adding test case

Author: PrajaktaPMohite

cookbooks/continental_compression_with_imposed_faults/continental_compression_with_imposed_faults.prm

@@ -8,6 +8,7 @@
 # Altai, which has experienced low magnitudes of compressional deformation
 # since the onset of the India-Asia collision and contains evidence for
 # reactivation of normal faults formed during prior phases of deformation
+# (Howard et al., 2003, https://doi.org/10.1046/j.1365-2117.2003.00198.x).
 # The faults locations and properties are defined using the Geodynamic
 # World Builder.
 
@@ -294,7 +295,8 @@ subsection Material model
     set Thermal conductivities        = 2.5
     set Heat capacities               = 750.
 
-    #The densities below are set to achieve the following densities at the reference temperature (273 K):
+    # The densities below are set to achieve the following densities at the reference temperature (273 K):
+    # upper_crust - 2800, lower_crust - 2900, background/mantle_lithosphere/asthenosphere - 3300.
     set Densities                     = background: 3216.374269005848, \
                                         crust_upper: 2729.044834307992, \
                                         crust_lower: 2826.510721247563, \

cookbooks/continental_compression_with_imposed_faults/continental_compression_with_imposed_faults.wb

@@ -1,14 +1,3 @@
-// Define the location of the first fault, which starts at x = 200 km on the model surface and then
-// dips at 60 degrees toward the left side side of the model. The length of the fault is 200 km,
-// but it is location is restricted to the uppermost 100 km through the max depth parameter.
-// The fault width is 5 km and the temperature is constant at 273 K, but significantly 
-// the initial temperature in the ASPECT model is not derived from the WB file. Assignment
-// of values to specific compositional fields follows the order the are listed in the ASPECT
-// PRM files, which is plastic_strain (0), noninitial_plastic_strain (1), viscous_strain (2), 
-// crust_upper (3), crust_lower (4), mantle_lithosphere (5), and asthenosphere (6). Here,
-// values of 1.5 in the fault center are assigned to the plastic and viscous strain fields, which
-// smoothly transition to 0.5 at the fault edge. The remaining faults defined below follow the 
-// same conventions as described above.
 {
     "version":"1.0",
     "cross section":[[0,4e5],[4.2e5,4e5]],
@@ -17,10 +6,10 @@
     {
             "model":"fault","name":"fault1","dip point":[0e5,2e5],    
             "min depth":0, "max depth":1e5,
-            "coordinates":[[2.0e5,8e5],[2.0e5,0]],
+            "coordinates":[[2.5e5,8e5],[2.5e5,0]],
             "segments":
             [
-                {"length":2e5,"thickness":[5000],"angle":[60]}
+                {"length":2e5,"thickness":[5000],"angle":[80]}
             ],
             "temperature models":[{"model":"uniform","temperature":273}],
             "composition models":
@@ -34,7 +23,7 @@
             "coordinates":[[2.25e5,8e5],[2.25e5,0]],
             "segments":
             [
-                {"length":2e5,"thickness":[5000],"angle":[60]}
+                {"length":2e5,"thickness":[5000],"angle":[70]}
             ],
             "temperature models":[{"model":"uniform","temperature":273}],
             "composition models":
@@ -45,10 +34,24 @@
         }, {
             "model":"fault","name":"fault3","dip point":[0e5,2e5],    
             "min depth":0, "max depth":1e5,
-            "coordinates":[[2.5e5,8e5],[2.5e5,0]],
+            "coordinates":[[1.4e5,8e5],[1.4e5,0]],
+            "segments":
+            [
+                {"length":2e5,"thickness":[5000],"angle":[110]}
+            ],
+            "temperature models":[{"model":"uniform","temperature":273}],
+            "composition models":
+            [
+                {"model":"smooth", "compositions":[0,2], "operation":"add", "side distance fault center":2500, "center fractions":[1.5,1.5],"side fractions":[0.5,0.5]}
+            ]
+                
+        }, {
+            "model":"fault","name":"fault4","dip point":[0e5,2e5],    
+            "min depth":0, "max depth":1e5,
+            "coordinates":[[1.85e5,8e5],[1.85e5,0]],
             "segments":
             [
-                {"length":2e5,"thickness":[5000],"angle":[60]}
+                {"length":2e5,"thickness":[5000],"angle":[90]}
             ],
             "temperature models":[{"model":"uniform","temperature":273}],
             "composition models":

cookbooks/continental_compression_with_imposed_faults/doc/continental_compression_with_imposed_faults.md

@@ -26,7 +26,8 @@ Following Howard et al. (2003), the configuration of these faults is motivated b
 ```{figure-md} fig:initial_plastic_and_viscous_strain_and_density
 <img src="initial_plastic_and_viscous_strain_and_density.svg" style="width:50.0%" />
 
- Initial plastic (left), viscous (right) strain highlighting the location of defined fault zones and randomized strain across a broader region in the upper 100 km and density (bottom) across model region.
+ Initial plastic (top left), viscous (top right) strain and density (bottom) highlighting the location of defined fault zones and randomized strain across a broader region in the upper 100 km.
+ The density plot contains temperature contours at intervals of 200 K, beginning at 373 K and ending at 1573 K (LAB temperature).
 ```
 
 The position, dip angle and direction, thickness (5 km), and composition (plastic and viscous strain) of each fault are defined with the [Geodynamic World Builder fault feature](https://geodynamicworldbuilder.github.io), which is illustrated below for a single fault.
@@ -39,7 +40,7 @@ The position, dip angle and direction, thickness (5 km), and composition (plasti
 ```{figure-md} fig:strain_rate_and_density_0_myr
 <img src="strain_rate_and_density_0_myr.svg" style="width:50.0%" />
 
- Strain rate (left) and density distribution (right) at 0 Myr in the upper 100 km from x = 100 to 300 km. Strain localizes in the upper crust along pre-defined fault zones, while density increases with depth, reflecting the compositional and thermal stratification of the lithosphere.
+  Strain rate (left) and density distribution (right) at 0 Myr in the upper 100 km from x = 100 to 300 km. Strain localizes in the upper crust along pre-defined fault zones, while density increases with depth, reflecting the compositional and thermal stratification of the lithosphere.
 ```
 
 ```{figure-md} fig:strain_rate_and_density_35_myr
@@ -51,3 +52,5 @@ The position, dip angle and direction, thickness (5 km), and composition (plasti
 Deformation preferentially localizes along the two pre-existing shear zones forming a grabben-like geometry ({numref}`fig:strain_rate_and_density_0_myr`), which reflects their optimal orientation and position within the model domain to accommodate the imposed convergence. After 35 Myr of convergence ({numref}`fig:strain_rate_and_density_35_myr`) deformation remains strongly localized along these faults,  with crustal shortening and thickening occurring between them forming approximately symmetric orogenic wedge. Some degree of asymmetry develops on the right side of the wedge, where the fault farthest to the right remains active in the upper crust and connects to the fault bounding the wedge near the brittle-ductile transition zone.
 
 Given the nonlinearity of the rheology and governing equations, minor variations in fault strength, geometry, lithospheric structure, and boundary velocities may lead to significant variations in the spatiotemporal evolution of deformation. This cookbook provides a flexible framework for exploring the effects of these parameters, and application to hypothesis-driven questions such as fault reactivation, inversion of rift basins, or the partitioning of strain in complex orogens.
+
+These results demonstrate the potential key role of pre-existing faults in guiding the evolution of lithospheric deformation. However, given the nonlinearity of the rheology and governing equations, minor variations in fault strength, geometry, lithospheric structure, and boundary velocities may lead to significant variations in the spatiotemporal evolution of deformation. Similarly, changing the numerical resolution is likely to also affect the results, as the brittle shear band width by introduced by the plastic damper (1e21 Pa s) is still likely not fully resolved at the maximum resolution of 1e21 Pa s. Furthermore, varying degrees of minor variations in the model results will likely occur if a stricter nonlinear solver tolerance is selected. This cookbook provides a flexible framework for exploring the effects of these parameters, and application to hypothesis-driven questions such as fault reactivation, inversion of rift basins, or the partitioning of strain in complex orogens.