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Climate change and Urban Vulnerability in Africa Assessing vulnerability of urban systems, population and goods in relation to natural and man-made disasters.

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Presentation on theme: "Climate change and Urban Vulnerability in Africa Assessing vulnerability of urban systems, population and goods in relation to natural and man-made disasters."— Presentation transcript:

1 Climate change and Urban Vulnerability in Africa Assessing vulnerability of urban systems, population and goods in relation to natural and man-made disasters in Africa 1 Training on the job Course on Hazards, Risk and (Bayesian) multi-risk assessement Napoli, – /02/2014Fatemeh Jalayer

2 20/02/2014Fatemeh JalayerSlide 2 Earth Structure Crust: The uppermost 5-70 km of the earth. There are two types of crust: continental and oceanic. Continental crust ranges from km thick and has a composition approximating that of granite. Oceanic crust, on the other hand, is approximately 5 km thick and has a composition similar to basalt, making it significantly denser than continental crust. Mantle: The middle portion of the interior of the earth, starting below the crust at 5-70 km below the earths surface and continuing to a depth of 2900 km. Core The innermost layer of the earth, which starts at ~2900 km depth. The core is composed mainly of iron and consists of a molten outer core and a solid inner core.

3 20/02/2014Fatemeh JalayerSlide 3 Plate Tectonics Subduction zonesMid-Ocean ridges

4 20/02/2014Fatemeh JalayerSlide 4 Map showing earthquakes from with magnitude greater than 3. Colors indicate depth of hypocenter, or origin of the earthquake: red is 0-33 km, yellow is km, green is km, and blue is >400 km depth. Data are from the Advanced National Seismic System. Plate Tectonics

5 20/02/2014Fatemeh JalayerSlide 5 Map showing volcanoes that have been active in the last 10,000 years. Colored triangles indicate different volcano types: red triangles are primarily calderas, green triangles are stratovolcanoes, blue triangles are shield volcanoes and fissure vents. Data are from the Smithsonian Institution, Global Volcanism Program. Plate Tectonics

6 20/02/2014Fatemeh JalayerSlide 6 Cross-section of the Mid-Atlantic Ridge near latitude 14° S. Blue triangle represents the location of fissure volcanoes. Colored circles represent earthquakes, color-coded by depth Divergent boundaries Transform boundaries Cross-section of the San Andreas Fault in California near latitude 36° N. Colored circles represent earthquakes, color-coded by depth Plate Tectonics

7 20/02/2014Fatemeh JalayerSlide 7 Cross-section of the South American subduction zone near latitude 22° S. Green triangles represent the locations of stratovolcanoes. Colored circles represent earthquakes, color-coded by depth Cross-section of the Tonga trench near latitude 21° S. Colored triangles represent the location of volcanoes, color-coded by type of volcano. Colored circles represent earthquakes, color-coded by depth. Oceanic meets continental Oceanic meets more oceanic Convergent boundaries Continental meets more continental Cross-section of the Himalayas along 88° E longitude. Colored circles represent earthquakes, color-coded by depth Plate Tectonics

8 20/02/2014Fatemeh JalayerSlide 8 Ipocenter and Epicenter

9 20/02/2014Fatemeh JalayerSlide 9 Distance Typology Fault Rupture Ipocenter Epicenter Site Epicentral distance Closet distance to the rupture surface Slant Distance Seismogenic Depth Closet distance to the seismogenic part of the rupture surface Ipocentral distance Joyner-Boore Distance

10 20/02/2014Fatemeh JalayerSlide 10 Fault typologies

11 20/02/2014Fatemeh JalayerSlide 11 Fault typologies

12 20/02/2014Fatemeh JalayerSlide 12 Fault typologies Strike-slip fault Normal fault Reverse fault Normal-oblique fault

13 20/02/2014Fatemeh JalayerSlide 13 Waves propagation p waves wave Rayleigh wave Love wave Body wavesSurface waves

14 20/02/2014Fatemeh JalayerSlide 14 Waves propagation

15 20/02/2014Fatemeh JalayerSlide 15 Site response surface waves reflected waves In alluvial basins on stiff bedrock, wave interpherences occur due to: - multiple reflections, - diffractions, - body to surface mode conversions. These phenomena induce, overall: - higher peak amplification - significant increase of duration with respect to 1D conditions.

16 20/02/2014Fatemeh JalayerSlide 16 Earthquake intensity Mercalli intensity scale The scale quantifies the effects of an earthquake on the Earth's surface, humans, objects of nature, and man-made structures on a scale from I (not felt) to XII (total destruction). Values depend upon the distance to the earthquake, with the highest intensities being around the epicentral area. Data gathered from people who have experienced the quake are used to determine an intensity value for their location. The Mercalli (Intensity) scale originated with the widely-used simple ten-degree Rossi-Forel scale, which was revised by Italian vulcanologist Giuseppe Mercalli in 1884 and 1906.

17 20/02/2014Fatemeh JalayerSlide 17 Earthquake intensity Mercalli intensity scale Damage map – Irpinia Earthquake, 1980

18 20/02/2014Fatemeh JalayerSlide 18 Earthquake intensity Richter magnitude His inspiration was the apparent magnitude scale used in astronomy to describe the brightness of stars and other celestial objects. Richter arbitrarily chose a magnitude 0 event to be an earthquake that would show a maximum combined horizontal displacement of 1 µm ( in) on a seismogram recorded using a Wood-Anderson torsion seismograph 100 km (62 mi) from the earthquake epicenter. This choice was intended to prevent negative magnitudes from being assigned. The smallest earthquakes that could be recorded and located at the time were of magnitude 3, approximately. However, the Richter scale has no lower limit, and sensitive modern seismographs now routinely record quakes with negative magnitudes.

19 20/02/2014Fatemeh JalayerSlide 19 Earthquake intensity Moment magnitude Fault moment M 0 = A D Rigidity G [F/L 2 ] Average offset Slip [L] Fault area [L 2 ] M 0 [dyne cm] Kanamori 1977 Moment Magnitude

20 20/02/2014Fatemeh JalayerSlide 20 Magnitude relationship In seismology, the Gutenberg–Richter law (GR law) expresses the relationship between the magnitude and total number of earthquakes in any given region and time period of at least that magnitude or Where N is the number of events having a magnitude > M; a and b are constants calibrated on a given set of events.

21 20/02/2014Fatemeh JalayerSlide 21 Magnitude relationship The constant b is typically equal to 1.0 in seismically active regions. This means that for every magnitude 4.0 event there will be 10 magnitude 3.0 quakes and 100 magnitude 2.0 quakes. There is some variation with b-values in the range 0.5 to 1.5 depending on the tectonic environment of the region. A notable exception is during earthquake swarms when the b-value can become as high as 2.5 indicating an even larger proportion of small quakes to large ones. A b-value significantly different from 1.0 may suggest a problem with the data set; e.g. it is incomplete or contains errors in calculating magnitude The a-value is of less scientific interest and simply indicates the total seismicity rate of the region.

22 20/02/2014Fatemeh JalayerSlide 22 Ground Motion prediction relations State-of-the-art estimates of expected ground motion at a given distance from an earthquake of a given magnitude are the second element of earthquake hazard assessments. These estimates are usually equations, called attenuation relationships, which express ground motion as a function of magnitude and distance (and occasionally other variables, such as type of faulting). Commonly assessed ground motions are maximum intensity, peak ground acceleration (PGA), peak ground velocity (PGV), and several spectral accelerations (SA). Each ground motion mapped corresponds to a portion of the bandwidth of energy radiated from an earthquake. PGA and 0.2s SA correspond to short-period energy that will have the greatest effect on short-period structures (one-to two story). PGA values are directly related to the lateral forces that damage short period. Longer-period SA (1.0s, 2.0s, etc.) depict the level of shaking that will have the greatest effect on longer-period structures (10+ story buildings, bridges, etc.). Ground motion attenuation relationships may be determined in two different ways: empirically, using previously recorded ground motions, or theoretically, using seismological models to generate synthetic ground motions which account for the source, site, and path effects. There is overlap in these approaches, however, since empirical approaches fit the data to a functional form suggested by theory and theoretical approaches often use empirical data to determine some parameters.

23 20/02/2014Fatemeh JalayerSlide 23 The ground motion at a site, for example Peak Ground Acceleration depends on the earthquake source, the seismic wave propagation and the site response. Earthquake source signifies the earthquake magnitude, the depth and the focal mechanism, the propagation depends mainly on the distance to the site. The site response deals with the local geology (site classification); it is the subject of microzonation. Ground Motion prediction relations The basic functional (logarithmic) form for ground motion attenuation relationship is defined as (Reiter 1990) ln Y = ln b1 + ln f1(M) + ln f2(R) + ln f3(M,R) + ln f4(P) + ln Where: Y is the strong motion parameter to be estimated (dependant variable), it is lognormal distributed; f1(M) is a function of the independent variable M, earthquake source size generally magnitude; f2(R) depends on the variable R, the seismogenic area source to site distance; f3(M,R) is a possible joint function between M and R (for example for an earthquake with big magnitude the seismogenic area is large and the source to site distance may be different); f4(P) are functions representing possible source and site effects (for example different style of faulting in the near field may generate different ground motions values Abrahamson and Shedlock (1997)); is an error term representing the uncertainty in Y

24 20/02/2014Fatemeh JalayerSlide 24 Ground Motion prediction relations Sabetta e Pugliese (attenuation law for Italy)

25 20/02/2014Fatemeh JalayerSlide 25 Seismic zoning Punctual source: this typology of modeling its used for fault very deep or very far from the interest area. Linear source: this typology of modeling its used with hypothesis that all the point of the line can be fracture point with the same probability. Planar source: this typology of modeling its used with hypothesis that all the point of the line can be fracture point with the same probability.

26 20/02/2014Fatemeh JalayerSlide 26 PSHA Probabilistic Seismic Hazard Analisis For each Seismic zones target is to evaluate the annual exceedance frequency of a given intensity trough the follow integral:

27 20/02/2014Fatemeh JalayerSlide 27 PSHA Probabilistic Seismic Hazard Analisis Starting from the knowledge of Seismic Zone Typology, of Attenuation Law and G-R Law is possible to evaluate: Extension to more Seismic Zones

28 20/02/2014Fatemeh JalayerSlide 28 PSHA Probabilistic Seismic Hazard Analisis To convert the annual rate of events to a probability, we consider the probability that the ground motion exceeds test level x at least once during a specific time interval. A standard assumption is that the occurrence of earthquake is a POISSONIAN process. For t=1 this probability is the annual hazard. Starting from previous relation is possible to obtain the Return Period of the generic event that has an exceedance probability of P in time t:

29 20/02/2014Fatemeh JalayerSlide 29 Deaggregation of Hazard The hazard curve gives the combined effect of all magnitudes and distances on the probability of exceeding a given ground motion level. Since all of the sources, magnitudes, and distances are mixed together, it is difficult to get an intuitive understanding of what is controlling the hazard from the hazard curve by itself. A common practice is to break the hazard back down into its contributions from different magnitude and distance pairs to provide insight into what events are the most important for the hazard.

30 20/02/2014Fatemeh JalayerSlide 30 Example The example site considered has two faults. Fault A, produces earthquakes with magnitude M=6 and distance R=10km from the site; and has an annual occurrence rate of =0.01; we denote this earthquake Event A. Fault B produces earthquakes with magnitude M=8 and distance R=25km from the site, and has annual occurrence of =0.002; we denote this earthquake Event B. Both events have strike slip mechanism. Site and Event description

31 20/02/2014Fatemeh JalayerSlide 31 Example PSHA Computation

32 20/02/2014Fatemeh JalayerSlide 32 Example In this simplified site, each event (Event j ) corresponds to a single magnitude (m j ) and distance (r j ). The conditional probability that each event causes Sa>y is given by follow equation: Deaggregation of Events

33 20/02/2014Fatemeh JalayerSlide 33 Example Deaggregation of Magnitude The deaggregation mean magnitude associated with a specific GMPM can be found using equation: Bold line

34 20/02/2014Fatemeh JalayerSlide 34 Example Deaggregation of Distance

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