Top 14 Natural Monuments around Stithians

Breathtaking views. Especially when combined with the blooming heather!

Naturist beach with views.

Pendennis point provides beautiful views of the coast and is only a very short distance from busy Falmouth. The name comes the Cornish Pen (Headland) and Dynas (Castle). Dolphins and Basking Sharks have been spotted here along with more frequent visits from seals. Pendennis Castle began life in the 16th Century as a gun fort and has guarded the entrance to Carrick Roads (Falmouth Estuary) since. It is looked after by English Heritage and open to visitors.

GB: In Cadjack Cove, tectonic features can be seen, such as faults (described in ⑦) and folds, which were formed during the Variscan orogeny as a result of pressure from the south. These folds are formed on different scales and range from a few inches to several hundred feet. In addition, the folds show different openings and curves. Very narrow folds with pointed angles are called kink bands. However, the folds seen in this bay are not the main folds of orogeny but represent folds that are folded in themselves. Another special feature in this bay is the pink to dark red coloring of the rocks. This is caused by iron-rich water that runs down the cliffs. EN: Tectonic phenomena can be seen in Cadjack Cove, such as faults (described in ⑦) and folds, which were formed by pressure from the south during the Variscan Orogeny. These folds are formed at different scales and range from a few centimeters to several meters. The folds also show different openings and curves. Very tight folds with acute angles are called kink bands. However, the folds seen in this bay are not the main folds of the orogeny, but rather represent folds that fold into themselves. Another special feature in this bay is the pink to dark red color of the rocks. This is caused by iron-rich water running down the cliffs.

The 7.3 km long circular route takes you back to a time when Cornwall was covered by sea and then became a Europe-wide mountain range. The sedimentary rocks of this area around Portreath were deposited in a deep marine environment during the Devonian age (ca. 393 - 373 million years): Greywacken: Gray rock with fine to coarse grains (0.3 - 2 mm; 0.01 - 0.08 inch), consisting of quartz, feldspars and fragments of foreign rocks. In some cases, shiny/shimmering components can be seen (mica), the rocks form layers and banks. Siltstones: Light gray rock with fine grains (<0.063 mm; <0.002 inch) that are not visible to the naked eye. Layers can be recognized based on the color difference. Slate: Gray to black, sometimes slightly red to greenish colored rocks with very fine grains (<0.02 mm, <0.001 inch), the rocks appear foliated with very thin layers, often alternating with greywackes. The originally horizontal sedimentary layers of Cornwall were tectonically overprinted around 323 - 299 million years ago during the Variscan orogeny (mountain formation). During this time, the southern major continent Gondwana collided with the northern major continents Laurentia and Baltica as well as smaller continent fragments (terranes) such as Avalonia and Amorica. The orogeny ended approximately 270 million years ago with the formation of the supercontinent Pangea. Due to the pressure from the south, the sedimentary rocks were compressed, folded and internally transformed under increasing temperatures. This is how slates emerged from the original claystones. There are no deposits in the area for the period between the formation of the Devonian rocks until 3 million years ago. During the Ice Age 3 million years ago, the region of modern-day Cornwall lay in a tundra area south of the glaciers that covered the Northern Hemisphere. Periglacial deposits from this period can be observed on the cliffs.

GB: In the surrounding area, small walls made of regional rocks, mostly greywackes and clay shales, can be found in several places. The rocks are already described in the geological overview and can be easily distinguished by the following characteristics: Layering/thickness, grain size, sorting, minerals, rock fragments and color. In addition, quartz veins occur in all rocks. These are a form of crystallization of quartz: a hard, transparent to white mineral. EN: In the following area there are small walls made of regional rocks in several places, mostly greywacke and shales. The rocks are already described in the geological overview and can be easily distinguished by the following characteristics: layering/layer thickness, grain size, sorting, minerals, rock fragments and color. In addition, quartz veins occur in all rocks. This is a crystallization form of quartz: a hard, transparent to white mineral.

GB: In Cadjack Cove, in addition to large faults, many folds can be seen. These folds are formed in different scales ranging from a few inches to several hundred feet. In addition, the folds show different degrees of openings and roundness. Very narrow folds with pointed angles are called "kink bands". Overall, the folds were formed during the Variscan mountain building phase/orogenesis (417 - 200 Ma). The high pressures from the south have deformed the relatively soft rocks. However, the folds seen in this bay are not the main folds but represent folds that are folded within themselves. Another special feature in this bay are the pink to dark red colored rocks. This change in color is caused by iron-rich water running down the cliffs. EN: In addition to large faults, many folds can also be seen in Cadjack Cove. These folds are formed at different scales and range from a few centimeters to several meters. The folds also show different openings and curves. Very tight folds with acute angles are called “kink bands.” Overall, the folds were formed during the Variscan orogeny (417 – 200 Ma). The strong pressure from the south has deformed the relatively soft rocks. However, the folds seen in this bay are not the main folds, but rather represent folds folded into themselves. Another special feature of this bay are the pink to dark red colored rocks. This discoloration is caused by iron-rich water running down the cliffs.

GB: In the lower Mirrose Well Cove one finds deposits with repeated sequences. In each sequence, a gradation of the layers can be observed, with the grain size decreasing from the bottom to the top. In the case of Mirrose Well Cove, coarser greywackes were deposited first, turning into fine greywackes, and followed by clayey layers. Altogether, the deposits reach a thickness of six to ten feet (2-3 m). This type of deposit is caused by turbidites (massive mud flows). To trigger a turbidite, minimal vibrations or the deposition of further sediment grains are enough. The sediments then flow down the slope in a turbulent stream along the water current - a slope inclination of 2-3° is enough here - and spread out into the deep sea in the form of a fan. In this way, sediments with a thickness of several dozens of feet can form within a few hours. EN: Lower Mirrose Well Cove contains deposits with repeated sequences. In each sequence, a gradation of the layers can be observed, with the grain size decreasing from bottom to top. In the case of Mirrose Well Cove, coarser greywackes were first deposited, which transitioned into fine greywackes, followed by clayey layers. Overall, the deposits reach a thickness of two to three meters. These types of deposits are due to turbidites (powerful turbidity currents). To trigger a turbidite, minimal vibrations or the deposition of further sediment grains are sufficient. The sediments then flow down the slope in a turbulent stream with the water current - here a slope of 2-3° is sufficient - and spread out in the deep sea in the form of a fan. In this way, deposits several tens of meters thick can form within a few hours.