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Table 3. Parameters Used for Flexural Modeling Shown in Figure 9c

Table 3 Parameters Used for Flexural Modeling Shown in Figure 9c

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Figure 3. The geometry of the Po Plain basins. Transition from the Messinian-Plio-Quaternary wedge- shaped basin to the Pleistocene-Holocene sag basin (dotted patterns) began in the west (up on the figure) and progressed to the east (down on the figure). (a) From Bertotti et al. [2006]; (b) from Bello and Fantoni [2002]; (c) from Picotti et al. [2007]; (d) our data (see Figure 8).
Figure 3. The geometry of the Po Plain basins. Transition from the Messinian-Plio-Quaternary wedge- shaped basin to the Pleistocene-Holocene sag basin (dotted patterns) began in the west (up on the figure) and progressed to the east (down on the figure). (a) From Bertotti et al. [2006]; (b) from Bello and Fantoni [2002]; (c) from Picotti et al. [2007]; (d) our data (see Figure 8).
*AEI, Emiliano-Romagnolo Inferiore Synthem; AES, Emiliano-Romagnolo Superiore Synthem, IMO, Imola Sand Formation (Sabbie Gialle) [Martelli e al., 2008]. Di Dio [1998]. “Marine oxygen isotope stage. “Average calibrated '*C ages from multiple dates reported. Table 1. Reno Terrace and Po Plain Stratigraphy and Ages
*AEI, Emiliano-Romagnolo Inferiore Synthem; AES, Emiliano-Romagnolo Superiore Synthem, IMO, Imola Sand Formation (Sabbie Gialle) [Martelli e al., 2008]. Di Dio [1998]. “Marine oxygen isotope stage. “Average calibrated '*C ages from multiple dates reported. Table 1. Reno Terrace and Po Plain Stratigraphy and Ages
Figure 5. Map of terraces in the lower Reno valley between Sasso Marconi (south) and Casalecchio di Reno (north). Yellow points are elevations in meters. Topography in the black outline is used for the swath profile of Figure 6a. The red line is the valley plane profile to which all longitudinal profile data are projected in Figure 7. Terrace stratigraphy is illustrated in Figure 6 and Table 1.
Figure 5. Map of terraces in the lower Reno valley between Sasso Marconi (south) and Casalecchio di Reno (north). Yellow points are elevations in meters. Topography in the black outline is used for the swath profile of Figure 6a. The red line is the valley plane profile to which all longitudinal profile data are projected in Figure 7. Terrace stratigraphy is illustrated in Figure 6 and Table 1.
Figure 6. (a) Topographic swath profile of the lower Reno valley between latitudes 44.48 and 44.45 with terrace locations and inferred ages. (b) Composite cross-section of the inner Reno valley showing the late Pleistocene terraces and numeric ages. Red: alluvium; yellow: colluvium. Inset photographs of soils F, E, C, and B illustrate changes in relative weathering characteristics of the terrace deposits and are described in detail in Epps et al. [2008].
Figure 6. (a) Topographic swath profile of the lower Reno valley between latitudes 44.48 and 44.45 with terrace locations and inferred ages. (b) Composite cross-section of the inner Reno valley showing the late Pleistocene terraces and numeric ages. Red: alluvium; yellow: colluvium. Inset photographs of soils F, E, C, and B illustrate changes in relative weathering characteristics of the terrace deposits and are described in detail in Epps et al. [2008].
Figure 7. Projection and correlation of Reno terrace data across the mountain front to subsurfac alluvial stratigraphy in the Po Plain. Numbers on inset graphs are incision or subsidence rates it millimeters per year. OIS, oxygen isotope stage, is used for stratigraphic correlation of deposits anc terraces for which there exists no independent numeric ages. Age of IMO (Sabbie Gialle Qsg cosmogenic; 0.9 + 0.4 Ma) is from Cyr and Granger [2008].
Figure 7. Projection and correlation of Reno terrace data across the mountain front to subsurfac alluvial stratigraphy in the Po Plain. Numbers on inset graphs are incision or subsidence rates it millimeters per year. OIS, oxygen isotope stage, is used for stratigraphic correlation of deposits anc terraces for which there exists no independent numeric ages. Age of IMO (Sabbie Gialle Qsg cosmogenic; 0.9 + 0.4 Ma) is from Cyr and Granger [2008].
Figure 8. Geological cross-sections for (a) modern and (b) restored for the early Pleistocene. See Figure 4 for cross-section locations. The Po Plain portion comes from a reinterpretation of the seismic line C of Pieri [1987]; the Apennines transect comes from a reinterpretation of the cross-section IV of Martelli ana Rogledi [1998]. The red lines in Figure 8a are active faults. The line denoting a fault in and out of the plane of the cross-section represents the Monghidoro earthquake [M 5.3, 2003; Piccinini et al., 2006]. The deep ramp structure is inferred from modeling results of observed deformation and river incision (see Figure 9).
Figure 8. Geological cross-sections for (a) modern and (b) restored for the early Pleistocene. See Figure 4 for cross-section locations. The Po Plain portion comes from a reinterpretation of the seismic line C of Pieri [1987]; the Apennines transect comes from a reinterpretation of the cross-section IV of Martelli ana Rogledi [1998]. The red lines in Figure 8a are active faults. The line denoting a fault in and out of the plane of the cross-section represents the Monghidoro earthquake [M 5.3, 2003; Piccinini et al., 2006]. The deep ramp structure is inferred from modeling results of observed deformation and river incision (see Figure 9).
Figure 9. Results of trishear modeling inverting for the depth, dip, and slip rate on a buried thrust. (a) Best fit results to the IMO stratigraphic horizon (thick gray line) are a fault tip at a depth of 16 km, with a ramp angle of 55°, a slip to propagation ratio of 1.5, a trishear angle of 30°, and total slip of 2 km. (b) Predicted strain at the surface given the trishear parameters in Figure 9a. Note the correct prediction of the location of the observed main normal faults. (c, inset) Deformation across the mountain front con- sidering flexure of regionally compensated vertical loads applied to an elastic plate of finite thickness and an erosion rate of 0.8 mm/year. Labeled lines correspond to different modeled elastic thicknesses (5— 15 km). Qt0-IMO, real deformation of the terrace-Sabbie Gialle stratigraphic horizon; cbe, constant model boundary erosion; cbl, constant model boundary loading. See Table 3 for flexural parameters used in the modeling.
Figure 9. Results of trishear modeling inverting for the depth, dip, and slip rate on a buried thrust. (a) Best fit results to the IMO stratigraphic horizon (thick gray line) are a fault tip at a depth of 16 km, with a ramp angle of 55°, a slip to propagation ratio of 1.5, a trishear angle of 30°, and total slip of 2 km. (b) Predicted strain at the surface given the trishear parameters in Figure 9a. Note the correct prediction of the location of the observed main normal faults. (c, inset) Deformation across the mountain front con- sidering flexure of regionally compensated vertical loads applied to an elastic plate of finite thickness and an erosion rate of 0.8 mm/year. Labeled lines correspond to different modeled elastic thicknesses (5— 15 km). Qt0-IMO, real deformation of the terrace-Sabbie Gialle stratigraphic horizon; cbe, constant model boundary erosion; cbl, constant model boundary loading. See Table 3 for flexural parameters used in the modeling.
*Allmendinger [1998], using FaultFold 4.5.4. Highlighted rows = fold half wavelength ~22 km. “Best fit model parameters to field data. Table 2a. Predicted Total Fault Displacement of a Modeled Blind Thrust Fault With a Trishear Geometry Fit, Fixed P/S ratio* = 1 and 800 m of Qt0-IMO Stratigraphic Displacement?
*Allmendinger [1998], using FaultFold 4.5.4. Highlighted rows = fold half wavelength ~22 km. “Best fit model parameters to field data. Table 2a. Predicted Total Fault Displacement of a Modeled Blind Thrust Fault With a Trishear Geometry Fit, Fixed P/S ratio* = 1 and 800 m of Qt0-IMO Stratigraphic Displacement?
Table 2b. Results of Trishear Modeling Solutions Considering Different Propagation-to-Slip Ratios and Fit Only to the Emergent Part of the Fold Defined By the Qt0 Terrace and Outcropping Portion of the IMO Deposits (Partial Fold Wavelength of 12 km) and Stratigraphic Separation of 800 m Across the Bologna Mountain Front *Allmendinger [1998], using FaultFold 4.5.4. Best fit model parameters to field data.
Table 2b. Results of Trishear Modeling Solutions Considering Different Propagation-to-Slip Ratios and Fit Only to the Emergent Part of the Fold Defined By the Qt0 Terrace and Outcropping Portion of the IMO Deposits (Partial Fold Wavelength of 12 km) and Stratigraphic Separation of 800 m Across the Bologna Mountain Front *Allmendinger [1998], using FaultFold 4.5.4. Best fit model parameters to field data.
Figure 11. Active deformation of the northern Apennines in the context of a partially coupled rollback- retreat geodynamic model.
Figure 11. Active deformation of the northern Apennines in the context of a partially coupled rollback- retreat geodynamic model.
Figure 12. A comparison of the major tectonic features of the northern Apennines to the central Alps. (a) Northern Apennines at present; (b) central Alps 19 Ma; (c) northern Apennines 20 My into the future, with continued movement of the mountain front blind thrust fault; (d) central Alps at present, with the Aar Massif splitting the upper crustal orogenic wedge following shortening on a crustal-scale blind thrust. c, crust; ml, mantle lithosphere. Dark lines indicate active faults. Dots indicate proforeland deposits.
Figure 12. A comparison of the major tectonic features of the northern Apennines to the central Alps. (a) Northern Apennines at present; (b) central Alps 19 Ma; (c) northern Apennines 20 My into the future, with continued movement of the mountain front blind thrust fault; (d) central Alps at present, with the Aar Massif splitting the upper crustal orogenic wedge following shortening on a crustal-scale blind thrust. c, crust; ml, mantle lithosphere. Dark lines indicate active faults. Dots indicate proforeland deposits.
Related topics:
GeodesySedimentary BasinsSubduction Zone ProcessesActive Tectonics
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