciable role in modulating the TC activity over NIO region [13, 16, 17, 77].
\nVariation of decadal frequency of cyclonic disturbances or depressions (D), cyclonic storms (CS) and severe cyclonic storms (SCS) over NIO region (smooth curved line). The bar diagrams represent SCS during 1891–2015. The dotted line indicates the moving trend and line shows the linear trend.
For the past three decades, the number of SCS has somehow decreased to a considerable value (Figure 4). However, Mohanty et al. [75] demonstrated that there is a considerable increase of SCS by about 65% during the warming period 1951–2007 by analysing the genesis and intensity of TCs over NIO basin in yearly scale. In the southern sector of BOB, a considerable increase of ∼71% in SCS is found in post-monsoon season. Rate of dissipation of SCS over BOB is also significantly reduced besides increase in mean SST in the warming scenario and these features contribute to increase in the number of SCS over NIO. In the western sector of AS, a significant increase in SCS is also observed in the warming conditions. Therefore, the intensity of the SCS is increasingly becoming significant in the changing climate scenario. When the ‘T Numbers’ of the cyclones are analysed in satellite era, it is found that the Odisha super cyclone (1999) was the strongest recorded CS in the NIO basin during 1990–2015.
\nAnalysing the track of cyclones over BOB and AS from e-atlas available at IMD, New Delhi, it is observed that most of the cyclonic systems developing over the NIO basin move in a northwesterly direction. However, there are cases of recurvature towards the northeast or east to southwest. The frequency of recurvature is higher towards the northeast compared to southwest or east. The probability of recurvature is higher over the AS when the system moves to the north of 15°N increasing the possibility of landfall over Gujarat coast. Over BOB, there is no such preferred latitude/longitude for the recurvature prospects. On the other hand, the probability of recurvature towards northeast region is higher during the pre-monsoon season.
\nOut of 1108 cyclones formed during last 124 years, 751 (68%) have crossed east coast of India, 214 (19.31%) Bangladesh, 57 (5.18%) Myanmar, 63 (5.68%) west coast of India and 26 (2.3%) numbers of cyclones crossed the coastal regions between India and Pakistan affecting the economy of both the countries. According to studies by Tyagi et al. [78], over 60% of TCs formed over BOB suffer landfall in different parts of east coast of India, 30% strike coasts of Bangladesh and Myanmar and about 10% dissipate over the sea itself. The differences in observed percentages are because of the obvious reason, that is, consideration of different time periods. However, it is evident that NIO basin is quite significant in view of the TC occurrence and highly populated and economically growing south Asian region.
\nIn order to improve the prediction of TC predictability over BOB region, the modernization of the observational system is being carried out by IMD, which includes setting up of two clusters of surface meso-meteorological networks: one along the coasts of Odisha-West Bengal and the other around Andhra Pradesh coasts [2]. About 443 numbers of existing automatic weather station (AWS) are there set up in different states of India. For NIO basin, it is considered very important to acquire weather reconnaissance aircraft facility to provide information on environmental winds and thermodynamical structures in the inner core region of TCs. The FDP (2008) is an attempt in this direction to determine the possible improvements in track and landfall predictions by using aircraft data.
\nThe programmes named as STORM and PRWONAM are carried out with the support of Ministry of Earth Sciences (MOES) and Department of Science and Technology. MOES is also involved in strengthening of the deep ocean and met-ocean buoys network. In addition, IMD has established high wind speed recorder systems, S-band Doppler radars and Global Positioning System (GPS) equipment along the coastal areas of India [79]. Under the Indo-French collaboration, Oceansat-II (was functional till 2014) and MEGHA-TROPIQUES satellite with capability of repeated scanning over BOB region are/were functional to provide data related to sea surface winds, clouds, humidity, temperature, rainfall and radiation. The earth receiving stations for METOP and MODIS satellite data have been installed at IMD. Products like cloud motion vector (CMV), water vapour wind (WVW), out-going longwave radiation (OLR), quantitative precipitation estimate (QPE), Sea Surface Temperature (SST), upper tropospheric humidity (UTH) and cloud top temperature (CTT) are derived from other satellites including KALPANA-1 and INSAT-3D.
\nSeveral research institutes such as National Centre for Medium Range Weather Forecasting, Noida; Indian National Centre for Ocean Information Services, Hyderabad; Indian Space Research Organization (ISRO), Air Force and academic institutes including IITs (Indian Institute of Technology), NITs (National Institute of Technology), universities contribute towards providing their valuable input through academic research regarding various aspects of TC activity over NIO region. With these inputs and in-house research and development, IMD has been able to strengthen its capability in recent past, both from numerical modelling as well as observational point of view by taking into account both in situ and satellite measurements.
\nDespite increased capability for TC prediction over NIO region, few aspects still need to be addressed. Those key areas include accuracy in track prediction, time and place of landfall, accurate storm surge prediction and improving the intensity predictability. In addition, the changes in tropical cyclogenesis need to be understood in the changing climate scenario. It is because the severity of TCs is found to be increasing in the warming environment [75]. The improvement in numerical model predictions can be done by improving physical parameterization schemes, incorporating observations from different sources including those from satellites and radars in the model initial and boundary conditions through appropriate data assimilation techniques and considering improved SSTs. In addition, better disaster management need to be done alongside in order to reduce the loss of lives and properties.
\nAccording to data from the World Meteorological Organization, global water consumption increased more than six-fold in less than a century, more than double the rate of the population growth, and continues to grow considering rising consumption in the agricultural, industrial and domestic sectors [1]. These data lead to the conclusion that in the coming years the global situation of water reserves will move towards a crisis, both in quantitative and qualitative aspects, if adequate water management actions are not taken. More recently, urban water supply crises (UWC) have been observed, a context characterized by water scarcity, as well as damage to the environment and population health, especially among poor populations. As human populations continue to grow, these problems are likely to become more frequent and serious. One example is the case of New York City’s water supply, which is facing a crisis. The social and economic development of New York City from the 1970s led to a sudden crisis in the city’s water supply system in the 1990s [2]. Other examples were also reported, such as in Palestine, where a UWC case was observed caused mainly by the inadequate access to freshwater resources and inappropriate management [3]. The city of Tijuana, in Mexico, has shown the highest rates of economic growth in the country, resulting in a rapid increase of water demand and consequently the emergence of a UWC [4]. From 1998 to 2000, the city of Campina Grande in Brazil faced a WSC caused by severe periods of drought and the complete absence of freshwater resource management [5]. This UWC caused serious water rationing in Campina Grande that lasted one year. This is not a unique case in Brazil as frequent water rationing has been observed in the cities of Recife and São Paulo [6]. In the Brazilian Federal District, rapid non-planned urbanization and land changes have had a considerable impact on water resources. From 2016 to 2018, the city of Brasilia also went through a UWC situation, and governance, regulation, as well as management support strategies in the urban and rural environment were implemented [7].
In another study, an investigation into Qatar’s sustainability crisis, originating from high levels of water, electricity and food consumption was carried out [8]. The high levels of consumption were made possible by the significant wealth of hydrocarbons, redistributive water governance of a generous rentier state and structural dependence on imported food and subsidies on food production. In this state, the water crisis is silent because it does not cause interruptions in supply or public discontent. The possible solution comes from programs that integrate the water, energy and food sectors [8].
The imprecise and ambiguity are inherent to the water supply system, e.g., pressures, flow rate supply and consumption, age and characterization of pipe resistance. Some researches that addressed this imprecise using Fuzzy Logic are briefly described below. A study to accommodate aleatory uncertainty was performed using stochastic analysis to represent the input uncertainties and to estimate resulting uncertainty in nodal pressures and pipe flows) [9]. Results of Fuzzy analyses for two realistically sized water distribution networks show that the proposed method performs with an acceptable level of accuracy and greatly reduces computational time [9].
The need to improve predictive models of hydraulic transients in water systems (water supply networks) was the subject of another study [10]. For this purpose, triangular Fuzzy numbers are used to represent the input uncertainties. Then, to obtain the extreme pressure heads in each location of the network and at each level of uncertainty, four independent optimization problems are solved. The results is found computationally fast and promising for real applications [10].
The Fuzzy Logic is a perfect tool among white-box methods (models based on laws of physics, chemistry, others, that govern the dynamic behavior of the system) for risk analysis due to the capabilities in dealing with limited data, subjective and temporal variables, and modeling expert opinions, among others [11]. For this reason, Fuzzy Logic was used as comprehensible framework for assessing water supply risk based on existing and under-construction projects in Mashhad city, Iran. The results showed that the framework based on the Fuzzy and possibility theory is befitting to information gathered from experts. Such a framework can provide a simple method to apply the proposed methodology to other water management projects, where, despite the high level of investment, there is no clear idea of the risks and their consequences [11].
Mathematical modeling is a well-known tool for water management. However, when considering UWC, there are some limitations of the conventional mathematical modeling that are related to vague and ambiguous data (e.g. real water-loss, real water availability, setting water tariffs, among others). In theory, the UWC problem can be formulated as a mathematical problem. In practice, rules are considered to be a more practical method. However, the combination of mathematical programming and Fuzzy rule has rarely been discussed in the literature [12]. The aim of this chapter is to describe the develop a mathematical model for UWC, dealing with this ambiguity and real data uncertainty.
UWC modeling was essentially based on the definitions of water crisis and Fuzzy Logic. The topics are presented briefly below.
A UWC case was presented in Iran, and information about its installation process, climatic characteristics of the region, range of per capita water consumption, among others was provided [13]. As the authors mention, up to 1990, water supply was not a critical problem and there was an acceptable relationship between water demand and distribution. Over the last decade, however, the problem has become critical and the reasons identified include rapid population growth. In addition, there is a reduction in the number of water supply systems (due to the loss of financial resources) and the widespread occurrence of droughts. Considering these observations, one can arrive at the concept of UWC, basically translated as a mismatch between water supply and consumption rates, according to Eq. (1).
In which: C is water consumption; A is the water availability.
According to [14], when clarifying the terms of water consumption (C) and water availability (A) and the definition of constraints, some issues then need answers. Is there a more suitable form of a mathematical model to represent water consumption (C)? Is there a mathematical model that is the water availability (A)? What and how many factors are there (socioeconomic, environmental, cultural, urban, and management conditions) that should be considered in these models? What restrictions should be imposed on the optimization model? The literature review suggests that Fuzzy Logic can help by incorporating imprecision and ambiguity in the translation of influential factors and field characteristics.
The advent of Fuzzy Logic originates from the need of a method that can systematically express inaccurate, vague, ill-defined quantities [15]. For example, instead of using a complex mathematical model, industrial controllers based on Fuzzy Logic can be implemented using knowledge from human operators, or heuristic knowledge. This makes the control action using Fuzzy Logic as good as using the raw knowledge (generally better) and always consistent. In decision analysis, Fuzzy Logic can be used in tasks in which individual variables are not defined in exact terms. Some examples of this have been provided in the literature [16, 17]. In the environmental area, the population’s preference for water conservation action, the assessment of the performance of environmental education programs and policies in preventing forest fires are examples of individual variables not defined in exact terms. The properties of Fuzzy Systems are demonstrated in several publications, as, for example, in [18]. An introduction to the theory of Fuzzy sets is presented below.
In general, a Fuzzy Set can be summarized as follows [15, 18, 19]:
Definition 1: a subset A of a set X is said to be Fuzzy Set if
Definition 2: a fuzzy set A of set X is said to be normal if
Definition 3: the height of A is defined and denoted as
Definition 4: the α-cut and strong α-cut is defined and denoted respectively as
Definition 5: let
Definition 6: if a Fuzzy number
Theorem 1: a fuzzy set A on R is convex if and only if
Theorem 2: let
Where:
The Fuzzy Linear Programming Problem (FLPP) with decision variables and coefficient matrix of constraints are in Fuzzy nature (Eqs. 3–6).
subject to
The triangular Fuzzy numbers A which can be represented by three crisp numbers s, l, r (Eqs. 7–10).
subject to
Where:
Theorem 3: For any two triangular Fuzzy numbers
subject to
As examples of membership functions for a Fuzzy number
Such membership functions are illustrated in Figures 1 and 2. More information about Fuzzy Mathematical Programming is available in the literature [15, 16, 17, 18, 19, 20, 21, 22, 23].
Fuzzy number m∼=(ms,ml,mr), triangular membership function.
Fuzzy number m∼=(ms,ml,mr), bell-shaped membership function.
The methodology of this work comprised the following steps: (1) identifying the influencing factors in UWC; (2) proposing a conceptual model for UWC; (3) data collection and data simulation; (4) optimizing the proposed conceptual model parameters (calibration); and (5) assessing conceptual model performance (verification).
For step (1), a literature review was conducted related to WSC management.
For step (2), the definition of UWC found in the literature was taken and the Fuzzy Non-Linear Programming (FNLP) was used [12, 15, 16, 17, 18, 19, 20, 21, 22, 23, 24].
For the third step (step 3), a case study was simulated in Brazil, more precisely in the Federal District, taking into account predictions made by some researchers. The necessary data were collected from the Brazilian Federal District’s water supplier and sanitation company (CAESB), from the National Institute of Meteorology in Brazil (INMET) and from the Brazilian Federal District’s Government (GDF). The simulation was conducted assuming the hypothesis of a significant increase in the water consumption in coming years, as well as managerial and political stagnation of the water supplier and sanitation company. The time series analysis refers to three years (2007, 2008 and 2009). The period for model calibration was considered for two years and the verification period was considered for one year. Data were normalized prior to optimization of conceptual model parameters. This was done to restrict their range within the interval of −1.0 to +1.0 to eliminate the difference among scales measuring the influencing factors, according to Eq. (18).
Where: xnorm is the normalized value; x0 is the original value; xmax is the maximum value; xmin is the minimum value.
For step (4), the minimization of the sum of squared errors and the Differential Evolution & Particle Swarm Optimization algorithm (DEPS) was adopted, using the spreadsheet from Open Office (Calc-Solver). As a justification for using the DEPS algorithm, it presents good performance to obtain global optimums, based on the synergy between Particle Swarm Optimization (PSO) and Differential Evolution (DE) [25].
In step (5), some tests used to model performance assessment were proposed, among them, the correlation coefficient (r), the determination coefficient (R2), the average relative error percentage (AREP) and graphic observed values versus estimated values.
A bibliographic review was conducted by [26] and resulted in a list of influential factors presented below:
Population growth rate.
Human population density.
Socio-economic level.
Education level.
Industry level.
Ambient temperature.
Relative humidity.
Rainfall.
Seasonality.
Size and topographic characteristics of the city.
Percentage of water metering.
Water tariffs.
Type of water tariff policies.
Existence of wastewater collection systems.
Human Development Index.
Pressure in the water distribution network.
Existence of conservation habits.
Number/type of hydro-sanitary equipment per household.
Constructed area per household.
Number of rooms.
Abundance or scarcity of water sources.
Water-loss.
Social representation and identification of each family.
Existence and type of municipal water resources policy.
Acceptance of the population to water conservation and rational use actions.
Typology of land use.
Type of consumers.
Type of municipality.
Predominant function of urban environment.
Existence of policies to promote water conservation.
Intermittence in the water supply system.
Energy consumption.
Existence of regulatory policy on water consumption.
Existence of environmental education program.
Dissemination of the belief: water is an inexhaustible resource and low-priced.
The UWC has appeared as an inadequate ratio between water consumption and water supply [12]. Water consumption and water availability are vague and ambiguous terms, because they are dependent on haziness measures, qualitative factors, scarcity data and low-quality data [27].
Design and analysis of water distribution networks (WDNs) are laden with uncertainty. There is natural randomness, such as variations in reservoir elevation heads, and there is epistemic randomness, i.e., incomplete knowledge, imprecise data, and linguistic ambiguity. Both are associated with the characterization of pipe resistance, nodal demands, and hydraulic responses [9]. The analysis of water distribution networks has to take into account the variability of users’ water demand and the variability of network boundary conditions, e.g. the presence of local private tanks and intermittent distribution [28].
Some of these factors were considered in this paper, the faulty water metering (
Where:
For a mathematical representation of the
Likewise, a Fuzzy mathematical behavior of the
The membership functions for the fuzzy numbers
Fuzzy number for water consumption, C∼.
Fuzzy number for water availability, A∼.
The membership functions for the fuzzy numbers (
Fuzzy number for pressure in the water distribution network, p∼.
Fuzzy number for total water-loss in water supply system, l.∼
All assumptions, from
subject to
subject to
Where:
Eq. (28) and (29) show the results of the parameter optimization in the proposed conceptual model when applying the previously described data normalized according to Eq. 4.
The collected and simulated data and its respective descriptions are shown in Table 1. Table 2 and Figures 7–12 show the results of the model performance.
Collected and simulated data | Average ± sd* | Symbol | Unit | Data source |
---|---|---|---|---|
Water consumption | 14,381.2 ± 773.8 | × 103 m3.month−1 | Simulated | |
Water availability | 15,234.0 ± 325.3 | × 103 m3. month −1 | Caesb** [32] | |
Ambient temperature | 21.1 ± 1.15 | x1 | °C | INMET** [33] |
Relative humidity | 67.83 ± 10.10 | x2 | % | INMET** [33] |
Rainfall | 113.21 ± 82.26 | x3 | mm.month−1 | INMET** [33] |
Collected revenues | 681.70 ± 41.05 | x4 | million R$.month−1 | GDF** [34] |
Water distribution network pressure | 54.63 ± 6.62 | mH2O | Simulated | |
Unemployment indicator | 16.85 ± 1.13 | x5 | % | GDF [34] |
Total water-loss in water supply system | 18.99 ± 4.41 | % | Simulated | |
Intermittence in water supply system | 35.32 ± 6.95 | x6 | hours.month−1 | Simulated |
Collected and simulated data.
sd is the standard error
availability of data on the Internet, partially simulated (fault fill)
Calibration | Verification | |||||
---|---|---|---|---|---|---|
Models | r | R2 | AREP | r | R2 | AREP |
Water consumption, | 0.8777 | 0.7704 | −7.95 | 0.5994 | 0.3593 | −40.15 |
Water availability, | 0.9755 | 0.9516 | 5.32 | 0.9412 | 0.8858 | −16.95 |
Results of calibration and verification of models.
r: correlation coefficient
R2: determination coefficient
AREP: average relative error percentage
Calibration C∼ model.
Verification C∼ model.
Calibration A∼ model.
Verification A∼ model.
Calibration model.
The calibration and verification results indicated that the proposed conceptual model has shown good agreement for the collected and simulated data, when considering some previous research. For instance, a study on water demand developed in the cities of Oklahoma and Tulsa Oklahoma State, USA, resulted in a statistical model to explain water demand with R2 range within the interval of 0.140 a 0.920 [35].
In a household water demand study in the northwest of Spain, the price, billing, climatic, and sociodemographic variables were used as explanatory variables and the results showed a R2 range within the interval of 0.198 to 0.891 [36].
Verification model.
Another study aiming to predict future water consumption from Istanbul, Turkey, was developed using the Takagi Sugeno Fuzzy method for modeling monthly water consumption, and the overall prediction presented an AREP of less than 10% [37]. In this study, AREP ranged from −40% to 5% indicating an opportunity to improve the model developed. In another regional water study, in the case of Tijuana, in Northwest Mexico, the purpose was to analyze monthly water consumption dynamics, and the empirical estimation results were considered fairly satisfactory with the R2 range from 0.4582 to 0.5932 [4].
The analysis in Figure 12, agreeing with the AREP of −40%, reinforces the difficulty of the model developed in the
In general, when considering the quality of the models developed (
It can be concluded that the UWC was adequately modeled, the ambiguity and the lack of precision of the real data availability was acceptably managed, and the fuzzy approach showed to be adequate for the problem studied. The conceptual model developed in this research can contribute to the water conservation in an urban environment, which is an important tool for water resource planning. More specifically, the model helps to predict the impact of actions such as reducing losses, reducing pressure on the water supply network and intermittent supply on the intensity of water crisis cases in cities.
The methodology used for developing the model can be replicated in other cases. Influential variables can also be adjusted according to the desired responses and available resources. For example, variables such as type of tariff policy, implementation of environmental education programs and incentives to reduce water consumption are possible to be considered in this model. Thus, Fuzzy modeling is a very promising tool and should be encouraged so as to deepen and expand similar models.
The ambiguity and haziness index of the real data should be considered in further studies. In the future, more influencing factors in water crises should be included in the model being developed, in order to improve prediction results.
Finally, studies focusing on selecting the best forms of representation of Fuzzy variables (Fuzzy membership functions and optimized parameters) should be considered.
The authors would like to express their gratitude for the financial support from the Brazilian agencies CNPq (project No. 556084/2009-8), CAPES and DPP-UnB.
The authors declare no conflict of interest.
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