GeoMod2008 Firenze, 22-24 September 2008 Figure 4. Sand model showing the impact of oblique convergence on strain partitioning, geometry of fault networks in the Island and escape tectonics occurring in the middle west and southwestern Taiwan REFERENCES Dahlen F.A., Suppe J. & Davis D.M.; 1984: Mechanics of fold and thrust belts and accretionary wedges: Cohesive Coulomb theory. J. Geophys. Res., 89, 10087-10101. Konstantinovskaia, E., and Malavieille, J.; 2005: Erosion and exhumation in accretionary orogens : Experimental and geological approaches. Geochemistry, Geophysics, Geosystems, Vol. 6, Number 2, 25 pp. Lohrmann, J., Kukowski, N., Adam, J. and Oncken, O.; 2003: The impact of analogue material properties on the geometry, kinematics, and dynamics of convergent sand wedges. Journal of Structural Geology, 25(10): 1691-1711. Lu, C.Y. and Malavieille, J.; 1994: Oblique Convergence, Indentation and Rotation Tectonics in the Taiwan Mountain Belt - Insights from Experimental Modeling. Earth and Planetary Science Letters, 121(3-4): 477-494. Platt J.P.; 1986: Dynamics of orogenic wedges and the uplift of high-pressure metamorphic rocks. Geol. Soc. Amer. Bull., 97, 1037-1053. Willett S.D. & Brandon M.T.; 2002: On steady states in mountain belts. Geology, 2, 175-178. UPLIFT AND EROSION RATES FROM THE SOUTHERN APENNINES, ITALY M. Schiattarella(1), P. Beneduce (1), D. Capolongo (2), P. Di Leo (3), S.I. Giano (1), D. Gioia (1), M. Lazzari (4), C. Martino (1) (1) Dipartimento di Scienze Geologiche, Università della Basilicata, Potenza (Italy) Dipartimento di Geologia e Geofisica, Università di Bari, Bari (Italy) (3) CNR-IMAA, Tito Scalo, Potenza (Italy) (4) CNR-IBAM, Tito Scalo, Potenza (Italy) (2) Summary Past studies of tectonically active mountain ranges suggested strong coupling and feedbacks among climate, tectonics and topography. Estimates of parameters useful for understanding evolutionary history of orogenic chains, especially values of both uplift and/or erosional rates and tectonic/sedimentary loading experienced by sedimentary successions, have gathered momentum during the last decade, and nowadays represents a powerful tool in which geoscientists are strongly interested (Burbank & Anderson, 2001; Kirby & Whipple, 2001; Pazzaglia & Brandon, 2001; Willett & Brandon, 2002; Schiattarella et al., 2003). Such parameters allowed in fact a better definition of exhumation age, timing and modality of the 470 GeoMod2008 Firenze, 22-24 September 2008 most ancient rocks in complex orogens as the southern Apennines (Schiattarella et al., 2003, 2006; Aldega et al., 2005). Further, a more exact genesis ascription of structural features of mountain chains, such as tectonic style, regional morphostructural setting, tectonic meaning and opening kinematics of recent intermontane basins, is also an important target that can be achieved by using such an integrated approach. Although theoretical links between climate, erosion and uplift have often received much attention, few studies regarding the southern Italian Apennines have shown convincing correlations between observable indices and parameters of these processes on mountain-range scales. The records about erosion rates exist, for example, from the hydrological practice of measuring sediment transport by rivers, but infrequently will that record include the full range of floods that have shaped the landscape. First studies dealing with uplift rates from the Italian Apennines appeared only recently. Many of these, referring to different sectors of the chain (Westaway, 1993; Basili et al., 1999; Amato, 2000; Schiattarella et al., 2003; Boenzi et al., 2004), were non representative of the entire orogenic system. Although stratigraphic characteristics of Quaternary deposits of the intermontane basins are generally well defined, a more precise assessment of the deposit ages is still needed to better date the morphological features (mainly land surfaces and terraces) used to estimate uplift rates. Anyway, new data and models for the comprehension of the regional morpho-structural settings of the northern, central, and southern Apennines are now available in Bartolini et al. (2003) and in Schiattarella et al. (2006). With respect to estimations of maximum palaeotemperatures (converted in sedimentary and/or tectonic loading) experienced by sedimentary successions, new multidisciplinary data on the south-Apennines chain are at present available in the literature (Schiattarella et al., 2003, 2006; Aldega et al., 2005). Integrating different methodologies represent the most conservative approach in studying thermal history of sedimentary successions involved in the formation of a chain. Such methodologies are based on clay minerals and their transformation through the tectonic/sedimentary evolution (Di Leo, 2003, and references therein) as well as on vitrinite reflectance, fluid inclusions, and apatite fission tracks (see Di Leo et al., 2005, and Invernizzi et al., 2008, for recent examples from the ophiolite-bearing units of southern Italy). The comprehension of the morphotectonic evolution of southern Italy needs to be linked together with uplift and erosion rate calculations, contribution of local tectonics to regional uplift, and with tectonic loadings from the units outcropping in the same area. In addition, a new effort has to be put to develop a more suitable methodological approach to understand the role of different paleoclimate scenarios controlling the landscape evolution. Further, mapping and assessing landforms and erosion in mountain environments is essential in order to understand landscape evolution and complex feedback mechanisms. DEMs and remote sensing data can be used to assess the properties of the topography and to estimate geomorphic indices mostly utilized in studies of tectonic geomorphology such as: hypsometric curve and hypsometric integral, drainage basin asymmetry, drainage density, stream length-gradient index, ratio of valley floor width to valley height (Keller & Pinter, 1996), and stream power. The role of remotely sensed data is still in its early stages in this field, partly hampered by the lack of an adequate regional modelling capability to assimilate and guide the data collection effort (Capolongo et al., 2002). This study aims to compare uplift rates with erosional rates (specifically to define the steady-state conditions of the orogenic wedge) as well as to compare uplift/erosion rates with the paleoclimate setting in which erosion and uplift processes interacted. To get this objective, geological and geomorphological makers (paleosols, alteration profiles, erosional surfaces, and paleolandslides, from chain and foredeep areas) have been used, as well as information on the paleoclimatic evolution during late Quaternary times has been obtained by the analysis of distribution of clay minerals in continental pelitic sediments, paleosols, and weathered horizons developed in depositional and erosional surfaces of different age from key-areas of the southern Apennines. In addition, absolute dating of geomorphological features and weathered horizons has been produced by different methods. The study areas are represented by seven Quaternary fault-controlled basins from southern Italy (Fig. 1): 1) the Tito-Picerno basin, with its main river flowing in an asymmetric valley of the axial zone of the Lucanian Apennine, including the homonymous villages, not far from the town of Potenza; this stream is a tributary of a network delivering to the Tyrrhenian Sea; the valley sides are characterized by four orders of erosional polygenic and/or depositional land surfaces, at least (Schiattarella et al., 2004, 2006); 471 GeoMod2008 Firenze, 22-24 September 2008 2) the valley of Pergola and Melandro rivers, flanked by the Maddalena Mts carbonate range to the west and by Lagonegro pelagic units to the east and filled by lower Pleistocene continental sediments (Schiattarella et al., 2003; Giano & Martino, 2003; Martino & Schiattarella, 2006, 2008); similarly to the Tito-Picerno basin, three orders of erosional land surfaces were also identified in the Pergola-Melandro basin. From a morpho-chronological point of view, these gently dipping surfaces can be confidently correlated to those from the basin previously described. The formation of the S1 land surface can be ascribed to the late Pliocene - early Pleistocene, as inferred by the presence of lower-middle Pliocene marine clastic deposits which were involved in the planation of the 1200 m a.s.l. palaeosurface (S1). Adopting a counting-from-the-top criterion and regional-scale basin correlations, the S2 and S3 land surfaces ages can be set up respectively at 1.2 and 0.8-0.7 Ma; 3) the high Agri Valley, located between the carbonate range of the Maddalena Mts and the SirinoVolturino massifs, made of Lagonegro-type pelagic successions, and filled by middle Pleistocene alluvial deposits (Di Niro et al., 1992; Giano et al., 2000); morphotectonic patterns and uplift rates are detailed in recent papers (Boenzi et al., 2004; Capolongo et al., 2005), showing a good fit with the other study areas, although the peak values are higher than the rates calculated for the Tito-Picerno and Pergola-Melandro basins; 4) the Auletta basin, located between the impressive carbonate ridges of the Alburni Mts to the south and Mt. Marzano to the north and filled by Pliocene to Pleistocene marine and alluvial successions (Ascione et al., 1992); the land surfaces setting is slightly different from the previously described basins, due to the complex Pliocene to Quaternary stratigraphic pattern; 5) the Sinni River catchment basin (upper to middle valley) in southern Basilicata, a complex area including very different geological units and contrasting geomorphological features; anyway, S2 and S3 erosional land surfaces are largely observable in the area; data about uplift rates are consistent with the previously collected data-set from the whole southern Apennines, but some significant differences exist between the erosion rates from the different study areas; 6) the Mercure basin, bordered to west and east respectively by the carbonate ridges of Lauria Mts and Mt. Pollino and filled by middle Pleistocene deposits showing fluvial and lacustrine facies (Schiattarella et al., 1994; Gioia & Schiattarella, 2006); 7) the Venosa basin, a mid-Pleistocene lacustrine depression located in the foredeep area (“Fossa bradanica”), close to the thrust front of the chain and not far from the Mount Vulture, a Pleistocene volcano which represents part of the source area of the sediments of the basin (Schiattarella et al., 2005; Giannandrea et al., 2006, and references therein); this area would represent a test-site of the whole foreland basin zone, for a comparison with the intra-chain basins. Figure 1. Location of study areas in southern Italy (numerated as in the table I) and related values of erosion rates. 472 GeoMod2008 Firenze, 22-24 September 2008 Figure 2. 3D image of uplift rates from southern Italy, showing a non homogeneous pattern. The highest peak is represented by data from Calabria Coastal Chain. Table 1. Study areas from southern Italy 1) Fiumara di Tito-Picerno basin 2) Valley of Melandro River 3) Upper Valley of Agri River 4) Valley of Tanagro River (i.e. Auletta basin) 5) Upper Valley of Sinni River 6) Mercure River basin 7) Fiumara di Venosa basin Erosion rates (mm/y) 0.20 0.23 0.35 0.25 0.17 0.11 0.17 In all the investigated valleys and surrounding mountains, uplift and erosion rates have been accurately defined. On the grounds of correlations among land surfaces inside the basin and between these ones and the nearby palaeosurfaces, uplift rates for the last 2 Ma have been estimated. On a regional scale, the uplift rates vary from 0.2 mm/y to 1.3 mm/y, with average values of 0.6 mm/y in the Campania-Lucania Apennine and about 1 mm/y at the Calabria-Lucania border (Schiattarella et al., 2006). In order to relate the different erosion processes to tectonic mobility of the axial zone of the chain, a geomorphic quantitative analysis has been carried out and the eroded volumes of rocks forming both the Mesozoic-Cenozoic bedrock and the Pliocene to Quaternary clastic deposits have been calculated, using cartographic methods and also converting the fluvial turbid transport data as evaluated by geomorphic parameters. The annual average erosion rate is about 0.2 mm/y. A summary of the erosion rates calculated for the single study areas is reported in Tab. I and geographically represented in Fig. 1. The comparison between uplift and erosion rates suggests in a first analysis that the fluvial erosion did not match the tectonic uplift of the axial zone of the southern Apennines, which therefore could result a non-steady system, strongly perturbed by other erosion phenomena. In such a framework, mass movements have to be necessarily activated to drop the disequilibrium triggered by rates differential. Nevertheless, uplift rates related to a smaller time-span, and in particular referred to the late Pleistocene – Holocene interval, revealed values of 0.2-0.3 mm/y, better fitting with the erosion rates calculated in the 473 GeoMod2008 Firenze, 22-24 September 2008 whole study area (indeed, a significant difference between uplift and erosion rates seems to persist during recent times in the Sinni Valley). This could testify a steady-state of the chain, in which landslide activity has been concentrated in particular periods of the recent geological past essentially because of climatic factors and is triggered during historical times also by seismic induction. On the other hand, the erosion rates calculated for the single catchment basins suggest that – if compared to the uplift rates from the adjacent ranges (average value of 0.6-0.8 mm/y) – the south-Apennines chain did not yet reach a condition of steady state, showing the features of a transient landscape. Such a conflicting hypothesis may be taken into account if we are inclined to admit that not all the sectors of the chain – in a fragmented tectonic patchwork like the southern Apennines – could stay in conditions of steady state during the same time-span. REFERENCES Aldega L., Corrado S., Di Leo P., Giampaolo C., Invernizzi C., Martino C., Mazzoli S., Schiattarella M., Zattin M. (2005) - The southern Apennines case history: thermal constraints and reconstruction of tectonic and sedimentary burials. Atti Ticin. Sc. Terra, Serie Spec., 10, 45-53. Amato A. (2000) - Estimating Pleistocene tectonic uplift rates in the Southeastern Apennines (Italy) from erosional land surfaces and marine terraces. In: Slaymaker, O. (Ed.), Geomorphology, Human Activity and Global Environmental Change. Wiley & Sons, New York, pp. 67-87. Ascione A., Cinque A., Tozzi M. (1992) - La valle del Tanagro (Campania): una depressione strutturale ad evoluzione complessa. Studi Geologici Camerti, vol. spec. 1992/1, 209-219. Bartolini C., D’Agostino N., Dramis F. (2003) – Topography, exhumation, and drainage network evolution of the Apennines. Episodes, 26, 212-216. Basili R., Galadini F., Messina P. (1999) – The application of palaeolandsurface analysis to the study of recent tectonics in central Italy. In: Smith B.J., Whalley W.B. & Warke P.A., Eds., Uplift, Erosion and Stability: Perspectives on Long-term Landscape Development. Geological Society, London, Spec. Publ., 162, 109-117. Boenzi F., Capolongo D., Cecaro G., D'Andrea E., Giano S.I., Lazzari M., Schiattarella M. (2004) - Evoluzione geomorfologica polifasica e tassi di sollevamento del bordo sud-occidentale dell'alta Val d'Agri (Appennino meridionale). Boll. Soc. Geol. It., 123, 357-372. Burbank D.W. & Anderson R.S. (2001) – Tectonic Geomorphology. pp 274 Blackwell Science. Capolongo D., Cecaro G., Giano S.I., Lazzari M., Schiattarella M. (2005) - Structural control on drainage network of the south-western side of the Agri River upper valley (southern Apennines, Italy). Geogr. Fis. Dinam. Quat., 28, 169180. Capolongo D., Refice A., Mankelow J. (2002) - Evaluating earthquake-triggered landslide hazards at basin scale. The example of the upper Sele River valley. Survey in Geophysics, 23, 595-625. Di Leo P. (2003) - Use of clay mineralogy in reconstructing geological processes: thermal constraints from clay minerals: Atti Ticin. Sc. Terra, Serie Spec., 9, 55-68. Di Leo P., Schiattarella M., Cuadros J., Cullers R. (2005) - Clay mineralogy, geochemistry and structural setting of the ophiolite-bearing units from southern Italy: a multidisciplinary approach to assess tectonic history and exhumation modalities. Atti Ticin. Sc. Terra, Serie Spec., 10, 87-93. Di Niro, A., Giano, S.I., Santangelo, N. (1992) - Primi dati sull’evoluzione geomorfologia e sedimentaria del bacino dell’alta Val d’Agri (Basilicata). Studi Geol. Camerti, vol. spec. 1992/1, 257-263. Giannandrea P., La Volpe L., Principe C., Schiattarella M. (2006) - Unità stratigrafiche a limiti inconformi e storia evolutiva del vulcano medio-pleistocenico di Monte Vulture (Appennino meridionale, Italia). Boll. Soc. Geol. It., 125, 67-92 (con carta allegata in scala 1:25.000). Giano S.I. & Martino C. (2003) - Assetto morfotettonico e morfostratigrafico di alcuni depositi continentali pleistocenici del bacino del Pergola-Melandro (Appennino lucano). Il Quaternario, 16, 289-297. Giano S.I., Maschio L., Alessio M., Ferranti L., Improta S., Schiattarella M. (2000) - Radiocarbon dating of active faulting in the Agri high valley, southern Italy. Journal of Geodynamics, 29, 371-386. Gioia D. & Schiattarella M. (2006) - Caratteri morfotettonici dell’area del Valico di Prestieri e dei Monti di Lauria (Appennino meridionale). Il Quaternario, 19, 129-142 Invernizzi C., Bigazzi G., Corrado S., Di Leo P., Schiattarella M., Zattin M. (2008) - New thermobaric constraints on the exhumation history of the Liguride accretionary wedge (southern Italy). Ofioliti, in stampa. Keller, E.A., Pinter, N., (1996) - Active Tectonics: Earthquake, Uplift, and Landscape. Prentice Hall, Upper Saddle River, NJ. pp. 338. 474 GeoMod2008 Firenze, 22-24 September 2008 Kirby E. & Whipple K. (2001) - Quantifying differential rock-uplift rates via stream profile analysis. Geology, 29, 415-418. Martino C. & Schiattarella M. (2006) - Aspetti morfotettonici dell’evoluzione geomorfologica della valle del Melandro (Appennino campano-lucano). Il Quaternario, 19, 119-128. Martino C. & Schiattarella M. (2008) - Relationships among climate, uplift and palaeo-landslides generation in the Melandro River basin, southern Apennines, Italy. Physics and Chemistry of the Earth, in stampa. Pazzaglia F.J. & Brandon M.T. (2001) - A fluvial record of long-term steady-state uplift and erosion across the Cascadia forearc high, Western Washington State. Am. Journ. of Sc., 301, 385-431. Schiattarella M., Beneduce P., Di Leo P., Giano S.I., Giannandrea P., Principe C. (2005) - Assetto strutturale ed evoluzione morfotettonica quaternaria del vulcano del Monte Vulture (Appennino Lucano). Boll. Soc. Geol. It., 124, 543-562. Schiattarella M., Beneduce P., Pascale S. (2004) - Comparazione tra i tassi di erosione e sollevamento dell’Appennino lucano: l’esempio della Fiumara di Tito e Picerno. Boll. A.I.C., 121-122, 367-385. Schiattarella M., Di Leo P., Beneduce P., Giano S.I. (2003) – Quaternary uplift vs tectonic loading: a case-study from the Lucanian Apennine, southern Italy. Quaternary International, 101-102, 239-251. Schiattarella M., Di Leo P., Beneduce P., Giano S.I., Martino C. (2006) – Tectonically driven exhumation of a young orogen: an example from southern Apennines, Italy. In: Willett, S.D., Hovius, N., Brandon, M.T., and Fisher, D., eds., Tectonics, climate, and landscape evolution, Geological Society of America Special Paper 398, Penrose Conference Series, 371–385. Schiattarella M., Torrente M.M. & Russo F. (1994) - Analisi strutturale ed osservazioni morfostratigrafiche nel bacino del Mercure (Confine Calabro-Lucano). Il Quaternario, 7, 613-626. Westaway R. (1993) - Quaternary Uplift of Southern Italy: Journ. Geophys. Res., 98, 21741-21772. Willett S.D. & Brandon M.T. (2002) - On steady states in mountain belts: Geology, 30, 175-178. DISCRETE ELEMENT SIMULATION OF ROCK-AND-SOIL AVALANCHES: 1. THEORY AND COMPUTATION A. Taboada, N. Estrada Montpellier - INSU - CNRS, cc. 60, Université Montpellier 2, Place E. Bataillon, 34095 Montpellier (France) ([email protected]) Summary We present a Contact Dynamics discrete element model for simulating initiation and propagation of rock avalanches, integrating the hillslope geometry, the Mohr-Coulomb rock behavior, the pore pressure before avalanche triggering, and the avalanche trigger. Avalanche propagation is modeled as a dense granular flow of dry frictional particles. Based on granular physics and shear experiments, we review some of the theories for the unexpectedly long runout of rock avalanches. Different causes are evoked, according to the strength (strong or weak) of the slip surface relative to the bulk. The mechanical fluidization and the acoustic fluidization theories state that agitation of rock particles reduces frictional strength, increasing runout. Conversely, granular mechanics proves that, as shear strain rate increases, granular material becomes more agitated, more dissipative, and more resistant. Another theory states that dynamic fragmentation of clasts creates an isotropic pressure that dilates the rock mass, driving longer runout. In contrast, granular mechanics suggests that fragmentation induces a stress drop, a contraction of granular material, and energy dissipation through inelastic collisions. Long runout is enhanced for column-like rock masses collapsing from steep hillslopes. Finally, long runout may also be linked to thermal weakening mechanisms along the slip surface (e.g., thermal pressurization, shear melting, and others), which may lower drastically the shear strength. The model is illustrated by a hypothetical example of rainfall-triggered avalanche mobilizing shallow monoclinal layers. Several phases are identified, including slope failure, avalanche triggering resulting from slip weakening, and avalanche propagation in which rocks are folded and sheared. 475
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