Cathedral Peak Granodiorite
The Cathedral Peak Granodiorite (CPG) was named after its type locality, Cathedral Peak in Yosemite National Park, California. The granodiorite forms part of the Tuolumne Intrusive Suite (Tuolumne Batholith), one of the four major intrusive suites within the Sierra Nevada. It has been assigned radiometric ages between 88 and 87 million years and therefore reached its cooling stage in the Coniacian (Upper Cretaceous).
The Cathedral Peak Granodiorite forms part of the central eastern Sierra Nevada in California. It is exposed in glaciated outcrops from the upper Yosemite Valley into the high Sierra Divide. It covers large parts of Mariposa County and Tuolumne County and also touches Madera County and Mono County. At its northern end it includes Tower Peak and Matterhorn Peak, at 12,264 feet (3743 m) its highest elevation. In its southwestern section rises the Cathedral Range with the 10,911 feet Cathedral Peak (3326 m) above Tuolumne Meadows. California State Route 120 traverses the granodiorite in its southern half. Due to the block-faulting and tilting of the Sierra Nevada to the west its drainage system is oriented to the west and follows mainly southwesterly courses, especially in the northern section.
The shape of the intrusion is a drawn-out rectangle or ellipse oriented roughly in the NNW-SSE-direction. Its long dimension measures about 30 miles (48 km), its width hardly reaches 12 miles (19 km) at the northern end. The surface area amounts to about 230 square miles (600 km2), roughly half of the total area of the Tuolumne Intrusive Suite. The granodiorite completely engulfes the Johnson Granite Porphyry in the south. It is surrounded in the southeast, southwest and northwest by the Half Dome Granodiorite. In its central belt region it touches the Kuna Crest Granodiorite. In the north and northeast it comes into contact with weakly metamorphosed country rocks, mainly Paleozoic and Jurassic metavolcanics and metasediments.
The Cathedral Peak Granodiorite is the third and most important intrusive pulse of the Tuolumne Intrusive Suite. The intrusions of this magmatic suite were spaced out over quite a long period. They started in the Turonian at about 93.5 million years BP and lasted right to the beginning of the Santonian at 85.4 million years BP. Radiometric dating of the cooling ages of the Cathedral Peak Granodiorite yielded 88.1 ± 0.2 down to 87.0 ± 0.7 million years BP, i.e. Coniacian.
The Tuolumne Intrusive Suite is accompanied by other major intrusive complexes in the Sierra Nevada: the John Muir and Mount Whitney intrusive suites, both further south and the Sonora Plutonic Complex to the north. The surface area of these four complexes surpasses 970 square miles (2,500 km2).
The Tuolumne Intrusive Suite was constructed over a long time span of 8.1 million years by the following magmatic pulses (ordered by increasing age):
- Johnson Granite Porphyry
- Cathedral Peak Granodiorite
- Half Dome Granodiorite, further subdivided into a porphyritic and an equigranular facies
- Kuna Crest Granodiorite – quartz diorite and granodiorite
This magmatic sequence shows the following geochronological and geochemical trends:
- decreasing age from the margin to the center, with the marginal Kuna Crest Granodiorte being the oldest magmatic pulse and the central Johnson Granite Porphyry the youngest.
- an increase in silica and alkali contents from rim to center, the composition of the rocks changing from mafic/intermediate to more felsic compositions.
- an increase in rubidium contents from rim to center.
- a steady decrease in Al2O3, TiO2, FeO, MgO and CaO contents.
- a decrease in barium, strontium and light rare earth elements such as scandium.
The immediately apparent trait of the grey-white Cathedral Peak Granodiorite is its porphyritic habit with very large megacrysts of alkali feldspar commonly reaching 10, occasionally even 20 centimeters. The grain size of the groundmass stays in the 5 millimeter range.
The Cathedral Peak Granodiorite is modally composed of the following minerals:
- plagioclase – 47.5 volume percent. Present as subhedral to euhedral, tabular oligoclase with An27–29. Shows normal zoning with calcium-rich cores and sodium-rich rims. Exhibits simple carlsbad and albite twinning. Grain size varies between 1 and 15 millimeters. Can be cataclastically broken and infiltrated/replaced by microcline in shear zone.
- alkali feldspar – 20.9 volume percent. Present as blocky, perthitic orthoclase with Or88. Phenocrysts with grain sizes up to 20 centimeters in length, normal range up to 10 centimeters, 2 centimeters wide. Exhibit carlsbad twinning. Grain size and abundance of the phenocrysts decreases inwards towards the Johnson Granite Porphyry. The megacrysts engulf ( poikilitically enclose) other smaller minerals such as biotite, hornblende, plagioclase and alkali feldspar due to a rapid growth rate. Cracks have been filled with opaque minerals, bigger fractures are in-filled with groundmass material. The surface is fractured with irregular edges. Some grains show signs of secondary alteration to clay minerals. Alkali feldspar occurs interstitially also in the fine- to medium-grained groundmass.
- quartz – 25.9 volume percent. Equidimensional subhedral crystals of medium grain size (10 millimeter).
- biotite – 3.5 volume percent. Equidimensional and subhedral. Main mafic constituent. Shows strong brown pleochroism, occasionally with pleochroic halos.
- hornblende – 0.8 volume percent.
- apatite – 0.3 volume percent. Prismatic crystals.
- titanite. Irregular fine-grained crystals. Can appear in euhedral habit.
- opaque ore minerals such as ilmenite and magnetite – 0.6 volume percent.
- accessories such as allanite and zircon.
- myrmekite in shear zone.
|Bateman & Chappell||Average
Burgess & Miller
|Bateman & Chappell||Average||Trace elements
Burgess & Miller
|SiO2||69,60||70,29 (67,0–72,0)||Q||24,52||25,58||Pb||17,5 (15–20)|
|TiO2||0,38||0,41 (0,3–0,6)||Or||21,67||20,64||Cu||4,9 (3,2 – 6,9)|
|Al2O3||15,34||15,37 (15,0–16,5)||Ab||36,79||35,81||Ni||3,0 (0,7 – 6)|
|MnO||0,06||0,06 (0,5–0,8)||Hy||1,63||1,82||Zr||135,9 (82–165)|
|MgO||0,70||0,72 (0,6–0,9)||Mt||1,87||2,01||Y||8,3 (4,9 – 11)|
|CaO||2,68||2,82 (2,2–3,2)||Il||0,73||0,77||Sr||633,2 (487–758)|
|Na2O||4,31||4,24 (4,0–4,5)||Ap||0,32||0,36||Ba||748,0 (410–1182)|
|K2O||3,64||3,50 (2,8–4,2)||Rb||132,5 (114–166)|
|P2O5||0,14||0,16 (0,12–0,20)||Nb||7,8 (4,9 – 10)|
|Mg#||0,55||0,54||Sc||3,6 (1,7 – 4,5)|
Compared with an average granodiorite the Cathedral Peak Granodiorite has a much higher silica content, shows elevated alkali values and is therefore a member of the shoshonitic high-K series. The rock is metaluminous, rich in sodium and belongs to the intrusive, mantle source-derived I-type granitoids. It is a typical calc-alkaline rock from the root zone of an ancient volcanic arc and associated with a subduction-type environment.
The trace elements demonstrate an enrichment in barium and strontium, nickel and chromium on the other hand have very low concentrations. The light rare earth elements LREE are also elevated but without a europium anomaly.
|K-feldspar||20%||(15% megacryst, 5% interstitial) %|
The Cathedral Peak Granodiorite reveals the following structures of magmatic origin:
- Layering underlined by the accumulation of hornblende and biotite. Two
magmatic foliations can be observed:
- a major NNW-SSE-striking, steeply dipping foliation bearing a steep lineation.
- a secondary ESE-WNW-striking foliation.
- Schlieren generally strike NNW-SSE (N 157 – with local deviations up to 50 °) and show a fairly steep dip of about 60 ° to the ENE.
- Ladder dikes represent tubular, locally confined magmatic upwellings. These structures are sometimes displaced by later magmatic motions.
- Microgranitoid inclusions are similar in their mineralogy to the host rock, yet contain a higher percentage of mafic minerals like hornblende and biotite. Phenocrysts are plagioclase and hornblende with a grain size of 5 to 8 millimeter. The inclusions are sometimes surrounded by up to 3 centimeter wide felsic rims. Their mode of occurrence is singular or in clusters without a preferred direction.
- Aplites form one to three centimeter wide dykes. Their mineralogy is fine-grained and homogeneous. They cut through all other structures with mostly sharp contacts. Larger dykes can host pegmatitic cores of quartz, plagioclase and alkali feldspar. Smaller splaying dyke terminations can end in a diffuse fashion in the host rock.
- Displacements in the magmatic state which can affect schlieren, ladder dykes and also the homogeneous granodiorite. They are later healed by aplitic material and concentrations of alkali feldspar. Displacements in schlieren are flat-lying, obliquely sinistral and show top to the WSW motion.
- on magmatic plagioclases
- on groundmass minerals like quartz
- along the edges of microcline phenocrysts
Structures that strongly hint at later-stage metasomatic changes are:
- substitution of primary plagioclase by microcline
Taken together all these structural phenomena reveal a very complex evolution of the Cathedral Peak Granodiorite showing the succession of magmatic, tectonic and metasomatic stages – and most likely their occasional synergy and interdependence.
Originally petrologists favoured a single magma chamber model for the genesis of the Tuolumne Intrusive Suite which underwent fractional crystallization and successively produced the different rock types like the Cathedral Peak Granodiorite. This somewhat simplistic model is now being questioned as underlined by the following facts:
- the extremely long activity of this magma chamber protracted over 8.1 million years. 
- inconsistencies in the distribution of the trace elements and in the initial isotope ratios of strontium and neodymium. 
Isotope ratios favour the mixing of two magmas, one with mantle affinities and another one with more felsic compositions approaching the Johnson Granite Porphyry in composition.
Feldspars, hornblende, biotite and magnetite often show unmixing in the lower temperature subsolidus region.
The Cathedral Peak Granodiorite cannot always be clearly distinguished from the porphyritic Half Dome Granodiorite in the field, at some places it shows gradual merging over about a hundred meters and apophyses are observed branching into the Half Dome rocks. The geochemical parameters of the two granodiorites also overlap, differences are mainly textural. They form a continuum and therefore cannot be clearly separated as two distinctive intrusive pulses.  The contact relationships with the Johnson Granite Porphyry are on the other hand sharp. 
The origin of the microcline in shear zones poses another problem. M.D. Higgins favours the possibility of recrystallization based on Ostwald ripening via metasomatic fluids.  L.G. Collins supports a metasomatic subsolidus growth ( potassium- and silica-metasomatism) that has been initiated by ongoing tectonic cataclasis.  To be fully effective this process is dependent on the cataclastic breaking-up of the original crystals as realized in a ductile shear zone along the eastern edge of the Cathedral Peak Granodiorite (Gem Lake Shear Zone).
- El Capitan Granite
- Geology of the Yosemite area
- Half Dome Granodiorite
- Kuna Crest Granodiorite
- Sentinel granodiorite
- Bateman, P.C. & Chappell, B.W. (1979). Crystallization, fractionation and solidification of the Tuolumne intrusive series. Yosemite National Park, California. Geological Society of America Bulletin, 90: 465–482
- Burgess, S., and Miller, J., (2008) Construction, solidiﬁcation and internal differentiation of a large felsic arc pluton: Cathedral Peak granodiorite, Sierra Nevada Batholith, in Annen, C., and Zellmer, G. F., eds., Dynamics of crustal magma transfer, storage and differentiation: London, Geological Society, p. 203-234.
- F. Solgadi, E. W. Sawyer, Formation of Igneous Layering in Granodiorite by Gravity Flow: a Field, Microstructure and Geochemical Study of the Tuolumne Intrusive Suite at Sawmill Canyon, California, Journal of Petrology, Volume 49, Issue 11, November 2008, Pages 2009–2042
- Coleman, D.S., Gray, W. & Glazner, A.F. (2004). Rethinking the emplacement and evolution of zoned plutons: geochronologic evidence for incremental assembly of the Tuolumne Intrusive Suite, California. Geology, 32, 433–436.
- Kistler, R.W., Chappell, B.W., Peck, D.L. & Bateman, P.C. (1986). Isotopic variation in the Tuolumne intrusive suite, central Sierra Nevada, California. Contributions to Mineralogy and Petrology, 94, 205–220.
- Gray, W., Glazner, A.F., Coleman, D.S. & Bartley, J.M. (2008). Long-term geochemical variability of the Late Cretaceous Tuolumne Intrusive Suite, central Sierra Nevada, California. In: Annen, C. & Zellmer, G.F. Dynamics of Crustal Magma Transfer, Storage and Differentiation. Geological Society Special Publication 304.
- Titus, S.J., Clark, R. & Tikoff, B. (2005). Geologic and geophysical investigation of two fine-grained granites, Sierra Nevada Batholith, California; evidence for structural controls on emplacement and volcanism. Geological Society of America Bulletin, 117, 1256–1271.
- Higgins, M. D., 1999, Origin of megacrysts in granitoids by textural coarsening: A Crystal Size Distribution (CSD) Study of Microcline in the Cathedral Peak Granodiorite, Sierra Nevada, California., in Fernandez, C., and Castro, A., eds., Understanding Granites: Integrating Modern and Classical Techniques. Special Publication 158: London, Geological Society of London, p. 207-219.
- Collins, L.G. and Collins, B.J. (2002). K-metasomatism of plagioclase to produce microcline megacrysts in a shear zone of the Cathedral Peak granodiorite, Sierra Nevada, California, USA